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TRANSACTIONS
OF THE
GEOLOGICAL SOCIETY
OF LONDON.
SECOND SERIES.
VOLUME IV.
Quod si cui mortalium cordi et cure sit, non tantum inventis herere, atque iis uti, sed
ad ulteriora penetrare ; atque non disputando adversarium, sed opere naturam vincere ;
denique non belle et probabiliter opinari, sed certo et ostensive scire; tales, tanquam
veri scientinarum filii, nobis (si videbitur) se adjungant.
Novum Organum, Prefatio.
LONDON:
PRINTED BY RICHARD TAYLOR, RED LION COURT, FLEET STREET.
SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY,
SOMERSET HOUSE.
1836.
a)
= ‘ A
sl ee
6
OFFICERS AND COUNCIL OF THE GEOLOGICAL SOCIETY
OF LONDON.
1835.
PRESIDENT.
CHARLES LYELL, Jun., Esq. M.A. F.R.S. & FLL.S.
VICE-PRESIDENTS.
Sir PHILIP DE MALPAS GREY EGERTON, EDWARD TURNER, M.D. F.R.S. L.& E. Pro-
Bart. M.P, F.R.S. fessor of Chemistry in the University of London.
RODERICK IMPEY MURCHISON, Esq. F.R.S. HENRY WARBURTON, Esq. M.P. F.R.S. &
& F.L.S. F.L.S.
SECRETARIES.
WILLIAM JOHN HAMILTON, Esq. | WOODBINE PARISH, Jun., Esq. F.R.S.
FOREIGN SECRETARY.
HENRY THOMAS DE LA BECHE, Esq. F.R.S. & F.L.S.
TREASURER.
JOHN TAYLOR, Esq. F.R.S.
COUNCIL.
GEORGE WILLIAM AYLMER, Esq. GEORGE BELLAS GREENOUGH, Esq. F.R.S.
FRANCIS BAILY, Esq. F.R.S. & F.L.S. & F.L.S.
ARTHUR K. BARCLAY, Esq. HENRY HALLAM, Esq. F.R.S.
WILLIAM JOHN BRODERIP, Esq. F.R.S. & JOHN FORBES ROYLE, Esq. F.L.S.
F.L.S. Rev. ADAM SEDGWICK, Woodwardian Professor
Rey. WILLIAM BUCKLAND, D.D. F.R.S. & in the University of Cambridge, F.R.S, & F.L.S.
F.L.S., Professor of Mineralogy and Geology in Lieut.-Col. W. H. SYKES, F.R.S. & F.L.S.
the University of Oxford. JOHN HENRY VIVIAN, Esq. M.P. F.R.S.
WILLIAM HENRY FITTON, M.D. F.R.S. & Sir RICHARD VYVYAN, Bart. M.P. F.R.S.
F.L.S. Rev. JAMES YATES, F.L.S.
CURATOR anv LIBRARIAN.
WILLIAM LONSDALE, Esq.
ADVERTISEMENT.
THE Editors of the Transactions of the Geological Society ari
directed to make it known to the Public, that the Authors alone are respon-
sible for the facts and opinions contained in their respective papers.
It is requested that all letters and communications to the Secretaries,
and presents to the Society, may be addressed to the Apartments of the
Geological Society, Somerset House, London.
OFFICERS AND COUNCIL OF THE GEOLOGICAL SOCIETY
OF LONDON.
1836.
PRESIDENT.
CHARLES LYELL, Jun., Esq. M.A. F.R.S. F.L.S.
VICE-PRESIDENTS.
Rey. WILLIAM BUCKLAND, D.D. F.R.S. GEORGE BELLAS GREENOUGH, Esq. F.R.S.
F.L.S., Professor of Mineralogy and Geology in F.L.S.
the University of Oxford. EDWARD TURNER, M.D. F.R.S. L.& E. Pro-
Sir PHILIP DE MALPAS GREY EGERTON, fessor of Chemistry in the University of London.
Bart. M.P. F.R.S.
SECRETARIES.
WILLIAM JOHN HAMILTON, Esq. | WOODBINE PARISH, Jun., Esq. F.R.S.
FOREIGN SECRETARY.
HENRY THOMAS DE LA BECHE, Esq. F.R.S. F.L.S.
TREASURER.
JOHN TAYLOR, Esq. F.R.S.
COUNCIL.
FRANCIS BAILY, Esq. V. P. & Treas. R.S. F.L.S. Viscount OXMANTOWN, F.R.S.
WILLIAM JOHN BRODERIP, Esq. F.R.S. JOHN FORBES ROYLE, Esq. F.L.S.
F.L.S, Rev. ADAM SEDGWICK, Woodwardian Professor
WILLIAM CLIFT, Esq. F.R.S. in the University of Cambridge, F.R.S. F.L.S.
Sir ALEXANDER CRICHTON, M.D. F.R.S. Lieut.-Col. WILLIAM HENRY SYKES, F.R.S.
WILLIAM HENRY FITTON, M.D. F.R.S. F.L.S.
F.L.S. HENRY WARBURTON, Esq. M.P. F.R.S.
HENRY HALLAM, Esq. F.R.S. F.L.S.
ROBERT HUTTON, Esq. Rev. WILLIAM WHEWELL, F.R.S. F.L.S.
RODERICK IMPEY MURCHISON, Esq.
V.P.R.S. F.L.S.
CURATOR anv LIBRARIAN.
WILLIAM LONSDALE, Esq.
ADVERTISEMENT.
THE Editors of the Transactions of the Geological Society are
directed to make it known to the Public, that the Authors alone are respon-
sible for the facts and opinions contained in their respective papers.
It is requested that all letters and communications to the Secretaries,
and presents to the Society, may be addressed to the “Apartments of the
“ Geological Society, Somerset House, London.”
CONTENTS.
PART I.
I. On the Geology of the Neighbourhood of Weymouth and the adjacent Parts
of the Coast of Dorset. By the Rev. William Buckland, D.D. F.G.S.
F.R.S. (Professor of Geology and Mineralogy in the University of Ox-
Jord), and Henry Thomas De la Beche, Esq. F.G.S. F.R.S. §c. . p. 1
II. Introduction to the General Structure of the Cumbrian Mountains ; with a
Description of the great Dislocations by which they have been sepa-
rated from the neighbouring Carboniferous Chains. By the Rev. Adam
Sedgwick, V.P.G.S. F.R.S. §c. (Woodwardian Professor in the Uni-
versity of Cambridge) . : - ; ; 4 : : p. 47
Ill. Description of a Series of Longitudinal and Transverse Sections through
a Portion of the Carboniferous Chain, between Penigent and Kirkby
Stephen. By the Rev. Adam Sedgwick, V.P.G.S. F.R.S. $c. (Wood-
wardian Professor in the University of Cambridge) : 3 : p. 69
PART II.
IV. Observations on some of the Strata between the Chalk and the Oxford
Oolite in the South-east of England. By William Henry Fitton, M.D.
P.G.S. FLRS. §c. . ; . ° 2 p- 103
V. Zoological Observations on a New Fossil user of Chine from
Cningen. By Thomas Bell, Esq. F.G.S. F.R.S. 5 ; . p. 379
VI. On the new Red Sandstone Series in the Basin of the Eden, and north-
western Coasts of Cumberland and Lancashire. By the Rev. Adam
Sedgwick, V.P.G.S. F. RS. §c. (Woodwardian Professor in the Uni-
versity of Cambridge) . . : : : : : p. 383
VII. On a Portion of Dukhun, East Indies. By Lieut.-Colonel William
Henry Sykes, /.G.S. F.RS. FDS. . : : : - p- 409
VII. On the Geology of the Environs of Bonn. By Leonard Horner, Esq.
PIGS, NSS. bg E, . « . : 5 Pe ails : p. 433
vi CONTENTS.
Index : : 2 - A 5 : , : : : ; ‘ p- 483
A List of Donations to the Library, to the Collection of Maps, Plans, Sections,
and Models, and to the Museum; from the Close of the 26th Session in
June, 1833, to the Close of the 29th Session in June 1836.
Explanation of the Plates.
Plates and Maps to the Volume.
*.* The Binder is directed to place the Lists of Officers and Council immediately after the
Title Page, in the order of their Dates ; and he is to place Plate X. b. before Plate X. a., that
both may fold out, and be examined at the same time.
ERRATA er CORRIGENDA.
Page106, line 5, for No. 1.) illustrates read No. 1.
and X. b. fig. 1. illustrate
——107, — 17, after No. 1. insert and Plate X. b.
fig. 1.
o
—— 108, Note*, for Section, Plate X.a. No, 1. read
Sections, Plate X.a. No. 1. and X.
b. fig. 1.
— 11], line 3 from bottom, for at read from
— 112, — 23, for subcristatus read cristatus ; and
add Plate XI. fig. 23.—See Appen-
dix A. p. 337.
15, for Hamites aculeatus read Ha-
mites spiniger
9 from bottom, add the words also at
Blackdown, Devon, Plate XVIII. p.
242.
9 from bottom, for Siphonaria, read Si-
phonia
— 130, — 20, for XXI. f. 7. read XXIII. fig. 7.
—— 131, — 14, for Trochus, read Pleurotomaria
—— 188, The thickness of the beds represented in the
Wood-cut differs in some respects
from those of the List, p.139; the
latter are the more correct.
—— 143, line 22, dele is
— ih
See 11D.
—— 153, — 3, for striata read gigantea
—— 164, — 3, for fig. 2. read fig. 3.
— — — 4, for No. 5. read No. 6.
— 167, — 11 from bottom, for (b.) read (@.)
—— — — 9 from bottom, for (b.) read (@.)
— — — 9 from bottom, for fluviorum read vivi-
para
—— 168, — 1, for (2.b.and 2. e.) read 2. B. and 2. ¢.
8, for 12 read 10?
— 11, for 2. a. read 2. a.
—— — last line, add p. 186, read (95.) p. 186.
—— 181, line 15, fe ppiuetond read Peppingford-
ar
—— — — 21, for Odontopteris read Sphenopteris
—— 182, — 13 from bottom, for No. 6. read No. 7.
—— 195, — 14, 15, 17, from bottom, for Gryphea
read Exogyra
—— 203, — 3, for Seligrimus read Selliguinus
—— 204, — 2, insert“ Anomiaconvexa. Plate XIV.
fig.7. Shore East of Shanklin Chine.
See p. 338.”
25, after Ostrea carinata insert ‘‘ Ostrea
retusa, Plate XIV. fig. 4.; from
Atherfield, in the Lower green-
sand.”
— 214, last line, for VIII. read IX.
—— 225, line 14, dele and
—— 230, — 9, for XX. read XXII.
Page 231, line 24, for tricristata read triserrata
—— 234, — 6, after thus: insert “ (see Plate X. a.
No. 11, and X. b. fig. 9.)”
a eee | for Stutchburiensis
read Stutchburianus
342, — 2, from bottom,
and Descript. of PI. X VIII.fig.1.
242, — 9, first column, for megastrema read
megatrema
—— — — 5, secondcolumn, add the words ‘“‘also
from Eastware Bay, in Kent; see p.
114, line 32.”
—— 252, — 15, for 4 feet to 7 feet read 4 to7
— 259, — 19, for in read or
— 260, — 8, for Berston read Benston
—— 262, — 26, for South read North
—.— — 382, for between Gin Cross read from
Gore Cross
—— 273, — 6 from bottom, for Aptychus read
Trigonellites
—— 292, — 23 and 30, for Aptychus read Trigo-
nellites
—— 297, — 10 from bottom, dele the semicolon after
suboolitic
—— 298, — 20, for Potamides carinatum read Pota-
mides? (a new species.)
—— 300, — 5 from bottom, for 286 read 206
—— 302, — 19, for Aptychus (Von Meyer),—read
‘* Trigonellites,(Parkinson); Ichthy-
osiagones, (Riippell); Aptychus,
(Von Meyer.)”
— 303, — 5, for 206. read 286.
—— 304, — 16 from bottom, for masses read matter
— — — 24, for masses read matter
— 305, — 9, dele the word “ chalk”
— 309, — 4, note }, for R.C. read C. B.
—— 316, — 6 from bottom, for Aptychus read Tri-
gonellites
—— 324, — 8, for (168.) p. 326. read (167.) and
(168.) pp. 326. and 329.
—— 339, — 9, for gigantea read striata
— 352, Inthe reference connected with Pentacri-
nites scalaris, for fig. 2. read fig. 4.
Tables 353, After Gastrochena, insert ‘“ sp. doubtful.—
In perforations in dicotyledonous
(silicified) wood ;—Gault, east of
Folkstone.”
— 355, In the reference Cytherea subrotunda, for
Pl. XXII. 2. read Plate XVII. 2.
355, After Cyclas media insert “ C media,
a gibbose variety, Pl. X XI. fig. 11.
(Hastings-said; Sussex, 177.—Pur-
beck strata; S. Wilts, 259.}”
— 358, note, dele ?? after the word adjective
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I
t :
I.—On the Geology of the Neighbourhood of Weymouth and the
adjacent Parts of the Coast of Dorset.
By tue Rev. W. BUCKLAND, D.D. F.G.S. F.R:S.
(PROFESSOR OF GEOLOGY AND MINERALOGY IN THE UNIVERSITY OF OXFORD.)
Ano H. T. De ra BECHE, Ese. F.G.S. F.R.S. &e.
[Read April 2 and 16, 1830. ]
FEW parts of the world present in a small compass so instructive a series of
geological pheenomena as those which are displayed in the vertical cliffs of
the south coast of England. An important portion of this coast, including
the Isle of Wight and the Isle of Purbeck, has been well described by Mr.
Webster*, and subsequently illustrated by Dr. Fitton+. In the Second Series
of the Geological Transactionst, Mr. De la Beche has published sections
of the coast from Bridport Harbour to Sidmouth; and in the same volume
Dr. Buckland has given drawings of the cliffs from Sidmouth to Beer Head,
and from Lyme Regis to the Isle of Portland§. The geological history of
the neighbourhood of Weymouth has been partially illustrated by Prof.
Sedgwick in the Annals of Philosophy || ; and it will be the object of this paper
to supply its full details, illustrated by a map and sections ; beginning our
observations at the point where Mr. Webster’s sections end, viz., at the Pro-
montory of White Nore, about eight miles E.N.E. of the town of Weymouth,
and continuing them to Weymouth and Portland, and thence westward along
the Chesil Bank to the cliffs west of Lyme Regis.
To our representations of the coast we shall add many inland sections of
the adjacent district, including all the strata which occupy that portion of the
south frontier of the county of Dorset which lies between the great south
* See Sir H. Englefield’s History of the Isle of Wight; the Geological Transactions, First
Series, vol. ii. p. 161—254; and Second Series, vol. ii. Part 1. p. 37 —44: also Annals of Philo-
sophy, vol. xxv. p. 33—51.
+ Annals of Philosophy, Nov. 1824, vol. Ixiv. p. 376.
t Geological Transactions, Second Series, vol. i. Part I. Pl. VIII. § Ibid. Plate XIV.
|| Annals of Philosophy, 1826, vol. xxvii. p. 346.
VOL. IV.— SECOND SERIES. B
2 Prof. Bucktanp and Mr. De ta Becue on the
escarpment of the chalk downs and the sea. We shall designate this tract
by the general appellation of the Weymouth District: it is a tract of no
small importance in the geological history of England :—
1. From its position near the south-western termination of several principal
formations of this island, including tertiary strata, chalk, greensand, Purbeck
and Portland beds, several members of the oolite formation, and lias.
2. As exhibiting a coast section which forms an interesting object of com-
parison with the north-eastern terminations of the same strata on the coast
of Yorkshire, which have recently been so well described by Mr. Phillips*,
and with their appearance across the Channel on the coast of Normandy, the
details of which have been described by Mr. De la Beche in the Geological
Transactionst, and subsequently by M. de Caumont in his Essay on the
Department of Calvados tf.
3. As affording remarkable examples of violent disturbances which have
affected all these strata since the period of their consolidation ; producing
elevations, depressions, fractures, and denudations, connected and continuous
with those which have operated so extensively in Purbeck and the Isle of
Wight, and through the wealds of Sussex and Kent.
We shall take a short review of the general physical features of this district
before we enter upon geological details. It will be seen by reference to our
map§, which is on the same scale as the Ordnance Survey, that the physical
features of the coast are:—I1. On the east a range of high cliffs extending
from the chalk of White Nore to the flat marsh lands of Lodmore near Wey-
mouth. 2. The marsh lands of Lodmore, divided only by a bank of pebbles
from the waters of Weymouth Bay. 3. A low range of cliffs, extending from
Weymouth Harbour to Portland Ferry. 4. The remarkable accumulation of
pebbles called the Chesil Bank, extending from the northern extremity of
Portland about sixteen miles north-westward to Burton Castle, and causing
the sea to be separated from the main land along nearly half this district by a
backwater called the Fleet. 5. A succession of cliffs rising gradually from Bur-
ton towards the west till they attain their highest elevation of about 600 feet
in the summit of the Golden Cap Hill, between Bridport and Charmouth.
The physical features of the interior divide it into two distinct compart-
ments, which we shall call the Vale of Weymouth and the Vale of Bredy.
The Vale of Bredy is bounded on the north and east by lofty escarpments of
* Tllustrations of the Geology of Yorkshire, by John Phillips, Esq. F.G.S. York, 1829.
+ Geological Transactions, Second Series, vol. i. Part I. p. 40—47.
t Essai sur la Topographie Géognostique du Département du Calvados, par M. de Caumont.
Caen, 1828. § Plate I.
‘‘iakar
es
a
Geology of the Neighbourhood of Weymouth, &c. 3
the chalk downs; on the south by Abbotsbury Castle, and a lower range which
slopes from thence continuously to Burton Castle ; on the west it is separated
by some hills of moderate elevation from the valley of Bridport.
Of the Vale of Weymouth the following are the three most prominent
features :—
Ist, The lofty escarpment of the Ridgeway which bounds it on the north,
running nearly in a straight line about twelve miles from east to west.
2nd, The elevated and inclined plane of limestone which constitutes the
Isle of Portland, and terminates this district towards the south.
3rd, Between this elevated Ridgeway and Portland is a space somewhat
triangular, composed of an alternation of low and nearly parallel, narrow
ridges and narrow valleys, which are terminated successively on the west by
the Chesil Bank, and on the east by Portland Road and Weymouth Bay ;
these all diminish in Jength successively, as their position is nearer to the
south, until the most southerly of them terminates in the sea at Portland
Ferry.
These ridges and valleys constitute a series of narrow belts, which are
crossed nearly at right angles by the road from Dorchester to Weymouth ; we
shall therefore designate these belts by the names of the villages that stand
upon or nearest to them: thus the names of Upway, Upway Street, Broad-
way, Nottington, and Radipole, will indicate five successive belts, composed
of five distinct and successive formations; namely, Portland stone, Kimmeridge
clay, Oxford oolite, Oxford clay, and forest marble,—all dipping north towards
the base of the escarpment of the Ridgeway chalk: nearly in the centre of
this belt of forest marble the dip changes suddenly towards the south ; and
the same succession of strata is repeated, dipping in an opposite direction
southwards, and disposed in corresponding belts, which may be designated
by the names of Melcombe, Wyke Regis, Portland Ferry, and Portland
Island. The formations superior to the Portland beds, if they exist south of
the island, are covered by the sea exterior to the Bill of Portland. At the
Race of Portland the agitation of the water is caused by the obstruction
which the subjacent mass of Portland stone offers to the tidal currents. The
line of section fig. 1,* exhibits the general structure of this district.
The forest marble{, with its clays and cornbrash, constituting the lowest
strata which rise to the surface, forms a double, central belt, elevated, as Mr.
* Plate Al:
+ The forest marble and cornbrash are so closely united throughout this district, that, except
in cases of minute local description, it will be most convenient to include them and their subor-
dinate clays under the common appellation of forest marble.
B2
4 Prof. Bucktanp and Mr. De ta Becue on the
Conybeare has stated*, into the form of an arch or saddle, on each side of
which the superior strata repose in corresponding order of succession, having
their dips respectively conformable to the north and south dips of the sides of
the arch, whilst their direction or line of bearing is nearly east and west, and
parallel to the axis of this central arch. Thus, on each side of our axis or
anticlinal line of forest marble, the Oxford clay reposes conformably, and
constitutes two parallel valleys, which extend from the sea in Weymouth Bay
to the Chesil Bank. 'To these succeed two similar parallel ridges of the
Oxford oolite formation, which are again overlaid by two parallel belts of
Kimmeridge clay, on which are still further superimposed two distinctly cha-
racterized deposits of Portland stone; and on the north side only, above the
Portland stone we find strata belonging to the Purbeck series, to the green
sand, the chalk, and plastic clay.
The superficial breadth of the belts on each side of the anticlinal line is in
the inverse ratio of their dip; and as this dip is most rapid on the north side,
the surface of the northern belts is less broad than that of the corresponding
belts on the south side.
Having taken this general view of the structure of the coast of Dorset, we
will again examine its component parts in a descending order, and point out
in regular succession the history and peculiar circumstances of each forma-
tion of which it is composed, beginning from the eastern extremity at White
Nore, and thus connecting it immediately with the observations of Mr.
Webster.
Tertiary Deposits.—Plastic Clay, &c.
It is well known from the maps of Mr. Webster f and Mr. Greenough {, that
the tertiary strata which fill the chalk basin of Hants and Dorset find their
western termination about three miles east of Dorchester. Between this ter-
mination and the great south-western escarpment of the chalk, there occur in-
sulated patches of the same tertiary deposits, and many large blocks of pudding-
stone and of gray-wether sandstone, which show that the original limits of the
tertiary formations extended far beyond their present outlines, and were pro-
bably almost coextensive with the chalk. Thus near Came Down on the Ridge-
way about four miles south of Dorchester, we have a deposit of rounded chalk-
flint pebbles, resembling the round tertiary gravel of Blackheath, near Lon-
* Outlines of the Geology of England and Wales, by the Rev. W. D. Conybeare, F.G.S. &c.,
and William Phillips, F.G.S. &c., pp. 182, 192.
+ Geological Transactions, First Series, vol. ii. Plate IX.
+ Geological Map of England and Wales, by G. B. Greenough, Esq. P. G. S. 1819.
Geology of the Neighbourhood of Weymouth, &c. 5
don: and at the summit of Black Down, six miles south-west of Dorchester,
which forms the highest hill within our district, we have a considerable series
of beds of similar pebbles, sand, brick earth, and plastic clay*, analogous to
the outlying fragments of the plastic clay formation which crown many of the
highest summits of the downs of Wiltshire and Hampshire, and are described
in Dr. Buckland’s paper on Valleys of Elevation f.
Upon the high table land of chalk, also, on which this plastic clay of Black
Down rests, we have numerous blocks of siliceous pudding-stone, scattered
over the surface of the fields, and composed, like that of Hertfordshire, of a
congeries of chalk flints imbedded in highly indurated siliceous sand: these
blocks also contain occasionally, though rarely, a few angular fragments of
chert from the greensand formation, and a few small pebbles of white quartz.
The chalk flints which make up the greatest part of their substance are not
all rounded, as in the Hertfordshire pudding-stone, but for the most part are
angular, as in the case of similar insulated blocks which occur on the hills of
greensand near Sidmouth ; and this angular condition deserves peculiar
notice, as it seems to connect them with the next deposits we are about to
mention, some of which may possibly be referred to the era of the plastic
clay formation. In two deep and steep combs excavated in chalk on the west
and south of Black Down Hill, viz. at Bride Bottom on the west, and at Por-
tisham on the south, these blocks of angular breccia are accumulated as thickly
as the gray-wethers in Clatford Bottom, near Kennet, on the Marlborough
downs : their abundance in Bride Bottom has caused it to be called the
Valley of Stones. This bottom forms the upper extremity of the Vale of Bredy,
where it contracts into a deep and narrow comb, at the head of which the
blocks are spread over a space of several acres, like a flock of sheep, often so
close together that a man may leap successively from one to another of them.
On the south side of the plain of Black Down we have another collection of
huge blocks of the same breccia in the steep comb which descends the chalk
escarpment into the village of Portisham: they are most abundant in the
village itself, where they lie so thick that they partly obstruct the street, and
when they occur in the line of the houses the walls are built upon them :
their extreme hardness and bulk have hitherto prevented their removal or
destruction by the hand of man. In the street at West Lulworth, also, similar
* These strata supply materials to a manufactory of bricks, tiles, and coarse pottery that is
established on this hill. The clay exhibits the same varieties of colour, viz. blood-red, yellow,
white, and black, which are so characteristic of the plastic clay formation, and are so well shown
in Alum Bay and at Reading.
+ Geological Transactions, Second Series, vol. ii. Part I., p- 119—130.
6 Prof. Buckianp and Mr. De ta Becue on the
blocks of the same stone lie in the line of the tront of some cottages, and are
built into the walls. In Dr. Kidd’s Geological Essay, p. 177, a similar col-
lection of siliceous boulders is described as scattered over a dry valley, high
up on the chalk downs of Berkshire, near Ashdown Park, on the south of
Swindon, so thickly as to render the road inconvenient, even to a foot tra-
veller. Although these blocks have been entirely separated from the matrix
in which they were formed, they are very slightly rolled, and have been
drifted but to a small distance from their native place.
We think it right to refer to the action of water, probably in more than
one period of the tertiary formations, certain deposits of angular gravel which
occur on the summits of many hills within our district. A remarkable ex-
ample of this kind, composed of an admixture of unrolled chalk flints with
yellow clay and sand, is seen in the upper margin of the cliffs at White Nore,
where it forms a continuous bed, varying in thickness from two to twenty
feet, level at its upper surface, but extremely irregular below, and filling up
deep holes and furrows (puts naturelles), which pervade the entire surface
of the subjacent chalk.
These deposits seem due to the effect of water dissolving the chalky matrix
of the flints, but not sufficiently agitated to roll them into pebbles, nor to
move them from the spot on which the dissolution of the chalk had taken
place. The most instructive example we know of the effects of this dissolving
operation is at Dunscombe Hill, on the east of Sidmouth, where, on the
summit of a ridge of chalk, of which the surface is furrowed with pits and
hollows that are evidently due to the action of water, we find an unstratified
mass of chalk flints, which have not undergone the slightest rolling, piled on
each other, and intermixed with Joose sand and clay; the outer portions of
this mass, from which the rain has washed away the sand and clay, lie loose
and hollow, like stones in an artificial barrow, or in a wall constructed without
mortar. It is scarcely possible to explain the actual state and position of
these flints but by supposing that the chalk in which they were formed has
been gradually dissolved in a quiet sea. To the same operation of quiet
solution we must also refer analogous deposits of angular chalk flints and
yellow clay which fill the irregular and deep troughs and hollows that fringe
the upper margin of the chalk in the cliffs from Lyme to Axmouth, in a
manner similar to that we have described at White Nore.
Cavities and projections of this kind appear to be universal on the surface
of the chalk wherever it is covered up with any kind of tertiary strata, and
has been protected by them from the levelling effects of atmospheric agents ;
in all these cases the actual surface of the land affords no indications of the
Geology of the Neighbourhood of Weymouth, &c. 7
irregularities which exist below: but however rugged be the subjacent surface
of the chalk, its irregularities are all obliterated and filled up with breccias
and gravel beds, presenting on their upper surface a smooth and continuous
outline, whilst their lower surface is curved and dentated downwards, con-
formably to the furrowed curvatures, and ridges and pinnacles that fringe the
upper surface of the chalk on which they rest; the existence of these pits
and cavities shows, that the chalk had not been exposed to the levelling
effects of atmospheric agents before the deposition of these breccias and
gravel beds.
The water which formed these breccias must have been subject to very irre-
gular currents and agitations ; for whilst in many places (such as those last
mentioned) the solution has been conducted in perfect tranquillity, in other
spots it has been attended or followed by agitations which have reduced the
flints to perfect roundness, as in the Hertfordshire pudding-stone and Black-
heath gravel; and again, in other cases, there is evidence of an intermediate
state of action, where only a partial rounding of the fragments has taken
place, as in the partly rounded and partly angular chalk flints which form a
thick bed reposing on strata of greensand on the summit of Haldon, on the
west of Exeter.
Another variety of angular gravel occurs in many beds of shivered chert of
the greensand formation, which seem to have undergone a certain degree of
decomposition, causing them entirely to break to pieces and crack into angular
fragments, and become converted into strata of loose and shivered gravel, on
which no mechanical attrition seems to have been produced by the operation
of water, but the fractures have resulted from the splitting to pieces of the
beds of chert still resting in their natural position. A remarkable example
of this kind may be seen in the cliffs that overhang the new road between
Lyme and Charmouth, and also on the summit of Abbotsbury Castle. In
the oolite formation also, about two miles west of Bridport, a similar dislo-
cation and splitting of the stone has converted to loose breccia the upper beds
of inferior oolite on part of the summit of Chideock Hill. This is the only case
we have noticed of such an occurrence in the oolite of the coast of Dorset.
It is not easy to distinguish between these undisturbed beds of shivered chert,
and accumulations of the same chert which have been very slightly agitated
by water, except in cases where the admixture of miscellaneous fragments of
other strata shows that moving water has operated in bringing these frag-
ments to their present position amongst the chert. There is also a difficulty
in distinguishing the deposits of angular breccia, both of this chert and of
the chalk formation, from deposits of diluvial gravel which have been removed.
8 Prof. Bucktanp and Mr. De 1a Becue on the
to a small distance only from their native place. The cliffs at Axmouth and
near Sidmouth exhibit deposits of such miscellaneous diluvial gravel, resting
on red marl, and adjacent to beds of uniform and angular chalk-flint breccia
that rest on the chalk.
These deposits of breccia on the coast of Dorset seem analogous to those
which are found in Normandy, reposing on the similarly corroded surfaces of
the chalk, and which occur also on the surface of other formations in that
part of France, each formation respectively being often covered with a cap-
ping of loose angular fragments composed of the hardest materials of the sub-
jacent strata. According to M. de Caumont, a breccia allied to the plastic
clay formation, and composed of angular chalk flints imbedded in red clay,
occasionally attaining the thickness of 80 and 100 feet, occurs in the valley
of the Rille, and various adjacent parts of Normandy*. M. de Caumont
speaks of all these breccias under the head of Diluvium,—falling into the same
common error with many other Continental geologists, of including under the
term Diluvium many pebble beds and breccias which belong to the tertiary,
and to older formations.
Chalk.
The lofty escarpment of chalk which bounds our field of observation on
the north, forms the margin of the chalk downs of the southern part of Dor-
setshire, and is the direct continuation of the south frontier of the great chalk
basin of Dorset and Hants. Along great part of this south frontier, from the
east extremity of the Isle of Wight to the west extremity of Purbeck, and
thence to the cliffs of White Nore, where we euter on its history, Mr. Web-
ster has shown its position to be sometimes absolutely vertical, but for the
most part dipping at a very high angle northwards towards the interior of the
basin f. This high inclination ceases a little east of the promontory of White
Nore, where the chalk suddenly sweeps round, and dips at an angle of a few
degrees only to the north-east. Along the range of its escarpment westward, for
nearly twenty miles from White Nore to its termination at Chilcomb Hill, on
the east of Bridport, the dip is almost constantly towards the north, at angles
varying from 10° to 40°. Its mean elevation along all this range may be taken
at about 500 feet. The base of this escarpment appears throughout to be
* See sections and description in M. de Caumont's Essai sur la Topographie Géognostique
du Calvados ; and De la Beche on the Geology of the North Coast of France, from Fecamp to
St. Vaast, in Geol. Trans. Second Series, vol. i. Part I. p. 73—89.
+ See Sir Henry Englefield’s History of the Isle of Wight, Plate 50; and the Geological
Transactions, First Series, vol. i1. Plate XI.
Geology of the Neighbourhood of Weymouth, &c. 9
composed of beds of the greensand formation ; but these are rendered invi-
sible in the greater part of the Weymouth district, in consequence of a fault
which runs along the escarpment for nearly ten miles, from Poxwell to Abbots-
bury, and brings up strata, subjacent to the greensand, into immediate contact
with the chalk: this fault we shall hereafter describe.
The promontory of White Nore is the last point in the South-west of Eng-
Jand at which the great bedy of the chalk touches the sea; those insulated por-
tions of this formation which occur in the cliffs between Lyme and Sidmouth
being only detached outlying masses, separated, by denudations of many miles
in width, from the south-west termination of the great chalk basin of Dorset-
shire*.
The mineralogical character and organic remains of the chalk in this
district present nothing unusual: the lower strata of the chalk pass into hard
chalk, devoid of flints, and interspersed irregularly with green grains of sili-
cate of iron.
Greensand.
The strata of the greensand formation, which at White Nore emerge
from beneath the lowest chalk, dip conformably with it to the north-east, and
attain a thickness of about 100 feet: their succession in a descending order
is:—1. Chalky glauconite, composed of greensand interspersed with cal-
careous cement. 2. Green, yellow, and brown sand, alternating with irre-
gular calcareous concretions, and with thick beds of chert. 3. Dark argil-
laceous greensand, with large nodular concretions, equivalent to the sandy
concretions called cow-stone, at Lyme Regis: the upper subdivisions of this
section also closely resemble some of those exhibited by the greensand for-
mation near Lyme.
We are unable to recognise distinctly in this district, or in any part of the
coast west of Weymouth, those regular and extensive threefold subdivisions of
fire-stone, gault, and lower greensand, which are so obvious in Hants, Sussex,
and Kent; although an approximation to the character of fire-stone may be
traced at White Nore, and still more decidedly in Devonshire, in the cliff and
quarries of Beer already described by Mr. De la Bechet.
For a considerable distance near White Nore and Osmington the green-
sand is visible at the base of the chalk escarpments, dipping always conform-
ably to the chalk; but along the great escarpment from Poxwell to Abbotsbury
it is seen only in two places, namely, near Sutton Pointz, and at Bincombe,
being elsewhere masked by the Portland stone, which the great fault that
* See Map, Plate I. + Geological Transactions, Second Series, vol. ii. p. 109.
VOL, IV.—SECOND SERIES. C
10 Prof. Buckianp and Mr. Dre 1a Becue on the
runs along this escarpment brings up into absolute contact with the chalk.
At these two places, however, its thickness is so great as to leave little doubt
that it continues in its proper place beneath the chalk, to the west extremity
of the fault near Abbotsbury, where it is again exposed, and forms a con-
siderable feature in the escarpment of White Hill, overhanging the village
of Abbotsbury, and projecting thence nearly two miles westward into the
summit of the long and elevated ridge of Abbotsbury Castle. From Abbots-
bury Castle it turns northward, still forming the sub-escarpment of the
chalk, along the entire east and north frontier of the Vale of Bredy. It ap-
pears also on the summit of Swyre Knoll, Hammerdon Hill, and Shipton
Beacon, which form three remarkable outlying hills on the flanks of the Vale
of Bredy, and in much greater force on the summits of the insulated hills of
Golden Cap, Hadden Hill, Stonebarrow Hill, Coneygore, and Conig Castle
near Charmouth ; and further north, on the lofty tops of Lewsdon Hill,
Pillesdon Hill, and Black Down near Broadwindsor*. In the escarpment on
the north of Abbotsbury we have a distinct section, displaying ledges of hard
coarse limestone, loaded with grains of quartz and silicate of iron, and alter-
nating with thick strata of chert; a little further west, at Abbotsbury Castle,
the calcareous matter ceases, and is replaced by strata of chert. These cal-
careous and cherty strata of the greensand at Abbotsbury, afford an interest-
ing object of comparison with those in the neighbourhood of Lyme Regis,
described by Mr. De la Beche f, as well as with those at White Nore. The
occasional presence of so much calcareous matter in the greensand, seems
to justify the appellation of crate chloritée, given by the French to the upper-
most strata of the greensand formation.
The greensand in our Weymouth district is found to overlie and repose
successively on formations of different ages; thus, in the valley of Upton on
the east of Osmington it rests on the Purbeck bedst ; in the south escarpment
of Upton Hill towards Ringstead Bay, on Portland stone$ ; on the west
of Osmington Mill, on Kimmeridge clay||; at Abbotsbury Common, on a
clay which is probably the Oxford clay; at Golden Cap Hill, on inferior
oolite**; near Lyme Regis, upon lias++; and at Axmouth and Beer, upon
red marltt. The same overlapping disposition of the greensand has been ob-
* See Map, Plate I. t Geological Transactions, Second Series, vol. ii. pp. 109, &c.
+ See Plate Il. fig. 2 & 3. § See Plate II. fig. 2.
|| See Plate ITI. fig. 9. G See Plate II. fig. 6 & 7.
** Geological Transactions, Second Series, vol. i. Part I. Plate VIII. and Plate XIV. No.1. In
these sections the inferior oolite was omitted by mistake, but is inserted in a section of the same
coast, in Pl. III. of Mr. De la Beche’s Sections and Views Illustrative of Geological Pheenomena.
tt Ibid. Plate VIII. tt Ibid. Plate XIV. No. 2.
Geology of the Neighbourhood of Weymouth, &c. 11
served by Mr. De la Beche* and M. de Caumont in Normandyf, where it
overlaps successively the formations of Kimmeridge clay, coral rag, and Ox-
ford clay. This circumstance derives an additional importance, at the present
time, from the recent paper of M. Elie de Beaumontf, in which he observes
that a connexion exists between the elevation of mountains and succeeding
deposits of extensive overlapping strata, e. g. the greensand and chalk in
the Jura mountains, filling the longitudinal valleys produced by the elevation
of the oolites. On the coast of Dorsetshire no elevation of the strata appears
to have taken place between the deposition of the lias and the plastic clay.
Hastings Sand, and Purbeck Beds.
Although the Wealden or Hastings sands do not enter the area of our
actual observation, they approach very near to its eastern extremity, becoming
gradually thinner in their progress westward through the Isle of Purbeck,
until they terminate a little west of Lulworth: this has been already pointed
out by Dr. Fitton and Mr. Webster$.
The identity of this Hastings sand with that of Swanwich Bay, at the east
extremity of Purbeck, has recently been further confirmed by the Rev. T. O.
Bartlett’s discovery of the remains of the Iguanodon and other reptiles in the
iron sandstone at Swanwich. Bones of this animal have also been recog-
nised by Prof. Buckland and by Mr. Vine in the same sandstone at Sandown
Fort, and other places on the south coast of the Isle of Wight.
The Purbeck beds enter our district on the north-west of White Nore, but
are seen only in two small insulated patches near the villages of Osmington
and Upway. The details of the beds composing the Purbeck series are so
fully given by Mr. Webster ||, that it is here superfluous for us to say anything
respecting them, further than that several of their most remarkable varieties
are recognised and wrought even to their final termination on the west of
Upway. We trace also throughout this district the remarkable beds of fi-
brous carbonate of lime that pervade the clay which alternates with the beds
of limestone throughout the Isle of Purbeck. The fibres of this limestone,
like those of satin spar, are at right angles to the planes of the beds which
they compose, and which vary from two to six inches in thickness. From
the resemblance of its small and parallel fibres to the fibres of animal muscle,
this limestone is known among the workmen by the name of “Beef”: it
* Geol. Trans. Second Series, vol. i. Part I. Pl. X. { Essai sur le Top. Geog. Pl. VI.
t Ann. des Sciences Nat. vol. xvii. Sept. 1829. § Annals of Philosophy, 1824, New
Series, vol. viii. p. 382: also Sir H. Englefield’s History of the Isle of Wight, p. 194.
|| Geological Transactions, Second Series, vol. ii. p. 36.
c 2
12 Prof. Bucktanp and Mr. De ta Becue on the
sometimes entirely occupies the place of the clay between the limestone beds
of this formation. One of the most important points in the geological history of
the Purbeck series, is the occurrence ofa bed of oyster-shells called the “cinder
bed,” often many feet in thickness, and almost wholly composed of dark-
coloured, small oyster-shells in the midst of a series of strata, some of which
contain exclusively shells of freshwater formation, and others an admixture of
freshwater shells with those which are marine: this circumstance has been duly
noticed by Mr. Webster and Dr. Fitton ; and although we cannot infer from
it the return of the sea for any long period in the middle of the Purbeck for-
mation, yet it shows that the district it occupies could not have been a lake of
pure fresh water, but was probably an estuary at the time when these oysters
occupied its bottom, and were accumulated to the thickness of many feet
over a distance of many miles*.
We are disposed to agree with Mr. Webster, and to adopt more confidently
than he has done the opinion he advances with respect to the propriety of
referring to the lower region of the Purbeck series the beds of white cal-
careous slate, usually destitute of organic remains, which occur between the
undoubted Purbeck beds and the Portland stone; these beds resemble the
compact varieties of Purbeck stone, which are devoid of shells, and which
near Lulworth attain a thickness of from 60 to 100 feet. In Portland the
* The following description of the actual state of the lake Menzalé at the mouth of the Nile, by
a modern traveller, is highly illustrative of the mode in which living animals of a mixed character
are associated together near the confluence of great rivers with the sea.
“The lake Menzalé is only five miles distant from Damietta. I should judge it to be sixty-five
miles long, and fifteen broad: it is not, properly speaking, a maritime lake, but formed by the
increase of the Damietta branch of the Nile; the depth is from three to five feet, and on pushing
an oar to the bottom I have observed it coated with the common mud of the Nile for about twenty
inches deep. Along all the length of the lake a narrow tongue of land separates it from the sea,
but not wholly: there are four passages through which it is possible for barks to sail; through
two of them I passed with a good deal of difficulty. At the mouth of each there is a bar of sand,
which makes the passage perilous from the sea. No sea or lake in the world can perhaps boast
of the same quantity of fish in a given space as the lake of Menzalé.
“‘The principal sorts of fish caught here are the Perca Luth, or Lot’s perch; another species called
kescher ; the charamoot or Stilurus anguillaris,—the fin is said to be poisonous; the burra, or red
mullet; the kelp el bahr, or sea-dog; the casheff, or Mormyrus anguilloides of Linnzeus ; this I
have seen weighing thirty pounds. The salmon of the Nile is found in the upper part of Menzalé
weighing from 80 to 100 pounds. The mixture of sea and river water in the lake causes it to be
neither salt nor sweet ; so that both river and sea fish are to be found here in equal quantity: but
both, in my opinion, of an inferior quality. The quantity of birds which cover the lake is pro-
digious. Pelicans, cormorants, cranes, and herons live only on the fish.”—Madden’s Travels in
Egypt, §c. vol. ii. p. 171—175.
Geology of the Neighbourhood of Weymouth, &c. 13
lowest of them form the surface of the island, and cover the true Portland
stone with a deposit of freshwater formation. ‘This formation presents beds
of chert containing freshwater sheils, near the Ridgeway fault, on the west
side of the road from Weymouth to Dorchester ; and also beds of chert con-
taining chalcedonic casts of minute freshwater shells, at the water’s edge, on
the east side of Lulworth Cove.
Section of the Dirt-bed in the Isle of Portland.
Calcareous slate. £- os : c| Freshwater formation.
re
= ——— i a
YY sxe a UY sf Ip Mf :
Dirt-bed. My sinned lie P i HUM, Ancient forest.
Marine formation.
We consider a small stratum, called by the workmen “ Dirt-bed,” to be by
far the most interesting and remarkable deposit in this district. It seems to be
made up of black loam, mixed with the exuviz of tropical plants, accumulated
on the spot on which they grew, and preserved during a series of years, in
which the surface of the Portland stone had for a time become dry land, and
accumulated a soil of about a foot in thickness, composed of an admixture of
earth and black vegetable matter, interspersed with slightly rounded frag-
ments of stone, which Mr. Webster ascertained to be from the lower part of
the Portland series. ‘These fragments are found to be almost coextensive
with the dirt-bed, and the fact that we have yet found with them no admix-
ture of pebbles derived from the subjacent oolites, or from any other more
ancient rocks, shows that no violent rush of water from any distant region
took place during the period in which these pebbles of Portland stone were
under the process of becoming slightly rounded.
This dirt-bed, as Mr. Webster has stated, forms the matrix of the silicified
trunks of very large coniferous trees, which are so abundant in the Isle of Port-
land, and are found there coextensive with the upper surface of the Portland
stone. Wherever the dirt-bed is laid open to extract the subjacent building-
stone, it is found to contain these silicified trees laid prostrate, partly sunk
into the black earth, and partly covered by the superjacent calcareo-siliceous
slate: from this slate the silex, to which the trees are now converted, must
14 Prof. Bucktanp and Mr. De 1a BeEcue on the
have been derived. A bed of snow falling on a modern peat-bog, and cover-
ing the upper portion of prostrate trees, whose lower portion has been sunk
by their weight into the substance of the peat, would represent the position
of the calcareous slate which immediately covers these fossil trees in Portland :
some of them extend to a length exceeding thirty feet, and bifurcate at their
upper end; but the branches are not continuous to their extremities, and we
find no traces of leaves. The leaves and small branches, and exterior parts
of the trunks, had probably decayed, whilst they lay exposed to air on the
surface of the peat. Amid these prostrate trees, many of which attain three
and four feet in diameter, we find silicified stems of plants closely resembling
the modern Cycas and Zamia: these have been described by Prof. Buck-
land under the name of Cycadeoidez*, and are important, as indicating that
the temperature in which they grew was much higher than that of our pre-
sent climate. We find also, at nearly the same intervals at which trees are
found growing in a modern forest, an assemblage of silicified stumps or stools
of large trees, with their roots attached to the earth in which they grew.
These stumps are from one to three feet long: they are mostly erect, whilst
a few are slightly inclined. The black earth which contains their roots
seldom exceeds one foot in thickness; the upper portions of the stumps, as
represented by Mr. Webstert, project upwards into the substance of the
superjacent stone (called “soft Burr’ and “ Aish’’), which gives indication of
their presence by hemispherical concretions accumulated around the top of
each stump of woodf.
Section of the Cliff east of Lulworth Cove.
er LE,
See Ayreon Soft burr.
as YES bas OE Zr Prag Ancient forest in the dirt-bed.
Lower Purbeck beds ig Ze, A Te ipritier 4
composed of calca- ee Ae
or
reous slate of fresh-~ ~
water formation.
Portland stone of
marine formation.
In the highly inclined strata of the cliff, about a furlong east of Lulworth
Cove, and represented in the above sketch, we find a considerable number
of these silicified stumps, some entirely laid bare by the washing of the sea,
others partly exposed and partly covered, and others still wholly encased with
* Geological Transactions, Second Series, vol. ii. Part III. p. 395.
+ Ibid. vol. ii. Part I. Pl. 6. fig. 3, 4. t See wood-cut at p. 13.
Geology of the Neighbourhood of Weymouth, &c. 15
concretions of soft burr, and all having their roots fixed in the dirt-bed, which
occurs here also of the same thickness, and in precisely the same relative
place, and interspersed with the same rounded fragments of limestone which
it contains in the Isle of Portland: the position of these stumps, at an angle
nearly of 45° to the horizon, affords a striking proof of the elevation which
the strata have undergone. We find the dirt-bed also on the top of the
Portland stone, in the sections of some quarries along the Ridgeway, e. g.
near Upway, on the north of Weymouth, and at the western termination of
the Portland stone near Portisham, at the distance of twenty miles west from
Lulworth. Dr. Buckland has found slight traces of this dirt-bed on the upper
surface of a stratum of Portland stone in the quarries about two miles north
of Thame, in Oxfordshire: it is here covered by a few feet of clay, in which
he found no other animal remains than fragments of some Testudo, too
small to point out the genus to which they belong. The recognition of this
very remarkable bed in a locality so distant from Portland seems to indicate
that it may be found to be nearly coextensive with the Portland formation
throughout England; and it well merits the attention of future observers to
search for it in the Vale of Aylesbury, and in the two localities of the Port-
land stone intermediate between Oxford and Dorsetshire, namely, at Swindon
and Tisbury. The probability of its occurrence at Tisbury is increased by
the recent recognition of the Cycadeoidew at this place by Miss Benett*.
We consider this dirt-bed as quite decisive in forming the barrier between
the Portland and Purbeck formations: its deposition must have proceeded
during a considerable period of time, antecedently to which the districts it
occupies were entirely submerged beneath the sea, and subsequently to
which the waters again returned to overwhelm them, first with a deposit
of about 1000 feet of the semi-lacustrine sediments of a great estuary (in-
cluding the united thickness of the Purbeck series and the Wealden sands
* Dr. Fitton has discovered this deposit on the opposite side of the Channel in the Bou-
lonnois, and has thus described it in the Annals of Philosophy, December, 1826. ‘ Some traces
of the lowest members of the group to which these two strata (Weald clay and Hastings sand)
belong, and which is remarkable from its containing throughout the remains of freshwater shells,
are visible on the summit of the cliffs between Gris-nez and Equinen, where a thin bed occurs of
somewhat bituminous clay, abounding in silicified wood, the cavities of which are coated with
minute crystals of quartz. This bed corresponds precisely to that which exists on the top of the
Isle of Portland, bearing there the name of ‘Dirt,’ and abounding in similar wood ; and on the
French coast it is associated with beds of limestone, different from the stone beneath, and contain-
ing shells in great numbers, apparently of the genera Cyclas and Ampullaria.” Dr. Fitton has also
recognised thin fissile beds of Purbeck stone containing freshwater shells, e. g. Cyclas and Cypris,
at Whitchurch in Bucks.
16 Prof. Bucktanp and Mr. De 1a Becue on the
and clays), and afterwards with a series of marine deposits amounting to much
more than 1000 feet of greensand and chalk.
Throughout the entire succession of all these changes there is no evidence
of any sudden and violent disturbance causing either elevation or depression
of the Portland stone, or of the subjacent oolites. The present high incli-
nation of all these beds is uniformly parallel to that of the beds of Purbeck
stone, greensand, and chalk ; and these all seem to have been raised simul-
taneously by the same convulsion which elevated the axis of the Weymouth
district, together with all the inclined strata in Purbeck and the Isle of
Wight.
We have a measure of the duration of the period during which the surface
of the Portland stone continued in the state of dry land, covered with forest,
in the thickness of the “ Dirt Bed,’ which has accumulated more than a foot
of black earth, loaded with the wreck of its vegetation. The regular and
uniform preservation of this thin bed of black earth over a distance of so
many miles, shows that the change from dry land to the state of a freshwater
lake or estuary was not accompanied by any violent denudation or rush of
water, since the loose black earth, together with the trees which lay prostrate
on its surface, must inevitably have been swept away had any such violent
catastrophe then taken place*.
* Prof. Henslow in the summer of 1832 found in the top cap of the Portland stone, imme-
diately beneath the dirt-bed, root-shaped cavities descending from the bottom of the dirt-bed into
the subjacent solid stone ; this top cap should seem, therefore, to have been occupied by the
roots of the trees which grew in the dirt-bed, and penetrated the Portland stone whilst it was yet
soft and unconsolidated. He also noticed in Portland two partial and very thin seams of black
earth; the uppermost at the distance of five feet, and the lowermost of seven feet, below the dirt-
bed: these seams of black earth are important, as they mark two short intervals during which
vegetable matter had begun to accumulate on the surface of the soft and gradually increasing ma-
terials of the uppermost beds of the Portland stone, whilst they were just rising above the level of
the sea. The incipient bed of vegetable matter was thus twice interrupted in its progress, and
buried beneath an influx, first of two feet, and next of five feet, of earthy sediment, before the
general surface on which the true dirt-bed rests had been raised entirely above the water.
The above cut represents an example which in the summer of 1832 occurred to Prof.
Henslow in the Isle of Portland, in a quarry where the surface of the burr had been laid bare,
E49)
Geology of the Neighbourhood of Weymouth, &c. 17
Portland Stone.
As the details of the component beds and fossils of the Portland series
have been sufficiently described by Mr. Webster and Mr. Conybeare, we shall
of an erect stump protruding through the burr stone into the superior stratum called Aish,
analogous to that represented by Mr. Webster in his section of the Portland beds (Geol. Trans.
Second Series, vol. ii. p. 1. Plate VI. fig. 3 and 4.), and which the workmen stated to be of rare
occurrence; this superior stratum exhibited to Prof. Henslow two or three of those conical and
dome-shaped protuberances which so generally indicate the presence of stumps of trees imme-
diately beneath them. In the case represented, the protruding stump being longer than the rest,
the burr stone was not deposited in sufficient thickness to cover it, but was heaped around it in
two circular ridges, with intermediate circular depressions. From these appearances we may infer
that a state of great tranquillity attended the deposition of the calcareous sediment of which the
dome-shaped caps that cover the shorter stumps were formed (See Section of the Dirt-bed,
page 13.) The circular ridges and depressions which surround the taller stumps (see page 16,)
seem to have been produced by an interruption of the undulations on the surface of water so
shallow that the waves were caught and broken by a stump but four feet high, whilst they passed
over the shorter stools immediately adjacent to them; these interrupted undulations being propa-
gated first downwards and then outwards along and around the stump whose top was high enough
to obstruct the ripple on the surface of the shallow lake, by which the dirt-bed was gradually
inundated.
Here, then, we have proofs of a tranquil state and gentle action of water in the period imme-
diately succeeding, as well as in that which preceded, the formation of the dirt-bed, upon a sur-
face that became dry land during a short time intermediate between the transition of the district
which it covers from a submarine state to that of a freshwater lake. The rapid possession which
in our modern tropics is taken by the Pandanus or Screw Pine and Cocca-nut Palm of the first
banks and reefs of coral islands that emerge above the level of the sea, affords an example of the
luxuriant growth of vegetables on the margin of land just rising above the water, analogous to
the ancient juxtamarine forest the remains of which contributed to the formation of the dirt-bed,
in the region which has now become the southern coast of Dorsetshire.
With respect to the silicified trees Prof. Henslow makes the following observations :—
“From what I saw I should think that all the erect stumps must have suffered considerable
decay before they had become imbedded, or at least fossilized, in the burr. They consisted of no
more than the central portion of the wood just above and below the neck of the trees, which had
every appearance of having grown in the places which they still occupy.
“In a quarry of very white and chalk-like Portland stone, at the base of Chalbury Hill, near
Preston, I found a cylindrical mass of flint ten inches in diameter, reposing upon a soot-like mass
of carbonaceous matter, probably resulting from the decomposition of leaves and bark, and
forming an envelope to the lower part of the cylinder, but not extending beyond it. Upon crack-
ing off as much of this cylinder as protruded from the side of the quarry, I perceived the central
portions, of three inches in diameter, to consist of fossilized wood. It appears to me most pro-
bable that the whole cylinder had occupied the space originally filled by the trunk or branch of
a tree; but that during the process of its becoming silicified, the organic structure of the outer
portions had not been impressed upon the flint. In the Isle of Portland the quarry-men collect a
similar black vegetable substance, which they use for blacking.”
VOL. IV.—SECOND SERIES. D
18 Prof. Buckianp and Mr. De 1a BeEcueE on the
only refer to their account of them*, and to our own detailed section of Black
Nore on the west cliff of the Isle of Portland. We have little to add to what
these authors have published, except the occurrence of bones of Saurians
which we discovered in the cliff of Black Nore, imbedded in compact Port-
land stone.
We have stated in our introduction that this district contains two distinct
ranges of Portland stone; one constituting the table-land of the Isle of
Portland, dipping southwards beneath the sea, and rising with an elevated
escarpment northwards towards the bay and valley of Weymouth ; the other
constituting a long and narrow line of elevated hills, parallel, and immediately
subjacent, to the chalk escarpment of the Ridgeway, and presenting a con-
tinuous and lofty escarpment towards the south. In fact, these hills occupy
the position which in districts that have been less disturbed is usually held by
the sub-escarpments of the greensand formation, where it emerges regularly
from beneath the chalk: such are the escarpments of greensand which in
Kent and Sussex extend from Folkstone, by Coxheath, Nutfield, and Leith
Hill, to Godalming. A glance at our map will show that along the northern
frontier of the Vale of Weymouth this ridge of Portland stone forms a con-
tinuous band from the east extremity of our district near White Nore to
Portisham, where it suddenly terminates in the great fault, and is found no-
where further west in England. Along nearly the whole of this tract it attains
a high elevation, rising near the central part at least 500 feet into the lofty
eminences of Preston Hill, Charlbury, and Bincombe Hill: at these three
places its elevation is little less than that of the chalk itself. On the west of
Upway it forms a narrow ridge or hog’s back from Upway to Portisham,
known by the name of Corton Hill and Waddon, dipping at an angle of
about 45° to the north. Although these Portland beds dip thus rapidly to
the north, through great part of the range now under consideration, yet
such is the dislocation and elevation they have suffered along the line of the
great fault, that their northern margin is seldom brought into contact with
any other strata than the chalk. On the west of Upway this line of contact
is marked by a longitudinal valley, flanked on its north side by the chalk
escarpment, and on its south side by the upper Portland strata of Corton
Hillt : thus, the Portland beds dipping to the north in Corton Hill, and south
along the fault, form a trough in which reposes a long and narrow strip of
Purbeck strata, extending more than a mile both on the east and west of
Upway, and dipping conformably to the double dip of the subjacent Portland
* Geological Transactions, Second Series, vol. ii. p. 37, &c. Outlines of the Geology of En-
gland and Wales, p. 172. ¢ Plate III. fig. 3. t{ See Map, Plate I.
Geology of the Neighbourhood of Weymouth, &c. 19
stone. The sudden and total disappearance and termination of the Portland
formation at Portisham, seems not to result from its accidental intersection
at that place by the great Ridgeway fault; but rather from the tendency
which is common to this, with most other great formations, to terminate
abruptly where they are accumulated to their fullest thickness; thus we find
the full thickness of the chalk and oolite formations exhibited for many
hundred miles along the line of their great escarpments throughout England,
and in like manner the full Portland strata terminate abruptly in the Vale of
Weymouth: they reappear and again terminate with equal abruptness in the
Vale of Tisbury, and exhibit nearly the same features of sudden termination
in the hills near Brill and Thame in Oxfordshire, and near Aylesbury and
Whitchurch in Bucks.
The fact of the interrupted deposition of the Portland formation in En-
gland, occurring as it does only in the limited districts just mentioned, and
in one other small spot at Swindon, is analogous to the interrupted deposits
of other strata, particularly the most recent members of the oolite formation.
We know not the cause of these irregularities ; the fact may be illustrated by
the case of the Kimmeridge clay, which attains at Kimmeridge a thickness
of 600 feet, is reduced to 70 feet near Oxford, disappears entirely in some
places along its line of bearing, and again resumes its strength in the Vale
of Pickering, and near the coast of Yorkshire. The Portland stone has not
yet been identified on the opposite coast of Normandy, but M. Elie de
Beaumont states that he has discovered it in Burgundy*, and M. Dufrénoy
says that it occurs largely in the vicinity of Angoulesmeyt. We think it pro-
bable that it will soon be recognised among the great calcareous formations
of the Alps and Apennines.
Portland Sand i
The consolidated and calcareous beds of the Portland stone are separated
from the Kimmeridge clay by the interposition of a deposit of sand and marly
sandstone at least eighty feet thick, exceeding the total thickness of the
Portland stone itself. This deposit is coextensive with the Portland stone
throughout nearly the whole of the coast of Dorset, and is well exhibited by
a vertical section near Black Nore, on the west cliff of the Isle of Portland,
and along the west shore from Black Nore to the village of Chesilton. Its pre-
vailing character is a siliceous sand, so abundantly mixed with grains of green
earth, as to be scarcely distinguishable from the lower strata of the green-
sand formation near Lyme and Seaton: it also contains large semicalcareous
* Ann. des Sciences Nat., July 1829. + Annales des Mines, 1829, vol. ii. p. 434.
i See Pl. IIL. fig. 1. n. 0. and fig. 3.
20 Prof. Bucktanp and Mr. De ta Becue on the
concretions resembling the cow-stones in the lower greensand at these two
places ; its fossils, however, are different, and more allied to those of the
oolite ; and its position beneath the Portland stone is decisive in separating
it totally from the greensand formation. We have adopted for this stratum
the name of Portland Sand, being that suggested by Dr. Fitton, who had
ascertained its relation in the Boulonnais and in Buckinghamshire*.
This Portland sand is of sufficient importance to be marked on our map by
a distinct colour along nearly the whole extent of the base of all the escarp-
ments of Portland stone ; its mineralogical resemblance to the greensand of
Lyme may be best seen at Corton, about two miles west of Upway, where
nearly one half of its substance is made up of grains of green earth.
The following list of fossils from the Portland sand has been prepared by
Mr. James Sowerby, from specimens we collected at Black Nore and Chesil-
ton, in the Isle of Portland, and at Corton.
Black Nore.
Serpula plexus, M. C. 598. f. 1. Pecten, with concentric lamine.
Mya? (Pullastra of Phillips), only a cast. Exogyra (Gryphea) nana, M. C. 383. f. 3.
Trigonia clavellata, M. C. 87. Ammonites triplex. M. C. 292, 293.
Plicatula, a new species, occurs at Weymouth.
Chesilton.
Mya? same as at Black Nore. Exogyra nana.
Venus, only a cast. Ammonites giganteus? young, M. C. 126.
Ostrea Hemicyclus, new species.
Corton.
Lucina? a fragment. Plagiostoma rusticum? M. C, 381.
Cardium, small fragment. Ostrea, new ?
Avicula concentrica, new species, very abun- Anomia? one valve imperfect.
dant. Belemnites, fragment.
Pinna viminea, new species; found also at Ammonites giganteus? Young, or possibly 4.
Down Cliff, Bridport, in inferior oolite. Vernoni of Phillips: it is much crushed.
Pecten, with concentric lamine. Echinus spines.
The prevailing character of this stratum, along the whole line coloured on
the north side of our map, is a bed of siliceous sand and green earth. It is
also sandy and full of green earth at the village of Chesil; but at the base of
the high west cliff of Portland, under the promontory of Black Nore, where
it attains a thickness of eighty feet}, it is mixed with marl, and exhibits
subordinate concretions, and beds of sandy marl and sandstone, both contain-
ing the same fossils that are found at Chesilton and Corton. Its lowest beds
become more argillaceous as they approach nearer to the subjacent Kim-
* See Phil. Mag. and Ann., May 1827, vol. i. p. 139. t+ See Pl. III. fig. 1 & 3.
Geology of the Neighbourhood of Weymouth, &c. 2)
meridge clay ; it seems to form a connecting link between the Portland stone
and Kimmeridge clay ; and, as has been observed by Mr. Conybeare™*, is pro-
bably identical with the beds of sand and green earth, full of large boulder-
shaped semi-calcareous concretions, that occur in Shotover Hill, near Oxford,
between Kimmeridge clay and the imperfect upper calcareous Portland beds,
which extend from Shotover to Brill and Thame and Aylesbury, and which
also are occasionally much loaded with grains of green earth. Dr. Fitton
has recognised this sand beneath the calcareous Portland beds at Whitchurch
in Bucks: it occurs also in the same position in the Quainton Hills; and
Mr. Lonsdale considers the sand which forms the escarpment close on the
north and west of the town of Swindon to be also identical with this Portland
sand ; the calcareous or upper Portland beds occur also beneath and a little
to the east of that town. In the Boulonnois, Dr. Fitton describes this forma-
tion as consisting of calcareous concretions of great size, as in Oxfordshire
and Bucks, abounding in petrifactions, and imbedded in yellowish somewhat
ferruginous sand ; between Gris-nez and Audreselles the shore is covered
with these enormous masses fallen from the sand f.
Kimmeridge Clay.
The general character and fossils of this formation have been already
described by Conybeare and Phillips. It is chiefly composed of beds of slaty
bituminous clay, interspersed with Septaria and beds of bituminous marlstone.
Near its middle region, in Ringstead Bay, it contains thin beds of marly
sandstone, full of well preserved organic remains, and through its whole
extent it is loaded with deltoid oysters, which are well known to be its most
characteristic shell in England ; it contains also the Gryphea Virgula, which
is considered characteristic of this formation in France, and abounds in it at
Shotover near Oxford.
Mr. James Sowerby has prepared the following list of fossils from this
marly sandstone in Ringstead Bay.
A carinated Serpula. Pinna granulata? a small fragment, M. C. 347.
Mya depressa, M. C. 418. Ostrea deltoidea, M. C. 148.
Pholadomya, near Ph. obtusa. Terebratula inconstans, M. C. 277. f. 3, 4.
Venus? Pleurotomaria reticulata (Trochus), M. C. 272.
Cardium ? eae
Trigonia elongata, M. C. 431. Ammonites, species between 4. decipiens and
Modiola bipartita, M. C. 210. f. 3, 4. A. mutabilis.
, a small boring species. Ammonites rotundus, M. C. 298. f. 3.
* Outlines of the Geology of England and Wales, pp. 166, 173, &c.
+ Philosophical Magazine, 1827, New Series, vol. i. p. 139.
22 Prof. Buckianp and Mr. De ta Becue on the
On the opposite side of the Channel the Kimmeridge clay occupies the
cliffs of Havre and Honfleur, where it lies next beneath the greensand, and it
has been further identified by M. Elie de Beaumont, and by M. de Dufrénoy
in the South of France. This formation exhibits its best sections and highest
elevation near the east extremity of our district in the cliffs of Ringstead Bay
and Osmington, where it attains a thickness of about 300 feet.
From Osmington Cliff it continues westward, without interruption, through
Preston and Upway Street to Abbotsbury, forming the narrow north belt of
clay which we have named from the village of Upway Street. Great part of
this belt is marked by a valley parallel and subjacent to the ridge of Portland
stone above described, and dividing it from the ridge of Oxford oolite which
forms its southern frontier: this belt of clay terminates suddenly about one
mile west of Abbotsbury. In the Vale of Bredy, the covered state of the
country renders it almost impossible to distinguish the Kimmeridge clay
among the different clay beds that occupy a large part of its surface ; but we
have identified it at Litton Cheney, immediately on the south of that village,
containing the Gryphea Virgula.
The southern belt of Kimmeridge clay near Weymouth, occupies a very
small portion of the surface, constituting a triangular area, the base of which
extends about a mile from Sandsfoot Castle westward, to the Chesil Bank,
whilst its apex is at Portland Ferry : but although so small a portion of this
belt of clay is here visible on the surface, we have evidence of its submarine
continuation from hence to Portland Island, in the clay bottom of the excel-
lent anchorage of Portland Road, beyond which also it appears above the
level of the sea in the base of the escarpment at the north extremity of the
Isle of Portland, and along its west shore also immediately south of the village
of Chesilton. Hence it is clear that the Kimmeridge clay forms the fundamental
stratum of the whole island, separated, as we have shown, from the Portland
stone by the Portland sand and sandstone last described. The rapid dip
of all these strata towards the south, causes the Kimmeridge formations to
sink below the level of the sea in the southern portion of the island; whilst
that part of its western coast, whose base is composed of these perishable
sands and clays, is defended from the tremendous south-western waves by a
natural breakwater of enormous masses of Portland stone that have fallen
from the summit, and form a barrier against any further encroachments *.
At a point near Portland Ferry, extending over many yards of the shore,
Dr. Buckland remembers to have seen, several years ago, a portion of Kim-
* See Plate III. fig. 3.
Geology of the Neighbourhood of Weymouth, &c. 23
meridge clay, which is now covered up with sand, and which at that time
presented the appearance of slate burnt to the condition of red tiles ; we
have now strong reason to presume that such combustion may have taken
place, since we have at this moment before our eyes the pseudovolcanic phe-
nomena that are exhibiting themselves in the same stratum of Kimmeridge
clay near the east extremity of Ringstead Bay, at Holworth Cliff, adjacent to
the promontory of White Nore. This pseudovolcanic combustion began in
September 1826, and during a period of many months emitted considerable
volumes of flame, probably originating in the heat produced by the decompo-
sition of the iron pyrites with which this shale occasionally abounds ; in the
same manner as in the year 1755, a spontaneous combustion arose and con-
tinued during several years in the bituminous shale-beds of the lias in the
cliffs at Charmouth ;—we have a description of this circumstance in the Che-
mical Essays of Bishop Watson : it is probable that in each case rain-water
acting on iron pyrites has set fire to the bituminous shale ; thus ignited, it has
gone on burning at Holworth unto the present hour, and may still continue
smouldering for a long series of years, the bitumen being here so abundant
in some strata of the shale, that it is burnt as fuel in the adjoining cottages ;
the same bituminous shale is used as fuel in the village of Kimmeridge, and
is there called Kimmeridge coal.
This pseudovolcano at Holworth commenced in the face of the cliffs about
twenty feet above the sea; its combustion was proceeding feebly when we
saw it in September 1829, and it emitted no flame ; there was no appearance
of any crater, nor has there ever been any kind of explosion. The extent of
the surface of clay which has been burnt does not exceed fifty feet square.
Within this space are many small fumaroles that exhale bituminous and sul-
phureous vapours, and some of which are lined with a thin sublimation of
sulphur ; much of the shale near the central parts has undergone a perfect
fusion, and is converted to a cellular slag. In the parts adjacent to this
ignited portion of the cliff, where the effect of fire has been less intense, the
shale is simply baked and reduced to the condition of red tiles, like that on
the shore near Portland Ferry. Should a similar ignition ever take place in
the cliffs at Kimmeridge, which are so much more abundantly impregnated
with bitumen, the fire may be propagated there for centuries, until the whole
of the bitumen is consumed.
Coralline or Oxford Oolite, and Calcareous Grit.
The general thickness of this formation near Weymouth is about 150 feet.
It contains beds of oolitic limestone resembling the oolite of Heddington,
o4 Prof. Buckianp and Mr. De ta Becue on the
Calne, and Scarborough, and in the sandy beds of its lower region, the same
huge semi-calcareous concretions that occur in the calcareous grit of Wilts
and Oxon. The corals which abound in this formation, in the two last-
named counties, and which there give it the name of Coral Rag, are rare on
the coast of Dorsetshire, just as reefs of modern corals occur at unconnected
intervals in our modern tropical seas. In the Annals of Philosophy * Prof.
Sedgwick has published a list of the beds composing the cliffs between
Portland Ferry and Weymouth Harbour, and of the principal organic
remains which they contain: he divides the whole series into nine groups,
which, in the following section, we have subdivided further into thirty-one
beds, included between the Kimmeridge clay at the top, and the Oxford clay
at the bottom, of the whole series.
Section between Portland Ferry and Weymouth.—(Order descending.)
1. Considerable thickness of Kimmeridge clay, 9. Grit bed,—Trigonize and Melania Hed-
containing an abundance of the Ostrea dingtoniensis abundant.
deltoidea. At about fifteen feet above 10. Grit bed,—Trigoniz abundant: the Tri-
No. 2, clay iron-stone two feet thick—
partly in nodules.
goniz fill more than half of the beds
Nos. 7, 8, 9, & 10.
2. Brownish red bed, about six feet—lime- 11. Grey marl.
stone with small vesicles at top, gritty at 12. More compact grit—few shells.
bottom—cylindrical and round concre- 13. Same as No. 10.
tions of iron—contains deltoid oysters,
Serpule, Pectines, Belemnites, and lig-
. Grit.
. Grit, with Melaniz.
nite. 16. Grey marl, about four feet.
8. Grey grit, full of concretions resembling 17. Sandy bed.
the stalks of Alcyonia, and crossing one 18. Limestone full of broken shells.
another horizontally like a mass of en- 19. Grit.
tangled and inosculating roots; the ex- 20. Dark grey sandy clay, four or five feet.
posed surface is ferruginous. 21. Light brown oolite,—jointed Ammonite
4. Grey marl-clay. —Joints filled by hornstone. 4mm. ver-
5. Ferruginous bed, with eagle-stones: at tebralis ?
first about one foot thick, afterwards 22. Grey marl, five feet.
swells out considerably under Sandsfoot 23. Oolite, three feet—marl parting.
Castle. Lima rudis? abundant. 24. Oolite, one foot.
6. Sandy grey and green marl—contains a 25. Gritty marlstone.
continuous bed of deltoid oysters—also 26. Grey marlstone and marl, tending to con-
lignite. cretions, twenty-five feet.
7. Grit bed,—brown grey, Aleyonium-shaped 27. Fox-coloured sands, twelve feet.
concretions —Trigoniz abundant—one 28. Grey marl, twenty feet.
foot. Clay parting. 29. Alternations of calcareous grit and marls,
. Grit bed,—Trigoniz abundant; clay part-
ing.
eighteen feet ;—Pectines, oysters, Nau-
tii, Trigoniz, Serpule.
* Annals of Philosophy, May 1826, p. 346.
Geology of the Neighbourhood of Weymouth, &c. 25
$0. Oolitic grit, —Trochus, Pecten—three beds stems of Alcyonia. Prof. Sedgwick has
alternating with marl. shown the resemblance of these beds to
31. Brown, reddish grit—oysters abundant,— those of the same formation near Filey
Pectines, Ammonites, Gryphea dilatata, Bridge and Scarborough Castle, where
G. bullata? Trigonie. the sandstone is similarly aggregated into
32. Yellow brown. sandy grit, forty feet,— irregularly branching cylindrical concre-
Gryphea dilatata, oysters, sharp-keeled tions.
Ammonite, other Ammonites, Pectines, 33. Oxford clay, abounding in Gryphea dila-
Nautili: the hard beds contain concre- tata.
tions resembling a mass of entangled
It appears from this section, that the Oxford oolite formation is composed
of alternations of imperfectly oolitic limestone and calcareous grit, with nume-
rous partings of clay. The superior beds are loose and sandy, and may be
considered analogous to the upper calcareous grit in Yorkshire, described by
Mr. Phillips; they are best seen near Sandsfoot Castle, where the uppermost
of them contain deltoid oysters, and become gradually more argillaceous until
they pass into Kimmeridge clay : the central beds are the most oolitic, some-
times loose and sandy, and at other times compact and in continuous beds: they
are most oolitic at the village of Wyke Regis and in the cliffs near Osmington,
at both which places they afford a light-coloured building-stone, which, but
for the vicinity of Portland, might have been applied to purposes of architec-
ture. In the cliffs west of Wyke Regis, they show the same oblique cleavage
which isso common in oolitic strata. Thus = —
M. Boblaye, in his paper on the Jura . oe 0 SOS
Formation in the North of France*, no-
tices that in the great oolitic quarries of Ballon near Stenay, lines of false
division cross the true stratification at angles of 45° or 50°. Examples of the
same kind are seen in the Oxford oolite quarries at Heddington, and in the
forest marble and great oolite along the road from Cirencester to Bath ;
similar parting occur also in the new red sandstone at Bridgenorth, but in
a manner much more complicated, and crossing the true strata in all possible
directions.
Beneath these central oolitic beds, strata of semi-calcareous sand and cal-
careous grit prevail, and display alternations of sand and sandy loam, with
continuous beds of calcareous grit and beds of large concretions lodged in
strata of sand. The entire thickness of these calcareous grit beds with their
largest concretions, is best exhibited in Ham Cliff, about three miles north-
east of Weymouth}. In the hill immediately on the west of Weymouth, the
* Ann. des Scien. Nat., Mai 1829. + See Plate II. fig. 8.
VOL. IV. SECOND SERIES. E
26 Prof. Buckianp and Mr. De 1a Becue on the
sandy loam beds of this formation afford an useful brick earth. The passage
of the lowest strata into Oxford clay is indicated by the presence of the Gry-
phea dilatata in the beds of grit, and this passage is analogous to that which
occurs at Heddington Hill near Oxford; but the presence of an upper cal-
careous grit and gradual passage of the superior strata at Weymouth into
Kimmeridge clay, show a more perfect development of this part of the oolite
formation in Dorset than in Oxfordshire. In the sections at Heddington the
upper grit is wanting, and the Kimmeridge clay reposes immediately on
the oolitic building-stone: the surface of this stone is also guttered over and
furrowed with water-worn cavities and small rock-basins, marking a destruc-
tive action of the sea before the deposition of the Kimmeridge clay : this
water-worn surface of the oolite is also decomposed and become rusty to the
depth of about a foot, in a manner unusual where the series of depositions
has been regularly continuous, and its decomposition seems to have resulted
from long exposure to water before the laying on of the Kimmeridge clay.
These circumstances are duly noticed by Conybeare and Phillips *.
All the beds of the Oxford oolite formation near Weymouth are loaded
with shells similar to those found in the same formation in Wiltshire, Oxford-
* Outlines of the Geology of England and Wales, p. 189, note.
Prof. Sedgwick, in his comparison of the appearance of the coral rag formation near Scar-
borough and Weymouth with that of Oxford (Ann, of Phil., May 1826), conjectures that the
upper portions of the Scarborough and Weymouth sections may be wanting near Oxford, and that
the coral rag and freestone of Heddington together, represent the central group of the Weymouth
and Steeple Ashton sections: thus, at its two extremities in the coast of Dorset and Yorkshire,
the superior members of this formation are most fully developed, whilst they are wanting, and
have been apparently removed from the central part of their range near Oxford. We entirely
agree with Prof. Sedgwick in these remarks, and in the consequences which he draws as to
the imperfection of the type of this formation near Oxford: the whole of this subject has
been fully illustrated by Mr. Phillips in his excellent work on the Coast of Yorkshire, and still
more recently by Mr. Lonsdale in his valuable paper on the Oolite District near Bath (Geol,
Trans. vol. ui. Part II. p. 262), in which he gives a section of the Oxford oolite formation at
Highworth, where the upper members are represented by about seven feet of alternating beds of
sand and rubbly oolite, or oolitic calcareous grit: he also shows that near Steeple Ashton the
superior beds appear under the form of ten feet of sand, resting on ten feet of ferruginous clay
interspersed with oolitic grains of hydrate of iron. Some bones of a Plesiosaurus have been found
in this clay by Mr. Mead.
According to M. de Caumont, a similar alternation of strata of sand and calcareous sandstone,
with beds of clay and of imperfect oolitic limestone, affords, on the coast of Normandy, a group
corresponding with the upper calcareous grits of Weymouth and the coast of Yorkshire, interposed
between the Kimmeridge clay and the coral rag. (See M. de Caumont’s Sectional Lists of the
Clif at Hennequeville; of the Hill of Glos near Lisieux ; and of St. Julien-sur-Calone near Pont
VEvéque. pp. 113, 114, 115.)
,
Geology of the Neighbourhood of Weymouth, &c. i
shire, and Yorkshire. The T'rigonia clavellata and Melania Heddingtoniensis
are among the most abundant.
Another feature which is wanting in Oxfordshire, is the highly ferruginous
character which this oolitic formation assumes near Weymouth, particularly
in its upper beds immediately below the Kimmeridge clay; the same fer-
ruginous character prevails also in other parts of its course through this
district, and very remarkably in the hills near Abbotsbury. In a ravine called
the Red Lane, immediately north of that village, the oolitic grains are com-
posed of a rich hydrate of iron, which, if the country afforded fuel, might
be wrought as an ore of the same quality with that which supplies so many
iron-foundries in France, from a similar granular ore in the oolite formation.
The extent of surface occupied by the Oxford oolite and its subordinate
grits in the valley of Weymouth, will best be seen on the Map ; it forms two
parallel belts of unequal breadth and length, subjacent to the two beds of
Kimmeridge clay before described, and reposing on two other parallel belts
of Oxford clay ; these oolitic belts terminate in two ridges, overhanging the
Oxford clay, with two escarpments that face towards each other ; the most
southerly of them extends nearly two miles west, from the town of Weymouth
to the Fleet at Linch, and is about one mile broad; the northern ridge and
its escarpment occupies a length of twelve miles, from the cliffs of Osmington
to the sea at Abbotsbury, terminating in an escarpment towards the south,
which presents its highest inland elevation in Linton Hill near Abbotsbury.
In no part of its course does it much exceed half a mile in breadth, excepting
at its western termination near Abbotsbury, where it widens to about a mile,
from the effect of the great fault hereafter to be described ; here also it
changes its dip from north, first to east, and then to south, bending round and
enlarging itself like the bowl of a spoon, whose handle is represented by the
long ridge of Linton Hill, just mentioned. ‘The towers of St. Catherine’s
Chapel at Abbotsbury, and of Wyke Regis Church, are two remarkable land-
marks, placed respectively near the western termination of the northern and
southern belts of oolite just described, and serve as points by which their
course may be recognised from the Dorchester road and hills adjacent to it
near Weymouth. In the Vale of Bredy, the oolite occurs only in a very
narrow band, extending about a mile from east to west, from Kingston House
to the village of Litton Cheney ; it is seen only in a few old quarries near
these two places, and in a hollow way at Litton Cheney, where it appears
much disturbed by a fault, and brought, as at Abbotsbury, almost into close
contact with the base of the escarpment of the chalk.
E 2
28 Prof. BuckLanp and Mr. De 1a Becue on the
Oxford Clay.
The Oxford clay in this district attains a thickness of about 300 feet, and
reposes immediately, and with conformable dip, on the central arch of corn-
brash and forest marble; on the south side of this arch it forms a belt of low
ground about a mile broad, extending from Melcombe Regis and Weymouth
Bay to East Fleet. It winds round the eastern extremity of the forest marble
at the Barracks, and the marsh of Lodmoor, and thence extends westward
along the north side of the central arch, forming a valley of less than half a
mile in width, to the Decoy and Swanery at Abbotsbury, where it terminates
in the Chesil Bank, Its eastern termination is seen in the lowest strata
at the base of Jordon Hill and Ham Cliff, about three miles north-east of
Weymouth *.
A distinct section of this stratum occurs in a low cliff under the Barracks
at Radipole, where it dips south at about 20°, and where, till lately, it pre-
sented, at low water, a pavement of large and beautiful Septaria, known pro-
vincially by the name of Turtle Stones. The veins of these Septaria are filled
with yellow semi-transparent calcareous spar, often passing into a rich deep
brown colour: their beauty, when polished, has, within these few years,
caused the greater part of them to be taken up and manufactured into slabs
and tables.
In this same section at Radipole Barracks large Ammonites and other
shells abound. The most characteristic shell is the Gryphaa dilatata, which
is as universally abundant in the Oxford clay throughout this district, as the
deltoid oyster is in the Kimmeridge clay. In consequence of the want of
sections, we have not attempted to trace the minute details of this clay in its
windings through the Vale of Bredy, in which it forms a marginal band round
the eastern and northern frontier of the forest marble. On the opposite coast
of Normandy this same Oxford clay occurs at Vaches Noires, and abounds
with the Gryph@a dilatata, and many other fossil shells.
Forest Marble.
The formations, which, for convenience of description we have united
under the name of Forest marble, and which are the lowest that occur in the
Vale of Weymouth, admit of a three-fold division ;—1. Cornbrash; 2. Forest
marble ; 3. Clay, and marlstone.
1, The uppermost region, or cornbrash, is composed of a loose rubbly
limestone, alternating with thin beds of clay and marl, and is so absolutely
* See Plate II. fig. 8.
Geology of the Neighbourhood of Weymouth, &c. 29
identical, both in its mineral characters and abundant organic remains, with
the cornbrash of Wiltshire, that no further description need be given of it
than may be found in Conybeare and Phillips’s account of Cornbrash*.
2. The middle region, consisting of the usual well-known varieties of forest
marble, sometimes constituting thick beds of stone composed of comminuted
shells, at other times passing into oolitic and sandy slate. The most perfect
condition of this forest marble is exhibited in the quarries of Bothenhampton,
one mile south of Bridport, where it contains that remarkable fossil the Brad-
ford Encrinite, Apiocrinites rotundus, together with fragments of Pentacrinite,
palates of fish, and fragments of lignite, all imbedded in indurated masses of
broken shells; it contains also the same Apiocrinite in the under-cliff between
Abbotsbury Castle and the sea, and in the cliffs immediately west of Bridport
Harbour.
3. The lower region is composed principally of strata of blue clay and grey
marl and marlstone, containing subordinate beds of imperfect stone.
The best section of this grey marl is seen in the cliff at Watton Hill, close
on the west of Bridport Harbour, attaining a thickness of about 150 feet ; it
is here capped by an outlying summit of forest marble, being the extreme
south-western termination of this rock on the coast of England+. The base
of this marl reposes on the sands of the inferior oolite. This grey marl also
forms a cap on the summit of the inferior oolite in Burton Cliff, on the east
of Bridport Harbour: it may probably be the equivalent of the Fuller's
earth in the vicinity of Bath. The predominating character of these three
deposits, which we have grouped together as forest marble, is clay; the
amount of their united thickness may be about 400 feet.
The extent of this forest marble formation in the Vale of Weymouth is con-
siderable ; it occupies a tract near six miles long, and from two to three miles
broad, constituting the lowest strata and central belt of that district. This
central belt emerges at Radipole from beneath the Oxford clay, and is less
elevated than the parallel belts of Oxford oolite and Portland stone, whose
escarpments overhang it on the north and south, rising towards each other as
if they once had been continuous, and had been separated by the elevation of
the central axis of forest marble, over which, if reunited, they would form a
continuous ridge. It is not of sufficient importance to trace separately the
extent of the individual beds of cornbrash and forest marble throughout this
central belt. The cornbrash occupies the uppermost place along the lines of
its junction with the Oxford clay, and occurs also on many summits and minor
* Outlines of the Geology of England, p. 202. + See Plate II. fig. 13 and 14.
30 Prof. Bucktann and Mr. De ta Becue on the
hills within its area. The valleys are usually cut down to the slaty forest
marble beds and their associated clays.
On the north, and east, and south, it is entirely surrounded by, and dips
beneath, the Oxford clay ; on the west it is terminated by the back-water of
the Fleet, cutting it in an oblique line for about four miles, from the village
of East Fleet to the Swanery of Abbotsbury. It has been already stated,
that it constitutes the axis or central arch of the Weymouth district, upon
each side of which, as on a saddle, all the more recent formations successively
repose.
After a slight depression beneath the surface at Abbotsbury, the forest
marble and its clays, or in most cases the clays without the marble, reappear
in strength in the Vale of Bredy, occupying an extent of surface about eight
miles long and four miles broad ; bounded en the east and north by the over-
hanging escarpments of chalk and greensand ; on the south by the sea and
Chesil Bank, and on the west by the subjacent strata of inferior oolite near
Burton Bradstock and Bridport. Throughout all this Vale of Bredy, the main
dip of this strata is towards the north.
Inferior Oolite.
Along the whole coast of Dorset, and indeed the whole south coast of En-
gland, there is a total absence of Bath oolite ; but the inferior oolite occurs in
the vicinity of Bridport, attaining a thickness of about 300 feet, and occupying
the cliffs for two miles east, aud three miles west, of Bridport Harbour. The
summits of the highest hills around the town are composed of the superior
strata of this formation, consisting of coarsely oolitic yellow limestone, resem-
bling that of Dundry Hill near Bristol, irregularly interspersed with oolitic
grains of hydrate of iron, as at Bayeux in Normandy : the most extensive
quarries in these upper strata of the inferior oolite, are at the summit of
Chideock Hill, on the west of Bridport ; these are wrought in a light brown
limestone full of large and small ferruginous grains ; a few beds also abound in
minute veins and cells lined with hydrate of iron. One stratum on this hill is in
great measure composed of fragments of Pentacrinite, others contain a variety
of organic remains,—Ammonites, Nautili, Belemnites, several Pectens, a large
Lima, Cucullea, Plagiostoma, Modiola, several species of Terebratula, and
fossil wood™.
Beneath this coarse limestone is a series of brown and yellow Joam and
sands, highly micaceous, and containing, in their upper region, strata of cal-
* The oolite of Chideock Hill contains caverns, but no bones have yet been noticed in them ;
in the same oolite beds at Burton Cliff, there are inaccessible fissures filled with diluvium.
Geology of the Neighbourhood of Weymouth, &c. 31
careo-siliceous sandstone, and in the lower region interrupted strata of large
concretions of coarse sandstone; the lowest strata of this formation become
gradually more blue and marly, and at length pass imsensibly into the upper
marl beds of the lias.
We observed a remarkable fact in some stony masses from the middle
region of the inferior oolite at Down Cliff on the west of Bridport, namely,
that some of these masses contained an oolitic breccia or conglomerate of
rolled fragments of coarse oolite, not differing in character from the strata of
which they form a part. The fragments in this breccia are not concretions,
but afford unequivocal evidence of having been rolled by water, in the fact
that many of them are perforated on all sides by the holes of small Lithodomi,
of which holes the lower extremities alone remain, their tops having been
worn away by the attrition which has reduced the fragments in which they
occur to the state of large subangular pebbles; these fragments must have
lain loose in the sea at the time when the Lithodomi perforated their surface,
for one side only could have been perforated before they were detached from
their native rock ; and the perforation of the lower side at least, if not of the
other sides, must have taken place in a period intermediate between such
separation and the completion of that moderate degree of rounding which
they have since undergone. We see at this time on the ledges of the shore
at Lyme, between high and low water mark, loose angular slabs of lias
recently torn from the subjacent strata, and perforated on all sides by boring
Mollusc, after the manner of the fragments in our oolitic breccia. This
perforated breccia at Down Cliff shows a lapse of time to have intervened, in
which there was apparently a suspension of the deposition of the inferior
oolite ; a time in which fragments were torn by the waters from the earlier
beds and became inhabited by Lithodomi, and subsequently rolled on the
shores, or at the bottom of the then existing seas ; they further show that the
lower strata of the inferior oolite were at once consolidated to the condition
of stone, hard enough to protect Lithodomi and to be rolled to pebbles, before
the upper strata of this same inferior oolite formation had been laid over them.
Lias.
The western extremity of our Map includes the upper marl beds only of the
lias formation ; these are exposed at the bottom of the valleys of denudation
round Golden Cap Hill, and on the sea-shore along its base : they are cha-
racterized by enormous deposits of Belemnites, and correspond with the Cal-
caire & Belemnite of the French geologists, as the lower and more stony beds
of lias at Lyme agree with the French Calcaire a Gryphite. One bed at the
ae Prof. Bucktanp and Mr. De ta Becue on the
base of Golden Cap presents an almost continuous pavement of Belemnites,
running for some distance along the shore; these marl beds also contain the
remains of Saurians. A detailed description of this lias formation at Lyme
having been published by Mr. De la Beche*, we deem it sufficient to refer
our readers to that paper.
VALE OF BREDY.
We have already pointed out details of the leading formations of the Vale
of Bredy in our description of the westward terminations of the strata that
occur in the Vale of Weymouth; we here sum them up in a few words. The
structure of the Vale of Bredy is much less complicated than that of the Vale
of Weymouth ; its strata do not, as there, dip in opposite directions from an
anticlinal line, but emerge regularly from beneath the chalk and greensand
escarpments of its eastern and northern frontiers, rising to the west and
south, until at their western termination they rest on the inferior oolite of
Burton Cliff and the hills near Bridport.
Around the eastern and northern frontiers, the greensand constitutes a sub-
escarpment to the chalk, and also forms the outlying summits of Abbotsbury
Castle, Swyre Knoll, Shipton Beacon, and Hammerdon Hill already men-
tioned : its southern frontier next the sea, is composed of forest marble and
thick beds of clay connected with it; its middle region also (constituting the
bed of the river Bredy,) is made up of these same clays, interspersed occa-
sionally with thin stony beds of forest marble. The entire face of this Vale of
Bredy is so destitute of roads and sections, and so covered up with grass from
the bottom of the valley to the escarpment of the hills, that it is extremely
dificult to trace the separation between these extensive clay beds of the
forest marble formation, and those which may be made up of the continua-
tions of Kimmeridge and Oxford clays, interposed between the forest marble
and the greensand.
EFFECTS OF DISTURBING FORCES.
Having thus far considered the character and extent of each formation which
occurs on the coast of Dorset, it remains only to examine the effects that have
been produced on them by disturbing forces: these may be divided into five
heads; namely,—1J. Elevation ;—2. Depression ;—3. Contortion ;—4. Faults ;
—5}5. Denudation.
I. Evevation.
The most important feature which pervades the whole Vale of Weymouth
* Geol. Trans. Second Series, vol. ii. Part I. p. 21. Plate II.
Geology of the Neighbourhood of Weymouth, &c. 33
is, the arch-like disposition of all the formations it contains ; the axis of this
arch passes east and west from Weymouth Bay to the Chesil Bank, forming
an anticlinal line, on each side of which all the successive strata dip respec-
tively to the north and south. This dip of the strata in opposite directions
from the anticlinal line, is represented in the general section, Plate ITI. fig. 1.
It affords, on a larger scale, an example of the same kind of valleys of eleva-
tion with those which have been described by Professor Buckland*. 'The
details of these arched strata in the Vale of Weymouth have already been
sufficiently set forth. We think there is evidence enough to show that the
strata were once nearly continuous and horizontal, and have been elevated
to their present position by a force acting from beneath in a line nearly east
and west, forming a continuation of the same line of elevation that extends
through Purbeck and the Isle of Wight, and parallel to that of the axis of
elevation of the Weald of Sussex and Kent. The period of elevation in all
these cases was apparently the same, viz. subsequent to the deposition of the
London clay, if not of the most recent tertiary strata in the Isle of Wight.
With respect to the analogous axis of elevation, which extends with
certain interruptions from the eastern extremity of the Mendip Hills along
the coast of South Wales to Milford Haven, it has been shown by Dr. Buck-
land and Mr. Conybeare that this elevation took place before the deposition
of the new red sandstone formation +; the direction of this line deviates from
east and west several points towards the north-west.
In these comparatively small instances, as in the elevation of the highest
mountains in the world, noticed by M. Elie de Beaumont{, it seems that
the operating forces have been exerted usually in straight lines, and that these
straight lies were often parallel to one another; and the fact that the
greatest mountain chains are for the most part thus disposed, more especially
those which are volcanic, as in the case of the Andes, leads us to refer the
elevation of them all to one and the same common cause,—namely, the expan-
sion of elastic vapours bursting upwards in longitudinal cracks along the lines
where the least resistance was presented by the incumbent strata§. The
comparative insignificance of the elevations we are considering in the South
of England, makes no difference in the principles we would apply to explain
their origin ; they appear to us to be faithful models, representing on a smaller
* Geol. Trans. Second Series, vol. ii. Part I. p. 119. + Ibid. vol. i. p. 210, et seq.
{ Annales des Sciences Naturelles, 1829—1830.
§ The movement of modern earthquakes along straight lines, added to the frequent rectilinear
ii of volcanic chains, adds still further probability to these conjectures.—See Hall’s South
merica.
VOL. IV.—SECOND SERIES. y
34 Prof. Bucktanp and Mr. De ta BeEcueE on the
scale, the self-same phenomena, which, in more gigantic magnitude, pervade
the highest Alps.
In the eastern part of our Weymouth district, we have examples of valleys
of elevation, on a small scale, in the three little circus-shaped valleys of
Moignes Down, Poxwell, and Sutton Pointz*. All these three valleys are of
an elongated oval shape, and so nearly resemble the interior of a Roman
circus, that if the basset ends of the strata were cut into benches, the central
area would be visible to persons seated on every part of them.
These three small valleys of elevation are on the same straight line, running
east and west, parallel to the grand axis of the Weymouth district, and also
parallel to two great faults adjacent to them, and immediately to be described +.
The western extremity of the first valley touches the eastern extremity of the
second, and the second is separated from the third, only for a small space, by a
ridge of Portland stone: each of these valleys has only one small lateral outlet
for the discharge of its waters ; the area of the Moignes Down Circus scarcely
descends below the Portland stone: those of the Poxwell Circus and Sutton
Pointz Circus descend into the Portland sand and Kimmeridge clay.
In the circus of Moignes Down and of Poxwell, the circumference is chiefly
composed of the basset edges of strata of Portland stone dipping outwards in
every direction ; but the circus of Sutton Pointz, which is much longer and
wider than the other two, is surrounded by Portland stone on three sides only,
the remaining north side being partially occupied by greensand and chalk,
in consequence of its being intersected by the great Ridgeway faultt.
Although the elevation of these circus-shaped valleys must have produced
vast piles of fractured strata on the line of elevation, there is no accumulation
of such fragments, nor any perceptible quantity of gravel of any kind within
their area; the clearing out of all the rubbish which must have encumbered
them at the time of their elevation, can only be referred to the contempo-
raneous or subsequent operations of very powerful denudation.
II. Depression.
Elevations of strata, such as we have been tracing, can scarcely have
arisen without simultaneous depressions in the spaces intermediate between
* See Plate II. fig. 2, 3, 4. + See Map, Plate I.
+ The circus-like inclosure of the Valley of Sutton Pointz is best seen from its eastern extremity
at the top of Osmington Hill, at a point on the old road near the western extremity of the Poxwell
Circus ; the new turnpike road from Poxwell to Osmington, enters the Poxwell Circus by the
outlet on its north side, and crossing its shorter diameter, cuts through the Portland stone on its
south side, and there enters upon the Purbeck beds, reposing on the back of the Portland stone,
and dipping towards Upton. See Plate II. fig. 3.
Geology of the Neighbourhood of Weymouth, &c. 35
the lines of elevation ; and accordingly our district affords examples of troughs
and depressions thus produced in the case of the Purbeck beds lying upon a
trough of Portland stone at Upway, and of Kimmeridge clay in a trough of
Oxford oolite at Abbotsbury *.
ILI. Conrortion.
At Upway in the quarries west of the Church, we have examples of con-
tortion produced by the elevation of the strata, similar to those represented
by Mr. Webster in his drawings of Lulworth Cove and the coves adjacent to
it, in the Isle of Purbeck. Throughout the whole Weymouth district, and
particularly along the lines of fault, which we shall next describe, contortions
of greater or less amount are too numerous to require individual speci-
fication.
IV. Fautrs.
In a district which has been so much dislocated, the elevations and depres-
sions just described lead us to expect still further disturbances in the occur-
rence of faults; and accordingly we find two very extensive faults on the
northern and north-eastern frontier of the Vale of Weymouth, and also two
others on the north-west of the Vale of Bredy and near Bridport, besides
many minor local fractures.
The two great faults in the Vale of Weymouth, run nearly in a straight
line from east to west, parallel to the general axis of elevation of the whole
district, and were probably produced by the same forces and at the same time
with this general elevation.
We shall call the most northerly of them the great Ridgeway Fault, the
other the Osmington Fault. Wherever we examine these faults, we find
double evidence of the movement that has taken place ; Ist, In the non-
accordance of the strata that form the opposite sides of the faults ; 2ndly, In
the fine parallel lines and vertical furrows resembling the lines and grooves
on Slikensides, and often also in the highly polished surfaces of the materials
that form the side walls of the fault, showing that these ponderous masses
have ground each other with prodigious violence in the act of separation and
movement from their original position. The great Ridgeway fault is an
upcast fault, elevating, on its south side, into contact with the escarpment of
the chalk strata that would otherwise have dipped beneath it, particularly the
Portland stone, nearly along the whole line which this fault traverses. The
Osmington fault is a downcast fault, throwing down, on its south side, strata
* See Plate II. fig. 1, 6.
F2
36 Prof. Bucktanp and Mr. De ta Becue on the
of chalk, greensand, and Portland stone, to a position lower than the strata
from whose extremities they have been snapped off*.
1. Great Ridgeway Fault.
The most important of these, the great Ridgeway fault, extends, without
interruption, nearly fifteen miles, from the eastern extremity of our district at
Moignes Down, to the sea near Abbotsbury, passing along the great escarp-
ment of the chalk at various elevations, from the top to the bottom of it; the
Osmington fault we could trace only about three miles, from South Holworth
near White Nore, to Ham Cliff on the north-east of Weymouth.
The first or great Ridgeway fault is one of the most curious and important
we have ever seen, in consequence of the variety of instructive sections
afforded along its course; these sections we shall describe in the order of
their occurrence, beginning at the eastern extremity f. The fault emerges
from the chalk formation at Moignes Down Farm, on the north side of the
circus of Moignes Down, and brings the truncated lower ends of strata of
Portland stone into contact with the truncated upper ends of strata of chalk,
both dipping to the northt. Here a valley of denudation runs exactly along
the line of fault, having its north side composed of chalk, and its south side
entirely of Portland stone. The strata have been raised on both sides of this
fault, but raised unequally ; whence it results, that on the north side the
chalk rises towards the fault, whilst on the south side the Portland stone
dips towards it, as if plunging beneath the chalk; whereas the Portland
stone has been elevated from its original position, relatively, though not
absolutely, much higher than the chalk: yet, notwithstanding this fracture
of the strata and dissimilarity of substances on the two sides of the valley,
the effect of denudation has been so equable, and the removal of the fractured
materials so total, that no other features are presented by the surface than
those of an ordinary valley of denudation on horizontal chalk.
Our next section§ is taken at Poxwell Hill, less than one mile west of
Moignes Down Farm. Here the circumstances of the fault on the north of
Poxwell Circus are similar to those at Moignes Down Farm, excepting that
at Poxwell there has been no denudation on the line of fault. Two miles
west of Poxwell in the valley of Sutton Pointz||, the exact line of the fault is
scarcely to be recognised, from the circumstance of the strata on both sides
of it being perpendicular. At fig. 5. in Sutton Valley, one mile west of
*® See Plate II. fig. 2, 3. + See Plate II. fig. 1, 2, 3, 4, 5, 6, 7, 12.
t See Plate II. fig. 2. § Plate II. fig. 3. || Plate II. fig. 4.
Geology of the Neighbourhood of Weymouth, &c. 37
fiz. 4, the Portland stone forms the south side of the fault; and greensand,
surmounted by chalk, the north side,—both dipping rapidly to the north.
The theoretical figure (Plate II. No. 12.) is intended to represent by the
dotted lines aa. bb. cc., effects that would be produced by denudation extended
to different depths along the line of a fault, traversing such strata as occur
along this part of the Ridgeway ; thus a denudation descending to aa. would
leave chalk and greensand on the north side of the valley so denuded, and
Portland stone on the south ; a denudation to bb. would give the same section
on the north side of the valley, and Portland sand on the south ; and in this
case it would be difficult to distinguish between these two sands, without the
aid of organic remains. A denudation to cc. would give again the same beds
on the north side, and Kimmeridge clay on the south: examples of all these
three theoretical representations are visible in the course of the Ridgeway
fault ; e. g. On the high crest which separates the valley of Bineombe from
that of Sutton Pointz, the Portland stone touches the chalk; the surfaces of
both rocks at the line of fault presenting a uniform appearance, and uniformly
level line, like the surface of fig. 12. Plate II. Near the north-western extre-
mity of Sutton Valley, a denudation, analogous to that represented by aa.
fig. 12. Plate II., shows the Portland stone touching greensand; a lower
point of the same denudation exhibits the Portland sand in contact with the
greensand, as represented at 5b. in the same figure; and on the north of
Sutton village the Kimmeridge clay also is brought into contact with the
greensand, as represented at cc.
At Upway, on the northern extremity of the general section, and near the
summit of the hill*, the Portland stone, covered by Purbeck beds, occupies
the south side of the fault, and nearly horizontal chalk its north side, the Pur-
beck and Portland beds rising at a high angle northwards towards the fault.
From Upway, for four miles westward, to the final termination of the Port-
land stone at Portisham, the Portland stone is continued on the south side,
and the chalk on the north side of this fault ; it is exposed by no section, but
the junction can be traced on the surface of the fields.
Near the village of Portisham, precisely at the western termination of the
Portland stone, the fault deviates to a south-western direction for about a quarter
of a mile, traversing the bottom of a deep and narrow dry valley or comb, by
which the road from Portisham leads up to Black Down; the east side of this
valley is composed of Portland stone, and the west side of chalk, both attaining
a considerable elevation above the bottom of the valley. In the village of
* Plate II. fig. 1.
38 Prof. Buckianp and Mr. De ta Becue on the
Portisham, the fault again resumes its westerly direction, and at the same time
brings up the Kimmeridge clay into immediate contact with the base of the
escarpment of the chalk; this contact continues for some distance towards
Abbotsbury. At Abbotsbury*, the Oxford oolite occupies the south side of
the fault; and greensand, resting upon clay, the north side; the two latter
are nearly horizontal, whilst the oolite rises to the north.
The irregularities of structure occasioned by this fault on the west of
Abbotsbury are considerable, and not totally made out by us. A compound
disturbance, similar to that which has produced the trough-shaped disposition
of the Purbeck and Portland stone at Upway, has caused an analogous
derangement near Abbotsbury, along a tract of about a mile in length, from
east to west, and nearly a mile in breadth+. This tract occupies the slope
and under-terrace, between the summit of Abbotsbury Common and the sea,
and is composed chiefly of ferruginous Oxford oolite, dipping regularly to-
wards the north, on that side of Abbotsbury which is nearest to the sea,
until it terminates abruptly in a hill called Zoles (immediately above the
mansion of the Countess of IIchester). In this hill it suddenly trends round,
changing its dip towards the east, and rising with an escarpment to the
west, for a short distance, until the dip again turns suddenly to the south, and
so continues along the line of fault, running east and west more than a mile
from Zoles to the town of Abbotsbury. By these three dips, the oolite is
thrown, at its termination, into the form of a spoon, rising outwards in three
directions from the lowest central line of depression, and terminated by high
escarpments on the south and west, and on the north partly by a false escarp-
mentt, and partly by abutting against the fault§.
The existence of this false escarpment (fig. 7.) is due to the agency of the
upcast fault, which has elevated, not only these Oxford oolite beds, but even
the subjacent beds of Oxford clay and forest marble irregularly along the
under-terrace, between the false escarpment of oolite, and the true south
escarpment of the lofty ridge of greensand and chalk composing Abbotsbury
Common ; so that beneath and parallel to this true escarpment, at a distance
varying from one to two furlongs, the false escarpment forms a broken under-
terrace || facing the true escarpment, with opposite dip; and between these
two escarpments a narrow band of forest marble is thrown up in great con-
fusion for about a mile, from the town of Abbotsbury west to Zoles. The
confusion is increased by land slips, which have brought down heaps of
rubbish from the greensand escarpment of Abbotsbury Common and Abbots-
* Plate II. fig. 6. + See Plate II. fig. 6 & 7. + Plate II, fig. 7.
§ Plate II. fig. 6. || See Plate II. fig. 7.
Geology of the Neighbourhood of Weymouth, &c. 39
bury Castle Hill, and spread them over the various broken beds of the oolite
formation, along the under-terrace and line of fault; and have also so com-
pletely masked and covered up all the lower beds of the true escarpment
below the greensand, that not one of them can be distinctly seen: and
although this great escarpment is at least 400 feet above the sea, none of its
lower strata are exposed to view, except a bed of clay, which, by casting out
a line of springs along its junction with the incumbent greensand, affords a
perpetual cause of the Jand slips which obscure the entire base of this escarp-
ment, and prevent our tracing distinctly the great Ridgeway fault at its
western termination into the sea*,
The depth of the dislocations occasioned by this great Ridgeway fault
along the escarpment of the chalk appears to vary to the amount of several
hundred feet.
2. Osmington Fault.
The range of the Osmington fault is east and west, and parallel to the
great Ridgeway fault we have just described, at the distance of about one
mile and a half to the south: its eastern extremity is lost in the chalk downs
near South Holworth, and its western termination is seen in Ham Cliff, three
miles north-east of Weymouth. Plate II. fig. 2% exhibits its most eastern
section at Upton Hill, in which horizontal chalk beds form the north side of
the fault, and subsided chalk, greensand, and Portland stone, the south side :
a lime-kiln excavated exactly on the line of fracture, exhibits the disposition
here represented. Ina section of the hill and water-course, one mile further
west, at Osmington Mill, the south side of this fault is formed of subsided
chalk and greensand, dipping north; and the north side formed of chalk,
resting on greensand, both inclined slightly to the south. Plate II. fig. 8.
shows the western extremity of this fault at Ham Cliff, where the Oxford
oolite on its south side has subsided to the level of the Oxford clay on its
north side.
3. Ringstead Bay Fault.
Plate I]. fig. 11. represents a third and very local small fault, produced
apparently by a fracture in the cliffs, and bringing a subsided mass of Port-
land stone and Portland sand into contact with Kimmeridge clay. This
fault is more oblique than any part of the two great faults we have been
describing ; like them it ranges east and west, but can be traced only toa
© On the north side of Abbotsbury Common, immediately below the Castle, a series of land
slips, similar to those on the south side, is indicated by a long range of narrow ponds, supported
by the bed of clay, across which the land slips have taken place. + Plate II. fig. 3.
AO Prof. Buckianp and Mr. De ta Becue on the
very short distance: the pseudovolcano we have described is in the Kim-
meridge clay which forms the base of this subsided mass.
Another minor fault is seen at Boat Cove, on the west of Osmington Mill*,
where an apparently false dip of the Oxford oolite has been produced by a
recent slip of the cliffs; it isso small and partial that it would be unworthy ~
of notice were it not that it is prominently exposed in the profile of the coast,
and gives an erroneous impression of the position of the strata in the cliff
from which it has fallen. Near this spot, also, at the cascade of Osmington
Mill, we have another small fault, exposed on the shore traversing the Oxford
oolite, and running outwards into the sea, just along the anticlinal line, where
the strata turn at this part of the coast.
4. Bothenhampton Fault.
Pl. IT. fig. 14. represents a downcast fault at Bothenhampton, one mile
south-east of Bridport. We believe that this fault was first noticed by Prof.
Sedgwick : it is of considerable depth, bringing the forest marble on its
south side into contact with inferior oolite on the north side, the forest
marble dipping at a considerable angle towards the fault; its general range,
like that of the rest, is nearly east and west, and although, from the similarity
of the clays which it intersects, we have not traced its uninterrupted con-
nexion, we think it continues eastward to Shipton Gorge, Litton Cheney, and
Long Bredy. At each of these three places, lying as they do nearly ona
straight line, there has been much dislocation and disturbance.
5. Bridport Harbour Fault.
At Pl. II. figures 13 and 14 represent the western termination of another
downcast fault in the cliffs about a mile west of Bridport Harbour, being the
last we have to mention. Its amount is considerable: on its north side are
beds of inferior oolite based on lias; on its south side are beds of forest
marble based on more than 150 feet of grey clay, and these are suddenly and
violently turned up when they come into immediate contact with the fault.
We believe this clay to be the same that occurs in such thickness in the Vale
of Bredy ; and although we have there considered it as subordinate to the
forest marble formation, we have no evidence to show that it may not also
represent the Fuller’s earth beds that occur between the great oolite and in-
ferior oolite of the neighbourhood of Bath. The eastern extremity of this
fault { presents a complicated double fracture, causing the lower beds of the
* See Plate Il. fig. 9. + See Plate II. fig. 9. + Plate II. fig. 13. a.
Geology of the Neighbourhood of Weymouth, &c. Al
grey marl and marlstone to assume a position partly vertical and partly tor-
tuous, between horizontal beds of grey marlstone on the one side, and of
inferior oolite on the other. These appearances may in part be due to sub-
sidence superadded to the fault; the point of the cliff in which they occur
is so much exposed to the action of the waves, that it may ere long be
totally removed, and the appearances represented in our section be entirely
changed.
It should be observed that not one of all these faults appears to have been
produced during the formation of the strata : not one is covered at its summit
by any overlying substance except diluvium ; and that those in the eastern
part of our district were evidently not produced until the time at which the
chalk and all the strata subjacent to it, in this district, underwent a simulta-
neous elevation.
V. DENUDATION PRODUCING VALLEYS.
In a country that has been the scene of such tremendous convulsions and
subterranean disturbances, it was probable that we should find on the surface
abundant ruins, and dislocated fragments of the rocks that have been sub-
mitted to such violence ; we should expect to discover masses of rubbish such
as we see in the wreck of modern land slips, and which cannot but have been
created in prodigious quantity along the line of the elevations and fractures
we have been tracing: but on examination we find that all this wreck has
vanished, and been so totally swept away, that scarce a trace of it can be
recognised throughout the whole district which it must once have covered.
It is obvious, from a mere glance at the Map, that the strata originally
occupied larger areas than they cover at present; and that if no further opera-
tions had taken place in the Vale of Weymouth beyond the elevation and frac-
tures we have described, we should have had little more than a series of arches
piled successively on one another, and extending over a large portion of the
whole district; the angle at which the strata rise being in many parts so
small that no very distant separation of the fractured parts could have attended
their elevation ; and thus the central cornbrash of the Vale of Weymouth
would have been arched over with bending strata of Oxford clay, coral rag,
Kimmeridge clay, and Portland stone; and the Vale of Bredy and the Brid-
port district would have been covered by nearly horizontal beds of greensand
and chalk, connecting the great greensand escarpment of the north and east
of the Vale of Bredy and Abbotsbury Castle with the outlying summits of
Swyre Knoll, Shipton Beacon, Eype Down, Golden Cap Hill, Lewsdon Hill,
Lambert’s Castle, and the entire group of insulated caps and ridges of green-
VOL. IV.—SECOND SFRIES. G
42 Prof. Bucktanp and Mr. De ta Becue on the
sand and chalk near Charmouth, Lyme, and Axminster. But as no such
arches exist in the Vale of Weymouth, nor any such continuity of the green-
sand strata in the vales of Bredy and Bridport, we cannot but infer that
some adequate cause has produced the removal of the vast masses of materials
which apparently must once have filled the spaces that are now left void ; and
we see no cause adequate to the production of such an effect, except the
denuding power of a mass of moving waters; a power which has removed
more than it has left of the entire bulk of nearly all the strata that appear on
the surface of this district, excepting the chalk.
Again, if we look for traces of ruin and violence on the surface along the
lines of fault, we find no such indications presented to us ; but however great
may have been the dislocation and subterraneous changes of level, the out-
lines of the surface are little affected by these changes: thus, our sections
Pl. II. fig. 1, 2, 3, 4, 5, and 6, afford examples of the summits and sides of
hills where we should be utterly unconscious, from the external form of the
land, that the least derangement or fracture has ever affected the subjacent
strata ; the general outlines are regular and rounded, as if no violent move-
ments had ever occurred below, and all the ruins and piles of rubbish that
must have been produced along the lines of elevation and fracture are swept
clean, clear, and smooth away.
If we traverse the great Ridgeway fault for fifteen miles, from one extre-
mity to the other, we see along the whole surface scarcely an indication of its
existence. Near Upway we have an obvious example of this fact, at the point
where the road from Bridport passes down the chalky escarpment of the
Ridgeway through one of those broad and sweeping dry combs which are so
common in escarpments of chalk: having descended nearly to the bottom of
the hill, where we should expect the outcrop of inferior chalk or greensand,
we are surprised to find Portland stone rising to the north, and abutting against
the chalk ; yet we see not the slightest change in the outline of the surface on
either side of this line of fault, nor is there upon its south side a single remain-
ing fragment of all the masses of greensand and chalk that must have been
elevated into a new and high position on that side of the fault when the frac-
ture took place; all traces of the enormous ruins that attended this great
convulsion have utterly vanished and been swept away ; so that scarcely the
residuum of an outlying fragment remains to attest the catastrophe that has
taken place: the sloping sides of the combs glide regularly and gently down,
as if they had been excavated in one undisturbed and uniform mass of con-
tinuous chalk. Nor is this outclearing and total removal of the broken frag-
ments peculiar to this comb on the north-west of Upway ; it is equally ap-
Geology of the Neighbourhood of Weymouth, &c. AS
parent in many others along the whole extent of the fault, particularly in the
deep combs of Elwell, Bincombe, and Sutton Pointz, that lie successively
adjacent to Upway on the east.
The deep and numerous dry valleys on the surface of the chalk hills that
bound our district partake of the general character of such valleys on the
surface of the chalk formation throughout England; and have no peculiar
features beyond those which they have derived from enormous volumes of
water, retiring in all directions from the higher to the lower levels, and
acting at all elevations and on all points to modify the previous forms of the
surface of the earth.
If we look for the cause of all this removal in any natural operations now
proceeding within the district, we find not the shadow of any satisfactory
explanation of that vast destruction of which it has been the scene. It is vain
to appeal to the action of rivers, for in many parts where the denudation has
been greatest, there is not even a streamlet, or a single spring. The greatest
streams we have in the district are the two insignificant rivulets of the Wey
and Bredy*. It is equally vain to appeal to meteoric agents, for we have a
measure of the total amount of their effects in the fragments accumulated in
the form of talus and land slips at the bottom of certain slopes and precipices,
and in a few small accumulations of mud and sand in the low grounds.
The only satisfactory solution we can find is in the waters of a violent
inundation, and in these we think we see a cause that bears a due ratio to the
effects that have been produced.
* The only river in the Vale of Weymouth is the small stream of the Wey, which, rising
suddenly at Upway, from a cross fracture in the Portland beds, runs about five miles from north to
south, into the sea at Weymouth, crossing nearly at right angles all the different formations, as well
as the hills and valleys that occur along its course, and receiving only a few tributary confluents
from the west. The Vale of Bredy is traversed by the small river of that name, running west from
the village of Little Bredy to the sea at Burton Bradstock. It is impossible to refer the excavation
of these deeply denuded valleys and the removal of the broken strata to the flood waters of such
streamlets, or to the agency of their waters accumulated into lakes by any imaginable series of
barriers, which the bursting of such lakes may be supposed to have removed. The east and west
portions of the elliptical valley of Sutton Pointz offer a good example of denudation, independent
of rivers. The only stream within this valley rises on its northern side, upon the line of the great
fault at the base of the chalk escarpment, and running direct across the shorter diameter of the
valley, escapes through a broad denudation, which intersects the Portland stone that forms the
south side of the ellipse. (See Map, and Pl. II. fig. 4.5.) We have a measure of the small
amount of the excavating power of this streamlet cooperating with meteoric agents in a ravine
five or six feet deep, and a few yards long, which the water has cut in a talus of chalk rubble, in
which it begins its course. A similar ravine of much greater length, and about twenty feet deep,
which occurs at the base of the chalk escarpment, on the south of Wantage, is there cut through
G2
44 Prof. Bucktanp and Mr. De 1a Becue on the
How far the causes of this inundation may be connected with the elevation
of the strata in the immediate neighbourhood or in distant regions, is a sub-
ject which at present we conceive it premature to enter into, further than to
suggest that the relation of the one to the other may possibly be nearer than
has been hitherto apprehended.
DILuviumM.
Although the excavation of valleys of denudation, and removal of broken
strata has been so considerable in all this district, we have no proportionate
accumulation of extensive and continuous beds of gravel. ‘The power and
rapidity of the currents which could excavate the materials that filled such
enormous spaces must have been too great to allow these materials to subside
so near the spots from which they have been torn away, and must have drifted
them far forwards into the prolongation of these valleys in the bottom of the
English Channel, whence perhaps many of them may have been cast up again,
and have contributed to form the Chesil Bank. The largest deposit of dilu-
vium we have noticed is at Upway Street, four miles north of Weymouth; but
in smaller quantities and irregular patches it is disposed over the whole surface
of the country, on the summits and slopes of the hills as well as in the valleys.
We have not heard of many organic remains in the diluvium of this district,
but the following are sufficient to show their identity with those found in
diluvial gravel in other parts of England. A few years ago a large rolled
molar tooth of an elephant was cast upon the Chesil Bank, from the diluvium
the chalk-marl with such regularity as to present the uniform width and uniform grassy slopes of
the deep foss of a military fortification, and affords a similar measure of the amount of the power
of existing agents on a substance of such uniform and perishable materials as soft chalk-marl.
The following list of the temperature of springs in the neighbourhood of Weymouth was taken
by Professor Henslow, with a good thermometer, in the year 1832 :—
20th August. Well at Chesilton, in Portland stone, near the middle of the ascent in
the yard of the Portland Arms. A pump was used ......... sic feted he te ees 54° O!
24th August. Spring at Preston, by the road side, in the Portland sand ..........+. 53° of
28th September. Large spring at Upway, the source of the river Wey, rising suddenly
in great force from a cross fracture of the Portland rock .........++- se ecenee 51° o!
20th Septemper. Pump at Corfe Castle ......... o, »(sielnae Cielo wr sinhy whine tene 52° 5!
20th September. Hill side (vertical strata), half way between Corfe and Worbarrow
Bay, junction of chalk and sands ............e0e0- + olosntetetere, «exec ioadheleRedencrniete 52° 0!
4th September. Top of Headon Hill, Isle of Wight: spring from the upper freshwater
formation, a few feet from the summit ........ eo ehente Stele cletete eked: neler Omar
5th September. Spring issuing from the sand rock under the fire-stone at Knighton... .51° 0!
Where the temperature was taken in pump-water, it was not done until all the water that had
filled the pipes was removed by long pumping.
Geology of the Neighbourhood of Weymouth, §c. 45
beneath the sea, and is preserved at Abbotsbury by the Countess of Ilchester.
Near Bridport also, at the villages of Burton Bradstock and Loders, the
gravel has afforded the remains of elephants and other terrestrial quadrupeds.
In the gravel that crowns the cliffs of lias, near the church of Lyme Regis,
many teeth of rhinoceros have been found, and portions of the tusks of
elephants ; and lastly, the cliff at the south termination of the valley of Char-
mouth, where, as at Lyme, the lias is covered with a cap of diluvium, has
afforded several nearly perfect tusks of elephants which tumble from the
summit and get mixed with the debris of lias, when masses of the cliff are
undermined, and fall down on the sea shore. A tusk nine feet eight inches
long, from the gravel of this cliff, was some years ago in the collection of
Mr. De la Beche, and is now in the Museum of the Geological Society *.
Two molar teeth of elephant, one weighing twelve the other thirteen pounds,
were found in this same cliff, in December 1832.
ConcLusion. ‘
We shall conclude with pointing out the following general results that
appear deducible from the facts we have been considering. We conceive
that we have before us sufficient evidence of the following succession of
changes in the state of that small portion of England which occupies the coast
of Dorsetshire. ‘They are analogous to those deduced by Mr. Mantell from
the phenomena he has described in the weald of Sussex.
Ist, We have a succession of marine deposits, continuous from the lias up-
wards through the oolites, and terminating in the deposition of the Portland
stone ; during the period of all these formations our district must have been
the bottom of an ancient sea: the presence of the remains of trees in the
oolite and lias shows that land existed probably at no great distance from this
sea; it is also probable that the waters were not very deep, in which Plesiosauri
were so abundant as they must have been, to supply such numerous remains
as we find imbedded in the lias at Lyme.
2ndly, The bottom of this sea appears for a certain time to have become
dry land, and whilst in this state, to have been covered with a forest of large
coniferous trees, and of Cycadeoideous plants that indicate a warm climate.
We have a measure of the duration of this forest, in the thickness of decayed
vegetable matter and soil, which has accumulated more than a foot of black
earth around the roots of these trees. The regular and uniform preservation
of this thin bed of black earth over a distance of so many miles, shows that
* See Geological Transactions, Second Series, vol. i. p. 421—422.
46 Prof. Bucktanp and Mr. De 1a Becue on the Geology of Weymouth, &c.
the change to the next state of things was quiet and gradual ; since the trees
that lie prostrate on this black earth would have been swept away had there
been any violent agitation, or sudden irruption of water.
3rdly, The dry land on which this forest grew became converted to some-
thing like an estuary, in which the lowest deposits contain freshwater shells ;
these are succeeded by a thick bed of oyster shells, and above the oyster bed are
strata containing an admixture of freshwater shells with shells that are marine.
We have evidence that this formation extended eastward from what is now
the coast of Dorset, through the Isle of Wight to the eastern extremity of the
weald of Kent; but of the boundaries of this supposed estuary we have not
the slightest indication beyond that which is afforded by the existing deposits
of Purbeck and Wealden freshwater formations.
The occurrence of the Purbeck strata reposing on the Portland stone at
Lady Down near Tisbury, on the west of Salisbury, in a position directly
north of the [sle of Purbeck, at the distance of about thirty miles, renders it
probable that the breadth of the estuary in this part extended over the inter-
mediate portions of Dorset and Wilts, which are now covered up with chalk.
Athly, We have a return of the sea over our estuary; and in this sea an
accumulation of the successive and thick marine deposits which constitute the
greensand and chalk formations.
5thly, We have in the Isle of Wight a reappearance of freshwater deposits
mixed and alternating with others that are marine, through the next great
periods of the tertiary formations.
6thly, All these deposits appear to have been succeeded by a tremendous
catastrophe, producing elevations, depressions, and contortions of the strata ;
and intersecting them with enormous faults.
7thly, These movements of the land have been succeeded by inundations,
competent to excavate the valleys of denudation, and partially to overspread
the country with diluvial gravel.
Sthly, This denudation has been followed by a state of tranquillity, which
has remained undisturbed to the present hour.
11.—Introduction to the general Structure of the Cumbrian Mountains ;
with a Description of the great Dislocations by which they have
been separated from the neighbouring Carboniferous Chains.
By tHe Rev. ADAM SEDGWICK, V.P.G.S. F.R.S. &c.
(WOODWARDIAN PROFESSOR IN THE UNIVERSITY OF CAMBRIDGE. )
[Read January 5, 1831. ]
§ 1. Introduction.
I HOPE, in a series of communications, of which this may be considered
the introduction, to lay before the Society the results of observations made
principally during the summers of 1822, 1823, and 1824, among the Cumbrian
mountains, and the neighbouring districts of the North of England. All the
central portions of the region, I propose hereafter to describe in detail, is
composed of rocks of a date anterior to the old red sandstone, but its outskirts
are covered by deposits chiefly of the carboniferous order. On the west side
it is washed by the Irish Sea; and on the east it presses against, and, in part,
blends itself with, the great calcareous chain which forms the separation of the
waters descending to the coasts of Lancashire and Yorkshire. To the north it
is prolonged, through an unbroken zone of mountain limestone, into the plain
of the new red sandstone, stretching down the vale of the Eden ; to the south
it sinks towards the shores of Morecombe Bay, and terminates in a succession
of flat-topped elevations, crowned with precipices of mountain limestone—the
remains of a calcareous ridge, once undoubtedly continuous from the higher
part of the valley of the Kent to the southern extremity of Cumberland.
It follows, from this description, and will be still more clearly seen by a
glance of the eye over the north-west part of the geological map of England*,
that the circular cluster of the mountains here described, presents, through
the greater portion of its circumference, a nearly unbroken band of mountain
limestone ; and on whatever side it is approached, we are struck with the
tameness of the outline of every portion of the calcareous zone, when con-
trasted with the fine serrated peaks of the loftier and more central elevations.
* A new edition of Mr. Greenough’s Geological Map of England is now in progress, and will
be shortly published.
48 Prof. Sepewick on the general Structure
From some of the ridges in the range of Cross Fell, the eye takes in, at
one view, the greatest part of the northern calcareous zone. Seen from that
distance, all its minor inequalities disappear, and I have often fancied that it
resembled a portion of a great semicircular redoubt formed near the base of
the older hills, and presenting a long, sweeping, irregular glacis towards the
valley of the Eden. On a nearer approach, an illusion of this kind must ne-
cessarily vanish, and I only mention it in this place to convey a general idea
of the external characters of the district, and of the relations of the great
formations to each other.
On the eastern side of the region, where the older rocks abut, as above
described, against the great central calcareous chain, the contrast of external
forms is perhaps still more striking. The calcareous mountains, though some-
times cut down into mural precipices, and having individual features of the
greatest beauty, and, though rising to such an elevation as to overlook the
more ancient formations in their immediate neighbourhood, seldom exhibit
any grandeur of outline, and in consequence of the horizontal position of their
beds, often terminate in great featureless and somewhat tabular masses. On
the contrary, the greywackeé hills on the confines of Yorkshire and West-
moreland have their sides worn down into deep combes and irregular sinuosi-
ties, and sometimes rise into sharp angular crests, forming outlines of great
variety and beauty.
Within the calcareous zone above described are several extensive masses
of granite, syenite, and porphyry ; but the greatest part of the region is occu-
pied by stratified deposits of a slaty texture, which may be subdivided into
four distinct formations. Ist, Various crystalline slates, resting immediately
on the granite of Skiddaw Forest, and forming the base of the whole stratified
series. 2nd, Black glossy clay-slate, sometimes passing into greywacké, but
containing no calcareous beds, and no organic remains. 3rd, Green quartzose
roofing slate, associated, in every variety of complication, with felspathic rocks
of porphyritic structure. This formation contains many beds effervescing
briskly when first plunged in acids ; but it contains no continuous bed de-
serving the name ef limestone, and no organic remains. 4thly, Greywacke
slate, often more or less calcareous, and having subordinate beds passing into
impure limestone, full of organic remains.
We owe our first accurate knowledge of these subdivisions to Mr. J. Otley
of Keswick, who not merely described them in general terms, but gave their
geographical distribution with a very near approximation to accuracy*.
* See an early Number of the “ Lonsdale Magazine,” and “ A Guide to the English Lakes,” by
Jonathan Otley of Keswick.
of the Cumbrian Mountains. 49
In subsequent communications I hope to prove: Ist, That the crystalline
unstratified masses form the true geological centres of the mountain groups ;
and that by their protrusion the schistose formations have been elevated into
the position they now occupy. 2ndly, That a true mineralogical axis may be
traced through the inferior divisions of the slate rocks on each side of which
the successive formations, as far as they are clearly developed, are arranged
symmetrically. 3rdly, That the beds of these formations, when we exclude
irregularities arising from local causes, have a nearly constant strike from
a few degrees north of magnetic east to a few degrees south of magnetic west.
And, lastly, That all these peculiarities of structure and position originated
in causes brought into action at a period anterior to the existence of the old
red sandstone.
On these several subjects I wish, for the present, to avoid any further de-
tails: I may, however, be permitted so far to anticipate the materials of a
future communication as to describe the range of the remarkable calcareous
beds, interposed between the green quartzose roofing slate and the greywacké
slate. Such a description will place in a clear point of view the kind of evi-
dence by which we determine the strzke of the slaty masses, and will at the
same time make us acquainted with a succession of dislocations which have
considerably modified the external forms of the Cumbrian mountains. It will
also form a natural introduction to the description of a second system of dis-
locations, by which, at a later geological epoch, these older mountain groups
were snapped off from the central carboniferous chain, and brought into their
present almost insulated position.
§ 2. Range of a band of Limestone and Calcareous Slate, between the
Quartzose Green Slate and the Greywacké Slate, &c. &c.*
This band is full of organic remains, and is separated by masses of enor-
mous thickness from all other caicareous strata with which it could possibly
be confounded: moreover, it occupies, as before stated, a place intermediate
between two entirely distinct formations. Hence, although varying in thick-
ness from 30 or 40 to 200 or 300 feet, it can be easily followed ; and in the
places where its continuity has been broken by great internal movements, we
can generally, in imagination, reunite the disjointed portions, and calculate
the amount of their dislocation, without running the very common risk of mis-
taking one bed for another.
The most western appearance of the limestone is at Beck, a farm in the
* See Plate IV.
VOL. IV.—SECOND SERIES. H
50 Prof. Sepawick on the general Structure
division of Cumberland called Millam. Thence it ranges through Corn Park,
over the Knot, into the Low House grounds; and, after crossing a marsh,
reappears in the same range above Water Blain, and terminates at the foot of
the village called Hill,—the mean bearing of the beds in the whole of this
range being about north-east by east, and the dip south-east by south.
Here we lose all trace of the limestone ; but after ascending several miles
up a rivulet, we find, immediately above Graystone House, among the hills
to the east of Duddon Bridge, a bed of limestone, identical in dip and range
with the one we had left behind. Moreover, the Graystone House limestone
is very nearly in the exact prolongation of the band of transition limestone on
the other side of the Duddon. Hence we may conclude that the Graystone
House and Water Blain limestones belong to the same formation, and have
been severed by an enormous fault, descending nearly in the direction of the
valley of Hallthwaite. ‘The quantity of dislocation estimated in the direction
of a perpendicular to the two parallel lines of bearing cannot be less than two
miles*.
Such a disruption of great mountain masses is not a little startling to the
imagination; but I may state, by way of explanation, that many of the neigh-
bouring mountains are penetrated by dykes of porphyry and syenite, probably
of the date of the eruption of the Bootle granite, and that the whole region
of Black Comb, which belongs to the oldest slate formation, has probably at
the same period been thrust out of the bowels of the earth, and elevated into
a position out of all symmetry with the structure of the neighbouring region.
The country between Millam and Duddon Bridge is, therefore, one where we
ought to look for the evidence of enormous dislocations ; and this evidence is
placed before us in the most impressive manner by that break in the con-
tinuity of the limestone, and that great lateral movement which I have just
described.
The beds of the Graystone House limestone would, in their prolongation,
* It is right to state that there is a difficulty in identifying the Graystone House and Water
Blain limestone, arising out of the mineral character of the overlying slates. In general we can
easily separate, even by hand specimens, the greywacké slate of the highest group from the
green slate under the limestone. But at Graystone House this is not possible, as the overlying
slates are in structure almost identical with those of the inferior group. Hence some one might
conclude that the Graystone House limestone formed no part of the calcareous band described
above, but was an accidental mass subordinate to the series of the lower green slate. There is not,
J think, much force in the objection; for there are other places where portions of the two slate groups
cannot be mineralogically distinguished: and, after all, it merely shifts the difficulty, as we shall have
(on this supposition) to interpolate an enormous fault, somewhere on the line of the Duddon, in order
to explain the position of the corresponding calcareous bands on the opposite sides of the river.
of the Cumbrian Mountains. 51
strike the south end of the range of hills on the north-east side of the Duddon ;
the limestone is not, however, found in those hills, but appears, with its usual
characters, and the same mean line of dip and sérake, in the lowlands on the
east side of the ridge. From this I conclude that a break of the strata passes
down the valley of the Duddon, accompanied with a lateral movement, not
however comparable in extent to the one last noticed. The further range of
the limestone is well defined by the following localities, viz. Hartley Ground,
Lum Holm, Broughton Mill, and thence up the bed of the river to Stock-
beck*. The limestone preserves an undeviating strike and dip; and in
consequence of the sinuosities of the channel, is seen, here and there, above
the mill, on different sides of the river. At Stockbeck the river bifurcates,
and the limestone runs along the north-west side of the eastern branch, close
to Appletreethwaite, where there is a transverse fault, throwing the pro-
longation of the limestone, about a hundred yards further to the north. ‘This
apparently lateral movement has no effect on the direction of the beds, which
preserve an almost perfect parallelism ; but it produces a slight deviation in
the direction of the rivulet.
From Appletreethwaite the limestone continues its course (about 70° or
75° east of magnetic north), and making a very slight deflection to the north-
east, passes on that side of Ash Gill quarries. Thence ranging over Torver
Fell, and across the rivulet, it passes along the line of the Seathwaite road,
and reaches one of the flanks of Coniston Old Man; up which it rises to a
considerable elevation, and in a plane nearly parallel to the steep side of the
mountain. On reaching the north side of Broadway Beck (one of the streams
descending from the mountain), the limestone is again cut off by a great
transverse fault, which appears to throw it to a point about 300 yards south-
east of its line of bearing.
After reappearing in Scrow pastures, it ranges through a wood, descends
down the north side of Mealy Gill, passes close to Old Mill, south of Silverbank,
and thence close to the road, and at the foot of a great precipice, to Low
Yew Dale, from which place it is prolonged across the low grounds to a point
close to Yew Tree. Here it is cut off by the great precipice of Raven Crag,
and a vast transverse fault has pushed whole mountain masses of green slate
* There can be no doubt of the identity of the Millam limestone with that which ranges through
the places enumerated in the text. Hence (though the Graystone House limestone, in consequence
of the difficulty alluded to in the preceding note, be excluded from the range), we must at least
suppose that the Water Blain and Hill limestone bands were once continuous with that of Hartley
Ground. But this supposition is quite incompatible with the general strike of the beds, unless, as
stated in the preceding note, we interpolate an enormous fault along the line of the Duddon.
H 2
52 Prof. Srepewick on the general Structure
and felspathic rock so far out of their line of bearing, that we are compelled
to make a southern traverse to a knoll above Coniston Hall (a distance of more
than a mile), before we can discover the broken ends of the beds of lime-
stone. The line of fault appears to be prolonged down the valley, nearly in
the direction of Coniston Water Head.
From the knoll above mentioned the limestone ranges, with a slight devia-
tion from its mean direction, through the hills which overlook the Tarns, and
descends to a point, close to the separation of the Skelwith and Ambleside
roads. Here the great masses of green slate, which had before encroached
on the strike of the beds, are suddenly thrown back at Pool Beck Scar, and
the limestone beds are cast, at a single heave, about a mile and a half to the
north of their former line of direction. This enormous fault, though it pro-
duces a considerable influence on the configuration of the neighbouring
country, is in one respect an exception to a general rule, inasmuch as its di-
rection is not marked by any valley.
In this part of the range the country is much covered with alluvial matter ;
but the continuation of the line is nearly defined by the lime quarries of
Holmes House, the beds under Pool House, and the old limeworks on the north
shore of Pool Wyke. Seen from Pool Wyke the quarries of transition lime-
stone on the east shore of Windermere are not more than 10° north of true
east; but had they been on the prolongation of the mean line of range, they
would have appeared about 35° north of the same point. From this we
may, I think, conclude, that there has been a break between the opposite
shores of the lake—that the beds, on the east side, have had a considerable
movement towards the south—and that the valley of Windermere, like all the
other great valleys cutting through the limestone range, has been scooped out
upon a line of fracture.
From the quarries about 400 yards above Low Wood Inn, on the east
shore of Windermere, the limestone beds range through the woods, and pass
just under Dove Nest, and on the north side of High Skelgill, near which
place they are expanded over a considerable surface, the rise of the mountain
side being nearly parallel to the plane of stratification. They are prolonged
in a direction a few degrees north of magnetic east, through the extreme
ramifications of the rivulet which runs down to Low Wood, and thence to the
top of the hill overhanging the village of Troutbeck. From this point the
range of the limestone on the opposite side of the valley, near the high pass
leading to Kentmere, is distinctly visible, and bears about 15° south of mag-
netic east. Now this change of bearing is exactly the opposite to that which
might have been expected ; especially after remarking the great elevation of
of the Cumbrian Mountains. 53
the pass before mentioned : for the beds being all inclined at a great angle,
and rising to the north-west, we have reason to look for the most northern
portions of their range at the points of highest elevation. This fact makes
the change of bearing above mentioned still more striking, and convinced
me, before I descended from the hill, that there was a great fault ranging
down the valley of Troutbeck.
On this subject we are not left to mere inference, for the limestone beds
descend the hill on the north side of the village, range through a point about
150 yards above the junction of the two roads, and are traced to a small
coppice near the river side, called Intake Wood. Near that place they are
cut off by a fault ranging down the river, which has caused a great movement
towards the south in the whole system of beds on the opposite side of the
valley. We are therefore compelled to descend about three quarters of a mile
before we can catch the broken ends of the beds we have left behind.
After being concealed in the alluvion of the valley, the beds again break
out behind Line Foot, and, ascending rapidly towards the north, with the
inclination of the hill, pass for some way on the north side of the Kentmere
road. At the top of the hill they range on the south side of the road, in a
direction difficult to ascertain in such uneven ground, but approaching mag-
netic east. In descending the hill towards Kentmere Hall they appear to be
dislocated, and shattered by a complication of faults, and one great mass ranges
down the brow, in a direction about 45° east of magnetic south. This very
anomalous bearing is accounted for partly by the movements of dislocation,
and partly by the great angle of dip and inclination of the surface. Another
disjointed mass of limestone ranges nearly in the mean bearing behind the
Hall, but is cut off by a fault before it reaches the chapel. Lastly, the beds
in regular order, beyond the faulty ground, cross the rivulet (with their usual
dip and strike) about 400 yards above the bridge, through the fields of Head
Lane farm.
From this place the beds rise into a ravine in the edge of Pike How, and
thence over the top of the hill, through a point about 200 yards south of the
mountain road. to Long Sleddale, and so down the hill to a place called Till’s
Hole. By taking, from Till’s Hole, the bearing of the corresponding beds on
the other side of Long Sleddale, we find that the limestone strikes the oppo-
site hills at a point several degrees out of its previous bearing ; which fact pro-
bably indicates the passage of a fault also down this valley. Everything is
however obscured by alluvion near the banks of the river; and if there be
any shift of position among the mineral masses in their strike across the valley,
it must be of comparatively small extent.
5A Prof. Sepewick on the general Structure
On the east side of Long Sleddale the beds of limestone are seen crossing
a rivulet, about 200 yards above the houses called Little London; and from
that place they may be traced up the southern branch of the same rivulet (called
Tron Crow Gill), for nearly half a mile, in a direction about north-east by east.
They then disappear under great accumulations of turf-bog, and alluvial mat-
ter, and are not again seen. Some peculiar felspathic rocks on which they
rest, and some thick beds of blue flagstone, by which they are surmounted,
may however be traced through a morass on the top of the mountain: there
can, therefore, be little doubt that the limestone beds are also continued past
the north side of a hill called Lord’s Seat, and thence into the turf-bogs on
the east side of Yarlside Crag, to a place not more than a mile and a half
from Wastdale Head.
Had this system of strata met with no interruption, it would, after a further
range of about four miles, have abutted against the zone of mountain lime-
stone. It is, however, cut off by a great boss of granite, which has deranged
the relative position, and changed the mineral structure of all the neighbour-
ing rocks: from which we may, I think, safely conclude, that the granite of
Wastdale Head (commonly called Shap granite), did not assume its present
position till some period after the formation of the transition limestone.
I have been the more minute in these details because they enable us clearly
to establish a series of important facts in the geological history of the Cum-
brian mountains.
First. They prove, that at a very ancient epoch, and probably during the
principal period of elevation, great cracks were formed, diverging from the
centre of the mountains, accompanied by great changes in the relative posi-
tion of the mineral masses on the opposite sides; and further, that these cracks
prepared the way for future valleys*. Now the principal valleys of these
mountains diverge towards all parts of the circumference, from a centre near
the high crests of Sca-Fell. Is it not, therefore, probable (though in the
absence of beds of limestone, like those above described, we cannot establish
the fact on direct evidence), that great lines of dislocation pass down the
greatest number of these valleys? In making this supposition we merely
* The usual appearance, on the opposite sides of the faults above described, is exactly that of
a great horizontal lateral movement, and is not, I believe, by any means entirely deceptive; for
expansive forces of elevation acting on oblique planes, might easily produce such a movement.
The effect was probably of a compound kind. When beds are highly inclined, a mere subsidence
on one side of a fault will, however, produce on the surface the exact appearance of a horizontal
slide. It is not, therefore, always possible, especially in the absence of underground workings, to
determine the exact direction of the movements which have accompanied a fault.
of the Cumbrian Mountains. 55
assume that similar effects have been produced by similar causes acting within
a very limited region. And, if this hypothesis be admitted, we can advance
a step further, and point to the probable origin of these great diverging
fissures: for the valleys start from a central region, which is violently broken,
where the dip and range of the stratified masses is unsymmetrical, and which
is marked by protruding mountains of granite and syenite.
Secondly. Notwithstanding the great dislocations of the masses of green
slate and porphyry, forming the support of the limestone, there is hardly any
instance in which they are bent and contorted. After seeing the violent contor-
tions of some portions of the other slate systems of the region, this fact might
appear inexplicable ; but we find a solution of our difficulty in the enormous
irregular masses of hard unbending felspathic and porphyritic rocks, im-
bedded in, and so intimately mixed with, the green quartzose slate, that we
in vain seek to separate the formations from each other. If, then, we
admit the igneous origin of the porphyries, in what way can we account for
the accompanying, and apparently almost contemporaneous, deposits of stra-
tified chloritic slate? I know no explanation so probable as that which sup-
poses igneous and aqueous causes to have acted together—the porphyries
to have been produced by some modification of submarine igneous action—
and the chloritic slates to have been deposited from the waters in the same
region, and in the same periods of time: the first operation supplying, at
least in part, the materials for the second, and similar operations being many
times repeated.
Thirdly. The previous details enable us clearly to determine the mean line
of bearing of the whole system of stratified rocks associated with the lime-
stone; and this line makes the schistose masses, one after the other, to abut
against the carboniferous zone. ‘This fact alone proves that the older and
newer systems are entirely unconformable—a conclusion confirmed by all the
sections which connect the slate rocks with the calcareous zone.
Again: There is no gradation between the two systems ; their position is
not only unconformable, but the transition from one system to the other is
instantaneous. Masses of red conglomerate are found here and there, near
the base of the older mountains, resting upon the edges, and filling up the
inequalities of the component strata, and upon these conglomerates are depo-
sited the lower beds of the carboniferous limestone. These facts seem to
prove, that the elevation of the cluster of mountains of Cumberland was sud-
den (which seems to be almost implied by the great faults and dislocations
above described, as well as by the regularity of the lines of bearing), and that
all those causes which produced the elevation of the older strata, and deter-
56 Prof. Sepawick on the general Structure
mined their line of bearing, had ceased to act before the completion of the
old red conglomerates.
In the region above described there is no connexion between the direction
of the valleys and the mean line of bearing of the formations ; and one of the
means successfully used by M. Elie de Beaumont in grouping together distant
mountain chains, would, in this instance, entirely fail us. I do, however, think
that the leading doctrine of the Essay on the Epochs of Elevation (viz., that
mountain chains elevated at the same period of time have, even when widely
separated from each other, a general parallelism in the bearing of their com-
ponent strata), receives a strong confirmation from the position of the older
formations of the British Isles.
It is now generally allowed that the old chains of mountains, mainly com-
posed of clay-slate and greywacké, which give so great an impress to the
physical character of this island (viz., the chains of Cornwall, of North Wales,
of the Isles of Man and Anglesea, of Cumberland, of Lannermuir, including
the whole range from St. Abb’s Head to the Mull of Galloway, &c. &c.), are
nearly of the same age, and were probably all elevated before or during the
period of the old red sandstone. Now if a line be drawn along the axis of
the Cornish chain ; a second parallel to the prevailing ranges of the higher
Welsh mountains, as laid down in Mr. Greenough’s map; a third in the direc-
tion of the strata of Anglesea ; a fourth in the axis of the greywacké chain of
the Isle of Man; anda fifth from St. Abb’s Head to the Mull of Galloway ;
all these lines will make a near approach to parallelism with the line of bearing
in the system of the Cumbrian mountains, as established by the previous details.
Is this parallelism accidental? I am unwilling to believe it; and although
there are even in England some remarkable exceptions to this arrangement,
I think that the facts here stated afford, as far as they go, a confirmation of
that principle on which are founded many of the bold generalizations of the
extraordinary essay of M. Elie de Beaumont, to which I have alluded.
§ 3. On the Great Dislocations by which the Cumbrian Mountains became
separated from the Central Carboniferous Chain, &c.
The internal movements which produced the derangement of the groups
of strata described in the preceding section were succeeded by a long period
of comparative repose, during which our whole carboniferous series was elabo-
rated. Had our island been laid dry immediately after that period, without any
change of relative position among the great formations, the Cumbrian moun-
tains would have appeared as a cluster of ancient rocks rising out of a great
carboniferous plain; extending north and south from the border of Scotland to
of the Cumbrian Mountains. 57
the very heart of England, and in a transverse line from the Gerinan Ocean
to the Irish Sea, and as far west perhaps as the Isle of Man. The remains
of the carboniferous strata in the northern and central parts of England, not-
withstanding the manner in which they have been dislocated, and afterwards
covered up by newer deposits, justify us in giving them this great original ex-
tent, and thus bringing them almost to the confines of the carboniferous system
of the Bristol Channel.
This carboniferous period (during which we have no indications of great
internal movements producing mountain masses with their strata in discordant
positions), was immediately succeeded by some of the most remarkable convul-
sions which have affected our island. During these convulsions, took place
some of those extraordinary dislocations of the coal measures on the confines
of the Bristol Channel (so admirably described in former memoirs read before
this Society *), and also the elevation of the great northern central chain, extend-
ing from the neighbourhood of Derby to the mouth of the Tweed: and during
the same period the calcareous zone surrounding the Cumbrian mountains
was torn off from that part of the great northern chain, which, after deflecting
a little to the north-west, is prolonged through the crests of Cross Fell to the
confines of Scotland.
I only mention the carboniferous system of the Bristol Channel for the pur-
pose of founding upon it one or two general remarks, and of contrasting it
with the northern chain of the same period.
First. The axes of the different coal basins on the Bristol Channel seem
to form a striking exception to the rule above quoted, viz., that regions of
contemporaneous elevation are marked by parallel lines of bearing. Among
the axes of these basins there is certainly no such parallelism.
Secondly. As the calcareous slates of North Devon and of a part of South
Wales do not conform to the rule which appears to govern the range of the
greatest number of our greywackeé chains; but, on the contrary, run nearly
east and west, in a direction parallel to the axis to the great elliptical coal
basin of South Wales ; is it not highly probable that the anomaly was caused
by the extension to North Devon and a part of South Wales of the same
forces which produced the actual configuration of that basin? Or, in other
words, may we not conclude, that the great elevatory movements of the grey-
wacké series of North Devon and of a part of South Wales took place after
the completion of the carboniferous series ; and, therefore, many ages after the
* See the sections accompanying the Memoir by Messrs. Buckland and Conybeare, Geol. Trans.,
New Series, vol. i. p- 210, &c.
VOL. I1V.—SECOND SERIES. I
58 Prof. Sepewicx on the general Structure
movements which produced the strike and dip of the Cumbrian mountains
as above described ?
Thirdly. The form and direction of the dislocations in the coal fields on
the Bristol Channel bear little resemblance to those of the northern carboni-
ferous chain—a circumstance probably originating, partly in the local nature
of the disturbing forces themselves, and partly in the fact that the application
of these forces in the two carboniferous regions was not contemporaneous.
After the first elevation of the central carboniferous chain of the north, the
lowest division of the new red sandstone group (rothe-todte-legende) was
immediately deposited. The movements of elevation were not merely followed
by, but were probably the mechanical causes of, this deposit ; which is com-
posed of sand, small pebbles, and other incoherent materials, drifted to the
outer and lower edges of the coal-fields ; even at this day is in many places
but imperfectly cemented; and contains, though rarely, a few drifted coal
plants*. In some districts it is perfectly conformable to the upper coal strata
on which it immediately rests, and seems to form a regular connecting link
between them and the overlying formations ; but, considered on the whole,
its position, as far as regards the inferior strata, is discordant. It was followed,
and perhaps interrupted, by movements of elevation, producing a considerable
derangement in its component beds, and, of course, also affecting the lower
formations ; and these movements were succeeded in several parts of York-
shire, and of the Cumbrian mountains, by deposits of magnesian conglo-
merate and magnesian limestone—unconformable both to the lower division
of the new red sandstone (rothe-todte-liegende) and to the coal measures +.
Now the overlying deposits of the Bristol coal-fields are perfectly analogous
to the series in the North of England, which commences with the magnesian
conglomerate ; but they appear to contain no representative whatsoever of the
lower division of the new red sandstone. Hence we may, I think, conclude
(not hypothetically, but on direct physical evidence), 1. That the movements
which gave the final configuration to the coal-fields on the Bristol Channel
took place after the deposition of the lower red sandstone, and were probably
contemporaneous with the second system of movements in the North of En-
gland, before alluded to. 2. That the movements (prior to the existence of
the lower red sandstone or rothe-todte-liegende) which gave the chief impress
* See Geol. Trans., Second Series, vol. iii. p. 64. Traces of vegetable fossils occur in this
deposit, on the coast of Cumberland, near Whitehaven. Stems of Equiseta and other vegetable
impressions have also been found in it at Hickleton in Yorkshire, by the Rev. W. Thorp of Don-
caster. I was unacquainted with these facts at the time the Memoir just quoted was composed.
+ See Geol. Trans., Second Series, vol. iii. Pl. VI. figs. 3. 4. 5. 6.
of the Cumbrian Mountains. 59
to the carboniferous chains of the North, took place during a time long an-
terior to the principal dislocations of our south-western coal-fields*.
Fourthly. Though the contortions of the carboniferous system of the
Bristol Channel are so very extraordinary, the actual elevation of the beds is
much less than that of the northern chain. This is perhaps the reason why
the secondary rocks, from the new red sandstone to the chalk, have in their
range from the south coast to the latitude of Derby, a direction nearly parallel
to the mean bearing of the greywacké chains—that is, the very direction they
would have had, provided they had been deposited immediately on the flanks
of the greywacké chains, without the intervention of the carboniferous series.
Thus, for example, the principal line of transition limestone in South Wales
is nearly parallel to the direction of the great oolitic terrace in the corre-
sponding latitudes. In making this observation (which must not be pushed
too far), all minor inequalities are, of course, left out of account, as well as the
changes of bearing produced by much more recent disturbing forces—such, for
instance, as the great saddle of the wealds of Kent, and the east and west range
of the vertical chalk through the Isle of Wight and a part of Dorsetshire.
Now if we follow the same secondary beds beyond the latitude of Derby,
we find a sudden change in their direction, bringing them nearly into paral-
lelism with the great central carboniferous chain of the North. From which
. it appears, that this chain was of sufficient magnitude to produce, by its eleva-
tion, a great change in the bottom of the neighbouring seas, and, conse-
quently, to produce an immediate influence upon the direction of all the strata
afterwards deposited, by the same seas, upon its flanks.
Leaving the consideration of subjects which may appear remote and hy-
pothetical, I now proceed to describe the nature of some of the greater dislo-
cations produced by the elevation of the northern carboniferous chain. The
disturbing forces, acting with their greatest intensity in a direction nearly
north and south, commenced in the latitude of Derby, and produced their
first effects towards the north in elevating the High Peak limestone and the
coal-fields on its eastern flank. They are marked by a system of great lon-
gitudinal faults ranging on the west side of this limestone region ft.
* I am aware that this conclusion has been objected to by some of our best geologists, but I
do not believe that they have personally examined the whole evidence on which it rests.
t See Pl. V. fig. 1. Some interesting phenomena connected with these faults are described
in Farey’s Geological and Agricultural Survey of Derbyshire. The accompanying section is
not intended to convey any details of stratification, but only a general notion of the position of
the great mineral masses. The toadstone beds of the High Peak limestone are intentionally
omitted.
12
60 Prof. Sepewick on the general Structure
Continuing the range towards the north, the elevatory forces seem to have
operated more feebly, as the limestone is not brought up to the surface. But
their line of action is, in some places, marked by an irregular saddle of mill-
stone grit, forming the water-shed between our eastern and western coasts.
The great saddle of millstone grit at Blackstone Edge, flanked by the Lanca-
shire and Yorkshire coal-fields, is a good example of this arrangement*.
A few miles further towards the north the mountain limestone is again pro-
truded: the chain gradually arises to a commanding elevation, and is continued
as far as Stainmoor, preserving throughout a great similarity in its external
forms, and an almost perfect identity in its internal structure.
Near that part of this range where the carboniferous mountains begin to
present a decided escarpment towards the west, commences a great longi-
tudinal fault (or perhaps a system of faults), which has been traced by Mr.
Phillips from the heart of Craven to the hills near Kirkby Lonsdale, and ex-
cellently described in a paper published in a former volume of our Trans-
actions}. I must refer to this paper for the proof that the great Craven fault
has rent asunder a part of the carboniferous chain, and produced such a down-
cast on the west side, that mountain masses of limestone are tumbled into the
neighbouring regions with an inverted dip ; and that a coal-field which ought
to appear above the top of Ingleborough, has sunk below the level of its
base f.
From beneath this coal-field the limestone beds again rise up, and after
passing in the form of a great arch over Farlton Knot, recover their hori-
zontal position, and are prolonged into those tabular hills mentioned above,
which form the south-western skirt of the Cumbrian mountains. From which
it appears, that the southern calcareous zone of the Cumbrian system, is cut
off from the central chain by the intervention of the great Craven fault.
I once imagined that this great fault ranged through the neighbourhood
of Kirkby Lonsdale and Farlton Knot, and there terminated. It is unques-
tionable that lines of dislocation do range in the direction here indicated (as
is proved by the position of the limestone of Kirkby Lonsdale bridge; and the
still more remarkable position of the limestone between Casterton and Bar-
bon); but after several subsequent visits to the neighbourhood, I found that
the leading branch of the Craven fault ranged along the line of junction of
the central chain with the skirts of the Cumbrian system, passing along the
south flank of Casterton Low Fell, up Barbondale, thence across the valley of
Dent, through the upper part of the valley of Sedbergh, and along the flanks
* See Pl. V. fig. 2. + See Geol. Trans., Second Series, vol. iii. p. 5—15.
t See Pl. V. fig. 3.
of the Cumbrian Mountains. 61
of Bawfell and Wildboar Fell, to the ridge between Mollerstang and Raven-
stone dale ; and that along the whole of this line there are enormous and most
complex dislocations. Some of these phenomena I hope to describe more at
length in a future communication ; and for the present I only observe, that a
great upheaving force acting at once upon the two contiguous and uncon-
formable systems, produced a great strain and separation of parts, accompanied
with fractures and dislocations, principally along the line of their junction*.
In a part of the range between Mollerstang and Ravenstonedale the cluster
of the older mountains, by deflecting to the north-west, quits the central car-
boniferous chain ; and it becomes a question of some consequence to deter-
mine the further range and nature of the great Craven fault. The ruptures
produced by it are fortunately on a scale too great to be overlooked or mis-
understood. It ranges through Mollerstang into the hills immediately south-
east of Kirkby Stephen, and thence skirting the escarpments which trend
towards Stainmoor, finally stops near the foot of the mountain-pass. Its pro-
gress is marked by a lofty ridge of carboniferous limestone, which has been
upheaved from the very base of the whole system, contorted and shattered,
and then sent headlong into the valley, where it is to be seen on edge for
many miles ; and where its lower extremities lie buried under accumulations of
alluvial matter and the horizontal conglomerates of the new red sandstone f.
In following these dislocated ridges in the opposite direction, we may trace
them into the calcareous hills of Ravenstone dale, where they expand them-
selves and assume a more horizontal position, and in this way gradually pass
into the unbroken calcareous zone which skirts the north side of the Cum-
brian mountains as far as Egremont. Thus, it appears that the northern and
southern calcareous zones of the Cumbrian mountains are cut off from the
central chain by the same fault, which, both in the neighbourhood of Ingle-
ton and Kirkby Stephen, has produced a great downcast on the western side
of its rangef.
So far it appears that we have a clear and consistent explanation of the re-
* See Pl. V. figs. 4. 5.
T See the southern extremity of the section, Pl. V. fig. 7.
t See Pl. V. figs. 3.7. The effects produced along the line of dislocation on the lower
beds of the carboniferous system vary with the circumstances of the case. Where the beds abut
against the steep sides of the greywacké chain, their broken ends have undergone a movement
of elevation. Under such circumstances a depression like that at Ingleton, or the still more eom-
plex derangement of the strata, like that in the valley above Kirkby Stephen, was obviously im-
possible. See Pl. V. figs. 4, 5. These two figures are ideal ; the former being intended to repre-
sent the undisturbed, and the latter the disturbed, position of the greywacké and carboniferous
series.
62 Prof. Sepewick on the general Structure
lations of the central carboniferous chain to the secondary zones of the great
cluster of the Cumbrian mountains. But there is still one difficulty to be
explained. Beyond Stainmoor, the western border of the central chain de-
flects, as before stated, considerably towards the north-west, and rises into an
escarpment, partly made up of mural precipices, which overlooks the plain of
the new red sandstone in the vale of the Eden, and in the crest of Cross Fell
reaches the elevation of 2900 feet. On the contrary, the northern calcareous
zone of the Cumbrian system dips under the plain of the new red sandstone,
and along the course of the Eden, lies buried probably many hundred feet
below the surface. This relative position is explained in a transverse section
from the central mountains to the ridge of Cross Fell: and it seems impossible
to account for the collocation of the two carboniferous systems without the
intervention of a faudt ranging somewhere near the base of the chain of Cross
Fell, and producing an enormous upcast to the north-east*. ‘The misappre-
hension of this fault formerly introduced a great error into certain published
sections, in which the new red sandstone of the Eden was placed wnder the
whole system of Cross Fell t.
Fortunately in this, as in the former case, we have better evidence than a
mere inference ; for in following the escarpment from any portion of the Cross
Fell chain to the foot of Stainmoor (the key of the whole position), we have
a manifestation of the true nature of the fault, and on a scale hardly to be
rivalled in any other part of our islandf{. A little before we reach Brough,
there commences a steep craggy mountain ridge, ranging parallel to the prin-
cipal escarpment; from which it is separated by a ravine several hundred
feet in depth. On entering this ravine, we find ourselves on the very line of
an ancient convulsion, by which the whole craggy ridge has been torn off
from the escarpment, and tumbled over into the valley, in which it now stands
on edge; every part of it being inclined at a very great angle. It is of vast
thickness, and probably includes nearly the whole calcareous system of Cross
Fell: but its upper beds are buried under the alluvion of the new red sand-
stone.
These inclined beds (on a part of which stands the town of Brough) are
prolonged to the foot of Stainmoor, and thus brought into contact with the
dislocated beds thrown down from the opposite side of the valley by the great
* See’ Pl. V. fig. 6,
{ See a paper by Professor Buckland (Geol. Trans., First Series, vol. iv. p. 105), in which this
mistake is rectified.
{ There are some other places near the base of the carboniferous chain where we meet with in-
dications of the‘nature of the Cross Fell fault. (See Geol. Trans., First Series, vol. iv. Pl. V. figs. 2
and 3.) But in none of them is the evidence comparable to that exhibited in the Brough section.
of the Cumbrian Mountams. 63
Craven fault. The transverse section from the hills above Brough to the
hills above Kirkby Stephen, shows the singular relations of these dislocated
masses™*.
It thus appears, that during the elevation of the central carboniferous chain
of the North, there were great changes of level among the component strata,
—and that the points of greatest stress not being upon the same straight line,
the fractures were sometimes inclined to each other—that the great Craven
fault and the great Cross Fell fault, intersecting each other at a considerable
angle near the centre of the chain, shattered and cut off from it a great trian-
gular mass of the component strata—and that this triangular mass, being thus
cut off by the disruptive forces of elevation, underwent a change in its rela-
tive level, and was at the same moment affected by a great downcast move-
ment; of which we have a most convincing proof in the present extraordinary
position of the mineral masses at the foot of Stainmoor, and on the line of
section.
I am far from supposing that in the preceding details I have pointed out all
the great movements whereby our northern mountain chains have been af-
fected. All I have attempted to do has been to explain the nature of certain
great dislocations of which we have direct evidence, and of which we can
determine the geological epoch ; and thence to show the general effects they
have produced on certain mountain groups in the North of England.
If I wished to speculate on the causes of these great movements among the
integuments of the mountains, I should point to the porphyries of the Cheviots
and the syenite of Charnwood Forest, rising at the two extremities of the
carboniferous chain. I should also point to the granitoid rocks near Dufton
Pike; and perhaps also to the Whin Sill, and the other masses of augitic
trap, associated so largely with the calcareous system of Cross Fellt.
If it were objected, that the porphyry of the Cheviots sometimes resembles
the old felspathic rocks of Cumberland, and sometimes passes into syenite and
granite ; and further that we have proofs of its existence before the conglo-
merates of the old red sandstone: we might on the other hand reply, that
such facts throw no difficulties in the way of supposing, that the Cheviot por-
phyry (like some of the other crystalline formations of Scotland), was elevated
en masse at some period subsequent to its first formation ; especially as we
can show, to the north of the Tweed, derangements exactly answering to such
an elevation. We might further reply, that the red porphyries of the Scotch
Border, however like each other in mineral structure, are not all of the same
* See.Pl. V. fig, 7. + See Geol. Trans,, First Series, vol. iv. p. 109, &c.
64 Prof. Sepewick on the general Structure
age ; inasmuch as some of them are unequivocally posterior to a portion of the
coal measures. The discussion of these subjects would, however, lead me too
far from the direct object of this paper*.
Many of the great movements above described, appear to have been pro-
duced by an action both violent and of short duration. The nature of the
fractures leads us to this conclusion, as well as the nature of the mineral
masses resting immediately upon the dislocated beds. In some portions of
our coal-fields there may be indications of a passage into the next superior
order of formations. But in the neighbourhood of the great faults above
described, there is certainly no such indication, or anything whatever which
could mark the slow progress from one system of things to the other.
That these great fractures were produced by some modification of volcanic
action is, to say the least of it, a very probable hypothesis. But, granting
this hypothesis, what proper measure can we set up for the intensity of vol-
canic power during any one geological period of the earth, except that which
is defined by the effects produced? Guided by this rule we assume nothing :
and though we fall into error from hasty generalizations, our conclusions,
unfettered by theory, are ever open to correction ; and as observations are
multiplied, gradually approximate nearer and nearer to the truth.
Of the cause of volcanic action we know nothing ; but we know enough of
* At Rodham, a few miles from Wooler, the carboniferous series is separated from the Cheviot
porphyry by an old red conglomerate forming the base of the stratified rocks. The conglomerate
contains many pebbles identical in structure with the porphyry, which must therefore have existed
before the carboniferous series: and the conclusion is confirmed by similar phenomena in Roxburgh-
shire. Judging, however, from the inclination of the stratified masses, we should, I think, be
led to infer, that the porphyry had undergone some movement since their deposition.
A porphyry perfectly identical with that of the Cheviots, in the same range, and sometimes
passing into a true granite, breaks out in Lamberton Hills, a few miles north of Berwick ; and
near Shiels runs down close to the coast. At this point the red sandstone (subordinate to the
old carboniferons formation of the Tweed), which forms the sea cliff, suddenly becomes vertical,
and in some places is moved more than 90° from its undisturbed position. ‘The phenomena are
correctly described in a paper published by Mr. Witham in the Newcastle Transactions: but the
important fact of the close approach of the granitoid porphyry appears to have escaped his notice.
It seems to prove, unequivocally, that the Lamberton porphyry assumed its present position after
the epoch of the carboniferous system of the Tweed. 1 mention these apparently contradictory
facts for the purpose of showing, how difficult it is to prove the age of igneous rocks by any single
set of phenomena.
Trappean rocks are very abundant in the higher parts of the Tweed, and have a great simila-
rity of mineral structure ; yet it is generally impossible to come to any certain conclusion respect-
ing their epoch. At Cowdenknows (a few miles north-east of Melrose), a red porphyry distinctly
overlies a red sandstone similar to that in the lower course of the river.
of the Cumbrian Mountains. 65
the effects of this action to be certain, that it cannot be ever brought under
the mechanical laws of any constant force. ‘To assume therefore, indepen-
dently of an incomparably wider induction from facts than has yet been made,
that volcanic forces have acted on the earth during all geological periods
with equal intensity, is so far from being sound philosophy, that it is a mere
gratuitous assumption—founded, it may be, upon a mistaken analogy be-
tween the calculated effects of constant forces, and the effects of other forces,
which are not only not constant, but which are unknown in their origin and
undefined in their power.
Judging from facts alone, and independently of all hypothesis, I adopt some
of the leading principles of the Essay on the Epochs of Elevation by M. Elie
de Beaumont, to which I before referred. They are certainly cpen to nu-
merous exceptions ; especially in low geological regions like many of those
in our Island. But among mountain chains which are well defined and of
considerable elevation, they are, I believe, of very extensive application and
of unquestionable importance. The two systems of dislocations, described in
the second and third sections of this paper, mark two epochs of elevation which
have had a great effect in modifying the structure of this Island.
Note.—1 hope I may be excused in very briefly anticipating some of the
conclusions which seem to follow from a detailed examination of the Cumbrian
mountains.
1, The crystalline structure of some of the slates appears to have been
superinduced after their deposit by an action from below. This seems to be
certain, as far as regards a zone of indurated slates which surrounds the boss
of Shap granite; and it is at least a probable explanation of the crystalline
structure of the lowest group of slate rocks in Skiddaw Forest.
2. There are, in many large tracts of the Cumbrian system, slate beds with
a decided transverse cleavage, alternating with coarse flagstone and grey-
wacké, and not associated with any igneous or unstratified rocks. Similar
facts are repeated in North and South Wales on a more extended scale, where
the slates sometimes pass into true chlorite slate, alternating with other unal-
tered slaty masses. In such cases we have no right to assume that the crystal-
line structure has been produced by any modification of igneous action. Hence
it appears to be a rash generalization to attribute the crystalline structure of
all primary slate rocks to direct igneous action. This negative conclusion is
further confirmed when we consider that secondary deposits, by the mere
chemical action of their particles, unaided by any igneous cause, sometimes
assume a perfectly crystalline structure. For example; many beds of moun-
VOL, IV.—SECOND SERIES, K
66 Prof. Sepewick on the general Structure
tain limestone are perfectly crystalline ;—and the large globular structure of
magnesian limestone has occasionally been superinduced on masses originally
deposited in thin lamine; as is demonstrated by the fact, that the lines of the
original lamine may still, in some instances, be traced through a congeries of
balls mutually compressing each other. ‘These peculiarities of structure are
found in places where there is not the least indication of any igneous action.
3. The highest greywacké group of the Cumbrian mountains contains beds
with numerous organic remains. The next inferior group (composed of green
slate and porphyry), and the third group in the descending order (composed
of fine, black clay slate and greywacké slate, &c.), contain no organic remains.
How can we account for the absence of organic remains in this third group,
except on the supposition that they did not exist in the seas where it was de-
posited? It is developed through large mountain tracts, and is, with very few
exceptions, composed of rocks unaltered by igneous action. Had there been
any organic beings where it was deposited, we should, I think, have found
their remains imbedded in it. We arrive at precisely the same conclusions in
traversing the whole slate system of Devonshire and Cornwall. The upper
part contains organic remains; the lower part does not. Yet in the lower
part there are large tracts where the rocks are unaltered, and contain beds
of limestone and calcareous slate, not more crystalline than ordinary beds
of mountain limestone. The same positive and negative conclusions are
strengthened by the phenomena of North and South Wales. I may state
generally, as the result of my own observations on the older strata of this
Island, that there is a line in the descending series where organic remains
seem entirely to disappear ; and that this line is by no means coordinate with
mineral changes superinduced by igneous action. It is true that igneous
action has in many cases produced a crystalline structure in stratified masses,
and obliterated their organic remains : but it is not by any means true that this
action always accounts for the absence of organic remains from the older strata.
4. 'The ancient separation of the old schistose deposits into two great groups
(the upper containing organic remains, and the lower not,) appears, therefore,
to be borne out by the phenomena of our Island. This separation is, how-
ever, on two accounts, of very little importance. First, Because the two
groups almost entirely interchange mineralogical characters. Secondly, Be-
cause, between the two extremes, there appears to be an enormous develop-
ment of rocks, in which organic remains (though appearing here and there)
are very rare. Hence it must always be difficult, and oftentimes impossible,
to draw any precise line between the two groups in question.
5. I believe, however, that there is a broad mineralogical distinction be-
tween the primary stratified rocks (including under that term all stratified
rocks inferior to the old red sandstone,) and the secondary,—and a still broader,
of the Cumbrian Mountains. 67
between the primary stratified groups and the deposits superior to the chalk.
In some instances secondary rocks have put on the exact appearance of
the primary: but is there a tertiary deposit in any country yet examined,
which could for a moment be confounded with the greywacké systems of
Cumberland or Devonshire? Through large regions of the earth, the epoch of
many deposits is not less defined by the mineral structure of the rocks than by
their organic contents. Accurate mineralogical distinctions, and an order of
superposition determined by natural sections, must form the first foundations of
the geology of every country. Organic remains often help us to unite together
disconnected base lines. They also enable us to subdivide the successive de-
posits of one epoch, in cases where all other means fail; and in speculating
on the former conditions of the earth they are invaluable: but they can in
no instance supersede the necessity of studying in detail the structure and
superposition of the great mineral masses composing the crust of the globe.
6. In the Cumbrian system, the elevation of the old slate rocks appears to
have been produced by the protrusion of mountain masses of granite and
syenite. In the higher parts of North Wales, the strata are thrown into vast
undulations ranging parallel to the principal mountain chain; but we find no
obvious centre of dislocation. This fact however throws no difficulty in the
way of the igneous hypothesis of elevation ; as we know that the most violent
volcanic action is often felt at a great distance from the focus of eruption.
The parallelism of the undulations seems however to prove, that they were
not produced by different shocks of earthquakes succeeding each other after
long intervals of time.
As the earth has apparently diminished in temperature, we have a right to
look for some indication of a contraction of its dimensions. May not some of
the great parallel corrugations of the older systems of strata have been pro-
duced by such a partial contraction ?
7. In stating that volcanic action could not be brought under the laws of
any constant force, I merely made a reference to the irregular and undefined
nature of its effects. The degradation of the solid portions of the earth by
aqueous action may in a certain sense be considered constant ; because there
is a demonstrable provision in the laws of nature for the perpetual circulation
of water over the surface of the globe. But who can point out, compatibly
with the known laws of chemical action, a provision for the eternal and uni-
form circulation of volcanic fire through all parts of the crust of the globe—
to go its rounds with regularity, and, during given periods of time, neither to
increase or diminish in intensity? If such a supposition be started, it can
only be regarded as a mere gratuitous and most complicated hypothesis ; and
ought not ever to be assumed as the basis of @ priori reasoning.
K 2
68 Prof. Sepewicx on the general Structure of the Cumbrian Mountains.
Every case of volcanic combustion may be only an instance of chemical
combination on a great scale ; in which case, after it ceases, the particles acted
on are held together by new affinities more powerful than those which existed
among them before, and are in a new condition of chemical equilibrium.
Each successive instance of volcanic action must bring the crust of the earth
nearer and nearer to a state of ultimate chemical quiescence: volcanic fires
like all other fires must exhaust themselves; and must cease entirely, when
the whole crust of the earth has reached its highest state of oxidation, or when
the solid parts are in that state of combination which represents the highest
order of chemical affinities compatible with the physical constitution of the
earth. Whether the earth is ever actually to reach that state, is a question
not affecting the hypothesis, and, of course, admits of no reply.
Or we may argue on another hypothesis—that volcanic action is produced
by the penetration of water through the surface of the earth, to a liquid mass
of highly heated matter far below. Even in this case there must be some che-
mical action: for we know that unoxidized bodies are always present ; and if
these produce some influence on volcanic products, they must also produce
some influence, however small, on the intensity of volcanic force. Let us,
however, exclude the effect of chemical action altogether ; still, volcanic action
must diminish in frequency and intensity, during the evolution of the succes-
sive geological periods, by the mere refrigeration of the earth (a fact implied
in the terms of the hypothesis), and by the greater difficulties offered to the
penetration of water through the parts which have gradually become solid.
Perhaps, however, it is best to exclude all hypotheses, and to acknowledge
our entire ignorance of the cause of volcanic action. In that case we have no
right to assume, that it either is, or is not, of the nature of a constant force.
To assume either the one side of the question or the other is perfectly gra-
tuitous ; as it can only be decided by induction from the geological pheno-
mena of every known epoch.
As a matter of observation, modern volcanic forces appear to have modified
the earth in two ways. First, by violent paroxysms, splitting up the crust of
the earth, and producing lines of volcanic vent (such as those described in the
works of Humboldt and Von Buch), generally of small curvature, and extend-
ing through great geographical regions. Secondly, by local action on the
great lines of vent, producing all the ordinary phenomena of volcanic cones
and eruptions of lava. To the former kind of action, the forces which have
produced the elevation of some of our mountain chains appear to have been
most nearly assimilated.
Walton, May 18233.
Appendix to Professor Sepawick’s Paper entitled “An Introduction
to the General Structure of the Cumbrian Mountains.”
[Read November 6, 1833.]
IN the preceding paper, p. 49 et seq., describing in detail the range of a band
of limestone and calcareous slate separating the upper from the middle division
of the schistose rocks of the Cumbrian mountains, I have mentioned two great
faults, between Coniston-water Head and Windermere; one throwing the
calcareous beds to the south, and the other to the north, of their line of
bearing. Both these faults are of enormous magnitude, and the calcareous
slate between them, ranging about 40° north of true east, past two or three small
mountain tarns, terminates in some broken masses, just where a cross road
strikes off from the Ambleside turnpike to Skelwith bridge; being there cut
off by the most northern of the two great faults above mentioned. This part
of the range is about a mile and a half in extent; and the calcareous bands,
commencing in a low hill north-east of Coniston Hall, exhibit some disloca-
tions which, although of comparatively small extent, deserve notice.
About one third of a mile from their commencement, the calcareous bands
are cut through by a fault, throwing them fifty or sixty feet towards the south-
east. The line of dislocation is marked by a small watercourse, and by some
masses of calcareous slate thrown out of their bearing. The beds then regain
their strike (about 15° north of magnetic east), and run to a round hill, due
south of the lowest tarn. There they are again cut off, and shifted about 150
or 200 yards, to a point south-east of the tarns. Thence they range (nearly
with the same strike as before) uninterruptedly for more than half a mile;
increasing, however, gradually in dip as they approach a mountain mass of
green slate and porphyry, called Pool Brow. Immediately beyond a mountain
road leading to Arnside, there is a third dislocation, throwing the beds about
120 paces to the south-east. Beyond this interruption the limestone is again
continued, but is soon after (in consequence, I believe, of a number of small
dislocations), spread over the brow of a hill (Lemestone Hill), and descends to
the angle of the Skelwith bridge road, the extreme point being marked by a
kiln on the Knipe Fold estate. Here the limestone bands are again cut off,
being thrown (as stated in p. 52) more than a mile to the north of their
bearing.
68* Appendix.
Such details as these may be considered of small importance, but they
belong to the history of the formation I am describing. There are, however,
other phenomena of more importance, and extremely well exhibited along the
line just described. The calcareous slates sometimes pass into strong beds of
limestone: but without exception they exhibit true cleavage planes, which often
almost obliterate the lines of stratification ; and the calcarecus beds (even where
they pass into a pure subcrystalline limestone), when struck with the hammer,
break into tabular masses, having their faces parallel to the cleavage of the
slates. These calcareous beds abound with Corals, Bivalves, Trilobites, &c.,
and have a south-easterly dip, varying from 30° to 60°. The planes of cleavage
generally dip toward the north-west, at a great angle. They sometimes strike
with the beds, and sometimes cut obliquely through them; but I could not
find any instance where the planes of cleavage and the true beds coincided.
I stated (in the paper before mentioned, p. 54) that the calcareous bands
were cut off by the Shap granite, and the assertion was, I believe, true: but
during the past summer I ascertained that these bands reappear, in their line
of strike, on the north side of the granite boss, in the new road cut through
the morass; from Shap Wells to the turnpike leading to the village of Shap.
The same calcareous bands appear also in the rivulet, about a quarter of a
mile north of the wells, nearly with the strike and dip above mentioned, and
so pass under the horizontal beds of the old red sandstone and conglomerates
which form the base of the mountain limestone ridges, stretching out on the
north side of the district. It deserves remark, that the calcareous slates are
broken through by porphyritic masses, but reappear in the form of calcareous
conglomerates imbedded in the greywacké. These conglomerates are im-
pregnated with pyrites, and give rise to the mineral waters of Shap Wells.
It appears, therefore, probable, from what has been already stated, that the
Shap granite interrupts the continuity of the calcareous bands, and is there-
fore of an origin posterior to them. The same truth is rendered probable by
the extreme induration of the upper greywacké series, where it approaches
the granite. The conclusion is, however, put out of all doubt by a fact I
observed for the first time, this summer; viz. that near the farm-house called
Wasdale Head, the granite is in two places seen to send veins into the
greywacké; which near its contact with the granite passes into a rock, very
much resembling the more crystalline varieties of the Cornish killas. ‘These
phenomena, taking place among the upper fossiliferous divisions of the slate
series, are of considerable theoretical importance ; but I shall not dwell upon
them, as I shall have to return to the subject in a subsequent paper.
{1].—Description of a Series of Longitudinal and Transverse Sections
through a Portion of the Carboniferous Chain between Penigent and
Kirkby Stephen.
By tHe Rev. ADAM SEDGWICK, V.P.G.S. F.R.S. &c.
(WOODWARDIAN PROFESSOR IN THE UNIVERSITY OF CAMBRIDGE. )
[Read March 2 and 16, 1831.]
§ 1. Introduction.
HAVING in the preceding communication pointed out some peculiarities in
the position of the great central carboniferous chain (which extends from the
neighbourhood of Derby to the Scotch Border), with the view of connecting
it with the calcareous zone of the Cumbrian mountains ; I now proceed to
describe in detail the composition of a very remarkable portion of it, forming
a mineralogical link between the High Peak of Derbyshire and the region of
Cross Fell. ‘The facts adduced will serve to explain some of the changes the
chain undergoes in its range between one extremity and the other; and will
also supersede the necessity of many details respecting the carboniferous zone
of the Cumbrian mountains, which once formed, beyond doubt, a continuous
part of the same system, and is now only separated from it by the great breaks
and dislocations described in the preceding paper.
The principal section * about to be described, commences at Penigent in
Horton parish, and, passing through the highest mountains of the range,
ends in the plain of Kirkby Stephen. T'wo other sections} connect this line
with the ridge of mountains on the west side of Swaledale. Nearly at right
angles to the same line are drawn a series of transverse sections+, prolonged
across the breaks connected with the great Craven fault. They will, I hope,
place in a striking point of view some of the internal movements which took
place when the chain was elevated, just before the period of the new red
sandstone.
The old red conglomerates do not appear in any part of the longitudinal
section, but they are exposed in one of the transverse sections§, and are seen
* See Plate VI. fig. 2. + Fig. 3. and 4. t Fig. 5. 6. 7. 8. and 9. § Fig. 8.
70 Prof. Sepe@wick on the Carboniferous Chain
in several other places, at the junction of the carboniferous chain with the
unconformable greywacké mountains of Westmoreland. ‘There can, there-
fore, be no doubt that the lowest beds of the carboniferous system of this
region rest upon an irregular surface of unconformable greywacke slate, from
which they are separated, here and there, by great irregular masses of old
red conglomerate. |
The whole overlying series is essentially composed of alternating masses of
limestone, sandstone, and carbonaceous shale, terminating in a great system
of beds connected with the millstone grit. The limestone groups are incom-
parably the most continuous and the best defined, and form a kind of frame-
work by which all the other component parts are held together. They are
six in number, and will be referred to in the several sections, under the fol-
lowing names :—Ist, Great scar limestone. 2nd, Black marble limestone.
3rd, Strong post limestone. 4th, Wold or Mosdale Moor limestone. 5th, Four-
fathom limestone. 6th, Main, or twelve-fathom limestone. The names given
to the Ist, 5th, and 6th groups are in common use in, the North of England,
and on that account ought not to be changed. The other three groups might
be conveniently designated in the section by the names 2nd, 3rd, and 4th
limestones: but these names would cease to have any propriety if applied to
remote parts of the same chain, and therefore ought not to be made use of,
except in local description.
To prevent a frequent repetition of nearly similar details, I shall commence
with an enumeration and description, in the ascending order, of all the re-
markable groups of strata which appear upon different parts of the lines of
section.
§ 2. General Section of the whole System, in the ascending order*.
1. Great Scar Limestone. otal thickness about 600+ feet.—The term
scar, in the dialects of the North, means any bare precipice on the face of a
mountain, and is applied with great propriety to this limestone, which in all
parts of its range is marked by grey precipices and mural escarpments. The
grey scars near the base of Ingleborough, of Penigent, and of Whernside ;
the mural precipices above Giggleswick and Malham, and the magnificent
cavernous gorge of Gordale, are among the striking exhibitions of this de-
posit, and present a nearly exact counterpart to the features of the same lime-
stone in the High Peak of Derbyshire.
* See Pl. VI. fig. 1.
+ This number is merely approximate, and there are only a few places where the whole thick-
ness is visible. It is probably very variable, as the deposit has taken place upon an uneven, un-
conformable surface.
from Penigent to Kirkby Stephen. va
Like the Peak limestone, the group, here described, is full of fissures and
clefts (often of unknown depth), in which the mountain torrents are engulfed ;
and, after running in subterranean channels, and uniting with the waters of
other sources, emerge in copious streams in the lower regions of the neigh-
bouring valleys. But of all the phenomena connected with the drainage of the
waters through the scar limestone, the beautiful reciprocating well above
Giggleswick is the most remarkable, and even to this may be found a counter-
part among the limestone hills of Derbyshire.
It contains, like the limestone of the Peak, many caverns of consider-
able extent ; some partly open to the surface, others only to be approached
through a narrow horizontal entrance. In some of these great subterranean
recesses we find waterfalls of no common grandeur; in others we see no
waters, but we hear them roaring among the inaccessible chambers of the
rock. Asa general rule, these caverns have perpendicular walls, and often
nearly flat roofs. However greatly modified, they have, therefore, not been
formed by the mere long-continued erosion of the waters passing through
them. When the conformation is such as I have pointed out, the opposite
walls are portions of the same stratum, and the flat roof is composed of the
superincumbent stratum ; and the cavern has the exact appearance of having
been formed by one of the beds sliding off horizontally from the side of a ver-
tical joint. Ido not think such a movement impossible. The component
strata, when first lifted up, were perhaps in a very unequal state of solidifica-
tion, so that one part would offer a greater resistance in any given direction
than another. The points of greatest stress might also be very unequally dif-
fused ; and, in consequence, the strata may have started among themselves,
and undergone considerable relative movements, not unlike those we may
observe among the timbers of a ship which has been wrecked, and thrown
violently on her beam ends. In this way some caverns may have been formed
by the sliding of solid beds upon each other, some by the gradual removal of
incoherent or imperfectly solidified portions of the rock, and others by both
causes combined. The subject is one of considerable difficulty, and I wish to
exclude no agent from its proper share in producing the existing appearances.
All I contend for is, that in such cases as I have alluded to, the slow erosion
of the waters flowing through the interior chambers of the scar limestone is
not the kind of action by which its great caverns have been scooped out.
The mineral characters of the scar limestone are too well known to be
detailed at any length. The great bottom shales found in so many parts of
England are almost entirely wanting in the line of section, and in the neigh-
bouring country. Perhaps they are represented, in a very obscure form, by
some dark-coloured beds of impure limestone, separated by bands of shale,
Wes Prof. Sepewick on the Carboniferous Cham
which occur here and there at the base of the series. In the same position
are rarely found some dark and nearly compact beds, resembling the black
marble series, but unfit for use; and in the prolongation of the longitudinal
section towards the north (for example, near Ravenstonedale and Kirkby
Stephen), beds of reddish sandstone alternate with the lower portion of the
sear limestone, and the whole group begins to approximate to the type of the
Cross Fell chain*.
There are no bands of coal subordinate to the limestone on the sectional
lines ; but carbonaceous and bituminous matter are the colouring principle of
all the darker beds. In some instances this colouring matter is so unequally
diffused, that after a recent fracture, or on a polished surface, it appears in
the form of dark cloudy blotches upon a light grey base. It is this arrange-
ment of colours, arising out of the irregular diffusion of the bituminous matter,
which constitutes the beauty of some marbles in the North of England f.
Near the line of section, however, no beds appear in this limestone which are
fit for polishing, and very few indeed which are well suited to the commonest
domestic architecture. In general they have an irregular fissured or shaken
texture, which unfits them for such uses. It is, perhaps, hardly necessary to
add—that their prevailing colours are light grey or bluish grey, from which
they change, through every variety of shade, into dark blue, or biuish black
—that their mineral characters are such as link them to transition limestone
—and that they contain in great abundance corallines, encrinites, and all the
ordinary well-known fossils of the carboniferous limestone f.
The highest beds of this group often become impure, and, for about thirty
or forty feet, alternate with beds of sandstone and calcareous shale; in this
way forming a gradual passage into the next superior group.
2. Group of Sandstone and Shale. Greatest thickness 150 feet.
The thickness of this group is extremely variable, being in some places not
more than twenty or thirty feet: but when it is best developed, it appears to
admit of the following subdivisions :—
(a.) Dark-coloured shale, with nodules of clay iron-stone.
* In various parts of the North of England, where the bottom beds of the scar limestone rest
immediately upon greywacké, they contain rolled pebbles of the inferior rock, and occasionally
pass into a coarse conglomerate form. (See Geol. Trans., Second Series, vol. iii. p- 10, &e. &e.)
This structure seems to have originated in the last feeble efforts of those causes which in other
places produced the great masses of old red conglomerate.
t The Beetham Fell marble, near Milnthorpe in Westmoreland, is the most remarkable instance
of this kind, and it is subordinate to the great scar limestone.
{ Some of the rare corallines, described by the late Mr. Parkinson, were collected from loca-
lities near the line of section. See “ Organic Remains,” vol. ii. Pl. VI. fig. 9. &c. &c.
from Penigent to Kirkby Stephen. 73
(b.) Alternations of sandy, micaceous shale, and brown, micaceous sandstone,
generally of a coarse, flaggy, or slaty structure.
(c.) Strong beds of hard, micaceous gritstone, alternating with similar
masses of slaty texture, and generally surmounted by a few beds of meagre,
sandy shale.
Wherever the shale beds abound, the thickness of the whole group is ex-
tremely variable. The micaceous flagstones of the middle portion are some-
times wanting, and the group is then composed of carbonaceous shale, iron-
stone, and gritstone. One of the finest exhibitions of this group is at the
waterfall of Hardraw Scar near Hawes. It is also well exposed by the many
torrents which descend from the mountains on both sides of the valley of Dent.
3. Second Limestone, or Black Marble Group. Greatest thickness about
45 feet; average thickness about 30 feet.
This group is distinguished from all the rest by the regularity of its strati-
fication, which often makes it look, on the face of a precipice, like a rude
work of masonry ; also by its dark-coloured, compact beds with a conchoidal
fracture*. Some of these beds take a beautiful polish ; and when they can
be raised in large slabs free from white spots, and without seams or cross
joints, are of considerable value. Unfortunately many of the quarries are
almost spoilt by the cracks and fissures which traverse all the component
strata: and many of the more solid masses are injured by the imbedded or-
ganic remains (such as Encrinites, Caryophylliz, Producte, Spirifers, &c.
&c.), replaced by pure white carbonate of lime containing little of the carbon
and bitumen which form the dark colouring matter of the rock.
The thin bands of bituminous shale, separating these limestone beds, also
contain organic remains ; and, among the rest, innumerable specimens of the
Producta latissima and P. Scotica, which may be almost considered as charac-
teristic of this group.
Nearly all the quarries, in the neighbourhood of the lines of section, from
which the black marble has been exported, are found in the valley of Dent.
I have however traced them, in the exact position here indicated, through
Horton parish, on both sides of Chapel Je Dale, in Kingsdale, and in Gars-
dale. They may be also traced through a part of Wensleydale, and appear
at the top of the precipice of Hardraw, over which tumble the waters of a
mountain torrent, forming one of the grandest waterfalls in the North of
England. They are there however so much changed in structure, that they
* Most of the beds before polishing have a bluish tinge, and their weathered surfaces are of a
greyish colour. On being burnt, they are reduced to a beautiful white calx, all the colouring bi-
tuminous matter being driven off.
VOL. IV.— SECOND SERIES. L
(C3 Prof. Sepewick on the Carboniferous Chain
are only identified by their relation to the other groups, and by beds of the
Producta latissima and P. Scotica which follow them.
4. Group of Sandstone, Shale, and Calcareous Grit, &c. Maximum thick-
ness 150 feet; average thickness about 60 or 70 feet.
The arrangement of the subordinate parts of this group is extremely vari-
able, as the different masses frequently seem to replace each other. In an
approximate way the group may be subdivided as follows.
(a.) Dark-coloured shale, with one or two bands of crow-limestone or cal-
hard.
(6.) Hard beds of brownish, siliceous grit, generally of a somewhat slaty
texture ; containing subordinate, strong, hard beds of a calciferous grit, some-
times ferruginous.
(c.) Alternating bands of hard, brown, flaggy grit and shale.
The beds of calciferous grit are extremely characteristic of this group, and
are sometimes so expanded as to form a prominent part of it. Within they
are of a greyish colour; but their weathered surfaces are generally brown,
from the presence of iron. The quantity of calcareous matter contained in
them is very variable, as they pass at one extreme into pure, close-grained,
siliceous grit; and at the other, where organic remains are abundant (which
is however rarely the case), into a nearly pure limestone.
The crow-limestone or calliard is not so characteristic, as it is, here and
there, subordinate to all the great masses which alternate with the six groups
of limestone. It may however be proper to explain these synonymous pro-
vincial terms, as they will be frequently used in the following details. They
are applied to a very impure variety of shelly limestone which is sometimes
associated with gritstone, and then passes irregularly into calciferous grit,
but most frequently is subordinate to the beds of dark-coloured shale. In the
latter position it sometimes appears in the form of concretions ; but more fre-
quently in irregular bands, seldom more than one or two feet in thickness.
The outer surface of this crow-limestone is very irregular, and is generally
covered with a thin, earthy coat of hydrate of iron. It is very ponderous, in
parts reaching the specific gravity of the nodules of argillaceous iron ore. It
is difficult of fracture ; but when broken almost always shows a bluish, cal-
careous interior; and rarely has a core of nearly pure limestone.
It contains innumerable organic remains, especially large specimens of a
species of Producta ; and from the crescent-shaped impressions of that shell,
the miners sometimes designate it by the name of horse-shoe limestone*. It
* The specific characters are generally obscure; but I believe the large Productz belong chiefly
to the species Producta Scotica.
from Penigent to Kirkby Stephen. 75
is obvious, that it owes its existence to the accidental presence of beds of
shells (chiefly of the genus Producta), during the deposits of the great masses
of shale—that these shells supplied a considerable portion of the calcareous
matter—and that they also caused the precipitation or separation of the ferru-
ginous and pyritous matter, and of the other constituents commonly found
together in these calliards.
In the upper division (c.) of the group here described, there is in some
places a band of coal: but as it is in general not more than a few inches in
thickness, it has never been worked to any profit*.
5. Strong Post Limestone. 'Thickness nearly the same as the black marble
series (No. 3.), averaging about 30 feet.
This group, in its mode of bedding, in its colour, and in the dark bands of
shale which alternate with the strata, nearly resembles the black marble system.
The beds are however stronger, thicker, and coarser ; and though generally
unfit for polishing, afford a beautiful material for the construction of door-
posts, small pillars, coignes, coping-stones, &c.+
I have traced this group in the position here indicated, through the flanks
of Ingleborough, Penigent, and Whernside; all round the valley of Dent;
through the upper part of Garsdale ; and through a part of the chain of hills
between Wensleydale and Swaledale. There can, therefore, be no doubt of
its continuity through all the country bordering on the southern and central
part of the principal section.
6. Alternations of Fissile Gritstone and Carbonaceous Shale. Greatest
thickness 150 feet ; average thickness about 120 feet. The alternations are
indefinite ; but on the whole the group may be conveniently separated as
follows. .
(a.) Alternations of gritstone and shale; the gritstone sometimes rising in
strong beds ; but more frequently micaceous and of a flaggy structure.
(6.) Carbonaceous shale and gritstone with a band of coal ; also with two
thin bands of crow-limestone or calliard.
(c.) Hard, brown, and light grey, micaceous grit, with bands of shale ; the
micaceous grit in some places highly fissile, and forming a good roofing slate.
The most important bed in this group is the coal in division (5). It is ex-
* TI have been informed that works were formerly opened in this bed at Load Gill on the south
side of Dent, and also on the north side of Garsdale, but with very little success.
+ Attempts have, I believe, been made, but without success, to polish some of the darker beds
containing many very small encrinital stems. A small, dark-coloured, encrinital marble, found in
Derbyshire, and other parts of the carboniferous chain, is provincially called bird’s-eye marble ;
and is occasionally found subordinate to the black marble group.
i be
76 Prof. Sepewick on the Carboniferous Cham
tensively worked in the Barbon and Casterton liberties, where it is about
fourteen inches thick. The lower part of this bed is however so impure, as
to be unfit for domestic use, and is chiefly consumed in lime-works*. An
attempt is now making to work the same bed in the adjoining liberty of Dent.
It is also worked at Stoth pits near Hawes, in Baw Fell above Sedbergh, and
at Kitchen Gill on the side of Naitby Fell near Kirkby Stephen ; and there
are many traces of old works in the same bed near Garsdale Head{. Iam
certain that in all these places the coal is very nearly on the same geological
parallel. It must therefore have been very widely extended. But it was by
no means continuous, as is proved by innumerable sections through this group,
which perpetually varies in its composition, and in which there is often no
indication whatsoever of the coal-bed. It deserves remark that the two thin
calliard beds appear to be continuous for many miles.
The slate-beds in division (c.) are next in importance. They have been
extensively worked in several places ; especially at Wydern and Kirkbank in
the valley of Dent: but the most beautiful example of these beds is in Cow
Gill, about five miles above the village, where there is a quarry of hard, white,
siliceous grit capable of being split into very thin flags, coated with silvery
mica, and forming the most beautiful roofing slate I have seen in the carboni-
ferous chain.
7. Mosdale Moor or Wold Limestone§. Average thickness from 30 to 40
feet.
* Section, in descending order, from the shaft of the Barbon coal-pits :—
Feet. Inch. Feet. Inch.
ils ANIME Roll, 85 coooa0gado0e 52 5. Alternations of gritstone and shale 12 0
2. Plate (calcareous shale) ...... 1 6 Goo haley. icis .sareieierietete svccssvees 30: 0
3. Limestone (the fourth, or Mosdale 7. Crow-limestone....... sieroieietels 20
Moor limestone, of the general 8. Plate, with a three-inch crow-coal 1 6
SECION) Wiatelsienerehcitaieues oe ielele 21240 OF IGritstonewlrcmi siete ieleis <r ei o:eveler ede.
A. s (GYIEStOME Uelol cielo sieiels oleieheusele >= 27.0 10: UC Galle isia epetetotekioteeiieir: Po Oi Ly G2
The crow-limestone (No. 7.) more commonly appears in the form of two distinct bands sepa-
rated by a bed of impure, pyritous shale. In this section, the beds seem to have run together ;
probably by the partial disappearance, or thinning out of the pyritous shale.
+ The attempt was unsuccessful, and the works have been deserted since the above passage was
written.
{ I have been informed that the coal of Kitchen Gill is eighteen inches thick; but I have seen
no accurate sections of the works. In the places where it has been most worked the average
thickness of the bed is not much more than a foot.
§ The group is known in some of the valleys under the name of Wold-limestone: as, however,
this word designates any tract of dry green pasture land rising out of the morasses of the carboni-
ferous chain; and as this kind of soil marks, more or less, the range of all the calcareous groups;
the term wold is a bad distinctive name for any one of them.
from Penigent to Kirkby Stephen. ig
This limestone is less regularly bedded than the two preceding groups
(Nos. 3. and 5.). The bottom beds are generally of a grey colour and of an
open, shaken texture. They are frequently surmounted by two or three
coarse, strong beds of a grey colour, not to be mineralogically distinguished
from the most ordinary varieties of the great scar limestone, containing
various fossils, apparently distributed without regularity. The higher beds
become thinner, more compact, and sometimes contain many encrinital stems,
and are occasionally of a dark colour. In the highest part of the series, the
beds alternate with bands of dark shale, become impure and ferruginous, and
frequently pass into the state of crow-limestone or calliard, with many large
Product.
Detailed sections of this division would, no doubt, offer many modifications ;
but few quarries have been opened in it, since it contains no beds of any pe-
culiar value, and many parts of it are obscured by alluvial accumulations. It
may, however, be tracked without any difficulty, wherever it rises to the day,
along the sides of all the mountains which range near the lines of section ;
as well as in all the various systems of valleys which branch among the moun-
tains between Askrigg and Kirkby Stephen. It has indeed been important to
make out its continuity, as it forms the roof of a series of beds to which the
Barbon coal seam is subordinate (No. 6. (5.))
8. Alternations of Sandstone, Fissile Gritstone, and Shale. 'This is by
much the most remarkable of all the groups alternating with the beds of lime-
stone. Its greatest thickness is perhaps as much as 350 feet; and its
average thickness in the central and southern parts of the section is about
200 feet.
Like all the other masses composed of sandstone and shale, it is extremely
variable in its structure, the subordinate parts either disappearing or replacing
each other. In some places the alternations are indefinite: but on the whole
it admits of the following approximate subdivisions.
(a.) Alternations of slaty, micaceous gritstone and shale, sometimes con-
taining bands of crow-limestone.
(b.) Shale with bands of gritstone.
(c.) Micaceous, fissile gritstone with thin bands of shale, and with subordi-
nate masses of coarse gritstone.
There are very fine quarries in the lower division (a.), especially at Raw-
thay Gill (between Ravenstone Dale and Sedbergh), where in colour the
gritstone somewhat resembles the Pennant stone of Bristol; but is more
micaceous and fissile, and generally of a more open grain. In the higher
part of the upper division (c.), the fissile beds have been extensively worked
78 Prof. Sepewick on the Carboniferous Chain
for roofing slate and flagstone, (e. g. Garsdale Hall pastures, High Pike in
Dent, and all round the upper precipices of Ingleborough, &c. &c.) They
are generally of a dark bluish grey colour, and are liable to decomposition.
Round Ingleborough they are however of a brownish grey colour, and of a
closer texture. Strong beds of grey sandstone occur in the lower part of this
division (c.); which sometimes, though very rarely, become of so coarse a
texture as to resemble millstone grit.
Two thin bands of bright coal have been found (at Rawthay Gill and Ingle-
borough), one in the lower (a.) and the other in the upper division (c.) of this
group: and between Brough and Stainmoor (to the north of the line of section)
it contains a bed of coal, which has been worked to a considerable extent.
In some of the hills near the head of Wensley Dale (e.g. Stag’s Fell near
Hawes, &c.) the shale-beds almost disappear; and the group passes into a
complex deposit of hard, grey, micaceous gritstone, some parts of which afford
a good building-stone, and other more fissile parts, a material for flagstone
and roofing slate.
9. Four-fathom Limestone. Notwithstanding the name by which it is de-
signated in the mining districts of the North of England, this limestone group
is of much more variable thickness than any of the three preceding (Nos. 3. 5.
7.): but I believe that it in no instance entirely disappears. In some places it
is not more than ten or twelve feet in thickness; in others it is much more ex-
panded, and is not less than thirty or forty feet thick. Changes ranging within
these limits are several times repeated, as may be proved by tracing these beds
through the mountains at the head of Dent and Garsdale. Its average thick-
ness in these regions is perhaps less than that which is indicated by its name.
The bottom of the series, as usual, is impure, and is deposited in irregular,
grey beds with traces of fossils. "The middle portion is much more regularly
bedded, and contains innumerable fossils, especially encrinital stems. Indeed,
where the middle and upper portions of this group are largely developed, we
find that large encrinital stems form the greater part of the substance of the
successive beds; and where the same portions are ill developed, the stems are
fewer in number and less in size *—a fact, which shows the large share these
extraordinary fossils had in the formation of the several beds.
At the top of this group we here and there find cherty, siliceous beds, with
casts of encrinital stems (like the well-known Derbyshire screw-stones) alter-
nating with bands of calcareous shale, containing innumerable, flattened Pro-
ducte. These beds, though unimportant in themselves, offer us a valuable
* In the hills south of Dent the variety called bird’s-eye marble abounds in this group.—See
above, Note + to page 75.
from Penigent to Kirkby Stephen. 99
analogy by help of which we compare them with the cherty beds in the four-
fathom limestone of the mining districts of Swaledale and Arkendale.
The strongest masses of this group (in which the fossils are all more or less
white and crystalline, and imbedded in a dull grey, nearly compact limestone),
are, on the north side of Garsdale, extensively quarried for the Kendal marble
works ; and works were opened on the corresponding strata in the valley of
Dent, but are now deserted; a better material having been there discovered
in the twelve-fathom limestone.
10. Gritstone, Coal, and Shale. Thickness varying from 50 to 80 feet.
The prevailing order appears to be nearly as follows :
(a.) Thin-bedded gritstone, sometimes coarse-grained.
(b.) Coal and carbonaceous shale.
(c.) Bands of light-coloured, micaceous grit.
The lowest division (a.) is of very variable structure. It is in some places
very coarse-grained ; but in Uldale, between Swath Fell and Baw Fell, it
passes into a dark, compact, siliceous mass, exactly like the metalliferous chert
of Swaledale. Along the line of section this cherty form is, however, an ex-
ception to the prevailing structure. The coal varies in thickness from a mere
trace to two feet, and is in many places of excellent quality*. When it reaches
its maximum thickness, it is, however, generally mixed with shale and other
impurities. 'To the north of Ingleborough, no member of the whole series is
more continuous than this coal-bed and its superincumbent shale ; and it has
been worked, more or less, in almost every mountain near the lines of section.
But in Ingleborough and Penigent the whole group here described thins out
to such a degree, that the four-fathom and twelve-fathom limestones become
confounded, and present a single unbroken escarpment. ‘T’o the north of the
line of section the same coal is now extensively worked in the neighbourhood
of Brough.
11. Twelve-fathom Limestone. 'This system of beds makes a striking fea-
ture in many parts of the carboniferous chain of the North, beg the highest
limestone group of sufficient thickness to give any character to the soil or to
produce a distinct escarpment. In some districts it forms the crown of a long
* This coal was formerly worked to a considerable extent, by means of horizontal drifts, under
Great Colm, on the south side of the valley of Dent, though not more than five or six inches in
thickness. It was of excellent quality, and in such request, that about seventy or eighty years
since, it was sent on pack-horses over the mountains as far as Kendal for the use of the black-
smiths’ forges, &c. I know of no fact which places in a more striking point of view the great im-
provements in internal communication within the period above mentioned, A supply like this
would now be utterly worthless. The extensive manufactories of Kendal have long been supplied
with fuel from the great Lancashire coal-fields.
80 Prof. Sep@wick on the Carboniferous Chain
succession of tabular hills; in others, it forms a terrace on the sides of the
mountains terminating a succession of green pastures, which rise in inter-
rupted slopes from the neighbouring valleys. Above it the strata often lie
concealed under accumulations of black turf bog ; and the highest summits of
the mountains terminate in great irregular masses of tabular millstone grit.
Near the line of section its greatest thickness is about eighty feet ; but in one
or two places it thins off and almost comes to an edge ; and its average thick-
ness is under twelve fathoms.
The mineral characters of the group are so nearly the same with those of
the four-fathom limestone, that the same description may almost serve for both.
Its prevailing colours are grey, and some of the beds exactly resemble ordinary
specimens of the great scar limestone. Most commonly this group is distin-
guished by the abundance of encrinital stems, which in some rare instances
so nearly constitute the whole mass of the strata, that the cementing principle
is almost wanting, and the weathered surfaces of the blocks rapidly disinte-
grate and fall into innumerable cylindrical fragments*. In general, however,
the encrinital fragments are held firmly together by a grey, subcrystalline, cal-
careous cement, and form hard beds, the most regular of which admit of a
good polish. The most beautiful variety of this fossil marble, is obtained from
one or two of the upper beds of this group, and is quarried at Snays-wold Fell,
between Dent and Garsdale. The dull grey base in which the fossils are
commonly imbedded, is there enlivened by many dark cloudy blotches, arising
out of the irregular distribution of the colouring bituminous matter. The
group appears to terminate in a few, thin, impure beds of dark bluish lime-
stone alternating with slaty gritstone and carbonaceous shale f.
So far the relations of the successive groups may be ascertained with a near
* Beds of this kind burn to a pure lime very readily: but on extracting it from the kilns, in-
stead of coming out in such lumps as are convenient for transport, the lime frequently falls at once
into a fine impalpable powder. Some beds of this kind overlie the coal-seam (No. 10 (0.)) at a
hill called The Cross in the valley of Dent.
+ Section of the marble quarry of Snays-wold Fell, in the descending order :—
Feet. Inches. Feet. Inches.
1. Carbonaceous shale............ 4 0 5. Hard, dark blue limestone, and a
Oe Mlagey, brown Grit cece. cle = ier 40 thin band of shale ......... wa T a6
3. Hard, dark blue, impure limestone 2 4 6. Fine, compact bed, with crystalline
4, Shale and gritstone irregularly mix- stems of Encrinites....... » 00 leg LO,
ed together, and containing much 7. Shattered beds and shale....... » 046
calcareous matter in nodular 8. Strong Encrinite bed...... Soca whe
masses, with large stems of En- 9. Lower calcareous bed, not exposed
CEIMITES .ce ee cere ews essences O10 in the section.
Nos. 6, and 8. are the only beds used in the marble works.
Srom Penigent to Kirkby Stephen. 81
approach to accuracy, as the various limestone deposits offer a series of good
base lines to which all the distant observations may be referred. But in the
remaining part of the ascending series we lose all our lines of verification ;
and the sections, as might have been expected, differ very widely in their
details. Out of much apparent confusion, we may, however, make out an
approximate order, and divide a great thickness of strata into groups suf-
ficiently extended to admit of a general comparison among themselves.
12. Great upper Shale. Thickness varying from 40 or 50 tonearly 200 feet.
This group is complex, containing, here and there, a band of crow-limestone,
and having many subordinate masses of grit, generally of a thin, slaty texture.
On the whole, however, it is characterized by a dark-coloured shale, and
makes a remarkable feature in the higher parts of many of the mountains,
being often laid bare by the deep water-channels which intersect the boggy
region between the first millstone grit and the twelve-fathom limestone.
On the south side of Baw Fell (in the brow above the marble quarry men-
tioned above (p.79.)), a five-inch coal is, I believe, subordinate to this group ;
and, on the west side of the mountain, it contains a strong band of crow-lime-
stone. In apart of Swaledale it contains the main chert, black beds, red beds,
iron beds, &c. enumerated in the detailed sections of the miners in that district.
13. First Millstone Grit. Thickness varying from 20 to 60 feet.
The term is here used with considerable latitude, being applied to a group
of strata, a part only of which has the true character of millstone grit. When
used more strictly, it designates a coarse, open-grained, siliceous gritstone very
irregularly bedded, often subdivided by lines not parallel to the planes of stra-
tification, and usually containing a considerable quantity of kaolin, and small
rounded pieces of opaque quartz interspersed irregularly through its mass.
The prevailing colour of the group, here described, is light grey ; but this
is by no means constant. The characteristic millstone grit is sometimes found
associated with all parts of this group ; sometimes only with the upper part ; in
which case the lower beds generally consist of a hard, light grey, thin-bedded
sandstone. Sometimes the millstone bands are entirely wanting, and then the
group (especially when the beds alternate with shale) cannot be easily sepa-
rated from that which is next superior to it.
It is finely exposed in the last precipice of Penigent, and in the strata which
form the crown of Ingleborough. It also forms a part of the higher escarp-
ment of Whernside and of Great Colm*.
* The open-grained varieties of gritstone in this group sometimes decompose into a sharp sili-
ceous sand, which is much used in the saw-mills where the marble blocks are divided into thin
slabs fit for polishing.
VOL. IV.——SECOND SERIES. M
82 Prof. Sepewicx on the Carboniferous Chain
14. Alternations of hard, thin-bedded, brown gritstone, and dark-coloured
carbonaceous shale, with two or three beds of coal. Average thickness along
the principal line of section about 60 feet.
In some of the neighbouring regions (for example among the mountains of
Swaledale Head), this group contains two or three thin beds of crow-lime-
stone, and its aggregate thickness is about 200 feet.
The only bed of coal which has been much worked, is in the lower part of
the group, and varies from eighteen inches to nearly four feet in thickness.
At Tan Hill near the highest part of the road from Brough to Arkendale, and
at Turna Fell near Hawes, this coal is of good quality, and is extensively
worked. Near the top of Penigent, of Whernside, and of Great Colm,
horizontal drifts have been carried into this bed ; but it is of bad quality, and
not fit for domestic use, being mixed with ferruginous and pyritous shale*.
The hard, brown beds of grit alternating with the carbonaceous shale, are
provincially termed szll-stones.
15. Second Millstone Grit. The limits of this group are very ill defined,
and its thickness varies from 40 or 50 to 120 feet.
At the top of Penigent and Whernside it is represented by an open-grained,
thin-bedded, siliceous grit, no part of which has the appearance of millstone.
But at the top of Baw Fell, Wildboar Fell, and some of the Swaledale hills, it
passes into great, thick heds of the finest millstone grit.
16. Alternations of gritstone and shaie, with traces of a thin bed of coal.
Thickness about 100 feet.
The band of coal is found, here and there, near the bottom of this division.
In general the subordinate shales are meagre, sandy, and micaceous; and
the alternating beds of grit are thin and open-grained, like certain bands
associated with the groups of millstone grit.
There is just a trace of this group at the top of Wildboar Fell, and perhaps
at the highest point of Whernside, under the soil and morass. It is best ex-
posed under the highest summit of Shunner Fell, and near the top of a part
of the high ridge between Mollerstang and Swaledale Head.
17. Upper Millstone Grit. Thickness 120 feet.
* As not less than three beds of coal are found, here and there, subordinate to this group, it
would be impossible to prove that in all the above-mentioned places the coal is precisely upon the
same parallel. It is, however, so considered by the miners of the neighbouring districts. Near
Kirkby Stephen it generally passes under the name of the Tan Hill seam, that being the locality
of the most valuable coal work, established upon the bed in question. There, however, the re-
lations of the coal to the neighbouring groups are somewhat obscure ; and in a general description
the Turna Fell seam is perhaps the best name which can be given to it.
from Penigent to Kirkby Stephen. 83
__A most characteristic exhibition of this group is seen at Shunner Fell top,
and on some other of the highest eminences of Swaledale ; but it does not
appear anywhere upon the longitudinal line of section. Like the other
groups (Nos. 13. and 15.), it varies in structure; but it contains, and passes
into, masses of the most characteristic millstone grit.
Here terminate the details of the general section; and with one limited
exception, no higher beds appear among the mountain ridges extending from
Penigent to Stainmoor, and to the mining districts of Arkendale and Swale-
dale.
Before commencing the description of the longitudinal section, it may be
expedient, for the purpose of easy reference, to give a tabular view of the
preceding detailed general section.
Carboniferous limestone series, &c., in the descending order*.
Greatest thickness
in Feet,
PPO pper WUlIstONe Grit, GLC. 66s soe sic cic.c cence ccce as nowtne cine daveceecescevcs 120
16. Gritstone and shale, with traces of a thin bed of coal .....eeecceeee siteieees. LOO
15. Second millstone grit, &c. ...... Daikiehis tale ae Li apSele's el dint oele siecle oblesiee De 4120
14, Alternations of hard gritstone, shale, and two or three beds of coal. Mean thick-
MessHADOULTOOVOL 10 ACCEL | is aialelerniejei$,9 eTep0,sse,0 soy epsieuesss Aoosécnacoddnoood. LO
13. First millstone grit, &c. .......... aielorevetele aietarereierote eqeilo.estrepecereteqereysie.a) S10:8 -- 60
12. Great upper shale..... rae aterete ste SWeicfo/atars Se oie e¥e' vlald wie arellshaa Raval oes ees - 200
er Pieleic-fathone HmestOnen cro sie sere oasis ec cscccdvececserene Silas « oats Sales |) «00
Be eiemiastOneNCoaly Aid Shalesh ASS «Jk win able bald vn bobo pide Wb wiescie ciele wees | 80
c. Bands of grey, micaceous grit. 6, Coal and shale. a. Thin-bedded grit.
Be hOmr- fai hom ImeStONe | dele «,o,00> sins c\0r0.0i06.0.0 0 o0 2108 Anan pOGe coo UF Sogont Z tin aA
8. Sandstone, fissile gritstone, and shale ........eeeeeseecees APGSHOBSOOS setsistene OD
c. Micaceous, slaty grit, with bands of shale and a trace of coal. 6. Shale with
bands of gritstone. a. Slaty, micaceous grit and shale, sometimes with a trace
of coal.
7. Mosdale Moor or Wold limestone ........ HE SANS FM Bh a Ad Wea Slelenarere ices veleft Seid. 45
6. Fissile gritstone, and carbonaceous shale, with a bed of coal........++eeeeee+- 150
c. Hard, micaceous, slaty grit. 6. Shale, coal, and grit. a. Grit and shale.
5. Strong post limestone ....... piateraters vocédocnotme sHeoocu eon doco cdospoptio: Ze
BeeaNGSrone, SHAlG;aNd CAICACCOMS OTE: stiscls cus cs cecccevvetetensecene pietaten 50
c. Hard, brown grit, shale, and a trace of coal. 6. Siliceous and calciferous grit.
a. Dark shale.
3. Second limestone or black marble group ...+++ssseeeee0% piv}s 6's © ele) oleleid o dzeie's «) / (45
2. Sandstone and shale ......... Se oadeticnoe se joo SbDOr sidalsis)sielewshets\slelelitisieien 4.10.0)
ce. Hard micaceous grit and shale, &c. 6. Sandy, micaceous shale and brown sand-
stone. a. Dark shale and iron-stone.
iF Ra CPMNSC OT TUUSTLCSLUTIC eter tot totale) oan rel cia sick Blea ciel ai'es ot lovelose'c¥ slamsile. tisioveiehteSitwidkcke 600
otalesc dace (2060
PV ES hig. 1.
mM 2
S4 ‘Prof. Srpewicx on the Carboniferous Chain
The thickness from the bottom of the whole system to the top of the twelve-
fathom limestone is 1735 feet, as determined by these numbers ; and from the
top of the great Scar limestone to the top of the twelve-fathom limestone, is
1135 feet. But asmall correction must be made on account of dip; anda
more considerable correction on account of over-estimate, all the beds being
taken at the maximum thickness, which is never the case in any one section.
After all the deductions, there must remain a thickness of about 1000 feet for
the alternating beds between the top of the great Scar limestone and the top
of the twelve-fathom limestone ; and as far as regards the mountains of Gars-
dale and Dent, 1 do not think that this is an over-estimate. It is, however,
right to state, that very few of the numbers in the preceding details are from
actual measurement. I wish them to be considered only as the average results
of a great many independent approximate observations.
§ 3. Longitudiual section from Penigent to the plains of the Eden near
Kirkby Stephen, &c. &c.*
This section might have been extended many miles further towards the
south, through a region which, though of less elevation than the one here
described, has nearly the same external characters, and is composed of similar
groups of strata: but I wish to confine it to the part of the chain I have per-
sonally and repeatedly examined.
Commencing at the top of Penigent, it passes just above the village of
Horton, and thence nearly in a straight line to the top of Ingleborough. The
summit of Penigent is, I believe, composed of beds subordinate to the second
millstone grit (Group 15.) ; and immediately below, the highest slope, Nos. 14.
13. 12, are finely exposed, and the coal bed of No. 14. has been worked in
horizontal drifts. Then comes a great limestone precipice representing
Nos. 11. 10. and 9.—No. 10. having nearly disappeared, and the twelve-fathom
and four-fathom limestones (Nos. 11. and 9.) making but one precipice. The
remaining part of the great escarpment is composed of No. 8.
From the swallow holes at the base of No. 8. to the level of Horton Beck,
all the successive beds (No. 7. to No. 1.) may be traced without a single
omission. The black marble beds (No. 3.) have been quarried above Hull
Pot, but are not of good quality ; and the group (No. 2.) is not more than
twenty or thirty feet thick+. The great Scar limestone is magnificently ex-
hibited ; and in it are Hull Pot and Hunt Pot. The former a great roofless
* Plate VI..fig.. 2.
+ Both in Ingleborough and Penigent the groups between the Scar limestone and the tnelve-
fathom limestone, are of less aggregate thickness than in many other parts of the principal section.
from Penigent to Kirkby Stephen. 85
cavern, with perpendicular walls, from which may be heard the roaring of
subterranean waters. The latter, an open crevice of unknown but great
depth, as is proved by the long-continued rumbling noise of the stones which
descend after many rebounds from its projecting ledges towards the foun-
dations of the mountain.
Below Dowgill Scar is a beautiful junction of the horizontal limestone and
inclined greywacké without the intervention of any conglomerate*. In the
prolongation of the section through Moulton Fell, the Scar limestone presents
no features deserving peculiar notice; but a little to the east of the line,
above the village of Selside, is an open chasm called Alum Pot, of enormous
but unknown depth. It is surrounded by grassy shelving banks, and many
animals tempted towards its brink have fallen down and perished in itt.
Further up the hill (at Moor Syke, &c.) are the black marble beds (No. 3.),
and after passing in succession all the intervening beds, we have, at the top of
Simon Fell, the slate quarries of No. 8.c. The upper portion of this group
makes a magnificent precipice on the north side of Ingleborough, and its
slate quarries may be traced all round the mountain. Over this group comes
a precipice of limestone, in which (as at Penigent) the twelve-fathom and the
four-fathom limestones are united, the intervening shale and coal (No. 10.)
having nearly disappeared. Over these comes the upper shale (No. 12.);
and then the first millstone grit (No. 13.), forming a great tabular mass on
the top of Ingleborough. The two highest groups of the Penigent section
are therefore wanting.
In descending from the great precipice of slaty grit and shale to the river
of Chapel le Dale, we pass in regular succession over every group from No. 8.
to the bottom of the Scar limestone. 'The upper groups are much concealed
by morass, but they break out, here and there, and are laid bare in the water-
courses on the sides of the mountain. In the bottom of the valley (about
half a mile below the Chapel) there is a beautiful junction of the horizontal
limestone and the inclined greywacké ; and just at that point all the mountain
streams, which in the higher part of the valley had been engulfed in the
cavernous Scar limestone, burst out in one copious spring, and form the river
which descends to Ingleton.
Following the line of section, we have at the base of Whernside some of
* The greywacké dips about south by west, at an angle of 45°.
+ The approach of cattle is now prevented by a strong, lofty wall; but there can be little doubt,
that during the last two or three thousand years, great masses of bony breccia must have accumu-
lated in the lower parts of this great fissure, which probably descends through the whole thickness
of the Scar limestone.
86 Prof. Sepewick on the Carboniferous Chain
the most characteristic features of the Scar limestone. It is traversed by
fissures, and hollowed out into caverns; in one of which (Weathercoat Cave)
is a waterfall of no common beauty, and doubly striking from the extraordinary
nature of the objects which are about it.
Ascending thence to the top of the mountain, we cross the groups in
regular succession, and end with a series of thin-bedded, coarse grits, nearly
on the same parallel with the beds on the top of Penigent, and therefore pro-
bably subordinate to No. 15. of the general section *.
The first millstone grit (No. 13.) makes a feature on all sides of the
mountain top, and the coal bed in No. 14. has been partially opened on its
north face. The coal bed in No. 10. (b.) has been worked in three or four
different places, and the group to which it is subordinate becomes regularly
expanded (though probably of rather less than its mean thickness) between
the twelve-fathom and the four-fathom limestones. Here, therefore, ceases the
anomaly of the Ingleborough and Penigent sections already noted ; and it is,
as far as I know, the only great anomaly in the structure of the districts through
which the lines of section range. ‘There is, however, a peculiarity (and it is
repeated on the east side of Great Colm) which deserves notice. The four-
fathom limestone all round this mountain is thicker than the ¢welve-fathom
limestone, one group being developed much beyond its average thickness, and
apparently at the expense of the other.
From Whernside the line deflects nearly due west (without producing any
confusion in the details, as all the groups are very nearly horizontal), and
ranges by High Pike across the pass from Dent to Ingletent. The four-
fathom limestone, and the slate quarries (No. 8. c.), form the top of the ridge ;
and on the north-east side of it, is a succession of waterfalls over the bare
escarpments of all the groups, from the fourth limestone (No. 7.) down to the
beds above the black marble series. Through the middle portion of these
falls, runs a north and south vein (partly filled with calc-spar), producing a
downcast of eight or ten yards on its west side. I mention this for the pur-
* The natural section is not good near the top of Whernside, the highest mountain of the whole
range; but the top beds may possibly represent a portion of the 16th group of the general section.
+ This fact has sometimes induced me to suppose that the great calcareous escarpment near the
top of Ingleborough and Penigent was chiefly composed of the four-fathom limestone ; and that
some bands of shale and thin beds of limestone near its top, might represent the two superior
groups (Nos. 10. and 11.) in a very degenerate form. I mention this only as a mere conjecture.
{ In the southern and central portions of the principal line of section, the beds, though nearly
horizontal, incline on the whole a little to the north-east. The part of the section deflecting nearly
due west, from the top of Whernside over High Pike to Great Colm, is omitted in the accom-
panying figure (Pl. VI. fig. 2.).
from Penigent to Kirkby Stephen. 87
pose of remarking the almost entire absence of great faults or veins in theneigh-
bouring mountains, and their consequent sterility in all metalliferous minerals.
From High Pike to the top of Great Colm, all the groups succeed each
other in regular order; but on that side of the mountain the twelve-fathom
limestone is still in a degraded form, and the four-fathom limestone has more
than its average thickness. On following them to the eastern side of the
mountain we may, however, remark, that one gradually increases and the other
diminishes in thickness till they assume their average proportions. Over the
twelve-fathom limestone (No. 11.) the three superior groups are well exhibited ;
and a bad two-foot coal has been partially worked in the group No. 14, which
is here about 60 feet in thickness. On the highest summit is a trace of the
second millstone grit (No. 15.), which, though rather thin-bedded, has here
the mineral structure indicated by its name. I do not, however, think that
these beds are so high in the series as those which form the highest peaks of
Penigent and Whernside. Here the section again deflects to the north, and
in the remaining part of its range is very nearly in a straight line*.
Descending from Great Colm top to the valley of Dent we commence, as
above stated, in the lower portion of the second millstone grit (No. 15.), and
cross in succession every group till we meet the upper strata of the great Scar
limestone, about 200 feet above the level of the river. We may remark,
during this traverse, the old coal-works in No. 10. (b.) +,—the slate quarries of
Little Colm in No. 8. (c.),—the old slate quarries and the Barbon coal-works
in No. 6. (0. c.),{—and the various quarries which have been opened in the
black marble beds (No. 3.).
In the higher part of the valley of Dent the river runs for several miles among
the upper beds of the Scar limestone, and we meet with a succession of objects
highly characteristic of the formation. The mountain-streams are engulfed,
and the strata interrupted by numberless grotesque caverns and open fissures,
resembling, on a miniature scale, the striking features of Chapel le Dale.
From Dent, the sectional line ranges over the top of Risell to the Garsdale
river, close to the chapel. On the ascending line, all the beds are laid bare up
to the Wold or Mosdale Moor hmestone, in a great ravine called Scotchergill.
On the eastern brow of Risell are quarries in the fowr-fathom and twelve-
fathom limestones ; and from the upper quarry is obtained a very beautiful
variety of fossil marble already noticed. On the western brow of the same
hill, the coal-bed (No. 10. 6.) has been partially worked ; and the summit is
composed of the lower beds of the first millstone grit (No. 13.).
* See Pl. VI. fig. 2. continued. + See above, Note to p. 79.
} See above, Note to p. 76.
$8 Prof. Sepawick on the Carboniferous Chain
On the descending line there is a fine exhibition of the slate quarries in
No. 8. c. Close to the chapel the river runs in the grit bands (No. 2. c.)
under the black marble ; but in ascending to Garsdale Head (where the road
turns off to Kirkby Stephen), all the beds up to the fourth Mosdale Moor lime-
stone (No. 7.) may be observed to cross the channel in succession.
Both sides of Risell are much covered with alluvial matter and vegetation ;
but independently of the localities above indicated, the position of the respec-
tive groups is defined by the rows of inverted green cones, provincially called
swallow-holes, which often mark the presence of the limestone bands when no
rock is visible at the surface. From many places, on the line of section, five
rows of these inverted cones, each indicating the presence of one of the cal-
careous groups above the Scar limestone, may be seen on the sides of the
neighbouring mountains *.
In ascending from Garsdale chapel to the top of Baw Fell we may find, by
the sides of various torrents, good sections of all the groups, from the black
marble to the twelve-fathom limestone. A thin coal band breaks out, here and
there, in the group (No. 4.) above the black marble beds. On the west flank
of this mountain, the coal bed (No. 6. b.) under the Mosdale Moor limestone
has been worked extensively ; and on the same flank the coal bed under the
twelve-fathom limestone has been attempted+. The quarries in the four-
fathom limestone, from which large encrinital blocks are extracted for the use
of the Kendal marble works, also deserve notice.
The groups of strata above the twelve-fathom limestone are of the aggre-
gate thickness of 500 or 600 feet, and terminate at the top of the mountain
in fine, horizontal, tabular masses of millstone grit, subordinate, if I mistake
not, to the second group of that rock (No. 15.). All the upper parts of the
* The origin of these cones is very clear. The several limestone groups abound in crevices and
fissures, through which the waters, descending from the higher regions, immediately sink, and
trickle down among the lower strata, till they meet some impervious bed which throws them out
again to the surface. Now on the sloping sides of the mountains these groups generally form long
horizontal terraces, more or less buried under masses of alluvial, incoherent matter: and through this
covering the waters freely percolate, till they meet the surface of the limestone beds; when they sink,
as above described, through some of the crevices, and carry along with them the finely comminuted
portions of the superincumbent materials. In this way the alluvial beds are slowly undermined,
and sink down into inverted cones—the inferior portions of which, being sheltered from the elements,
and kept dry by the action of the crevices below, become covered with a fine green sward abound-
ing in such plants as are commonly found only in the lower regions of the mountains.
t Not far below the works in No. 6. 6. a trial was made, a few years since, in some highly in-
clined, carbonaceous shales, probably subordinate to No. 4. of the general section. The coal was
abundant, but of very bad quality, and difficult to work ; being close to the disturbance produced
by the passage of the great Craven fault. See the preceding Memoir, p. 60.
from Penigent to Kirkby Stephen. 89
section are extremely obscured by morass ; but we have, I think, evidence
enough to show—that a five-inch coal (breaking out about 100 feet above the
twelve-fathom limestone) is subordinate to the great upper shale (No. 12.),
which is here very largely developed,—and that a second bed of four-inch
coal, about 200 feet above the preceding, is subordinate to the alternating
beds (No. 14.) above the first millstone grit. ‘The evidence for this arrange-
ment may be considered obscure; but it is at least made probable by the struc-
ture of the nearest mountains of the chain.
Descending from Baw Fell top to the head of Uldale (after crossing a region
of thick morass), we meet with magnificent sections of a great series of beds
commencing with the twelve-fathom limestone. Under this limestone the
coal bed (No. 10. 5.) has been partially worked. We then cross a series of
cherty beds, analogous to those on the same parallel in the Arkendale and
Swaledale sections: and further down the torrent is a great precipice (com-
posed of the four-fathom limestone, resting on the gritstone bands and thick
shales of No. 8.), over which the waters shoot in a single plunge, and form
one of the grandest falls in the carboniferous chain*. Below the fall is one
of the finest gritstone quarries of the chain (No 8. a.); and a few hundred
yards further down the valley we find great masses of highly inclined and
dislocated limestone, connected with the range of the Craven fault.
The phenomena, last described, are a little to the west of the line of section,
which at Uldale Head makes its nearest approach to the greywacké region.
Thence it ranges over Swath Fell, to the top of Wildboar Fell, through a
country almost buried under turf bog and alluvial soil. The top of Swath Fell
appears to belong to the same group (No. 15.) as the top of Baw Fell, but it
does not quite reach the same elevation.
At the top of Wildboar Fell we have just a trace of the group (No. 16.) ; but
* Tn all chains of mountains composed, like those I am describing, of horizontal strata in very
different degrees of induration, waterfalls are necessarily abundant. The harder groups have an
obvious tendency to form terraces over which the waters break with a violence proportioned to the
nature of the descent. The steep sides of the hills are, however, often composed of solid beds of
sandstone or limestone, resting on thick masses of soft, incoherent shale: and when such combina-
tions cross the direction of a mountain stream, they almost always produce an overshot fall. For,
had the inferior shales ever projected so far as to produce a gradual descent, they must soon have
given way to the friction of the water, till they arrived in such a position as to be protected from
its action. And even when removed from the direct effects of erosion, they often continue to ex-
foliate so rapidly, that the hard superincumbent beds form a projecting ledge, over which the waters
leap at once into an inferior basin. In this way the great waterspout of Hardraw Scar commences
in the black marble group, and plunges into a basin of the shales subordinate to No, 2. These
appearances are so very common and obvious as perhaps hardly to require notice.
VOL. IV.—SECOND SERIES. N
90 Prof. Sepewick on the Carboniferous Chain
the magnificent tabular escarpment overlooking Mollerstang is composed ex-
clusively of the second millstone grit (No. 15.) ; and on the same face of the
mountain we have a succession of the finest sections, exposing all the groups
down to the twelve-fathom limestone. They are, perhaps, of as great a thick-
ness as at Baw Fell; but in consequence of the degenerate form of the first mill-
stone grit (which is here an ordinary, open-grained, whitish sandstone), they
are not well defined. Subordinate to No. 14. is a bed of coal about eighteen
inches thick, which has been partially worked, but hitherto without profit.
Descending from the crown of the hill, along the edge of its eastern escarp-
ment, to the level of the white grit beds representing the first millstone
(No. 13.), we cross (close to a place called Dolphin Sty) the line of a great
vein or fault, which throws all the beds on its north side about 150 feet below
their level. In consequence, the coal-bed (No. 14.) and the accompanying
grits and shales are once again repeated. ‘This vein strikes the opposite hills
(producing the same northern downcast), and is prolonged into the mining
district of Swaledale.
After reaching the level of the twelve-fathom limestone, we cross the bearings
of one or two other veins, which have partially deranged the position of the
groups. I have attempted to convey only a general notion of them in the
accompanying section, for the country is so much covered with alluvion that
their exact effects cannot be easily ascertained.
Continuing to descend, we come upon the edges of the dislocated masses
thrown up by the great Craven fault. The horizontal beds of the great Scar
hmestone lie far below the bottom of the neighbouring valley*: but the
broken ends of the whole mass have been torn up from the foundations of the
mountain, and jammed against the edges of the upper horizontal groups.
The vast force of elevation is indicated by the enormous extent and contor-
tions of the dislocated masses ; and the line of greatest stress is indicated by
an anticlinal axis, on the north side of which the Scar limestone, after many
breaks and undulations, gradually falls down to the level of the Eden, and is
buried under the conglomerates of the new red sandstone, where the longi-
tudinal section ends.
* The Mosdale Moor limestone (No. 7.) is, I believe, the lowest calcareous group to be seen in
the deep valley at the eastern base of Wildboar Fell.
+ It deserves remark, that in some places near Kirkby Stephen the direction of the anticlinal
axis is traced by a small vein, which, here and there, has been worked for lead. ‘This seems to
prove that, at least, some of the lead veins of the carboniferous chain originated in fissures pro-
duced by the great elevatory movements before the period of the new red sandstone. I believe,
partly on the evidence afforded by the details of this paper, that many of the lead veins of Arken-
dale and Swaledale had their origin during the same period.
SJrom Penigent to Kirkby Stephen. 91
Such are the striking phenomena along the line of section. In order to
make the structure of the region still more clear, and to connect it with the
mountain tract at the head of Swaledale, I proceed to describe, very briefly,
two other sections—one commencing at the top of Penigent—and the other
at the top of Whernside, and both diverging considerably from the bearing
of the principal line.
Section from Penigent to the top of Stags Fell, near Hawes ; mean bearing
about N.N.E.*
The strata of Penigent have been already described. If the line of section
be made to range along the south side of the valley, above the village of
Horton, we shall arrive at the great vertical chasm called Ling Gill, which
gives a series of fine, bare sections, through almost every part of the Scar
limestone.
Continuing the section nearly in a straight line, over the summit of Cam
Fell, we first cross the outgoings of all the groups up to the twelve-fathom
limestone, forming the great plateau above Cam Houses, and find that the three
groups (Nos. 9. 10. 11.) which were confounded together in Penigent, are
here exhibited with their true relations. We then cross the great wpper shale
and the first millstone grit (No. 12. 13.), and rise to the summit of Cam
Dod, which is buried under peat moss ; and from that point may see the pro-
longation of the twelve-fathom limestone down Wensleydale, forming on both
sides of the valley the crown of a long range of flat-topped elevations +.
Descending to Hawes, which stands upon the upper part of the Scar
limestone, we cross all the successive groups in regular order. The coal
(No. 10. b.) has been worked both on the east and west sides of Cam, and
the lower coal seam (No. 6. 0.) is still worked near the village of Gale.
In the range of the sectional line, on the other side of the valley, over
Stags Fell, we again cross the same successive groups, in the ascending
order, till we reach the great overhanging plateau of the twelve-fathom lime-
stone; and we may remark, by the way, that it is traversed by a cross vein,
with a downcast of several fathoms towards the south-east. Rising from this
plateau to the top of the mountain ridge, between Wensleydale and Swale-
dale, we first cross the upper shale (No. 12.) and the first millstone grit
(which is not far from the highest level of the road from Hawes to Muker) :
* Plate VI. fig. 3.
+ The summit of Cam Dod is probably composed of beds subordinate to the group (No. 14.)
over the first millstone grit.
Nn 2
92 Prof. Sepewick on the Carboniferous Chain
above them are the grits, shales, and coal bands of No. 14*; and the series,
though almost lost among the accumulations of peat earth, terminates, I be-
lieve, in the beds of the second millstone grit (No. 15.).
Notwithstanding the constancy in the position of the several groups, there
are changes of mineral structure which, had we not so many terms of com-
parison, might lead to some confusion. Near the eastern end of this sec-
tion, the black marble beds (No. 3.) lose that mineral character which gives
them their chief value, and resemble the beds of the higher group (No. 5.);
and with these beds they might easily be confounded, as, in some places near
Hawes, the shales of No. 4. are wanting, and the sandstone beds of the group
are not more than twenty or thirty feet in thickness+. Near the same place
the shales of No. 8. become insignificant, but the micaceous, slaty beds are
well developed.
Section from the top of Whernside to the top of Shunner Fell ; mean bearing
about N.N.E.t
The line here ranges from Whernside into the higher part of the valley of
Dent, about five miles above the village (where the river runs upon the top
beds of the Scar limestone); thence over the Cross to Mosdale, and over
Cotter Fell to the top of Shunner Fell, without making any very great devia-
tions in its course §.
The strata of Whernside have been already noticed, and the same groups
succeed each other in regular order on the side of the next mountain, where
however we may remark, that the four-fathom limestone is of less, and the
twelve-fathom limestone of greater, than their average thickness; just the con-
trary of what was observed among the groups of Whernside ; and another
instance of what was remarked before,—viz., that each of these two limestone
* This coal bed is not worked, as it is only about eighteen inches thick, and is inferior in qua-
lity to the thirty-inch coal of Turna Fell, in the same range of hills, and only at a short distance
towards the north. -
+ Further down Wensleydale these three groups of the general section (viz. Nos. 3. 4. and 5.)
probably lose all distinctive character, and appear as one group: for I have remarked, that in the
hills below Askrigg there are only five, instead of six, distinct limestone groups, from the Scar lime-
stone (which is partially expanded in the lowest parts of the valley) to the twelve-fathom limestone
inclusive. Between Askrigg and Bolton Castle the whole system is intersected by metalliferous
veins, producing (like ordinary faults) contortions, upcasts or downcasts, and other disturbances of
the component strata.
t Plate VI. fig. 4.
§ The Cross (a mountain of which the summit is sometimes called Naughtberry Hill) must not
be confounded with Cross Fell, the highest mountain of the carboniferous chain north of the Eden.
Jrom Penigent to Kirkby Stephen. 93
groups is of variable thickness, and that each of them appears to be sometimes
developed at the expense of the other*.
Above the twelve-fathom limestone, the upper shale and the first millstone
(Nos. 12. and 13.) are in their characteristic form, and over them are the car-
bonaceous shales, coal bands, and grits of No. 14. and perhaps a trace of
No. 15; but the summit of the hill is buried in morass.
Following the sectional line, we find in Mosdale all the beds denuded,
down to the Mosdale Moor limestone (No. 7.) ; and on the east side of the
valley we have an extensive tract of green pastures, crowned with a plateau
of the twelve-fathom limestone, under which are many traces of old coal works
in the group (No. 10. 5.).
From this plateau to the top of Shunner Fell there are strata more than
100 fathoms in thickness ; but all of them are buried under the peat mosses,
till we reach the grey crags of millstone grit, on the last ascent towards the
crest of the mountain. We there cross the outgoings of the second millstone
grit (No. 15.); of the shale and gritstone (No. 16.); and we reach the
highest plateau after passing the rugged escarpment of the upper millstone
grit, the last group of the general section f.
* There is a very fine natural section of all the groups, from the upper beds of the Scar lime-
stone to the four-fathom limestone inclusive, in the sides of a torrent called Artingill, near the old
pass over the Cross between Dent and Hawes. Immediately above the highest point of this pass,
are extensive coal works (in No. 10. b.) reached by shafts sunk through the twelve-fathom lime-
stone.
¢ As the strata from the plateau of the twelve-fathom limestone to Shunner Fell top are not, on
the whole, well exposed along the sectional line, I subjoin a more detailed, ascending section through
the same series, as exhibited near the Turna Fell coal works, a little further to the south.
Feet. Inches, Feet. Inches.
1. Twelve-fathom limestone. 7. Hard; brown git oi. aa )s oi0s)es 7
2. Shale, with bands of grit........ 20 0 See UIANO | a cnia eh lola iayisimsinsnybia’ #60.) itollte
3. Quarry grit, with bandsof shale40or50 0 9. Hard, brown grit ........-.
4. Sill stone (hard brownish grit) with 10. Shale,with bands of soft, tough grit
bands of dark shale...... 200r 30 0 11. Bands of open, coarse grit, passing
BMA sie. o's) o0'sin/ aes vies) sii eaiere coon @ 6 into the upper group ...... 20 or 30 0
6. Shale with bands of brown gritstone, 12. Millstone grit, &c. ......... as 120.0
and a three-inch coal near the 13. Coarse, thin-bedded grit and shale .100 0
EOP oi a:e a's di0ininjciniain sas oe /0.0r 80.0 14. Upper millstone grit, &c. ...... 120 0
The thickness of the beds from the coal, No. 5. to No. 10. inclusive, is very nearly thirty-three
fathoms, as determined from the sinkings of an air-shaft. The other numbers are only approxi-
mate. Nos. 2. and 3. represent, in a degraded form, the upper shale and the first millstone grit.
All the beds from No. 4. to No. 10. inclusive may be considered as one group, representing
No. 14. of the general section: and the remaining groups represent the three highest divisions of
the general section in their most characteristic form.
94 Prof. Sepewick on the Carboniferous Chain
I could have wished to extend the two diverging sections, just described, as
far as the metalliferous hills between Arkendale and Swaledale ; but I am not
sufficiently acquainted with that region to represent the prolongation correctly.
I may, however, state in general terms, that the four-fathom limestone and
the twelve-fathom limestone range through the hills on both sides of Arken-
dale, and are among the best lead-bearing beds of the country. ‘They are
known by the miners under the names wnderset lime and main lime, and are
immediately surmounted by a group about 100 feet in thickness (composed
of shale, chert, and gritstone, with some peculiar masses called red beds and
iron beds), which, on the whole, may be considered to represent. the upper
shale of the general section (No. 12.). Over this group is a strong deposit of
coarse grit, upwards of sixty feet in thickness, which probably represents the
first millstone grit (No. 13.).
The coarse gritstone last mentioned is surmounted by a very complex succes-
sion of deposits about 160 feet in thickness. In the lower part of this series we
have alternations of gritstone and shale, with a subordinate twelve-inch coal—
over these are alternations of chert and shale, with a bed of crow-limestone of
the extraordinary thickness of twelve feet—and the system terminates in a mass
of shale about eighty feet thick, containing three subordinate bands of impure
limestone. It has been stated above, that bands of crow-limestone are found,
here and there, subordinate to all the great shales of the carboniferous chain.
But their number, and the thickness of one of them, in so high a division of
the Arkendale section, must be considered anomalous. I have, however, little
hesitation in identifying this complex group (especially as it is immediately
surmounted by a deposit of mzllstone grit nearly 100 feet thick) with the 14th
division of the general section.
The preceding details of this paper explain the structure of a part of the
carboniferous chain. ‘Those which follow show the effects produced by the
prolongation of the great Craven fault, and the movements which took place
among some of the mineral masses when the chain was elevated.
§ 4. Transverse Sections, from five points of the Longitudinal Section,
through the dislocated strata on the line of the Craven Fault*.
The first transverse section (fig. 5.) commences from the top of Penigent,
and ranges (about south-west by west) through the village of Horton, over
Moughton Fell; and thence over a second plateau of the Scar limestone, to
the calcareous hills immediately north-east of Clapham.
* Plate VI. Transverse Sections (fig. 5. 6. 7. 8. 9.).
Jrom Penigent to Kirkby Stephen. 95
The successive groups of strata on the side of Penigent have been noticed
above* ; and the various phenomena exhibited at the junction of the carboni-
ferous system with the greywacké have been very clearly explained by Mr.
Phillips in a preceding memoir of our 'Transactions+. My object is to con-
nect the longitudinal section above described, with section (D.) of that me-
moir f.
From Clapham to the hills north of Ingleton, the range of the Craven
fault is marked by an anticlinal line or break, apparently formed by the pro-
trusion of the slate rocks during the elevation of the limestone chain. This
line passes through Clapham Beck about a mile above the village, as is indi-
cated in the section.
The second transverse section (fig. 6.) commences at the top of Great
Colm, passes in a direction nearly due south over Gragreth ; thence, deflecting
a little towards the east, crosses the foot of Kingsdale and becomes united
with section (A.) in Mr. Phillips’s paper$.
The strata of Great Colm have been described above|| ; but in consequence
of their gradual rise towards the south-west, some of the lower groups are
brought out in the Gragreth range, the top of which is composed of the fissile
gritstone (No. 8. c. of the general section){. In descending from the top of
Gragreth to the waterfall called Thornton Force, at the foot of Kingsdale,
we cross all the groups from No. 8. down to the great Scar limestone. On
crossing the line of the great fault, the dislocation is precisely of the same
kind as in Clapham Beck ; but is incomparably more striking. The whole
Scar limestone has been tumbled into the valley, and seems to pass under the
Burton coal-field.
Some of the dislocated masses may be considered, in their prolongation, to
reappear in the inclined beds of Kirkby Lonsdale and Farlton Knot. The
principal line of fault passes however (as stated in a former paper)** by Ease
Gill and Barbondale, and thence in a direction about north by east to the
foot of Stainmoor. And in all this portion of its range, the nature of the
dislocations of the carboniferous strata are modified by the immediate contact
of a lofty greywacké chain, as will be seen in the three next transverse sec-
tions.
The third transverse section (fig. 7.) commences at the top of Crag or Cas-
terton High Fell (the north-western extremity of the ridge of Great Colm),
* Supra, p. 84. + Geological Transactions, Second Series, vol. iii. p. 5—15.
£ Ibid. Plate I. (D.) p. 12. § Ibid. Plate I. (A.) p. 9. || Supra, p. 87.
{| Some of the grits (subordinate to No. 8. of the general section) along this line are of coarse
texture, and have been used for millstones. ** Supra, p. 60.
96 Prof. Sepewick on the Carboniferous Chain
and ranging in a direction about west by north, cuts through the junction of
the carboniferous and greywacké chains.
The highest strata of Casterton High Fell are of millstone grit; and
desending in the direction above indicated, we cross every bed in regular
succession down to the strong post limestone (No. 5. general section). But
at a place called Short Gill, on traversing the line of the great fault, we find
that all the lower groups, including the Scar limestone, have been torn up
from the foundations of the mountain, bent into a saddle, and afterwards
jammed between the edges of the horizontal beds and the steep face of the
neighbouring greywacké ridge.
In order to explain this appearance, we must remember—that the grey-
wacké chains existed in some form or other before the deposit of the carbo-
niferous system—and that the beds of this system, before their elevation, must
have abutted against a series of inclined planes presented by the submarine
portions of the old greywacké chain. During a subsequent elevation, both
the greywacké and carboniferous systems appear to have been violently acted
on at the same moment, and a great strain, accompanied by a relative vertical
movement, to have taken place all along the plane of their junction. Buta
relative vertical movement of the inclined flanks of the older mountains might
not only break off the ends of the carboniferous strata abutting against them ;
but would also necessarily produce a great horizontal thrust, which may, I
think, account for such a curvature of the dislocated masses as is indicated in
this section.
This example has been selected on account of its complexity. There are
many places along the line of dislocation, where the lower groups have been
torn off, by the pressure of the greywacké hills, from the horizontal’ system,
and tilted up at a great angle, without undergoing any flexures or contortions
like those at Short Gill.
The fourth transverse section (fig. 8.) presents still more complex disloca-
tions. It ranges nearly east and west, from the top of Baw Fell to Hebble-
thwaite Hall Gill, and thence across the upper part of the valley of Sedbergh
to the Howgill Fells.
The west end of Baw Fell top is, if I mistake not, composed of the second
millstone grit (No. 15. general section) ; the inferior groups along the line of
section are much concealed under morass ; but several of them may be dis-
covered by ascending the different water-courses. ‘The fowr-fathom limestone
and the Mosdale Moor limestone are both well exposed, and the horizontal
system terminates with flaggy gritstone and carbonaceous shale, containing a
subordinate bed of coal which has been extensively worked. (General Section
from Penigent to Kirkby Stephen. 97
No. 6. b.) After crossing on the descending line (immediately below the coal
shale) about fifty feet of micaceous slaty gritstone (No. 6. a.), we suddenly
come to the great fault, beyond which the beds dip at a high angle about
west-north-west. They now seem to succeed each other in a regular ascend-
ing order ; but on the contrary we find a succession of groups representing,
if I mistake not, Nos. 4. 3. and 2. of the general section ; and at length reach
the great Scar limestone (No. 1.), the beds of which have a fan-shaped ar-
rangement: the first portion dipping at a great angle in the direction above
indicated,—the middle portion being elevated into broken vertical masses,—
while the lowest strata gradually acquire an opposite dip (about east-north-
east), and rest on the conglomerates of the old red sandstone.
Descending by Hebblethwaite Hall Gill, we have masses of old red conglo-
merate resting unconformably upon irregular, protruding beds of greywacke ;
and in the lower part of the valley these conglomerates become of very great
thickness. From beneath them on the opposite side of the valley of Sedbergh
rise the steep escarpments of the greywacké ridges in which various tributary
branches of the Lune have their source*.
By comparing this description with the accompanying section, it appears,—
Ist, That by the prolongation of the Craven fault under Baw Fell, all the
groups below No. 6. were cut off from the horizontal system.—2ndly, That
forces of elevation, acting irregularly upon the dislocated masses, pushed a
portion of the great Scar limestone above them all into a vertical position.—
3rdly, That by this movement a portion of the Scar fimestone, and three or
four superior groups were actually inverted.
It is obvious, from this section, that great masses of old red conglomerate
were formed on the flanks of the nearest greywacké hills before the existence
of the carboniferous series ; and the beds of this series may perhaps never
have abutted against the neighbouring greywacké chain. The first effect of
elevation seems to have been exactly the same with that which is indicated in
the preceding section at Short Gillf. ‘The lower groups were torn off from
the base of the mountain ; but not being exposed to the same horizontal thrust
from the greywacké chain, they had more room to expand themselves, and
fell into the remarkable position just described.
5. The last transverse section (fig. 9.)is drawn from the top of Wild Boar Fell
(in a direction about west-north-west) through some dislocated masses, forming
* The beds in many parts of the greywacké chains, near the lines of section, are violently con-
torted. The lines drawn through the greywacké in the accompanying sections are ideal, and
merely intended to contrast the inclined position of its strata with that of the horizontal carboni-
ferous system. + Plate VI. (Transverse Section, fig. 7.)
VOL. IV.—SECOND SERIES. 0
98 Prof. Sepewick on the Carboniferous Chain
bare hills called the Clouds*, and thence to the greywacke chain of Raven-
stonedale. The phenomena are here less complex than in the preceding
section, though the dislocated beds have undergone a greater movement of
elevation.
The top of Wild Boar Fell is chiefly composed of the second millstone grit
(General Section No. 15.), and along the descending line we cross all the
groups to the fowr-fathom limestone (No. 9.). The line of the great fault
crosses the section in a deep morass very near the outcrop of the last-men-
tioned group (No. 9.); and at a very short distance the highly inclined beds
of the Scar limestone rise into the bare hills, called the Clouds, and are con-
tinued (sometimes in a vertical position and sometimes contorted) to the rivulet
where they are cut off by the greywacké chain.
It is possible that some of the groups above the Scar limestone may be con-
cealed among the dislocated masses under the morass : but it is at least evident,
that a portion of the Scar limestone has been broken off from the bottom of the
carboniferous system, and lifted up to its present position over the edges of
all the groups of the general section from No. 2. to No. 8. inclusive.
The first and second of these five transverse sections (Fig. 5. & 6.) connect
the facts described in this paper with those already published by Mr. Phillips + ;
and the last three sections (Fig. 7. 8. & 9.) show the very complex nature of
the movements along the line of fault, where it ranges close to the junction
of the carboniferous and greywacké chains.—By combining these details with
those given at the end of the preceding paper, ‘‘ On the general Structure of
the Cumbrian Mountains, &c. &c.”’ ¢ we shall have a sufficiently minute account
of the whole northern range of the great Craven fault, and of the structure
of the neighbouring carboniferous chain.
§ 5. Conclusion.
1. I will not repeat what I have so recently stated on the changes of
the carboniferous system in its range from Derbyshire to the valley of the
‘Tweed§: but I may observe, that the region above described seems by its
structure to form a natural link between the northern and southern portions
of the chain.
* The hills are probably so called from the light grey colour of the dislocated rocks of Scar
limestone.
+ Geol. Trans., Second Series, vol. iii. pp. 12. and 9. t Supra, p. 60.
§ See Anniversary Address, Feb. 18, 1851. Proceedings of the Geological Society, No. 20.
p. 286—288. ,
from Penigent to Kirkby Stephen. 99
The whole series of strata composing the mountains along the line of sec-
tion may be divided into three great natural groups: Ist, The Scar limestone.
2nd, All the alternating subordinate groups (from No. 2. to No 12. inclusive),
ending with the great upper shale over the twelve-fathom limestone. 3rd, All
the various deposits (from No. 13. to No. 17. inclusive) associated with mill-
stone grit*.
The lowest of these groups is almost identical with the formation of moun-
tain limestone at the base of the carboniferous series of Derbyshire and the
Bristol Channel. The middle group has, on the contrary, little in common
with the carboniferous series of Derbyshire, and, perhaps, still less with that
of the Bristol Channel: but it conforms very nearly to a portion of the car-
boniferous system in the chain of Cross Fell. The third group appears in
some form or other through the whole extent of the carboniferous chain ; and,
though by no means constant in its characters, undergoes perhaps less modi-
fication in its long range than either of the other two.
A fourth great group might include all the richest deposits of our northern,
midland, and south-western coal-fields ; and the analogies they present both
in structure and position are obvious; but they belong not to the subjects
considered in this paper.
In the North of England the deposit of mountain limestone was exposed to
many interruptions, arising from drift, mud and sand, mixed with the wreck
of numerous trees and plants. Upon such masses as these, encrinites and
corals would obviously refuse to grow, till the incoherent sediment became
compacted by calcareous matter, upon which they would again find an appro-
priate resting-place. ‘The calcareous beds would then go on increasing till
they were again interrupted by a new incursion of mud and sand. Effects
like these were many times repeated.
In the valley of the Tweed these disturbing forces were in full action from
the first commencement of the deposit of mountain limestone ;—in Yorkshire
(as appears from the previous details) they produced very considerable effects
long before the complete development of the formation ;—in Derbyshire, and
in the south-western coal-fields, on the contrary, they produced but a small
modification of the carboniferous system before the deposit of mountain lime-
stone was completed.
I hope in a subsequent paper to describe several similar modifications of
structure in the northern calcareous zone of the Cumbrian mountains.
2. Many of the coal-beds above described must have been deposited under
* The three longitudinal sections, fig. 2. 3. and 4, are coloured on this principle, the detailed
subdivisions appearing only in fig. 1.
0 2
100 Prof. Sepewick on the Carboniferous Chain
the waters of a sea of considerable depth ; and I never saw any shells of
decided freshwater genera in the carbonaceous shales alternating with the
mountain limestone*; but these shales sometimes contain thin beds of ma-
rine shells, chiefly producte. I am of course aware that freshwater shells
occur abundantly in some of our rich coal-fields; and in such cases the de-
posits may have taken place in lakes, or more probably in shallow bays and
estuaries. It is, perhaps, in very few instances necessary to consider them
of purely lacustrine origin ; especially when we remember, that in a part of
the great Yorkshire coal-field (far above any of the groups represented
in the preceding sections) there are beds abounding in pectens and am-
monites.
3. Certain species of marine fossils abound in particular groups of the lime-
stone strata, and so far become in some measure characteristic of them; but
1 am not sure that any one species is actually confined to one limestone group.
Most of the fossils of the Scar limestone may be found, here and there, in the
twelve-fathom limestone, and vice versdt. Wherever there is a sudden change
of mineral character, we may, however, remark an equally sudden change in
the fossil species.
Thus, for example, very few of the corallines, encrinites, bivalves, &c.
(abounding in the limestone) are found in the alternating beds of shalef ;
and impressions of coal-plants hardly ever occur in the limestone groups,
though they abound in the alternating groups of sandstone and shale. This
distribution obviously originated, partly in the habits of the animals above-
mentioned, and partly in the mechanical causes by which the beds themselves
were produced.
4. The several groups of limestone, so remarkable above all the other
strata for their regularity and continuity, were evidently the result of a slow.
tranquil deposit, assisted by the action of organic bodies ; and most of the
* Some geologists have contended, not merely that all coal-beds are lacustrine, but that
they once existed as turf bogs,—a supposition surely inapplicable to the carboniferous chains of
Northumberland and Yorkshire. To bring such a theory into action, we must suppose that the
chains in question were elevated, and again submerged under the ocean, at least as many times as
there are beds of coal alternating with beds of encrinite limestone ;—-a most cumbrous, and, I think,
an incredible hypothesis, which never could have been started by any one who had examined the
coal-fields in the basin of the Tweed, or even the carboniferous chains of the North of England.
+ T may, however, remark, that I have never seen trilobites, ammonites, orthoceratites, and
perhaps some other rare fossils of the mountain limestone, in any part of the series above the great
Scar limestone.
+ The bands of calliard or crow-limestone, above described, may seem an exception to this rule;
but the number of species they contain is, if I mistake not, very limited.
from Penigent to Kirkby Stephen. 101
fossil remains subordinate to them have lived and died on the spots where
they are now found. On the contrary, some of the other alternating strata
have originated in an action decidedly mechanical, and their imbedded ligneous
fossils have been drifted from a distance. Hence it is that these strata are in
general much less regularly continuous than the groups of limestone. The
observation must not, however, be strained too far; as some of the thin bands
of coal above described are, on any hypothesis, of astonishing regularity and
continuity *.
5. The bottom beds of each calcareous group are often impure, and contain
very few traces of organic remains, and do not generally alternate to any con-
siderable extent with shale and sandstone. We may also remark, that the
corallines, zoophytes, &c. found in such positions are commonly of small size.
At the top of each limestone group, on the contrary, the alternations of shale
and sandstone are universal, and the fossils are numerous and full-grown.
From all which it seems to follow—that each limestone group commenced at
the beginning of a period of repose—that the marine animals which assisted
its growth were at first few in number and ill-developed—that they gradually
became vigorous and full-grown; and were at length destroyed only after
repeated irruptions of mud and sand.
6. The valleys in the carboniferous chain, near the longitudinal sections,
are not generally excavated on any lines of fault; and are, in the severest
sense of the term, valleys of denudation. Yet the actual erosion on the
ledges of solid rock at the numerous waterfalls (of which I have attempted to
point out the origin), is in general so small as almost to demonstrate, that
there must have been a great change in the distribution of the water-channels
at some period, very recent when compared with that of the first elevation of
the carboniferous chain, before the deposit of the new red sandstone.
* As an example of this, I may state that at Cross Pits, in the valley of Dent, the coal-seam
under the twelve-fathom limestone is divided by a band of clay, half an inch thick, into two parts,
with distinct mineral characters; and that the same coal-seam, with exactly the same subdivisions,
has been found in the mountain on the opposite side of the valley, at the distance of three or four
miles measured in a straight line. This seems to prove that a bed, not more than a fraction of an
inch thick, was originally continuous through an area, probably several miles in diameter.
Ay OR
iia)
Fon re
ata i
, ‘s
1V.—Observations on some of the Strata between the Chalk and
the Oxford Oolite, in the South-east of England.
By WILLIAM HENRY FITTON, M.D., F.R.S. P.G.S., &c.
[Read June 15, 1827.]
a.) IN a paper published in the Annals of Philosophy for November and
December 1824*, I gave an account of the order and characters of the strata
which occur beneath the chalk on the coast of part of the Isle of Wight and
of Dorsetshire, and stated some reasons for supposing that a similar arrange-
ment would be found to exist in the interior of England.
The principal objects of that paper were; First, to distinguish as a separate
group, the series of strata now called the Lower Green-sand ;—which had pre-
viously been confounded either with the beds containing green particles
immediately below the chalk, or with the sandy and ferruginous strata conspi-
cuously exhibited on the coast at Hastings, and then called “ Iron-sand.’’
Secondly, to indicate more clearly than had been done before, the peculiar
characters of the group, which succeeds in a descending order to that just
mentioned, and is remarkably distinguished by its fossils from the strata imme-
diately in apposition with it, both above and below. For this latter group,
which includes the Weald clay, the sand of Hastings, and the Purbeck lime-
stone, and is well entitled toa separate denomination, I have adopted the name
of “Wealden,” proposed by Mr. Martin, in his valuable memoir on the West
of Sussex.
(2.) The objects of the inquiries which have produced the following pages
were, to compare some portions of the series of strata between the chalk and
the Oxford oolite, in different parts of the South-east of England ; to ascer-
tain the existence of the Wealden in the interior; and, if possible, to deter-
mine its boundaries.
* Annals of Philosophy; New Series, 1824, vol. viii. pp. 365, 458, &c.
+ “ Memoir on a Part of Western Sussex”: 4to, London, 1828.
104 Dr. Frrton on the Strata below the Chalk.
In stating the result of this investigation, I shall give a series of sections of
the strata below the chalk, at places which I have myself examined *, beginning
on the coast near Folkstone, and following the outline of the chalk thence to
the sea on the N. West of Norfolk. The relative situation of these places is
shown in the map annexed to this papert. The intermediate country, in
general, I have not examined in detail, and some points of importance I have
never seen; but those who may have opportunities of continuing the inquiry,
will find, I hope, no difficulty in connecting their observations with mine.
(3.) The series of strata about to be described extends from the Chalk down
to the Oxford oolite or coral-rag, and is composed of alternating but irre-
gularly distributed beds of Sand, Clay, and Stone.
Among the sandy strata, it is important to discriminate not only between the
Lower green-sand and that of Hastings, but to distinguish both from a third
group, consisting principally of sand abounding in green particles, which lies
beneath the Portland stone.
Clay, of several varieties, occurs in all parts of this series; but three groups,
constituting the Gault, the Weald-clay, and the Kimmeridge-clay, derive pe-
culiar importance from their generally occupying valleys, or depressions, at
the foot of the escarpments of the Chalk, the Lower green-sand, and the Port-
land stone, respectively, and thus producing conspicuous natural features in the
tracts where this succession is observable.
The stone of the tracts under consideration is either limestone; indurated
sand-rock; chert; or siliceous matter intimately mixed with carbonate of lime,
in the form of grit,—which has commonly a concretional structure, and seems
to pass into continuous beds only by the approach and ultimate union of the
concretions.
But the most remarkable distinction, in the suite described in this paper, arises
from the great difference of character in the organized remains which the
principal groups include. The fossils of the chalk and green-sands and those
of the Portland stone, are all marine, and the species numerous. But in the
Wealden, between the lower green-sand and the Portland stone, although the
fossils are abundant as to quantity, the species are comparatively few, and by
far the greater part of them belongs to fresh water. The whole of the phe-
nomena, in short, presented by this remarkable assemblage of beds, are such
as to accord with the hypothesis of their having been deposited in fresh water
communicating with the sea.
* Plates X. a, and X. b. -
+ Plate IX.—The detail, upon a larger scale, will appear in the new edition of Mr. Greenough’s
Geological Map of England.
Dr. Firron on the Strata below the Chalk. 105
(4.) Combining these sources of distinction, the following arrangement and
subdivisions may be adopted, the nomenclature of which, however exposed to
criticism, is now probably too well established to be changed without incon-
venience™.
{ Upper. 7
Cuarx.... < Lower.
L Marly. Fossils, marine: species nu-
Upper green-sand. e merous.
Green-sanp < (Gault. |
L Lower green-sand. J
( Weald-clay. 7
WEALDEN.. Q Hastings sands. > of fresh water: species
L Purbeck strata. j few.
A
Portland stone.
Fossils, for the greater part,
Part of the Portland sand. Fossils, marine: species nu-
Ooxrtic Surtees ) Kimmeridge and Weymouth clay and sand. merous.
Oxford oolite (Coral rag).
(5.) I proceed now to describe the Sections of these strata, beginning with
the coast of Kent; and I shall connect with each section a list of such fossils as
I have either found myself, or obtained on good authority from the places men-
tioned. The whole of the shells in these lists have been examined and named
by Mr. James Sowerby, by whom also the drawings of the supposed new
species were made, and the annexed engravings executed}. It is right to
mention this explicitly, both that I may take the opportunity of expressing
my acknowledgments for Mr. Sowerby’s valuable and assiduous cooperation,—
and that, being myself but very slightly acquainted with Conchology, I may
place the portion of the following pages which relates to that subject on
better authority than my own.
Vicinity of Fouxstone, Kent.
(6.) The small map, (Plate VII. fig. 1.,) reduced from the Ordnance Survey,
represents the country in the immediate neighbourhood of Folkstone and
* | have stated in another place (Annals of Philosophy, vol. viii. pp. 461, 462,) some objections
to the employment of names for geological strata, which refer to characters not essentially con-
nected with the structure or position of the objects to be designated. But the term green-sand,
however faulty, besides the universal use of it in England, has been adopted both in Germany and
France ;—where, however, it may be regarded, in some measure, as free from the disadvantages
of a significant name.
} Plates XI., et seq.
VOL. IV.—SECOND SERIES. P
106 Dr. Firton on the Strata below the Chalk.
Sandgate,—the relative position of this tract being shown on the general map,
(Plate IX.). The View (Plate VIII.), for which I am indebted to the kind-
ness of my friend the Rev. J. D. Glennie of Sandgate, shows the actual appear-
ance of the coast from Eastware Bay to Hythe; and the section (Plate X a
No. 1.) illustrates the succession of the strata, on a part of the shore which
is not distinctly visible in the more direct view from the sea.
(7.) The chalk cliffs in the vicinity of Dover have been described in detail
by the late Mr. William Phillips* ; and the presence of the upper green-sand
which had escaped the notice of Mr. Phillips, has been pointed out by
Mr. De Basterot}. These, with Mr. Conybeare’s more general description {,
and Mr. William Smith’s coloured map of Kent, are the only modern geolo-
gical illustrations of this part of England with which I am acquainted. But
there is a publication of much earlier date,—Packe’s “Chart of East Kent,”
with its explanatory memoir entitled ATKOTPA®IA, printed in 1743, which,
though not strictly geological in its immediate object, points out very correctly
the connexion between the external features and the disposition of the strata
in the tract to which it relates, and contains such excellent views in physical
geography as to demand especial notice in this place§.
(8.) As the chalk rises, in proceeding from Dover towards Folkstone, the
upper beds disappear ; the cliffs represented in the view and section consist-
ing entirely of the lower members of that stratum. The rise of the marly chalk
above the sea level occurs about a mile and a half to the east of the escarp-
ment of Folkstone hill, and the place is well marked by the breaking out of
a very copious and perennial spring, called ‘“Lydden Spout,” which issues
from the top of these marly beds|| ;—a situation probably corresponding to
that of the springs which everywhere appear in the interior, along the foot of
the chalk range. Near the “Spout” the cliff is about 450 feet high; the
upper part consisting of very white chalk, with a bed of flint nodules, the
rest of chalk without flints, gradually assuming a greyer hue as it descends.
About the middle of the cliff'a thick bed has acquired by exposure a rough
and darker surface, by the aid of which it can be traced towards the west ;
* Geol. Trans., First Series, vol. v. p. 16.
+ Geol. Trans., Second Series, vol. ii. p. 334.
* Outlines of England and Wales, p. 119—184.
§ A more full account of this valuable work, which had been previously mentioned by Mr, Co-
nybeare, will be found in a tract on the Progress of Geology in England, by the author of the
present paper :—London and Edinburgh Philosophical Magazine for 1832, vol. i. p. 447, &e.
|| A new species of Tornatella, named by Mr. Sowerby elongata, was found in the chalk marl
at this place, by the Rev. G. E. Smith. See Plate XI. fig. 1.
Dr. Firron on the Strata below the Chalk. 107
and on the shore there are numerous detached masses, composed of round
portions of grey marly chalk united by a yellowish-brown cement. The shore
itself, at this place, is a firm floor of light bluish grey marl, the beds beneath
being of a still darker hue. The vertical face of the cliff retires from the sea
about 2000 paces west of Lydden Spout ; and the intermediate shore, thence
to Copt Point, is occupied by a mass of ruin, which has fallen from above,
in consequence of the rise and erosion of the soft argillaceous beds beneath.
The sudden transition to this ruinous under-cliff from the vertical face of
chalk is very remarkable. A stratum abounding in green particles, intimately
mixed with marl, appears at low water, in several detached places on the
shore west of Lydden Spout, and is succeeded by the blue clay of the gault,
which continues to Copt Point, where it rests upon the sand and grit of lower
green-sand :—the prominence of the Point itself, and of the shore to the west
of it, being evidently produced by the greater firmness and durability of the
latter stratum.
The succession of the beds is best seen in the retiring portion of the shore,
immediately on the north of Copt Point, (see Plate Xa. No.1.) A small outlier
of the lowest chalk, with green-sand beneath it, is there exposed at the summit
of the rounded hill on which stands the Martello Tower No. 3. Copt Point
itself consists almost entirely of gault, which tops the low cliff thence to the
village of Folkstone. The lower green-sand, rising gradually from the Point,
occupies the whole cliff west of the village ; and being continued without in-
terruption, through Sandgate and in the heights above Hythe, its outcrop turns
from the coast into the interior, at Aldington Corner. Finally, the Weald-
clay, rising on the shore beneath Shorn Cliff, occupies the greater part of the
heights and sloping ground on which the town of Hythe is placed, and ex-
tends about four miles farther to the west, where it gives place to the
Hastings-sands. |
In my obervations on this part of the coast, I shall confine myself to the
beds below the chalk; referring for a detailed account of that stratum to
Mr. W. Phillips’s paper, already mentioned.
(9.) Upper Green-sand. The upper green-sand near Folkstone, is but
a scanty representative of the formation, as it occurs in the Isle of Wight,
Surrey, Western Sussex, and some other places in the interior; its total
thickness probably not exceeding five-and-twenty or thirty feet, and the stony
strata and concretions of chert being altogether wanting. Its rise upon the
shore is concealed; and the stratum is first seen in its proper situation be-
neath the Martello Tower No.2. A small outlying portion about fourteen
feet in thickness, occurs beneath a cap of grey chalk marl about eight feet
P2
108 Dr. Firron on the Strata below the Chalk.
thick, at the top of the hill on which the Tower No. 3. is placed*; and in this
place the stratum consists of a soft marly sand, traversed in every direction
by stem-like cylinders, which have within them cores of darker green matter.
It also contains some irregular masses of a bright brown or orange hue;
but the greater part is composed of grey calcareous marl, like the lowest
chalk, so thickly interspersed with green particles as to exhibit only their
colour.
The fossils which I found in this stratum were few in number, and in-
distinct: the only species that could be ascertained was the Pecten orbicu-
laris}, one of the characteristic shells of the lower chalk and upper green-
sand in Hampshire and Western Sussex. .
(10.) The green matter, which abounds in this stratum near Wissant, on the
opposite coast of France, has been examined by M. Berthier{ ; who found it to
consist principally of silica and protoxide of iron, with ten per cent. of potash.
For the purpose of comparing the green-sands of different places and forma-
tions, my friend Dr. Turner, Professor of Chemistry in the London Univer-
sity, was good enough to examine some specimens from the upper and lower
green-sands of Folkstone, of the Vale of Wardour, and the Boulonnois, and
also particles of the same kind which abound in the sand and concretions
beneath the Portland stone, in the Boulonnois, and in England. I subjoin
the result of this examination§, whence it appears that in all these cases the
* See Plate VIII. and the Section, Plate Xa. No. 1.
+ Mineral Conchology, tab. 186.
+ Cuvier and Brongniart, Environs de Paris, 2nd edit. 1822, p. 249. See also Annales des
Mines, iv. 1819, p. 625.; and v. 1820, p. 197.
§ The following passages are transcribed from the notes with which Dr. Turner has favoured
me upon this subject.
“The colouring matter of green-sand sometimes appears in the rock of its ordinary green tint,
and sometimes in grains of so deep a green that they seem black. The former generally occurs in
sand, or where the sandstone is porous, and in this state an ochreous appearance is often observed,
due to the green particles being partially decomposed, and their iron having passed into a higher
state of oxidation; whereas the black-looking grains are met with in highly calcareous sand-
stone, where the texture is too firm to admit of the percolation of water. From either kind of rock
the green matter may be obtained by washing with water and subsidence, since the colouring matter
subsides less readily than grains of quartz, and more readily than calcareous and argillaceous sub-
stances. For the purpose of analysis it is best procured from those calcareous sandstones where
the cement predominates, as in the neighbourhood of Hythe and Folkstone in Kent. On reducing
such samples to powder, washing away the finer particles with pure water, and separating any
adhering carbonates by dilute muriatic acid, the colouring matter is left, mixed only with small
grains of quartz. It then always appears in the form of earthy particles of a deep green tint.
“ The green matter, when not previously weathered, is very feebly attacked by concentrated acids,
Dr. Firton on the Strata below the Chalk. 109
green matter is of the same nature. A slight examination of the green par-
ticles, which Sir John Herschel had previously the goodness to make for me,
intimated the same results.
(11.) Gault. The rise of this stratum on the shore is also obscured by ruins
of the superior beds; but it is visible in detached points, at low water, in
Eastware Bay, and forms the greater part of the cliff at Copt Point, where
many of the more beautiful specimens of the Gault fossils, seen in collections,
have been obtained. It appears also below the outlier of the upper green-
sand already mentioned (Plate X a. No. 1.); and occupies nearly the whole
of the grassy and ruinous cliff between the base of the Martello Tower No. 2,
and the sea. Its total thickness is about 130 feet, and it may be divided into
even by the nitro-muriatic. It gives out water when heated, and becomes brown from its iron
passing into the state of peroxide. As it has been supposed to owe its green colour to the pre-
sence of phosphoric acid, it was carefully examined, with the view of detecting that acid, if present.
It was accordingly fused with carbonate of soda, the alkaline filtered solution neutralized by nitric
acid, and evaporated to dryness, and the neutral solution tested by nitrate of silver and nitrate of
lead. Of two samples of green-sand, thus examined, one was found to be quite free from phosphoric
acid, and traces only were detected in the other. The former was also free from lime, and the latter
contained but a small portion. It is hence obvious, that neither lime nor phosphoric acid are
essential constituents of the colouring matter of green-sand, and their presence must be regarded as
casual.
In order to determine the chemical constitution of the colouring matter, I collected some green
particles from the calcareous sand of Eastware-bay, near Folkstone, removing all foreign matter
as far as possible, by washing with water and dilute acid. The only impurity which I could detect
after this treatment consisted of small grains of quartz, the quantity of which varied in different
samples.
“A portion of green particles thus purified, very free from oxidation, and dried at 212° Fahr.
lost 7-0 per cent. of water when heated to redness.
“Another portion of the same sample was fused with carbonate of soda, and the earthy ingredients
subsequently separated and weighed in the manner usual in such analyses.
‘A third portion was heated with carbonate of baryta, and examined for potash, traces of which
were readily found. According to the total result, the green particles consist of
[M. Berthier’s analysis of the green particles from
near Havre gave the following proportions ;:—
CO SHC Wae She ania ae eA co OT Oe 48°5 SiliGaitectate ic steve afets oterelere ae Heats 50°0
Black Oxide of Tron). ...065.0..0 22°0 Protoxig@e Of [LOM sie'e)e)=/eleraieiere 21:0
AMINA’... se. sleatetearete ole Sette ee moll AD PATTATTITTIANs of cies sree) si sicietel skexelel ets 1 (U
MARNESIA. ». 2s see's vise Seniesa SE iepeeiolS
Speman Sait, MSTA sheild sate Go eA TO Wiaterierracie css, crecicheisiviecie sine clkcO
PMs) sts onic ickteale os via «'e sles! tFaces Potash Uae(a)./ece ACOUDOUOO BNET 10°0
“ 98-3 99°0.]
“Tt is superfluous to speculate on the precise atomic constitution of the green particles, since they
were not obtained in a state of perfect purity. The ingredients which appear to be essential,
110 Dr. Fitton on the Strata below the Chalk.
two portions. ‘The upper part immediately succeeding the upper green-sand
contains green particles; and thence, for some feet downwards, it is harsh
and sandy. The lower portion consists of a smooth, uniform, very plastic
clay, of a light bluish grey colour, much in request for the fabrication of tiles
and common pottery. It is in this part of the cliff at Copt Point, that the
perfect and beautifully iridescent Ammonites, Inocerami, Hamites, and other
fossils, have been obtained. From the Point the stratum rises gradually to
the west, forming the summit of the hill, about 108 feet in height, on the
east of the town of Folkstone; and some traces of it also exist at the top of
the next cliff, on which the church stands. From the coast the gault can be
traced in a corresponding situation in the interior, along the foot of the chalk
escarpment ; its presence being everywhere indicated by a depression of the
surface, and by the marshy aspect of the soil, which generally produces rushes
and is strongly contrasted with that both of the chalk above, and of the lower
green-sand beneath.
It is not improbable that in the Isle of Wight and some other situations
where the fossils of the gault are rare, the upper and more sandy portion
only of this stratum may exist. At Cheriton Tile-works near Folkstone, the
workmen expressly state that it is the lower part only of their pits which
affords the shells.
(12.) Throughout the gault, but chiefly in the inferior portion, concretions
of iron pyrites are found, generally approaching to a globular or cylindrical
figure, and of a radiated crystalline structure within, or in long thin vermi-
cular rods, which at first sight might be taken for vegetable stems. On the
opposite coast of France, near Wissant, the pyrites is so abundant in the
gault as to have given origin, some years since, to a manufactory of sulphate
of iron*; but near Folkstone the quantity is comparatively inconsiderable.
hoth from the quantity in which they occur, and their constancy in the colouring matter of
green-sand from different localities, are silica, alumina, oxide of iron, magnesia, and water. I
should hence consider the green matter as a hydrated silicate of alumina, magnesia, and black
oxide of iron, and as being, in all probability, the true green earth, or earthy chlorite of mineralo-
gists. The analyses of chlorite hitherto published are so discordant as to prove, either that dif-
ferent compounds have been examined under the same name, or that the specimens under exami-
nation were very impure. The essential ingredients, however, appear to have been the same as in
the subject of my analysis.
“Though the foregoing description applies more immediately to the colouring matter of the
green-sand from the vicinity of Folkstone, I have obtained similar results on examining that from
Hythe and several other places. Indeed, from the examination of many samples of green-sand
collected by Dr. Fitton from various localities in England and France, I believe the colouring
matter to be precisely the same in all.”
* See Annales des Mines, 1819, p. 623.
Dr. Fitton on the Strata below the Chalk. lil
(13.) Other nodules and irregular masses are also found throughout this
stratum, which resemble coprolite in their chemical composition, though no
traces of animal structure are apparent in them. These are often associated
with pyrites, and traversed by veins of that substance, as in septaria. Inter-
nally they are in general of a dark brownish hue, and the fracture is even or
splintery, like that of some varieties of chert. The form of these nodules
is sometimes very like that of coprolites; but though portions of shells are
sometimes found within them, I have not detected any fragments of bone or
scales of fishes. The surface of some of the detached masses is eroded, as if
by worms ; to the action of which, therefore, they were probably exposed be-
fore they were enveloped in the clay. In other cases they are of a very irre-
gular figure, surrounding or incorporated with fossil remains, especially of
Ammonites, the interior of which is filled with matter of the same kind.
Concretions of this description occur not only in the gault of different
places, but are also numerous in the bottom of the lower green-sand at Ather-
field in the Isle of Wight; and a mass found by Mr. Lyell in the crag at
Southwold in Suffolk, which is mentioned by Dr. Buckland*, appears to have
been of similar character. The concretions of the gault in Kent evidently
agree with those of Havre and Wissant, analysed by M. Berthier, and found
to contain about 57 per cent. of phosphate of lime, with a considerable portion
also of carbonate of limet. It can hardly be doubted that they are derived
from the remains of animals, though no traces of bony texture are now per-
ceptible ; and it is not improbable that they may have been the contents of
the intestines of marine animals, which fed upon each other, though not in
all cases moulded into the form of coprolite.
The abundance of phosphate of lime, especially in submarine strata, will not
appear surprising, when it is recollected that not only the bones, spicule and
scales of fishes afford that substance in large quantities, but also the covering
of the Echinodermata, and of crustaceous animals, in a smaller proportion f.
* Geological Transactions, Second Series, vol. iii. p. 234, note.
t Dr. Prout, soon after his examination of the Coprolites, of which Dr. Buckland has given an
account in the Geological Transactions (Second Series, vol. iii. p. 237 &c.), was good enough to
examine some of the concretions from the gault of Kent and the Vale of Wardour, and from Ather-
field, and found them all to contain phosphate of lime, united with carbonate of lime and oxide of
iron, in different proportions, the dark-coloured varieties containing the largest proportions of the
phosphate. They all, likewise, yielded, more or less, the peculiar smell given out by coprolites
when dissolved in muriatic acid. Dr. Turner has since examined other specimens, from the gault
beneath Blanc-nez, and at Lottinghen on the east of the Lower Boulonnois, and finds them to indi-
cate 2 similar chemical composition.
{ Hatchett “On Shell and Bone, &¢.”; Philosophical Transactions 1799, p. 323, and 1800, p. 373.
2 Dr. Frrron on the Strata below the Chalk.
(14.) The following is a list of the fossils of the gault in this neighbourhood,
in my own collection, and in those of Mr. Hills, of Court-at-street near Lympne,
of Mr. Sowerby, and some other of my friends. I take the present oppor-
tunity of expressing my obligation, especially to the Rev. Gerard E. Smith
and Mr. Hills, for their kindness in supplying me with all the new species
of their collections, many of which are figured in the plates annexed to this
paper. Lord Greenock also has been so good as to allow me to have drawings
taken from some specimens collected by himself.
List of Fossils from the Gavuut, in the vicinity of Fotkstone, Kent*.
Ammonites auritus. Fleur de Luce pits near Folkstone. F.
A. Benettiz. Leacon Dill, about two miles S.W. of Charing, Kent. S.
A. Beudantii. (Brongniart; Env. de Paris, tab. vii. fig. 2.) Cheriton. F,
A.? circularis. PJ]. XI. f.20. Burham near Maidstone. So.
A.crenatus. Pl. XI. f.22. Tile-works at Cheriton. F.
A. dentatus. (Syn. A. serratus, Parkinson.) Leacon Hill. S. Fleur de Luce. F.
A. inflatus. Folkstone. F.
A. lautus. Leacon Hill. S. Folkstone. Min. Conch.
A. minutus. Folkstone. Min. Conch.
A. proboscideus. Folkstone. Min. Conch.
A. Selliguinus. (Brongniart; Env. de Paris, tab. vii. f.1.) (Syn. A. levigatus ?
Min. Conch.) Cheriton, near Folkstone. F.
A. splendens. (Syn. A. planus? Mantell.) Leacon Hill. S. Tile-works, Cheriton. F.
A. subcristatus. (Brongniart; Env. de Paris, tab. vii. f. 10.) Fleur de Luce near
Folkstone. F.
A, symmetricus. Pl. XJ. f.21 and 23. Clay-pits near the Fleur de Luce, Folk-
stone. F.
A. tuberculatus. Weacon Hill. S. Fleur de Luce pits, near Folkstone. F.
A. varicosust+. Folkstone. M. C.
* In this and the subsequent lists of fossils, the names are disposed in alphabetical order, for
facility of reference. The new species are in Roman type, the rest in Italics. A systematic list of
all the genera and species of the several lists will be given at the close of these pages.
In the statement of localities, the capital letters after the names of places denote the persons to
whose authority the occurrence of the several species is referred ; H. signifying Mr. Hills, of Court-
at-street near Lympne; S., the Rev. G. E. Smith, A.M.; So., Mr. Sowerby; G., Henry H. Good-
hall, Esq.; F., the Author of this paper. The letters M. C., or Min. Conch., denote the Mineral
Conchology of Messrs. Sowerby; Geol. Soc., the Museum of the Geological Society.
+ Mr. Parkinson has mentioned other species of Ammonites; 4. ornatus, from Folkstone and
Cambridge, 4. pansus, from Folkstone and West Malling, Kent (Geol. Trans., First Series,
vol. v. pp. 57 and 58). The A. serratus of Parkinson is 4. dentatus of Sowerby.
Dr. Firron on the Strata below the Chalk. 113
Auricula inflata. PI. XI. f.11. Copt Point? S.
Belemnites alttenuatus. Weacon Hill. S. Near Folkstone. F.
B. minimus. (Syn. B. Listeri.) Folkstone. F.
Cardium? decussatum. Copt Point. S.
C. (species doubtful). Indistinct specimens, apparently different from C. decussa-
tum.
Caryophyllaa. Folkstone. F.
Corbula striatula. Folkstone. Min. Conch.
Corystes? Mantell, Sussex. Pl. 29. fig. 13. Near Folkstone. S.
Cytherea parva. (Syn. Venus parva; M.C.) Eastware Bay and Leacon Hill. S.
Dentalium ellipticum. Copt Point. S.
Exogyra conica. Near Hythe. H.
Gastrochena (species doubtful). Found in perforations of dicotyledonous wood. Kast
of Folkstone. S. and F.
Hamites aculeatus. Pl. XII. f.4. Copt Point. H. and S.
The Rey. G. E. Smith’s observations on the new points in the structure of this
genus will be found hereafter, with Mr. Sowerby’s description of the species
figured in the Plates annexed to this paper. The figures in Pl. XII. are from
drawings by Mr. Smith.
HT. armatus. Near Folkstone. F.
Hi. attenuatus. Pl. XII. f. 3. Copt Point.
HI. compressus. Fleur de Luce near Folkstone. F.
Hi. gibbosus. Fleur de Luce near Folkstone. F.
H. elegans. (Parkinson, Geol. Trans. v. p. 58.) Folkstone. S.
Hi. intermedius. Leacon Hill, and Fleur de Luce pits. F.
H, maximus. Leacon Hill. S. Fleur de Luce. F.
H nodosus. Near Bythe. H.
HI. rotundus. Pl. XII. f.1 &2. Copt Point. S.
HI. tenuis. Near Folkstone. F.
Inoceramus concentricus. Beautiful specimens of I. concentricus and sulcatus, with va-
rious Ammonites, retaining the pearly lustre of the shell, are found in great num-
bers about the middle of the cliffat Copt Point. F. Folkstone; W. Malling, Kent;
and Cambridge : (Parkinson, Geol. Trans. v. p. 57, 58.) Also at Leacon Hill. S.
I. Cripsii?’ Mantell, Geol. Sussex, P]. 27. f. 11. Near Sandgate.
I. sulcatus. Folkstone; W. Malling, Kent; and Cambridge: Parkinson.
Modiola bella. Pl. XI. f. 9. Near Hythe. (Lower Green-sand?) H. and F.
_ Murex calcar. Folkstone? F.
Natica canaliculata. (Syn, Ampullaria canaliculata, Mantell,) Pl. XI. f.12. Near
Folkstone. S. and F. The specimen a, } is filled with brownish (coprolitic ?)
phosphate of lime.
Nucula bivirgata. Pl. XI. f.8. Eastware Bay. H. and G. Leacon Hill. S.
N. ovata. Mant., Geol. Sussex, Pl. 19. f. 26.27. Folkstone. Mantell.
N, pectinata, Copt Point and Leacon Hill. S. Fleur de Luce pits and Cheriton. F.
W. Malling, Kent; and Cambridge: (Parkinson, Geol. Trans. v. p. 59.)
VOL. IV.—SECOND SERIES, Q
114 Dr. Fitton on the Strata below the Chalk.
Nucula? undulata. Copt Point? S.
Ostrea macroptera? Fleur de Luce near Folkstone. M. C. and F.
Panopeaa plicata. (Mya plicata, Min. Conch.) Near Folkstone. M. C.
Pentacrinus. P\. XI. f. 4. Copt Point. H.
Plagiostoma elongatum. Folkstone. Specimens have been found 1; in. wide, # in.
deep, and 3 in. thick. G.
Pleurotomaria Gibsii. (Trochus Gibsit of Min. Conch.) Copt Point and Leacon
Hill. S.
Plicatula pectinoides. East of Folkstone. S.?
Pollicipes levis. Pl. XI. f. 5. Copt Point, Folkstone. H.; with the following
species :—
P. rigidus. Pl. XI. f.6*. Copt Point. H.
P.unguis. Pl]. XI. f.5*. Copt Point. H.
Pyrula?}+ Smithii. Pl. XI. f. 15. Copt Point. S.
Rostellaria buccinoides. Pl. XI. f.17. Eastware Bay. G.
. calcarata. Near Folkstone. S.
.carinata. Pl. X1.f.19. Eastware Bay. S.
. elongata. Pl. XI. f. 16. Copt Point, Folkstone. H.
.-marginata. Pl. XI. f.18. Copt Point. H.
R. Parkinsonii. Copt Point and Leacon Hill. S.
Serpula antiquata. Near Beachborough, Folkstone. M.C. (Upper Green-sand ?)
S. articulata. Folkstone. M. C.
S. rustica. Eastware Bay. M.C. (Upper Green-sand ?)
Solarium conoideum. (Min. Conch.) Pl. XI. f. 14. Near Folkstone. S. and F.
S. ornatum. Pl. XI. f.13. Fleur de Luce near Folkstone. S. and F.
Spatangus argillaceus. (Phillips, Geol. of Yorkshire, Pl. II. f. 4.) East of Folkstone.
Teredo? In fossil Dicotyledonous wood, Leacon Hill. S. Kolkstone, and Cam-
bridge: (Parkinson, Geol. Trans. v. p. 58.)
Terebratula biplicata. Folkstone (in gault?). S.
T. sella. Near Folkstone (in gault?). S.
T. sulcata. Folkstone, and Cambridge: (Parkinson, Geol. Trans. y. p. 59.)
Tornatella? affinis. Plate XVIII. fig. 9. Eastware Bay. S.
Trochus Gibsii? See Pleurotomaria Gibsii.
Turbinolia Kenigii. Weacon Hill. Very abundant. S.
Turritella (species doubtful). Folkstone. S.
Venericardia tenuicosta. Pl. XI. f.7*. Eastware Bay. H.
Venus parva. See Cytherea.
V.?tenera. Pl. XI. f.7. Copt Point near Folkstone. H.
OU
t In naming this genus, and some others mentioned in this paper, respecting which doubts may
be entertained, Mr. Sowerby appears to have been influenced by a desire to produce all the infor-
mation which the specimens could afford, conceiving that even if the names be erroneous, the
figures may still have some value as objects of future comparison.
Dr. Firron on the Strata below the Chalk. 115
Wood, dicotyledonous. East of Folkstone. Perforated by Gastrochena; near Folk-
stone. S. Sometimes surrounded with pyrites. Mr. Parkinson states that “fossil
“ wood occurs plentifully in the marl (gault) of Folkstone; lying chiefly at the
“ bottom of the stratum, on the green-sand.”’ Geol. Trans. vy. p. 59.
(15.) Lower Green-sand.—T he uniform surface of this stratum, extensively
shooting out beyond the chalk, forms a conspicuous feature of the country,
which is well seen from the ascent of Folkstone Hill on the road to Dover*.
The analogy in this respect to the appearance of the sands at the Black-
down Hills in Devonshire, is obvious and striking. The Bagshot sands, above
the chalk in Surrey, also exhibit long and uniform platforms, the section of
which presents a linear and almost horizontal top, with a rapid escarpment at
both extremities.
(16.) One of the principal circumstances in the internal structure of the
Lower Green-sand at Folkstone, is the distinctness with which it is divided into
three groups ; and this subdivision probably occurs wherever the formation is
fully developed in the South-east of England. It is clearly seen in Surrey ;
I have evidence from Mr. Martin of its existence in the West of Sussex ;
Mr. Lonsdale believes it to hold also near Devizes in Wiltshire ; and though I
did not become acquainted with it till after 1 had examined the Isle of Wight,
I have little doubt that it will be found there also.
a. The first of these subdivisions may be characterized as consisting prin-
cipally of sand, white, yellowish, or ferruginous, with concretions of limestone
and of chert, frequently in false stratification. It forms commonly a flat, but
sometimes an irregular hilly surface, rising from the valley of the gault, and
bearing a dry, barren soil.
b. The second member abounds in green matter, is retentive of moisture,
and contains comparatively little stone: it occupies a flat and marshy tract,
between the first and third divisions.
c. The third and lowest member contains a greater proportion of calca-
reous matter, and includes some of the principal beds of stone bearing the
name of “Kentish Rag”; which commonly form a prominent ridge at its
outcrop, adjoining the valley of the Wealdt.
* From Folkstone Hill the ridge of Fairlight Down, near Hastings, is a very striking object :
its range is evidently parallel to that of the chalk outcrop, as might be expected in the axis of
elevation of the tract by which it is surrounded.
+ In Mr. William Smith’s Geological Map of Kent, two ranges are indicated, by darker co-
lours, in the tract between the coast and Maidstone; one running parallel to the chalk, from
Sandgate through Ashford and Bursted to Penenden-Heath, on the N.E. of Maidstone; the lower,
less regularly, from Hythe along the verge of the WealdClay. These lines, I have no doubt, indi-
cate a subdivision like that mentioned in the text: but in the explanatory table of the map, the
stone of the tract thus coloured is said to be the Portland-rock.
Q 2
116 Dr. Frrton on the Strata below the Chalk.
The situation and relative space occupied by these subdivisions near Folk-
stone, are shown in the small Map, Plate VII. fig. 1., and in the View,
Plate VIII.
(17.) a. The uppermost subdivision is about seventy feet thick. It rises
upon the shore on the west of Eastware Bay ; and some of the firm siliceous
beds which it includes near the top, coming up from the sea a little to the
east of Copt Point, are continued in the cliff thence to the west of Sandgate ;
between which place and Folkstone distinct sections are disclosed. The
greater part of the country from Folkstone, through Cheriton, to Newington
is occupied by this bed, and the heights of Dibgate and Sine Farm, where
it finally disappears, are capped with it.
(18.) Where the sand emerges from beneath the Gault, it is often loose,
and of a white or buff colour; but at the immediate junction there occurs, in
many places, a course, from six inches to a foot in thickness, of concretions
of pyrites, often investing fragments of silicified coniferous wood, of a dark
brown colour. 'The composition of this bed resembles, in several respects,
that of the Blackdown sands in Devonshire, the stone which it includes con-
sisting principally of siliceous spongy concretions, like the whetstone of that
place. ‘The most instructive specimens are to be found in the loose decom-
posed masses on the shore. In the vertical faces of the cliffs, the surface
exposed by fracture and falling away is at first clean and uniform, no traces
of the stratification appearing ; but after a time the sand crumbles from the
surface, while the stony portions remaining fixed, become prominent.
The whole of these cliffs consists, in fact, of sand and conglomerates more
or less firm, produced by the agglutination of the loose materials which formed
the original submarine deposit. The strata vary in texture and composition,
from the state of sand to that of very hard limestone or chert, of various
shades of grey and brown; the latter passing into chalcedony, with which the
cavities are sometimes coated*. The transition from the sand into compact
stone is sometimes very rapid ; in other specimens the gradations are almost
insensible.
(19.) The principal components of these conglomerates are the following:
1. Quartz, in rounded fragments, from the bulk of a large pea to the
minutest visible size, of several shades of grey and white, varying from trans-
parent to nearly opake, and in some instances passing into chalcedony.
2. Small, worn fragments of quartzose jasper, red, or greenish; with flat
surfaces, in some cases, indicating stratification.
* It is remarkable, that notw:thstanding the abundance of siliceous matter in the concretions
near Folkstone, few or none of the petrifactions are formed of it; while at Blackdown in Devon-
shire most of the shells in this formation are casts in chalcedony.
Dr. Frrron on the Strata below the Chalk. 117
3. Fragments, frequently much larger than those above mentioned, of very
compact, dark brown, black, or grey flinty slate. Sometimes the appearance
of these fragments is internally that of hornstone, approaching to jasper.
4, Fragments, often angular, or slightly rounded, of schistose granular
quartz, or sandstone, interspersed with very minute particles of mica; not
effervescent; its colours varying from smoke grey to greenish.
5. Near Ashford, in the ferruginous sand at the top of the formation, frag-
ments are found of brown hematitic iron ore; but much less abundantly than
in the corresponding part of the section at Redcliff, near Sandown, in the Isle
of Wight, and at other places.
6. Near the top of the sands, in the blocks of fenotnpésed stone, upon the
shore, lumps are found, from the size of a walnut downwards, of a dark
brown substance, externally spongy, and of irregular surface, and within
having the fracture and appearance of the phosphate of lime described in
Section (13)*. In these brown masses are also some grains of quartz, and
small portions of shell. This occurrence of phosphate of lime, both in the
gault and at the upper part of the lower green-sand, is an additional proof
of the continuity of their deposition.
(20.) The stone of the more uniform beds (‘ Kentish-rag,”’) has great
variety of characters, from those of a granular or sparry compound to com-
pact limestone, some specimens of which might be taken for that of older
formations. In many cases, the calcareous cement is so crystalline, that light
is reflected continuously from extensive surfaces, although the face of the
fracture is thickly set with small pebbles of quartz; in other cases the stone
is a dense conglomerate, composed of quartz grains with a small proportion
only of the cement. All the varieties contain disseminated grains of the green
matter above described in section (10); which is frequently so abundant as
to give its colour to the stone. In many of the rolled fragments on the shore
near Folkstone, this constitutes more than half the compound, the remainder
being decomposed carbonate of lime, inclosing grains of quartz and flinty
slate. In the more advanced state of decomposition, the mass has the ap-
pearance of mortar ; and, in most cases, the stone effervesces copiously with
acids, the green particles remaining undissolved.
The chert of this upper stratum is frequently of a dark grey colour, and
* The specimens here referred to were sent me from the shore immediately on the west of Folk-
stone, by my friend the Rev. J. D. Glennie ; but there can be no doubt of their having fallen from
the adjacent cliffs. Among the darker masses mentioned in the text were portions of the claws of
an Astacus. On the shore hereabouts plicated Terebratulze were found in nodules of arsenical
pyrites,
118 Dr. Fitton on the Strata below the Chalk.
very like chalk flint. In some specimens, this dark variety adjoins, with
scarcely any gradation, a light grey, or white siliceous agglomerate, in which
the original sandy structure is still discernible ; while in the adjacent darker
chert the fracture is flat-conchoidal and splintery, with the glimmering lustre
of hornstone, all trace of the grains having disappeared ;—as if a sand of wax
had been consolidated by gentle softening, in a heat not sufficient for its
liquefaction. In its passage to chalcedony, the siliceous matter often assumes
a white colour, the aspect being nearly that of porcelain, and it becomes
translucent when moistened.
(21.) A section of the upper part of this member (a) of the lower green-
sand, in the cliff about midway between Folkstone and Copt Point, was as
follows :
Top of the Lower Green-sand.
Feet. Inches.
Bluish grey clay (Gault), a few feet in thickness, at the top of the cliff: then—
1. At the junction of the clay and sand is a bed consisting of pyrites in lumps,
more or less decomposed; about ..... srevatoteretsietere Ssscolazevoere, efetlevehers 10 veg DLO
2. Grey quartzose sand, with numerous green particles .....+.2seeeeeeeees « 4/90
3. Sand, in which lines of false stratification are conspicuous ...... Bogoopmone sb
Ae SiMilarpDUticOArserssand earyererereieteeieieiieiiiere Richer stetcrererereverels Rioteleletehete srevsie’ OR
5. Sand, yellowish, slightly concreted, irregular in thickness; much more solid in
the eastern partiofithe icliff; "about... 1c s:. bie « = sieve sio'ejieierars een ccceee - 8&8 @
Gem Sandiesretetetetelelaicielelsjolersioreiencicvere GOOD DO AUTOR GAOCO COO Od0 06 MeooooDGddD |
7. Irregular siliceous concretions .....00+++seeeee- «i.e, 6 s1']s 8 ayo'e oe myais-siejeieie oon) Ol am
8. Sand, nearly as above, with a few dispersed concretions ........ occ ecece .) oo
9. Irregular concretions, like No.7 .........6. sole eisteie) o(etsvelchele etstsleiaiateneatete 1's
10. Sand, with a few scattered concretions ........cssecccsccccccvesece ccoee ORE
11. Irregular concretions, in sand; more dispersed ........+-+.0+ Somd0a0000N 2 ©
12. Sand, as above..... atau lorageherieveroveyoie re sxe lols) ¢+s) «lope teraveueseie enero lover detehonomeneeetete 4 6
SH eConcretions) 1-16 //e1sle\el abies sicisieperskere /oletelsiets oretave: stelelieve:cheredeetenenerenerenern tere . Ov Sito
{ASI Sandeaspaboves DUtINer + AD OUL,. «cle /cle) alors ciclete oie lcle ol cialersicietetercielerneroneteiete by (0)
15. About four courses of concretions, with sand between ......--.2eseee0e Pe
16. Sand ;—to the foot of the cliff.......... araralelecatclereig i cise alee eieteterercketene oct A eo
Total; about =... coum0e
The concretions of Numbers 5, 7, 9, 11, 13, 15, consist of siliceous spongy
stone, like the whetstone of Devonshire, varying from a loose friable mass, to
the consistency of chert. In many instances the surface has the form of cylin-
drical stems.
* The height of the cliff at this place is really not more than thirty feet; but the proportions
are nearly as above given.
Dr. Fitton on the Strata below the Chalk. 119
(22.) In another section of this part of the stratum, at one of the quarries
about midway between Risborough and the east of Sandgate*, the detail
was thus:
Surface of the hill. Feet. Inch, Feet. Inch.
1. A group, consisting of alternate courses of sand and irregular siliceous 7
concretions :—
a. Sand, with a few interspersed concretions .....eeseeeeeeeeee O 8
b. Stone, in irregular spongiform concretions, including fragments
of Oysters or Gryphites, and passing into grey, compact chert,
which in some instances graduates into chalcedony ;—retaining,
however, traces of the original sandy structure. The concre-
tions include also minute fragments of calcareous matter, so
that the surface effervesces in detached points; about ...... 0 2
c. Sand; loose, somewhat coarse, consisting principally of grains of
about
QUATEZ «cc ccccccescecreserccveccrccccccsesscecsesees 0.6
3.0
d, Stone; in loose spongy concretions, white, opake, and in some
places more compact within, like chalcedony; not effervescent. 0 4
e. Sand; coarse, dark brown, not effervescent; a great part con-
sisting of grains of translucent quartZ .....eeesscecsecceee O 6
f. Stone; in roundish, flattened concretions. A conglomerate of gra-
nules of quartz, with some portions of flinty slate, and dark green
specks, cemented by sparry carbonate of lime: from 2 inches to 0 8
g. Sand; dark greenish grey, not effervescent, including casts of
PTAC AY THES 9 os + o!05 ala.o's sels «sie pio winieialoicicwis alvclae <0
i, SUBWE 660 boat b0 6066 SAREE OER nee Donn BORE aneae
o
m Oo B
t. Sand; dark greenish grey, gritty, not effervescent .........++6 0
the whetstone of Blackdown; not effervescent .....-eceesececcecs
3. Beds of sand, partially concreted, somewhat coarse, soft, effervescing
copiously, and including concretions of cherty stone. The false stratifi-
cation of this part of the cliff is very conspicuous ......20.ese0eee:
4. Stone, alternating with sand: thus :—
a. Stone, in somewhat compact concretions, oblique to the general
stratification, including cylindrical portions, like the stems of
Siphonaria; the greater part siliceous, white and opake, but
effervescing in detached spots; about ......sesesccecseeee
b. Sand, greenish grey, effervescing copiously........seeeeee0e.
c. Stone, in loose, spongy, irregular concretions ........2+e+200
oo 0 6
oon 6
d. Sand, loose, greenish grey, effervescent ......ssseseeeeeeees
e. Stone, in spongiform concretions, like 1. 6, above, passing into
eh Sacchi ia loleti =: mpicipicip in p)a'vid-s\nydyesa.nieswiessie mya
ei civieli chic gislniaensilaspinsisincenceesensae 0. 9
g. Stone, in spongy concretions; as at Blackdown ......0++.ee00%
J
2. A bed of siliceous and porous concretions, nearly continuous; very like |
o
aS
* See the Map, PI. VII. fig. 1.
120 Dr. Firron on the Strata below the Chalk.
5. Sand, with concretions; greenish grey, uniform, not effervescent, At the 2
bottom of this bed is a course of concreted sand passing into stone, with
seams oblique to the general stratification. The stone is in some places
opake and white, like chalcedony, including however minute dark green |
particles: the looser pieces are spongy, like the Blackdown whetstone. .
6. Sand and stone: thus :— 7
a. Sand, resembling that of No. 5, but of darker colour ........-
b. Stone. A dark grey, compact, fine-grained, conglomerate of cal- |
careous spar and grains of quartz, in some places traversed by about
EMI VEINS OL SPAT -teloledeteiede ate ole Kelateroh stole cl orelaeenetetele sia ete tetas 3. 0
c. Sand, resembling a, uniform, not effervescing..........2+. ts
d. Stone ; a compact conglomerate, including small portions of dark
SS
flintyiislateitenstyeteleteeteltedelercts¥- wieteitsteletsi ee el ois) visdelrcelvere retake
es
Total .... about 16 0
In another quarry, immediately beneath this one, the composition was ap-
parently the same ; but the beds of chert were more numerous.
(22.) The false stratification above alluded to, or the subdivision of the
beds by lines oblique to the general course of the stratification, is a promi-
nent circumstance in the upper part of the lower green-sand in this neigh-
bourhood. It is observable in several places on the road from Hythe to
London ; and was very well exhibited in the sides of the road through the hill
between Sandgate and Folkstone, where the sketch subjoimed was taken.
4 SS
rk a
(oa 5
Sear ee A Ch ae
In the beds, of which a portion is here represented, not only the lines of
division, but the concretions within the strata exhibit the oblique arrange-
ment; and in some instances, the larger cherty masses, the general direction
of which is that of the prevailing stratification, send out offsets in the direction
of the false strata, as expressed in the sketch. ‘There is no appearance of
Dr. Firton on the Strata below the Chalk. 12]
variation in the circumstances under which the different strata were deposited,
although some of those traversed by the lines above described alternate with
others, in which no traces of them, or scarcely any, are to be seen.
(23.) The concretional masses described in the preceding sections give
rise to. some questions of great interest in geology. ‘There can be no doubt
that all these strata were originally deposited in the state of sand and gravel ;
but in the quarries of East Kent all stages of gradation can be perceived,
from distinctly separated concretions of stone*, to others so nearly uninter-
rupted, that the next step into perfect continuity can be easily conceived.
The sands below the Portland-stone the coral-rag and the inferior oolite,
afford examples of the same character: and in all these cases the concretions
must have been formed after the deposition of the sand which includes them,
and probably beneath a great depth of compacted materials. In such a mass,
shut off from the free access of air and change of temperature, there is no
obvious reason for disturbance of the affinities which maintained the original
form of the components, except the decomposition of the animal and vege-
table remains diffused among the stony substances; yet here we have not
only solid limestone, where nothing but loose sand and gravel were before,
but firm siliceous concretions, pervading, and so identified with, the separated
particles of the quartzose sand, that the whole is nearly homogeneous. If the
decomposition of the organized substances, continually acting throughout very
long periods of time, be not sufficient to produce the whole of these effects,
perhaps it may be supposed that electricity is the cause which sets free the
elements, and disposes them to combine anew f.
(24.) The second, or middle subdivision (b.) of the lower green-sand, first
* Concretions nearly globular occur, in the uppermost yellowish sands, at Parkhouse, near
Folkstone.
+ In preparing nitric acid in a chemical laboratory where I was attending some years ago, the
glass retort broke towards the close of the operation, and a quantity of the concentrated solution
of bisulphate of potash oozed out through a very fine crack into the surrounding sand. On re-
moving the retort some time afterwards, a large part of the sand was found to be agglomerated into
beautiful concretional masses, like bunches of grapes, the greater portion of which, of course, was
sand, and the cementing substance the crystallized salt. ‘The masses of gravel frequently found
cemented by carbonate of lime, or of iron, in consequence of the escape of the carbonic acid which
had held those substances in solution, is an example of another mode of concretion. In the first
of these two cases the loss of heat, in the latter the escape of a chemical solvent, has obviously
been the cause of the consolidation. But the case mentioned in the text is distinct from both.
Dr. Turner justly remarks, respecting substances usually considered as insoluble, that “ although
“the weight of such bodies is not perceptibly diminished by trials conducted in the laboratory,
“ during a short interval of time, and with small quantities of water, the effect of the same opera-
VOL. 1V.— SECOND SERIES. R
122 Dr. Firron on the Strata below the Chalk.
appears upon the shore on the west of Folkstone, at a point immediately be-
neath the church*, which is well marked by the breaking out of a spring. It
is there conformable to the strata described in the preceding sections, and the
whole of it has risen to some feet above the sea, on the east of Sandgate,
where rocks of the subjacent group (c.) make their appearance on the shore.
This second stratum forms the middle of the cliff above and behind the
village of Sandgate, but thins off and disappears in the heights on the west of
Nail-Down, where some outlying portions of the superior sand (a.) cap the
summit of the hills. Its thickness appears to be from 70 to 100 feet: it
abounds in green matter, and in some places in pyrites; from the presence
of which substances (though in what manner is not obvious), or perhaps of
some portions of clay, it acquires a retentive property ; so that the soil over
it is marshy, and ponds are frequent upon its surface. The tracts, therefore,
which it occupies, have in some cases in the interior been erroneously sup-
posed to belong to one of the beds of clay subjacent to the green-sand.
(25.) The boundaries of this middle bed, where it is disclosed by the
streams having cut through the incumbent sands, are sufficiently indicated
on the map. In following up the streams towards Inbrook and Frogwell, the
contrast of the two strata is very conspicuous, the junction of this retentive
middle group with the sands above being indicated by the breaking out of
springs}; and a line drawn through the heads of the streamlets thus arising
would be throughout at distances from the outcrop of the chalk nearly pro-
portioned to the inclination of the strata.
(26.) The presence of this stratum occasions frequent falls of the incum-
bent sand beds, and has given origin to an under-cliff covered with vege-
tation, which extends from Folkstone to Sandgate. The sections therefore
are obscured; but enough is visible to prove that it contains no prominent
beds of stone, and that concretions are comparatively rare in it. Near its
junction with the stony strata beneath, the consolidated sand affords several
characteristic fossils; and about the middle of the heights over Sandgate f,
a line of ferruginous nodules has been found, inclosing fossils, like those of
‘tion, as performed on the great scale in the mineral kingdom, during hundreds and thousands of
‘years, and with unlimited quantities of the menstruum, might be, and doubtless was, very dif-
“ferent.” —‘ Report of a Lecture on the Chemistry of Geology’; Lond. and Ed. Philosophical
Magazine, 1833, vol. iil. p. 24.
* See the View, Plate VIII.
+ It is not impossible that the site here mentioned may correspond to that of the Sandrock
spring, in the Isle of Wight. A ferruginous spring, I was informed, does exist in the vicinity of
Sandgate.
+ In the grounds of Encombe, the seat of Mr. Dawkins. The place is indicated in Plate VIII.
Dr. Firton on the Strata below the Chalk. 123
Shanklin Chine in the Isle of Wight, and of Parham Park in Western
Sussex.
(27.) The following sections, at a prominent point of the cliff, between
Sandgate. and Folkstone, include a portion of the first or upper member of
the lower green-sand (a.), with the upper part of the middle stratum (0.).
Section of the Cliff between Folkstone and Sandgate.
(
(a.)
Feet. In. Feet. In.
1. Sand, with numerous courses of concretional stone, and traces of false
about
BELHEMCAPION. | ‘ejais of eerste claieietals 8:6 60 CAOIOG ROH AES eC AO renee as TO 0
2. A prominent group of sand and concretional stone ;
qa, Stone. Firm, uniform, fine-grained, sparry, conglomerate, with 3)
minute, dark green particles. |
Some of the blocks on the shore, apparently fallen from this | about
bed, consist of close-grained splintery limestone, somewhat + 2 0
sparry, including minute dark grains, disseminated in small one
proportion. They afford excellent specimens of the ‘Kentish 8 ? 0
“5 feo op GbE GSO BebOr CNBr ae Stevesatelers.« Heidaden- “5
b. Sand, including concretions of chert; about ........ sieretelege ek ia
c. Stone. Loosely concreted conglomerate, including shells, effer- about
vescing copiously ; when decomposed looks like mortar .... i a
3. Several courses of sand and concretional stone ;
@. Sand.........+: BEM Iels aia elelS nis, © 5.0356, 01 0'6.0 is ¢ sealers cp oe 4 49
b. Thin course of concretional cherty stone, nearly continuous.) 9g 4, |
The chert passes into chalcedony, and the spongy portions to I
A CINGEe SHEIIS' ‘srcctelelayeles cles o sicic.c siavole sloletetebeletercvateterernrcicie 0 6 altogether
ec. Sand, with spongy concretional stone, approaching to that of } 4 aaa
Blackdown, but IGoser wee cose eveccnsse eyopdate sie ore oe 5
EU EME )< acis sc crs ow sieges os rehe o/s: ai-n/e\ eit ele clots «00S st mci e Abiko ?
e. A bed of siliceous masses, like the stems of Siphoniz ; about . 0 .6
Batu. cas. be hee ene 4 As ele ED - r |
g. Greenish grey concretional stone, in irregular masses........ 2 J
about 25 feet.
(5.)
4, Greenish grey and yellow sand, including various concretions ;
MIENSAMhs vias oieleen cartes Siete ora colaio aiata c's ele ce u's s about 5 or 6 0 7
b. Very large concretional nodules, consisting of greenish sand, : | woe
Sada COMER EL (oh: 515 ove /alci «sje sim/e.0's:6's «,< 6.0.6 0.0 506-0, and
ce. Sand, without prominent beds of stone; about....... ap ein shee 40 0 50 0
Total ...... from 70 to 80 feet.
Beneath is the plateau of the under-cliff, supporting ponds, and producing
R 2
124 Dr. Firron on the Strata below the Chalk.
rushes ; probably thirty-five to forty feet in thickness, down to the sea :—of.
part of which the section is as follows :—
( b.) By rs
1. Yellow sand; face nearly vertical, from a recent fall.........seeeeee eiereherotorete { ; to 7
2. Dark smoke-grey, crumbling, sandy clay, or cohesive sand, greenish at the about
NXE oo oodosdongp0adoDbdGDDR00DONDD ED DOUDANDAGH solleloleraiateiolelelslelotst= } 8 0
3. A band of firmer green-sand, splitting horizontally into very thin layers, from the
interposition of lighter-coloured sand, which seems to occupy the place of ain |
cylindrical stems or twigs.
In this bed the hammer leaves a mark of a vivid green colour, but the general above
hue is dark greenish grey. It consists of very minute particles of quartz, in- 0. a3
timately mixed with a large proportion of the silicate of iron, soft, and of a
full green colour ; not effervescent, except in minute spots. The gradations from
this compound through all shades of colour and consistence, to brown, and even
yellow, sand, axeumaperceptibler <-jjclelstetekettetefetareisteteletelel= telet=(ole:<olcloy= Bhioo ac J
4. Dark greenish grey sand, apparently continuous with, and passing into, the tena- } about
cious matter of the lower beach..........+es0. Resisleisdeitkeleiars KOCOBEO OO C 6S 6 Oo
Total, about...... 20 feet.
The bottom of this group is concealed by the loose gravel of the beach.
(28.) A striking characteristic of the middle group (0.) is the great diversity
of hue and consistency which it assumes under different circumstances. The
colour when dry is frequently a rusty yellow ;—but in other states, con-
nected perhaps with the different degrees of oxidation of the iron, or with
the decomposition of the pyrites, which it frequently contains, it is of a dark
greenish hue, and passes rapidly from the consistency of loose dry sand to a
tough cohesive mass. In these respects it resembles the middle portion of
the cliffs in the Isle of Wight.
Near the bottom, immediately above the stone of the group (c.), this middle
stratum consists of a dull greenish, sandy, and mud-like substance, appa-
rently a mixture of clay with the green particles, which becomes plastic,
and almost black in water. In these dark sands, near Seabrook, are decom-
posed fragments of petrified coniferous wood*.
(29.) The third group (c.) of the Lower green-sand first rises on the shore
* The Rev. G. E. Smith informs me, from Sir John Tylden, that the high tides in the spring of
1833 having laid bare the strata, the latter had an opportunity of observing the lowest bed, of
what he not unaptly calls the ‘ Blue Division,’ on the shore between Shorn Cliff and the village
of Sandgate. ‘It is,” he says; ‘very marly, and includes a great quantity of wood and pyrites,
‘and in places resembles the gault of Eastware Bay.” The “ very marly” beds may probably be
the equivalent of the Fuller’s earth of Surrey, &c., which has not, that I know of, been distinctly
seen in this part of Kent.
Dr. Firron on the Strata below the Chalk. 125
beneath low-water mark, about midway between Folkstone and Sandgate :
and the projection of the land to the south, immediately on the west of Folk-
stone, and thence to Sandgate, appears to have been produced by the firm-
ness of the barrier which this solid base of the cliff opposes to the sea. It
becomes visible again above high-water mark, about a furlong west of Sand-
gate, is seen in detached places along the shore under that village, and
rising above the beach at Shorn Cliff, beneath which place the Weald clay
makes its appearance, can be traced readily in the heights to the westward,
being opened in several places for stone.
(30.) From Hythe this group of strata forms the escarpment of the cliff,
as far as Aldington Corner, where it turns inland, towards the north-west ;
and thence, along the valley of the Weald clay, a similar barrier of stone
forms the boundary of the green-sand formation. The line of coast, from
Copt Point to near Aldington, not being exactly parallel either to the strzke*,
or to the dip, but oblique, the inclination of the stone beds appears in the
coast section to be less than the truth; and where, as at Lympne, between
Hythe and Aldington, the escarpment becomes parallel to the strike, the
strata appear to be horizontal.
In the progress of this lower ridge to the north-west, from near Aldington
Corner to a hill above Singleton Green on the south of Great Chart, there is
a remarkable interruption of the escarpment, where the line of heights
retreats towards the north; so that the streams which take the opposite
directions,—westward to supply the Medway, and northward to join the
branches of the Stour which pass through Ashford, are there nearly united f.
An obvious explanation of this effect might be, that the concretions of stone
were wanting in this portion of the strata, so that the sands thus unsupported
were more easily carried away.
(31.) The relations of this lowest bed to the remaining groups are very
well displayed in the ground between Seabrook and Saltwood, especially in
the road leading from Dibgate to Sine Farm, and thence to Hythe. On the
* I adopt this term, suggested by Professor Sedgwick, to express the course of the intersection
of strata with the plane of the horizon, in preference to direction, commonly employed ;—the
latter term being ambiguous in its application.
+ In Packe’s “ Map of East Kent” above referred to, this is called “a Grand Inosculation,” and
is thus described: “From this quarry of rag, east of Chart Magna, to the other quarry of the
“same, west of Aldington, the Weald of Kent and the Ashford Vale meet, and are upon very
“gentle ascents towards each other, inosculated by the extremities of the valleys insensibly into
‘one another, the stone hills receding to Ashford, Wilsborough, Sevington and Mersham, the soil
“of both being the same deep clay; and these stone hills are the true philosophical boundaries of
“both these regions.”
126 Dr. Firron on the Strata below the Chalk.
west of Sine Farm the upper stratum is no longer found, the middle and
sloping portion of those hills consisting of the greener beds (b.), with a cap
of the upper sands (a.) on the tep. An outlier of the middle stratum resting
upon the lowest (c.), forms the summit of the ground between Saltwood
Castle and Hythe.
Springs break out both from the top of the Weald clay below this group
of stone, and from the cohesive sandy clay above it; a considerable thick-
ness of the latter being interposed between these stone beds and the sands
which cap Sine Farm and Nail-Down Hills.
(32.) Though in a general view the rise of this and the other members of
the lower green-sand accords with that of the chalk, the dip being at a small
angle to the east of north, the beds of stone which are uncovered at low tides,
upon the shore under Sandgate, dip at an angle of not less than 40° towards
the north-west. This place, therefore, would appear to have been the site of
some disturbance*.
At the west end of the cliff also, between Sandgate and Folkstone, the beds
at the bottom of this lowest group dip inland, or towards the north, at an
angle of about 40° or 45°, and the strike is from about 5° to 8° north of west,
to the south of east, the vertical thickness being less than sixty feet.
Sir J. Tylden mentions, that in a quarry close to the brook at Underhill,
the strata are so highly inclined as to be almost perpendicular ; “ curving,”
he says, “‘something like the flints in the chalk at the Isle of Wight, as if
“they had been forced up.” No traces of such disturbance met my observa-
tion on the coast ; but this fact is deserving of notice, from the distinct proofs
of elevation observable in a part of ‘the series which corresponds to that here
referred to, at Brasted, in West Kent, as will be mentioned hereafter. (38.)
(33.) The lower group seems, generally, to contain more calcareous matter
than the upper divisions ; and this in some specimens is splintery limestone,
almost void of quartz, with but little of the green substance interspersed, in
very minute grains. In such cases small portions might be taken even for
mountain limestone. The concretions are commonly traversed by contempo-
raneous veins of calcareous spar, at right angles to the surface, and inter-
secting each other, one set being parallel to the strzke, and the other nearly
at right angles to it; they divide the mass, therefore, into pieces approaching
* Jt is not improbable that in this and other cases, where extensive subsidence has taken place,
as at Eastware Bay and the back of the Isle of Wight, the occurrence was not confined to the
period during which the sea has stood at its present level. If the level were ever higher than it
is now, this would account for the ruins of the upper beds of the cliffs, which are frequently ob-
servable in the sea, beneath low-water mark.
Dr. Fitton on the Strata below the Chalk. 127
to rhomboids ; and sometimes, as in Septaria, they are thick in the middle of
the beds, thinning off towards the top and bottom.
(34.) Some of the best sections of the group (c.) are to be found in the
quarries about Seabrook*. In one of these the order was thus :—
Feet. In.
1. Very green-sand, alternating with courses formed principally of stem-like or
vermicular branches of whiter sand, and including ferruginous patches. The
petrifactions of this bed are very numerous. Gryphea sinuata in great
abundance.
2. A group of stone beds ; separated by yellowish calcareous sand and clay, called
“Hassock” by the quarry-men. The upper portion especially abounds in
petrifactions. The beds of stone are 18 inches to 2 feet in thickness: they
are concretional, but nearly continuous.
The total thickness visible is about 12 0
(35.) The lower beds are extensively worked in quarries, both for building
and lime-burning, at Pluckley on the north-west, and at Great Chart on the
south-west, of Ashford; and generally along the outcrop west of Aldington
Corner, where the Weald-clay comes very near to the stony strata, a few feet
only of sand rock being interposed. The line of junction is almost every-
where marked by the coming out of springs. The beds are nearly horizontal ;
and though the stone occurs in continuous masses, of sufficient size to answer
well for building, these are evidently concretional. The interior of the blocks
is frequently of a blueish colour, containing throughout minute dark grains :
the exterior crust is brown.
(36.) The following is a list of the fossils which I have obtained or col-
lected from the Lower Green-sand of this neighbourhood; in which, however,
those of the three groups are not always distinguished: the statement of
localities containing all that I find upon this point in my notes.
Fossils of the Lower Green-sanp, in the vicinity of Folkstone.
Ammonites furcatus. Pl. XIV. f. 17. Lowest beds near Hythe. F.
A Monile. Between Sandgate and Folkstone. S. and Min. Conch.
A Nutfieldiensis. Wythe. Also Nutfield, Surrey. Min. Conch.
A Fragments of a very large new species occur in greenish “rag,” at the
bottom of the lowest beds of stone, in the quarries above Hythe. H.
Anomia levigata. Pl. XIV. f. 6. In Kentish rag, near Sandgate. S. and So.
Lympne. H.
* Those near Court-at-Street, which have furnished so many fossils to the collection of Mr. Hills,
I have not examined.
128 Dr. Frrron on the Strata below the Chalk.
Anomia radiata. Pl. XIV. f.5. Near Sandgate. S.
Astacus. (Claws of a small species.) Near the contact of the gault and green-sand. F.
Astarte obovata. Near Hythe. H.
A
Fragments, apparently of three different new species, but too indistinct to
be determined, were found at Lympne. H.; and Sellinge. S.
Astrea. Folkstone. Geol. Soc.
Avicula pectinata. Pl. XIV. f. 3. In siliceous rag, near Risborough. F.
A——. A smooth species, probably new. Upper sand beds, between Sandgate and
Folkstone: in concretional siliceous stone, passing into chert. F.
Belemnites. (Species doubtful.) Indistinct specimens in the quarries at Hythe. F.
Cardium? dissimile. A cast. Quarry near Ivy Cottage, Sandgate. Lowest beds of
lower green-sands. F.
Corystes. (Species doubtful.) Lower green-sand, near Hythe. H. and S.
Cucullwa costellata? Near Seabrook. F.
C. decussata. Quarry near Ivy Cottage, Sandgate. S. Also near Court-at-
Street. H.
C glabra. Quarry near Ivy Cottage. F.
C New species ; indistinct. Ivy Cottage. F. Near Seabrook. S.
Cidaris scutiger, (Goldfuss.) Court-at-Street. H.
Cyathophyllum, (Goldfuss.) Folkstone. Geol. Soc.
Cyprina angulata. (Syn. Venus. Min. Conch.) In soft greenish calcareous sand rock
of the middle group; shore between Folkstone and Sandgate. F. Quarries
above Hythe, and near Lympne. H.
Echinus. (Species uncertain.) Court-at-Street. H.
E arenosus. Pl]. XIII. f.1. Quarry near Hythe.
Exogyra levigata. Court-at-Street. H.; and vicinity of Sandgate, near Seabrook; F.
(Perhaps the full-grown state of Chama conica?) Mr. Sowerby.
Gastrochena ? Near Sandgate. S. Quarries above Hythe. H. In the shell
of an Ostrea; in compact stone, full of dark green particles.
Galerites subuculus, (Goldfuss.) Near Hythe. S.
Gervillia aviculoides. (Perna. M.C.) Court-at-Street. H. Also in the lowest group
of stone, near Sandgate and Seabrook, and in the quarries above Hythe. F.
A new species? Court-at-Street. H.
G
Gryphea sinuata. Near Court-at-Street. H.; and Sandgate. F.; also near Ash-
ford. Min. Conch.
Hamites* gigas. Quarry, west of the Pesthouse, Sandgate. S. Also Lympne. H.
H
H
grandis? From Lympne. H.
Hillsii. Pl. XV. figs. 1. and 2. Quarries near Hythe. H. Court-at-Street,
near Lympne. ‘This species is named from Mr. Hills, whose collection has
thrown great light on the fossils in his neighbourhood.
nodosus. Near Hythe. H.
H
* The character and relations of the Hamites are still so obscure, that the species are here
given with considerable doubt.
Dr. Frrron on the Strata below the Chalk. 129
Tsocardia similis. From Sandgate. F.
Lima semisuleata. PJ. XI. f. 10. (Plagiostoma semisulcatum of Nillson; Petrif.
Suecana. Tab. IX. f.3. p. 25.) In the Kentish rag, near Court-at-Street ; small
specimens. H. Vicinity of Hythe. Miss A. Smith.
Lingula ovalis. Lowest green-sand, near Sandgate. S.
ZL— ? truncata. Pl. XIV. f.15. Near Hythe. S.
Lucina? Near Court-at-Street. H.
Tutraria? Lympne. H.
Madrepora, Goldfuss, (Pocillopora, Lamarck). Folkstone, Geol. Soc.
Modiola aleformis. Near Court-at-Street. H.
M. aspera? From Hythe. F.
M— lineata. Pl. XIV. f.2. Vicinity of Hythe. H. and F.
M.- parallela. Near Maidstone. Min. Conch.
M ? Casts. Near Lympne. H.
Mya plicata. (See Panopea.)
Nautilus elegans. Near Hythe. H. and F.
N— inequalis. Folkstone. Min. Conch.
N. simplex. Very much compressed. Probably from the lower part of the
middle green beds, near Sandgate. F.
plicatus. Near Lympne. H. Some specimens 8 inches high, and 8 in diameter.
The zigzag markings on the outside are very characteristic.
N.
—s)'
: ee
Ne Se/fi
RE AY
ett Wt
Vis
rn}
a ap i cf
4 1
Seas saa li
N— undulatus. Lympne. H.
Nucleolites carinatus. (Goldfuss, Tab. XLIILI. f. 11.) Court-at-Street, H.
Nucula ovata. Near Lympne. H. and F.
Ostrea carinata? Near Court-at-Street. H.
O—— macroptera. Folkstone. F.
O (Species doubtful.) A very thick shell. From the upper sand beds, near
Sandgate. S.
O (Species doubtful.) Shell thin. In the upper beds. S.
Panopea plicata. In the green middle beds, near Ivy Cottage, Sandgate. F. Ina
mass of deep-green colour, near Court-at-Street. H.
Panopea? rotundata. Pl. XIII. f.2. Near Court-at-Street. H.
Pecten obliquus. Near Court-at-Street. H. In firm greenish rag: quarries above
Hythe. H.and F.
VOL. IV.—SECOND SERIES. s
130 Dr. Fitton on the Strata below the Chalk.
Pecten orbicularis. Lowest group of stone beds; near Hythe. F.
P— quinquecostatus. Upper sand, between Sandgate and Folkstone. S. Also in
the lowest group, near Court-at-Street. H.
Pectunculus umbonatus. Middle green beds, Ivy Cottage, Sandgate. F.
Pentacrinus. Stems and branches. Between Sandgate and Folkstone, in calcareous
sandstone. S. Also found in a quarry near Lympne. H.
Perna tetragona. Near Lympne. H.
Pholadomya. A fragment. Near Court-at-Street. H. Perhaps the same with
specimens found near Pulborough by Mr. Martin.
Pholas?? giganteus. Pl. XIV. f.1. Near Court-at-Street, Lympne. H. and G.
P priscus. Sandgate. Middle green beds, behind Lord Darnley’s house. S.
Pinna? crassa. New species. The specimens are large, but indistinct. Court-at-
Street. H. and S.
Plagiostoma elongatum. Lowest beds, near Court-at-Street. H.: and Folkstone.
M.C.
Plicatula pectinoides. Near Court-at-Street. H.
Pollicipes radiatus. Pl. XI. f.6. Near Lympne. H.
Rostellaria. (Species doubtful.) Near Court-at-Street. H.
Serpula antiquata. Near Folkstone. M. C.
S variabilis. Pl. XXI. f. 7. Near Court-at-Street, in hard green Kentish
rag. H.
Siphonia, (Parkinson.) Stems. Upper beds of the lower green-sand; in spongy
siliceous concretions. Valley north of Sandgate. S.
' Spatangus retusus. (Goldfuss, Tab. XLVI. f.2.). Near Sandgate. S. F.
S Three other species, apparently new, but indistinct. Near Court-at-
Street. H.
Sphera corrugata? Casts in the lowest part of the middle said. Quarry near Ivy
Cottage, Sandgate. S. Also near Court-at-Street. H.
Terebratula biplicata. Lowest group of the sands, near Court-at-Street. H.
T: convexa. Pl. XIV.f.12. Near Hythe. H.
T. elegans. Pl. XIV. f.11. Near Lympne. H.
T. elongata. Near Court-at-Street. H.
T: Faba. Pl. XIV. f. 10. Between Folkstone and Sandgate. S.
T. Gibbsiana. Near Sandgate and Folkstone. S.
T——— latissima? Near Hythe, and Court-at-Street. H.
T— oblonga. Near Hythe. F.
T— ovalis. “Middle stratum, between Sandgate and Folkstone; and near Ivy
Cottage, Sandgate, S. and F.: also in the lowest group, Court-at-Street. H.
St ovata. Quarry above Hythe: young and small. S.
T——— prelonga. Pl. XIV. f. 14. Near Ivy Cottage, Sandgate; and shore be-
tween Sandgate and Folkstone. S.
T-——— quadrata. PI. XIV. f.9. Near Hythe. H. and S.
$f—
Sella. Near Court-at-Street. H.: and quarries near Hythe; very nu-
merous, in clusters. F. Also at Chart, Kent. Min. Conch. |
T——— Tamarindus. PI]. XIV.f.8. Near Hythe. S.
Dr. Firron on the Strata below the Chalk. 131
Terebratula. 'Two or three other species, probably new. Near Hythe. S.
Thetis major. Lowest beds of the middle group, near Ivy Cottage, Sandgate. S, and F.
Trigonia aleformis. Near Court-at-Street. H. Ivy Cottage, Sandgate. Middle
beds of the lower green-sand. F. Also near Seabrook. G.
T — clavellata. Seabrook. S. Also about Court-at-Street. H.
T——— elongata. (var. of T. costata. Min. Conch.) An imperfect specimen. Near
Court-at-Street. H.; and Ashford, Kent. Mantell.
T——— nodosa. Near Seabrook. S.
T——— spinosa. (Minch. Conch.) Near Seabrook. S. Also near Pulborough.
Mr. Martin.
T- spinosa var. P}. XIII. f. 3. Shorn Cliff, near Sandgate. G. and F.
T———. New, but indistinct. A cast. Hythe. H. The same with a fossil of
Shanklin, Isle of Wight. So. .
Trochus. Species doubtful. Pl. XIV. f.16: Near Court-at-Street. H. Also Bough-
ton-Mount quarries, near Maidstone. F.
Venus angulata. (See Cyprina.)
V. caperata? (See Cytherea.)
V. ovalis? Lowest beds of the middle group: quarry near the Ivy Cottage,
Sandgate. S.
V——. Cast of a small species. Lowest group of stone: quarries above Hythe. H.
Vermetus polygonalis. Near Court-at-Street. H. Near Sandgate, and Seabrook.
Min. Conch. Also from Bonchurch, and Ventnor Cove, Isle of Wight: but in
the upper green-sand, or in gault. F.
Wood. Coniferous, silicified. Near Folkstone, and Wilsborough. Rolled fragments
are frequent, at the junction of the gault with the top of the sands.
InTERIOR OF KENT.
(37.) I have dwelt the longer on the description of the coast near Folkstone,
on account of the distinctness with which the strata are disclosed there, and
of the geological celebrity of the place; which has the advantage, also, of
being easily accessible to foreigners, from its proximity to France. The
details above given will supersede the necessity of minute description in many
of the following sections.
The strata succeeding the chalk offer but little variety between the coast
and the vicinity of Godstone, in Surrey. The Upper green-sand is throughout
comparatively obscure. The gault, which in general occupies but a small and
narrow valley at the foot of the chalk escarpment, is extensively unveiled at
the entrance of the river gorges, and in those cases its surface is varied by
hills and other inequalities. The Lower green-sand agrees generally, both as
to structure and composition, with that of Folkstone, but the proportion of
calcareous matter decreases from Maidstone towards the west.
82
132 Dr. Firron on the Strata below the Chalk.
(38.) Extensive quarries have long been worked in the lowest part of the
green-sand at Boughton, on the south of Maidstone, the geological relations
of which are the same as at Hythe. The stone for the construction of
Westminster Abbey is said to have been procured there. It is a variety of
Kentish rag, like the Hythe stone, in nearly continuous beds, alternating with
a soft sandrock, called by the workmen “hassock,’”’ and passing occasionally
into chert *.
At the top of these quarries irregular fissures or cavities, approaching to a
conical figure, called “vents” by the workmen, are frequent. These are
filled with loose rubbly stone and sandy clay. In one of them the bones
of hyenas were found, in 1827, by the late Mr. Braddick, of Boughton
Mount, under circumstances like those in which similar remains occur in
fissures in other parts of England. My specimens include several fragments
of the long bones and jaws, with the canine and incisor teeth, some of
which are much worn down by use; and these are accompanied by Album
Grecum +.
Fragments of chalk-flints are found upon the surface near Boughton,
about four miles and a half from the outcrop of the chalk: a fact which de-
serves attention, as such remains of the superior strata have been supposed
either not to occur, or to be extremely rare, within the space between the
North and South Downs.
(39.) The manner in which the rivers make their way to the sea, by an ap-
parently unnatural course, across the ridges both of the chalk and the inferior
strata, is one of the most interesting points in the general structure of
Kent; and has been already dwelt upon by Mr. Conybearet, Mr. Scrope§,
and Mr. Martin |.
(40.) The great variation in width of the space occupied by the strata between
* This better stone is called here “Calkstone” (Kalkstein?). Foreign workmen were often em-
ployed formerly in the British mines and stone works; and in some other instances,—as at the
mines of Lead Hills in Scotland, they have left traces of their native languages in the technical terms.
+ Since these pages have been at the press, the remains of an animal, which Mr. Mantell himself
has ascertained to be distinctly an Iguanodon, hitherto found only in the freshwater beds of the
Wealden, have been discovered by Mr. Brinstead, at Rockhall, near Maidstone, in a stratum of
Kentish rag, abounding in the usual fossils of the Lower green-sand. They confirm the propriety
of referring to the same animal the great bones and the teeth, previously discovered at Tilgate
and other places in Sussex. See Jameson’s Edinb. Journal, July 1834. (Vol. XVII. p. 200.)
A full account of these and other new remains of this extraordinary reptile, will be laid before
the Royal Society by Mr. Mantell.
+ “ Outlines,” &c., pp. xxvii. and 145.
§ “On Volcanos,” p. 213.
|| “ Memoir on Western Sussex,” pp. 12—57.
Dr. Fitton on the Strata below the Chalk. 133
the chalk and the Weald clay is another very prominent feature of this part
of the country ; and though it arises, in part, from the extensive denudation
at the entrance of the gorges where the principal rivers traverse the chalk
ridge, yet even if these were filled up, and the range of the downs between
the coast and Dorking rendered uniform, the space occupied by the lower
strata would be found to vary considerably*. The chief cause of this irregu-
larity is the difference of the angles at which the strata rise in different places ;
the heights also which the sands attain, having a proportionate variation.
(41.) In the upper part of the Lower green-sand between Sevenoaks and
Godstone, a ridge or saddle can be traced for several miles, in a direction
nearly parallel to that of the central range of the Hastings sands, its course
being from about 10° south of west to 10° north of east. The places where
I have seen the structure of this ridge most distinctly, are on a line passing
from Montreal Park, through Sundridge, to the grounds of Brasted Place, in
the course of which several sections have been exposed. The strata consist of
yellowish and somewhat ferruginous sand, and “hassock,”’ including beds of
a bluish stone, like that of the Boughton quarries and the vicinity of Folk-
stone: the fossils, also, are the same.
The ridge just mentioned is probably continued eastward ; but my obser-
vations in that direction did not extend beyond a place called Cold Harbour, im-
mediately on the west of Montreal Park, where the beds rise towards the south,
atan angle of about 20°; the bend, also, or summit of the ridge being there ex-
posed, on the verge of a small wood, but less distinctly than at Brasted Place,
hereafter mentioned. Its continuity, however, is in several places interrupted
by breaks or openings, from 50 to 100 paces in width, where a uniform
surface at a much lower level is continued from north to south, across the
direction ; as if the ridge had been cut away in those places, or wide trans-
verse fissures had been partially filled up and levelled over +. The first of these
breaks is about sixty paces from west to east, and the summits of the heights
* On the coast line the distance from the chalk at Folkstone Hill to the outcrop of the lower
green-sand at Aldington Corner, is about ten miles; but from Lenham to the outcrop is not more
than two. A line parallel to the last, from Boxley, passing through Maidstone, is rather more
than six miles long; but from Wrotham to the outcrop is Jess than four; at Tandridge, on the
east of Godstone, less than one and a half; and at Reigate little more than one mile. On the west
of Reigate the lower green-sand again runs out four miles, to Leith Hill, which is 993 feet above
the sea. These details could not be expressed on the small map annexed to this paper: for
better illustration the reader is referred to Mr. Greenough’s Geological Map of England, and
to the Ordnance Survey.
+ A remarkable break of this description occurs between two portions of wood immediately on
the north of the letter “ y,” of the word “ Dry-hill” in the Ordnance map.
134 Dr Frrton on the Strata below the Chalk.
which it separates are about seventy feet above their base. ‘The strata, which
form the southern slope of the ridge, dip southwards at an angle of about
45°, and the apparent distance (or chord of the curve) from the beginning of
the rise on either side is rather more than a furlong. The wood near
Cold Harbour is full of old quarries, which seem to have been dug into the top
of the saddle.
(42.) A very good view of these elevated strata is disclosed on the east of a
Jane which strikes off from the main road between Bessell’s Green and Sun-
dridge, passing Dry Hill Farm; quarries having been opened there in two
detached points, marked A and B in the subjoined sketch. It is difficult to
estimate the width of the ridge at this place from north to south, its termi-
nations not being distinct, at either extremity, but it seems to be about 1200
paces.
North. South.
isvocecseeccedsseosccsasvorsacisocsassesesslsccsseseres GDOUe UA MACeScenensacscesscscscscssosserpaassssncpsh a= seslees i est taenane >
~
At the more northern of these quarries, A, the beds are distinctly, but
slightly, curved; and the strike is not parallel to the general course of the
ridge, but runs from about 16° east of north to 16° west of south ; forming, with
the direction of the ridge, an angle of about 64°. At the second quarry, B*,
(of which a sketch on a larger scale is given below,) both sides of the saddle
are visible within the distance of a few paces, the beds on the north rising
at an angle of about 60°, while on the south they decline at an angle of
about 45°.
North. 3 South.
In the southern portion of this section, which is about twenty-two paces
in length, and twenty-five feet high, I counted twenty-two beds of concre-
tional stone alternating with sand, and varying in thickness from eighteen
inches to nine.
* This place is immediately on the east of a barn on the road-side, north of Dry Hill Farm,
and about 270 paces distant from A, on a line bearing about 36° west of south.
Dr. Frrron on the Strata below the Chalk. 135
A second break or open space, like those above mentioned, (p. 133.),
occurs immediately on the west of Sundridge Church, which stands on the
northern slope, very near the summit of the ridge ; and a third break, with a
flat of about 100 paces, separates the continuation of that height from
another, occupied by a small wood belonging to Brasted Place, and called
by the inhabitants the “New World”: and here the top of the curve is
visible in several places, from one of which this sketch was taken. The
cracks in the principal bed here
represented, (which is about nine-
inches thick,) are wide and irre-
gular; but the stone has every ;
appearance of having been once
continuous.
The bending of the strata is also very well disclosed in the grounds of
Brasted Place itself, at the opposite side of the lane by which they are
separated from the little wood of the “New World.” The curve is there less
rapid than in the wood ; and the thickest bed of stone, marked A, is traversed
by cracks from a quarter to half an inch in width, the separated portions being
somewhat displaced, as if they had been forced out of continuity. |
North. : 2 nai, 58 te South.
(43.) A continuation of the ridge above described may be traced westward
from Brasted Place, for about four miles; and on the roadside ascending to
the Chart near Moorhouse, about midway between Westerham and Lympsfield,
beds are exposed, which dip rapidly to the north ; obviously forming a por-
tion of a saddle, like that of Dry Hill, and, to all appearance, a prolongation
of it.*
From what I have seen in other parts of this country, I have little doubt
that many of the ridges within the tract occupied by the lower green-sand
may be ascribed to similar disturbances of the strata. A slight indication of
something of this kind near Folkstone has been already referred to (32.). On
the Ordnance map a prominent range is represented as running nearly
north-west and south-east, from the village of Seal, through Seal Chart, to the
* Marks of disturbance along a line of direction different from that described in the text, are
observable also about half a mile south of Dry Hill, near the Manor Farm House; where the beds
on one side of the ravine dip towards a point about 20° south of east, while on the opposite side
they are inclined to the west of north.
136 Dr. Firton on the Strata below the Chalk.
heights above Stone Street on the south of Ightham Common. This, if not
very much exaggerated, is probably a derangement like those just mentioned.
The greater ridge of the Hog’s-back itself, on the west of Guildford in
Surrey, of which the direction is nearly continuous with that of the ridge at
Brasted, may be also connected with it; since the line of the Hog’s-back,
if prolonged eastward, would pass through the high range of sand _ hills
between Shalford and Martha’s Chapel, and thence almost directly through
Park Hill, Cockham Hill, and Tilburstow Hill, which last-mentioned place
is the seat of a similar disturbance. The distance from Tilburstow to
the inclined strata at Moorhouse, is not much more than four miles, and
the whole course of this elevated line is almost uniformly from east to
west; the line from Moorhouse to Montreal, through Sundridge, deviating
from that direction only:a few degrees te the north. Mr. Martin has
described similar cases of much greater prominence and interest in Western
Sussex *.
(44.) The abrupt rise of the beds in many of these ridges, and the speedy
return of the ground to its general inclination, imply the action of a force
which, if direct, must have been very near the surface, and too much circum-
scribed to be reconcilable either with the effect of gaseous expansion or the
impulse of mineral matter in a state of fluidity. The space between the north
and south chalk downs seems, in fact, to have been elevated, not by the mere
protrusion of one central ridge, but to have been broken up in several different
places, so that large portions were thrust outwards, or bent into ridges, by a
lateral push, as when a cloth is wrinkled on a table; a mode of accounting
for the formation of such inequalities of the surface, which seems more
probable than the action of any direct violence from beneath F.
* Memoir ec. Ps) 01 et seq.
+ There is indeed another hypothesis, which would account for the ‘formation of promi-
nences of small extent, by forces originating at very great depths. If we suppose a series of
strata, comparatively soft and flexible, to be deposited over a tract composed of older rocks, with
hills and ridges on its surface, and the whole to be then thrust outwards by a force beneath,
the protuberances of the lower mass would compress and bend the strata above them into forms
corresponding with their own;—just as in bound books the little inequalities of the cover, or
any of the leaves, are impressed on the adjacent pages, and sometimes propagated through a large
part of the volume. Nor is this case wholly imaginary. The masses of granite which are found, in
many instances, to project above the disturbed strata adjacent to them, must have been elevated
after they had cooled,—when their comparative solidity must have been very great :—and among the
newer formations, the interval of time between the deposition of many of the groups, now in im-
mediate contact, (as of the red mar! and the oolites, near Bath,—the mountain limestone and green-
sands in the Lower Boulonnois,) must have been more than sufficient both for the condensation
of the lower strata, and their subsequent erosion into prominences and valleys, even if the original
surface had been uniform.
Dr. Firron on the Strata below the Chalk. 137
SURREY.
(45.) Godstone.—The upper green-sand assumes a new character near
Godstone ; and a step-like projection at the foot of the chalk appears there
more distinctly than in the country to the east. As the productions of
the little district between Godstone and Reigate are valuable in commerce,
and its structure has been a subject of some doubt, I have given a separate
map of it, in Plate VII. fig. 2.* The section, Plate X.a., No. 2., on the
line from the chalk through Godstone, shows the position of the firestone
beds in the upper green-sand; with the site of a remarkable elevation of
the strata at Tilburstow Hill, an account of which has been already published
by Mr. Mantell+: and No. 3., the section through Merstham, includes the
site of the Fuller’s-earth pits of Nutfield.
(46.) The firestone subordinate to the upper green-sand, in this part of
the country, was, in 1827, extracted only between Godstone and the west of
Reigate. The principal pits were situated on the west of the London road
to the former place. ‘The stone was obtained by an adit between five and
six feet in height, and the succession of the beds affording it was thus:
Section of one of the Firestone Pits near Godstone.
Feet. In.
- “Hard roof.” This, like the firestone beneath, is a uniform fine-grained con-
glomerate or sandstone, effervescing strongly with acids, and easily cut into
any desired form, Throughout the stone are dispersed numerous minute
scales of mica, and dark particles, scarcely perceptible without a lens.
forms a roof to the mines, of such firmness as to support itself to a width 2
17 feet, extending indefinitely inwards.
23
but harder and somewhat finer in grain, easily broken down into sand, effer- ‘fa
vescing. The beds 2. 3. and 4. though separated by seams of stratifica-
4, tion, are of nearly uniform character. 0 10
“Green bed” of the workmen. (Firestone.) Stone of the same nature as the last, i 8
5. A bed of bluish grey siliceous concretions, called ‘‘flints” by the workmen, pass- }
ing into stone like that above mentioned. Fracture flat-conchoidal. Yielding
with great difficulty to the knife; but effervescing slightly. The greyer stone
near these concretions is much harder than elsewhere. The siliceous
matter as it becomes more pure acquires greater hardness, with a splintery
fracture and a glimmering lustre; and the micaceous particles, which are
numerous in the softer varieties, are then scarcely apparent. J]
6. “Green bed ;”—like 2. 3. and 4.¢ .......00ceeace Bahr clalaat enenesssareseretetfevose 0 10
* In the small maps of this Plate the inequalities of the surface are not expressed: but the
oon can easily be transferred to the Ordnance map. Tt “Fossils of Tilgate,” &c., p. 22.
{ The more uniform and softer rock of these pits is used, principally, for ieaip fire-places
VOL. IV.—SECOND SERIES. x
South.
138 Dr. Firton on the Strata below the Chalk.
7. Bottom of the quarry. Stone unfit for working, from its containing much flinty
matter.
All these strata dip at a very small angle to about 20° west of south. The rock is traversed
by fissures, which divide it into somewhat rhomboidal masses; and smaller cracks are
sometimes found within the blocks of stone.
(47.) The gault hereabouts occupies a tract which bears the name of “ Black-
land,” and forms a slight depression below the band which affords the firestone.
(48.) The lower green-sand has distinct indications of a subdivision into
three, like that of the vicinity of Folkstone (16.)._ On the line of section,
No. 2. Plates VII. and X. ponds are frequent, in a situation corresponding
to that of the greener middle group (24.); the surface being comparatively
low, with vegetation of a somewhat different character. The stony beds of
the lowest group then rise to form the escarpment of Tilburstow Hill*, which
is nearly on a level with the chalk downs; and at the highest point, there is
decisive evidence either of a sinking towards the chalk, or of elevation in an
opposite direction ; for at the top of the hill, the beds, which on the north of
that place rise uniformly at an angle of not more than 10°, are suddenly
thrown up to about 45°. The appearance of the section here is represented
in the sketch subjoined :
WU \ KK
‘.
> Neer
oe
and furnaces, but is employed also for buildings under water. Great care is necessary, in build-
ing, to place the blocks so that the planes of stratification shall be horizontal. The equivalent of
these beds in the upper green-sand of the continent, (the Pliner kalkstein of the Germans,) is
employed for exactly the same purposes, at Aix-la-Chapelle and other places.
* This is the spelling of the Ordnance map: the word in the country is pronounced ‘* Tilbuster.”
Dr. Fitton on the Strata below the Chalk.
139
Inclined Strata, near the bottom of the Lower Green-sand, Tilburstow Hill.
Soil and loam (marked a a in the cut).
1, Soft nearly uniform sand; when dry of a bright buff colour .........-++.+++
rae)
This has the appearance of having slid or subsided upon the next bed below.
Immediately above 2. the sand is green.
Fuller’s-earth; very like that in the upper part of the pits at Nutfield, hereafter ]
mentioned, and also like that which occurs in the lower green-sand at Brill in
Buckinghamshire. This clay becomes soft and is diffused in water, but does
not break down with the rapidity of common Fuller’s-earth. The bed varies in
thickness from 6 inches to 12: the masses of which it is composed have
smooth surfaces and a saponaceous feel, with the aspect and lustre of bee’s
wax, probably produced by compression and motion on each other ........
A bed consisting of chert and soft sandrock (“ Hassock”), intimately mixed,
Feet. In,
about
Gand
3
and passing into each other; about Oe AC
This and the beds 4. 5. and 6. end abruptly above, as represented in the
sketch.
4, A course composed of almost continuous bands of brownish grey chert, from 3
or
on
10.
is like that on the northern surface of the hill, where it is much used for re-
pairing the roads. By exposure it becomes divisible into slaty portions, ap-
proaching to.a rhomboidal figure... .......ccccecccccssccccsevesvvctes
to 6 inches thick, alternating with, and passing into, soft sandrock. This ef
. Soft sandrock (“ Hassock”), including green particles: the hue is various where ie
exposed. In some places tinged with oxide of iron .......cceeseeceeees
. Sand; green while it is moist, but when dry and exposed nearly white, containing }
layers which consist of stem-like or vermicular portions of white, translucent,
quartzose sand, surrounded by sand of a green colour. This contrast of |
colour becomes indistinct in dry specimens, but is very conspicuous when
they are moistened. The white vermicular portions have a border of darker
green than the rest: they are generally about 3th of an inch in diameter,
somewhat curved, and in some cases have short lateral branches with round
extremities. This remarkable structure is very characteristic of several parts
of the lower green-sand, and is probably connected with the former presence
mere AHI Ze DOGIEG, 2 <e ateleiplello| sie sis.eft v0 arse 0 0 isisicloie @aidaiowie
. Here ferruginous matter is more abundant, and the sand is concreted irregularly
into nodular masses nearly continuous. 7 and 8 together are about 15 feet thick
. Ferruginous bands, like 8: a conglomerate of quartz grains, cemented by oxide
of iron, with adhering sand, which in some places is white, and looks like
MONCALeM DUG COSMO EMERVESCE™ Haarere steals nicis esis cie.eleie e/e\s/0)ei'e/s\s:0)/6 oje'sl «iste
Sand, with dark particles, and irregular tortuous seams of a ferruginous com-
pound, like the carstone of Norfolk, consisting of fine rounded grains of
quartz, cemented by hard, dark reddish brown, oxide of iron. This passes
at the bottom into a less ferruginous sand, which is apparently continued down
to the Weald clay. 9 and 10 together are about 15 feet thick. ..........
pe
varying
ri E
. Coarse yellowish —— a
15
Total thickness....about 60 feet.
140 Dr. Frrton on the Strata below the Chalk.
(49.) Merstham.—The aspect of the amphitheatre formed by the outcrop
of the chalk and upper green-sand around this village is very characteristic :
a prominent ridge of the latter stratum, passing from Blackditches to the
south of Gatton, in a nearly circular curve, above which the chalk downs rise,
with a similar curvature (see Plates VII. fig. 2., and X.a. No. 3.). Merst-
ham occupies nearly the middle of the line which has been worked upon for
firestone ; the extreme points to which the quarries have extended of late years
being near Godstone on the east, and Buckland Green on the west. The
village stands on the confines of the upper green-sand and the gault*, a
little to the south of an opening or gorge in the chalk, through which runs
one of the principal roads from London to Brighton. The beds dip at a
very small angle, towards the north; and those which include the firestone
are visible to a thickness of about thirty feet, projecting like a step beyond
the foot of the chalk escarpment. The works had been discontinued for some
time before I visited the place ; but the following list of the strata was given
to me by the person who had superintended them +.
List of Beds at Merstham, Surrey.
[Lower beds of the Chalk. |
NACHO Karey lovelelsiaotsres psi eiaio(s tele! © oohelsicl Saud oyohetaleleierain iu airoleh«.0 eters
2: “eLimestone.. (Grey marly) chalk: jabowtiei1stocy-\hei-see stall emote 150 0
3. “ Burry chalk: the ‘‘Craie Tufau” of the French. This will not burn i us 0
toilime, but, goes to;dustsin the Juilngs tye sayin vic) oni + oynhs'ectnye oie 60 0
[Upper Green-sand. |
4. “ Quarry stone ;” (Firestone) subdivided thus:
a. ‘* Roof,” (sand 2 feet, soft stone 2 feet)? Total, about ........ 4 07
This stratum is of great firmness and stability: the roof sup-
porting itself perfectly in the drifts worked into the hill, which are nae
30 feet wide. 25 0
b. “ Firestone;” including “‘flints” (chert), about 2 feet from the top: about 5 6
c. “ Good hard building-stone.” ...... sialv stele derek # Cidisidte aiproneteets 20g
dig Burry stone's? about 66.0 66s siceis 060 ss 0 4.0 5 vb vl tntereenene 16 oJ
[ Gault. |
5. “Marl.” Gault: the apparent thickness of which, in this part of the
COUNtLYs agrees WIth that OM the COASE... sc c.s)+e cits wintecleisretela ice about 150 0
All the beds become thinner towards the outcrop.
* A well at the Feathers-Inn is 150 feet in depth, with a boring of 60 feet at the bottom (in the
whole 210 feet), all in “clay” and “marl.” The boring, 23 inches in diameter, after going down to
60 feet, brought up such a quantity of water, that the well-sinker was drawn up in great haste,
and the water rose to within 40 or 50 feet of the surface. Much sand, which had come up through
the bore, was afterwards found in the bottom of the well.
+ Amore full account of the Firestone pits here, has been published by Mr. Webster, Geol.
Trans., First Series, vol. v. p. 355.
Dr. Firron on the Strata below the Chalk. 141
(50.) The rise of the Lower green-sand is here very well defined; and
the soil over the upper ferruginous beds of the formation is called “hazel-
mould,” in distinction from the “black-land’’ upon the gault. Immediately
on the south of the ridge formed by this first member of the sands, a slight
valley or depression, with a moist and more fertile surface, is occupied by
cohesive sand ofa dark greenish hue and softer texture, which corresponds to
the middle group of Folkstone, above described, (16.) and (24.). The re-
tentive quality of this latter stratum, which gives a somewhat marshy cha-
racter to the tract in which it occurs, and the approach of its hue and texture
to those of clay, have deceived even experienced geologists, and given rise to
some mistakes respecting the lower strata of this neighbourhood. The sec-
tion No. 3, I believe, expresses their true order and relations.
(51.) Fuller’s-earth has been dug in this part of Surrey, beyond the memory
of the oldest inhabitant. At present the extraction is confined to the neigh-
bourhood of Nutfield. The beds come up near the top of the lowest
member of the green-sand, and occupy a line on the north side of a
ridge, which extends from the east of Nutfield nearly to Redstone Hill,
on the west of Copyhold Farm. About two miles west of Nutfield, nearly
upon the ridge, was a pit, by which the earth was extracted from a stratum
six to seven feet thick; and at Colmonger’s Farm another, of which the
section was thus:
Fuller’s-Earth Pit, near Nutfield.
Feet. In.
1. Greenish sand, occupying irregular cavities on the top of the clay, 2.......... aed
2. Very tough clay (impure Fuller’s-earth) with the aspect of steatite. [See ul)
INo-\2..0f the Secfion at) Tilburstow Hill, p. 139.) ......0.60ccccvecccces
3. Sandrock, abounding in green particles; about ........sesseeeeccereccees 4 0
4. A range of sandy nodules, of firmer consistence than 3. «2... see ee ee eeee 1 0
a. fnin’courses ‘of bad Fuller’s-earth. 225.6. ecw ess nec ces csccnscescecsecn { abe .
6. Continuous sandstone, forming the roof of the “earth-pits,” and sustaining itself } 5 ue,
without support to a width of 11 yards......cssscecesceccecceseccass
emer INE OUI CLAN ah ato! lolafetretmet ail cta/etcrs stele vx «5.6 cee 210-6 0) > Facial’ 6's ele'sa o'e\s'e! o's a -
Seehullers-carthwon an uniorm) bluish! colour ™. 02.1.1. 0 .elee sees os ccees oe oe 7
In this stratum, about 3 or 4 feet from the top, detached nodules are found, |
(from six inches to nine in diameter,) of sulphate of barytes, crystallized in > 16 0
oblique four-sided prisms, truncated at the edges and bevelled at the extre-
mities, semi-transparent, and of a wine-yellow colour...........+++ee00
9. White sand.
The thickness of sand beneath,—between this stratum and the Weald clay, I did not ascertain.
The dip of the strata above detailed is about one in fifteen: (the angle, therefore, between 5°
and 4°,) towards a point about 40° west of north.
* This was sold at the pits (September 1828) at 5s. per ton. The yellowish earth of another
142 Dr. Firton on the Strata below the Chalk.
(52.) Reigate-—The map and sections, Plate VII. fig. 2. and X a., Nos. 2.
and 3., sufficiently indicate the general relations of the beds here, which have
been already the subject of a paper in the Geological Transactions by Mr.
Webster* ; where a sketch is given of the history of the remarkable ancient
quarries at this place. The firestone forms a terrace beyond the chalk, nearly
level with the top of the remotest sand-ridge ; and the gault runs out from
the base of the terrace, at first horizontally, and then rises towards the
tunnel, by which the road is conducted through the first ridge of the Lower
green-sand{+, here composed of cream-coloured and yellowish sandrock.
From the town of Reigate the strata rise again towards Cockham Hill: so
that there are here two ridges ; first, that through which the tunnel is cut, and
secondly, the southern ridge, formed of the lowest sand beds,—with what ap-
pears to be the middle, greener sand between. At Earlswood Common, about
a mile to the east of the outcrop, the clay of the Wealds is found. The sud-
den fall from the chalk to the valley of Reigate and the abrupt rise thence
to the outermost ridge of Red Hill, &c., is exceedingly striking. At Reigate
Heath, on the west of the town, the vale which seems to be occupied by
the middle sands is rushy and moist, bearing pools upon its surface: but the
fall of the ground still farther west, where the continuation of the outer ridge
of sands might be expected, is also a remarkable feature.
(53.) In proceeding westward, the rise of the sands at Buckland is like-
wise very rapid. ‘Thence to Holmwood Common, on the south-west, no ob-
servations have been made, but the boundary between the green-sands and
the Weald is less obviously marked ; and there is a strong contrast between
this space and the prominent ridges of Leith Hill; the lower tract, it will be
observed, being that in which the streams converge to join the Mole before
its passage through the gorge at Dorking. .
(54.) It will be seen, even from the map (Plate IX.), that the outcrop of
the Lower green-sand, from Reigate to the head of the valley of the Wealds,
is not continuous ; two, if not three, distinct tracts of this formation, bounded
pit was more in request; the price, however, the same. It is necessary for the purposes of the
woollen manufacturer, that the Fuller’s-earth should be free from any admixture of ochre or sand,
which are found to cut the cloth.
* First Series, vol. v. p. 353, &c.
+ The relations of a stratum of dark greenish sandy clay, about seven feet thick, immediately
above the tunnel at Reigate, are at first sight doubtful. It might be taken for an advanced portion
of the gault; but is, more probably, a subordinate bed within the first division of the Lower
green-sand ;—a detached portion, as it were, of the middle greener beds, which it resembles in
mineral character. A similar bed occurs, in a corresponding situation at Pulborough, which Mr.
Martin, with whom I examined it, has since ascertained to belong to the place here mentioned.
Dr. Fitton on the Strata below the Chalk. 143
on the south by almost rectilinear escarpments, projecting successively be-
yond the narrow and comparatively regular line of the previous outcrop,
on the east*. The breaks between these steps coincide with the gorges of
the Mole and the Wey; a fact in favour of the hypothesis which ascribes the
formation of these gorges to transverse fissures. 1.—The first of these tracts
of sand lies between Leith Hill and the opening cut across the sands towards
Guildford, by the south-eastern branch of the Weyt, in which the Surrey
and Sussex canal has been dug. Its southern verge extends from Leith Hill,
through Holdenbury Hill, to Bearland and Stroud-Green, with a mean
breadth from the chalk of about 31 miles. 2.—The next step projects about
3 miles further south, with an average breadth of about 6 miles; and its
escarpment is nearly parallel to the Hog’s-back throughout the greater part
of its length, from the Telegraph Hill, south of Hascombe, to Emily Farm,
a little east of the centre ofa line from Hindhead to Thursley. The anticlinal
line, hereafter mentioned, along the top of Grayshot Down, may perhaps be
the continuation of a ridge, or saddle, of which the beds rising towards
Hascombe are the remaining northern portion, the southern slope having
been carried away by denudation}. 3.—The sands on the north of the valley
between Ludgershall and Harting-combe, may possibly be considered as a
third step in these parallel outcrops, though much less regular than the two
just mentioned: the lofty summit of Blackdown, at its eastern extremity,
is standing out like a promontory, about two miles beyond the other parts of
the escarpment on the south of Hindhead. It is impossible not to connect
these appearances with the general action of the force by which the whole of
this country has been upheaved; all the features coinciding with the hypo-
thesis of its elevation on a line or lines parallel to the axis of the forest
ridge.
(55.) Dorking to Leith Hill, &c.—The tract between Leith Hill and
Guildford affords nothing particularly deserving of notice, except the great
height (993 feet) to which the outcrop of the lower green-sand rises, at the
point on which the tower is placed. The space included between the escarp-
* To understand the structure of this country, the reader ought to have before him a map on a
much larger scale than that in Plate IX., as Mr. Greenough’s Map of England ;—or the eighth
sheet of the Ordnance Survey,—which, however, is by no means equal, in correct representation
of the surface, to the more recent portions of that work.
‘} This stream has no name in the Ordnance map.
{ Another anticlinal line, but in a direction oblique to that here mentioned, is indicated by the
line of heights which runs from Milford, through Godalming, and thence by Unsted and Sum-
mersbury to Western Street, near Albury; the strata on the south-east of this line, near Godal-
ming, dipping at a’small angle to the south-east, obliquely from the range of the Chalk Downs.
144 Dr. Firton on the Strata below the Chalk.
ment and the downs from Dorking to Guildford is of nearly uniform character :
but in approaching the latter place, the Lower green-sand rises with such
rapidity, that Martha’s Chapel equals or out-tops the chalk, though less
than a mile distant from it horizontally. Slighter indications, also, of dis-
turbance are evident throughout this tract. ‘The lower marly chalk at
Deerleap above Wotton is divided by smooth surfaces, produced by the
sliding of large masses upon each other: and where the road rises from the
mill towards Abinger Church, at a point which corresponds with a con-
tinuation of the ridge above mentioned, near Brastead and Sundridge, the
beds are curved, so as clearly to indicate derangement.
(56.) The road west of Dorking, between Westgate Heath and the Rookery,
is cut through the first beds of the Lower green-sand, the top of which is
eroded into irregular cavities, resembling those which are found, through_
out the south-east of England, on the surface of the chalk; and, like them,
filled with reddish loam and fragments of chalk flints. This being one of
many indications, on the margin of the great Wealden valley, that the agents,
whatever they were, by which the chalk was excavated, acted in tlie same
manner on the beds beneath it, and filled up the cavities with similar mate-
rials, at least as far down as the Lower green-sand.
Wave c eres Surface.
a ...-dteddish Loam and Gravel.
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ie
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Bye avalareatave Loner Green-sand.
The lower strata of the quarries near Cold Harbour, immediately under
the tower at Leith Hill, are almost identical with those of Tilburstow,
(p. 139); consisting of very green sand and soft sandrock, which alternate
with chert, and include green matter, with white, vermicular or stem-like
bodies, as at that place.
(57.) Guildford, Godalming, Farnham, Hindhead.—The tract on the south
and west of Guildford, and thence to Hindhead, forms one of the most ex-
tensive surfaces of the Lower green-sand to be found in England; and the
section from the heights on the north-west of Farnham to the Weald, (Plate
X a., No. 4.) includes a succession of strata, from the Bagshot sands, one of
the highest members of the English series, down to the Weald clay.
Dr. Fitton on the Strata below the Chalk. 145
The quarries on the roadside between Guildford and Shalford, disclose a
good section of the chalk, with numerous flints, dipping at an angle of about
5° or 6°, a little to the west of north; and on the opposite side of the Wey,
beneath St. Catherine’s Hill, the relative position of the lower strata is very
well displayed.
(58.) The Hog’s-back.—The remarkable ridge called the “ Hog’s-back,”
which runs from Guildford to a point about two miles from Farnham, has
been produced evidently by an upthrow of the chalk, and the breaking
off of the southern portion of the curve. The inclined position of the
remaining side of the flexure is very well seen at the western extremity of a
large chalk-pit between Guildford and Puttenham, where the strata dip
towards the north, at an angle of about 30°. The upper beds are very
white, with courses of the usual dark flint nodules; and a remarkable
feature in this quarry, is the distinctness with which the chalk is divided
into masses approaching to a rhomboidal figure, by seams oblique to the
stratification ; the angles of the portions thus bounded, standing out in
the face of the cliff, like splinters in the shattered fracture of a crystal.
The Upper green-sand forms a slight projection along the foot of the Hog’s-back ; the Gault,
a corresponding narrow depression along its whole length; and the Lower green-sand rises so
rapidly beneath, that one or many inflections are necessary to account for its wide extent to the
south. In approaching Farnham, the gault, near its contact with the sands, abounds in nodules
containing a large proportion of phosphate of lime; resembling those of the vicinity of Folk-
stone (13.). The upper beds of the Lower green-sand rise, like the chalk, at a very high angle,
and must have been bent suddenly in an opposite direction, since they are now continued, with a
moderate inclination, several miles to the south, Along the north of Puttenham Common, the
sand is reddish, and very like that of Red-cliff at Sandown Bay, in the Isle of Wight. A nearly
continuous surface of the sands extends towards the south from Compton to Hurtmore, and
North Brook Place, and is resumed on the south of the river, through Westbrook and Upper
Eashing. It is again cut through by the stream, which the London road accompanies, on the
south-west of Godalming ; but recurs, in the heights south-east of the town, from Holloway-hill
and Crown Pit to Munstead Heath, which seems to be nearly on a level with the top of the
Hog’s-back. On the west, the upper beds of sand form several prominences, among which
Crooksbury-hill is the most conspicuous ; their elevation having probably been the effect of pro-
trusion. On the south-west of Crooksbury, the upper sands seem to expand, and to occupy a
still wider horizontal space in that part of the denudation which corresponds to the less inclined
beds about Farnham.
(59.) The general thickness of Lower green-sand here seems to be nearly
the same with that of the coast, and may be taken as between 350 and 400:
feet; though, from its superficial extent, a much greater thickness might
be ascribed to it, if the disturbance and inflexion which it has undergone
were not kept in view. ‘There can be no doubt, both from the features of the
VOL. IV.—SECOND SERIES. U
146 Dr. Firron on the Strata below the Chalk.
surface, and the hue and texture of the strata, that the subdivision into three,
which is conspicuous near Folkstone, and not much less distinct in Western
Sussex, exists also in this tract. But the precise boundaries of these groups
are by no means obvious, for there are not hereabouts those characteristic
beds of stone, which are found near the coast; their place being supplied,
in the uppermost group, by concretions of a coarse conglomerate, which
in the country bears the name of “ Bargate Sione*;” and, in the lowest
group, by chert and indurated sandrock, like those of Leith and Tilburstow
hills. This comparative scarcity of calcareous matter is one of the principal
differences between the eastern and western tracts of this formation.
The more ferruginous concretions, (the “ carstone” of Norfolk,) which are very abundant in the
upper part of the Lower green-sand of this neighbourhood, are often so compact as to ring under
the hammer, and are thence called “ clinkers” by the quarrymen; sometimes forming plates or
flakes, a quarter of an inch and upwards in thickness, and curved so as to resemble portions of
concentric layers of petrified trees. This stone furnishes an excellent material for the roads, and
gives a remarkable reddish hue to some of those which are macadamised in this country. Frag-
ments of brown hematite also, like those of the Red-cliff near Culver in the Isle of Wight, are
found at many places in this vicinity; as at Thursley, &c.
(60.) Godalmng.— The heights about Godalming afford excellent sections,
which may with some probability be assigned to the lowest part of the
Green-sand formation. The order in general was thus :—
Holloway-Hill, Godalming.
Feet. In.
1. Green and variegated sand, abounding in large concretions of chert, and of cal-
careous conglomerate, (‘“‘ Bargate-stone ;”) which is hard and sparry, and in
some places passes into chert. It contains traces of shells and of alcyonic a
stems. False stratification is here remarkable; the concretions also following
theiobliqueronmalseslinests: 283 .kietok ochre ote stat oy. oe tie eee eee eres gj
Some of thelarger masses of this rock are precisely like the concretions
on the shore near Folkstone (20.);—a very compact sparry variety of
‘** Kentish-rag.” In the upper sands of Polstead, near Puttenham, irregular
concretions of this compound occur, imbedded in soft sandrock, and contain-
ing carbonate of lime in rhombs.
2. Sand, of the same kind, without concretions; but including thin beds of a tough] about
clay, like pBallleris-earthnte tric eet Licks vie oslo ciel eve ole sieeve elt ee } 25 0
The dip here is towards the south of east, and all the summits are flat and
uniform.
* The origin of this term is somewhat doubtful. A place called “‘ Burgh-gate,” from whence
it may have been derived, occurs in the Ordnance Map, on the south of the escarpment be-
tween Hambleton and Hascombe.
+ The Fuller’s-earth would refer these strata to the lowest division of the sands. Thin
beds of that mineral, however, are found throughout this formation.
Dr. Frrron on the Strata below the Chalk. 147
Among the looser sandy materials of Holloway-hill are spongy concretions, which show, when
moist, the same vermicular structure as at Tilburstow-hill. ‘
Blackheath, south-east of Guildford, seems to have been once a continuation of the sands near
Godalming. Its top is nearly level with the chalk range, but lower than Martha’s Chapel hill.
On the south, the ground descends to Farley Heath, with a sort of escarpment like that of Crooks-
bury and Farnham commons, hereafter mentioned; and the road thence by Farley-green to
Hound-house is in a richer sand, supporting pools in several places, and probably belonging to the
middle group.
Crooksbury Common seems to consist of the upper members of the formation, impending, like
an outcrop 150 to 200 feet thick, over the valley of the Wey, between Elstead and Tilford; and
on the south of the stream the heights of sand are renewed. Farnham Common is analogous to
that of Crooksbury, and apparently a continuation of the same plateau, deeply cut through by one
of the principal streams of the Wey. On the south of these, is the lower tract of Frensham and
Thursley commons, and thence the ground rises rapidly towards Hindhead, the ascent consisting
of sand deeply trenched into channels. A conspicuous group of barren, somewhat conical hills,
on the south of Frensham Common, called the “ Devil’s Jumps,” is apparently the remaining por-
tion of a stratum of sand reduced by abrasion to the present irregular form; and the pebbles and
rolled masses on Thursley Common, immediately on the north of Hindhead, are sandrock, passing
into chert, which seems to be unmixed with other matter, and to be the debris of the beds now
removed.
(61.) Hindhead.—The crest of Hindhead is on the north-east of a de-
pression called the “Devil’s Punchbowl,” round which the road is conducted.
The highest part of the curve, or anticlinal bending, of the Lower green-
sand, seems to be just at a point where the new road, on a lower level than
the old, has exposed a face of 10 to 25 feet in height. The flexure is
very slight, but sufficiently perceptible, occurring in such a place, to be de-
serving of notice. The strata consist of soft sandrock, containing con-
cretions, and nearly continuous beds of chert, passing into chalcedony, of
various shades of yellow and brown ; with occasional layers of bright yellowish
sand, in which the lines of false stratification are conspicuous. All over Gray-
shot Down the subsoil is a soft, loose sand of the same description.
(62.) The whole of the tract here occupied by the sands, though not
unpicturesque, is wild and barren in its aspect, destitute of wood, producing
only ferns, heath, and furze. The surface is in fact, to this hour, nearly
such as it may be conceived to have been when first uncovered by the
departure of the sea; and its structure is just what may be imagined to
result from the levelling effect of water under the influence of motion
of no great violence. In crossing this desolate region by the main road
from London to Portsmouth, it is difficult to believe that we are only forty
miles distant from the capital, and midway to one of the chief naval
establishments of the empire: but the nature of the soil effectually prevents
improvement, and it is not improbable that this tract may remain for centuries
U2
148 Dr. Firron on the Strata below the Chalk.
unchanged, and still exemplify the power of geological causes in modifying
the civil condition of countries, as well as their external features.
In the bottom of the “ Punch Bowl,” perhaps 200 feet beneath the road, a small stream arises,
and the north flank of the highest ridge of Hindhead, which runs nearly west from the summit, is
furrowed by nine or ten similar and nearly parallel trenches: the deepest of these is called Hack-
ham Bottom, the stream from which is continued along the verge of Thursley Common to the
Wey at Elstead. The ridge represented in the section No. 4. is that of Grayshot Down, as it
appears from the lower ground on the north. It declines westward to Harem, and also to the
south; so that there is here distinctly an anticlinal line, more than three miles north of the
central valley of the Weald between Ludgershall and Harting-combe.
(63.) Although Hindhead is the most prominent point in this part of the
country, it is not, strictly speaking, the escarpment of the Lower green-sand ;
for the strata, which rise very gradually on the west of the denudation, run out
to the east beyond the highest summit, and caps of sand are preserved on some
of the advanced ridges and in several detached points. For the same reason,
Blackdown Hill, about four miles south of Hindhead, is no more than a
massive cap of sand, resting with a very slight inclination upon the Weald
clay : and all the deep ravines which separate the heights and ridges on the
west and north-west of Blackdown, towards Lynchmere and Haslemere,
have sand only at top; the clay rising here to not much less than six hun-
dred feet above the sea. Blackdown forms the north-eastern promontory
of what may be called the central valley of the denudation; the opposite and
converging side of which is a similar escarpment of the Lower green-sand,
extending from Harting-combe to Bexley-hill. The floor of the narrow
intermediate space consists of the Weald clay, which, close to the junction,
abounds in Cypris Faba; and where the valley opens into the wider expanse
of the Wealds, the first range of the Wealden sand and sandrock, described
by Mr. Martin, about 25 feet thick, and at a vertical distance of about 200
feet from the top of the clay, forms a sort of bar, or elevated ridge, across the
entrance ; occupying an extensive surface between Ludgershall upon the Lod,
and Northhurst, and being thence continued, at a corresponding distance from
the top of the clay, all round the denudation. The course of the Lower
green-sands on the south and south-west of this valley having been pointed out
by Mr. Murchison, it is unnecessary to pursue this description farther.
(64.) Weald Clay.—The lowest beds of the tract near Guildford have
recently been exposed in a pit for the extraction of gravel at Pease-marsh,
an extensive flat on both sides of the London road, between Arlington,
south of Guildford, and Godalming. On examining the place, to which
my attention was called by Mr. Murchison, I found beneath a thick-
ness of four or five feet of flint gravel and sand, distinct strata of blue clay,
Dr. Frrron on the Strata below the Chalk. 149
nearly horizontal, though with an irregular surface, including flat nodular con-
cretions of iron pyrites, also horizontally disposed. No fossils were visible;
but from the situation and characters of the clay, it seemed most probably
to be that of the Weald, brought up into this close proximity to the chalk,
by the general elevation of all the strata. It is indeed probable that the
Weald clay is very near the surface in many other places ; but as the middle
group of the sands is also retentive of water, and capable of sustaining ponds,
the distinction can be ascertained only by attention to local circumstances.
The difference of level is so small in the different portions of the Wey,
from Pease-marsh, by Godalming, Pepperharrow, Elstead, and Tilford, that
this clay may be the base of the stream throughout ; but many of the ponds
which occur at higher levels, in the tract between Dorking and West Sussex,
may safely be referred to the middle group of the sands *.
(65.) Tucksbury-hillt, &c——The summit of this hill, which forms the
northern extremity of the section, Plate X. a. No. 4. is an outlier composed
of siliceous and ferruginous sand, upon the surface of which are numerous
angular fragments of pale yellowish flint. The ground descends from it
on all sides, but with the greatest rapidity towards the valley of the Wey ;
and it affords an excellent view, both of the successive outcrop of the strata
in the lower country, on the south-east, and (especially) of the tract on the
north, occupied by the Bagshot sands}, to which the cap of the hill
seems to belong; the flat-topped ranges and the lower barren tracts of
that formation being seen from hence very distinctly. The summits of
Romping-down and Chobham-ridge project above the surrounding country,
with escarpments towards the east, nearly at right angles to the range of
the Chalk Downs; but the general rise of the sands is towards the south,
conformably to that of the chalk§. The succession of strata observable in
* Such are probably the ponds of Berry-hill, Lonesome, Wotton, and Abinger, near Dorking ;
of Thorncombe-street, Wormley-heath, Witley, and Lea-house, near Godalming; Frensham
Great Pond; and many of the pieces of water in Woolmer Forest. Several of the ponds near
Pulborough can with certainty be referred to the geological place mentioned in the text.
+ This name of the hill is taken from the Memoir connected with Mr. Greenough’s map. Ir
the Ordnance map, one point on the summit is called Farnham Beacon.
{ Warburton: in Geol. Trans., 2nd Series, vol. i. page 48.
§ I had proof of this rise, in passing along the main road from Guildford. At an early hour of
the morning, in October, all the flat country on the north was occupied by a dense uniform
fog, which filled the inequalities at the foot of the sand-heights on every side. Above this sea or
lake of mist, which afforded a sort of fluid level, the tops only of the ridges were visible, like long
dark islands, the southern extremities of which were uniformly higher than the northern; the
intermediate line declining at a very small but perceptible angle.
150 Dr. Firron on the Strata below the Chalk.
descending from the elevation to the valley of the Wealds, is very in-
structive.
At the west end of the hill, beneath Warren’s-corner, on the road to Basingstoke, Septaria are
found in a stratum of the London clay, which occupies a considerable thickness on the slope of
the hill, below the cap of sand. I was informed that “ Pot-earth,” of a different quality, occurs
lower down, in Clarehouse-Park, in the situation of the Plastic clay ; and I have seen the Chalk in
the decline of the hill, between Lower Old Park and Halfway-house.
The Upper green-sand forms a slight prominence beneath this chalk, on the south of Dip-
penhall-house, between the words ‘ Dean’s-farm’ and ‘ Ridgway’ on the Ordnance map, the strata
dipping not much more than 5° to the north. The rock, which is there called ‘ Marl-stone,’ does
not precisely agree with any I have seen between this place and the coast, but is very like some of
the strata in the corresponding place at East Knoyle, on the north of the Vale of Wardour. It is
a subcalcareous sandstone, or variety of “ fire-stone,” very soft, uniform, of a yellowish-grey or
cream-colour, scarcely effervescent, and remarkable for its lightness ; and it includes concretions
of a hard splintery limestone, approaching to chert, and of much greater density than the stone
which surrounds them.
The Gault, on the line of the section, first comes up on the road descending from Ridg-
way to the river Wey, but is more distinctly seen at the extremity of Wracklesham; and, in
consequence of the more gradual rise of the strata, on the south-west of that village, it occupies
a more expanded surface in Alice-Holt Wood, as described in Mr. Murchison’s paper above
referred to.
On the south of the main London road, where it is crossed by the road to Wracklesham, is a
bank with the Lower green-sand at the bottom, rising towards the village. The surface is waved
remarkably; and the inequalities are filled up with gravel, consisting of broken flint pebbles, in
large proportion, mixed with red loam, and in immediate contact with the yellowish sands below.
The top of the gravel, is nearly level; but its depth to the sand varies from 1} to 4 feet. This
fact is analogous to the erosion of the sands near Dorking, mentioned above (56).
(66.) The mode in which the drainage of the north-western portion of the
great valley of the Wealden is effected, and the different manner in which
the streams escape, in this part of the country, from that of their egress
through the North and South Downs, support the hypothesis of Mr. Scrope
and Mr. Martin, that the gorges themselves were not produced by simple de-
nudation, but at least prepared, by antecedent fissures cutting entirely across
the Weald: while the appearances of the surface, above described, are so
unlike those which would have been produced by rapid diluvial action, as to
indicate either a long period of submersion, at no great depth, or very gradual
drainage and long-continued decay.
The principal branch of the Wey, from its rise near Alton, to Farnham, is nearly straight, in a
direction from south-west to north-east; but immediately below Farnham, instead of cutting
across the chalk downs, it turns abruptly to the south-east, to join another branch; which likewise
runs in a straight line nearly parallel to the former, from its source in the chalk near Selborne,
through Kingsley, by Frensham, to Tilford Bridge, where the streams unite: and then taking a:
tortuous course, but in a general direction parallel to the Hog’s-back, the river cuts deep
Dr. Frrron on the Strata below the Chalk. 151
through the platform of the sands, on the north and west of Godalming, receiving several stream-
lets by the way. But there, instead of continuing its direction, it turns suddenly to the north ;
and receiving another branch from beyond Cranley, far within the valley of the Wealds, cuts
almost directly across both the green-sand and the chalk, and makes its way to the Thames at
Weybridge. The mere closing-up of the defile at the mills on the north of Godalming, would
convert the whole of Pease-marsh, Frensham, and Thursley commons into a lake :—and, on the
other hand, a slight excavation towards the north, through Frensham to the river, would drain the
great pond there.
The sudden change in the direction of the Wey, near Farnham, is the more remarkable, as the
Blackwater, which rises on the northern slope of the chalk downs between Farnham and Alder-
shot, about two miles from the angle of the Wey near the west end of the Hog’s-back, runs on
the Bagshot sands, towards the north and west, by Frimley, Blackwater, &c., to join the Lodden,
not far north of Strathfieldsay, in its course to the Thames near Shiplake. The line of the Wey,
therefore, from Alton to Farnham, is nearly a continuation of that of the Blackwater* ; the two
streams being separated only by the prominence of the chalk between the Hog’s-back and the
foot of Tucksbury Hill.
The gorge of the Wey is nearly opposite to that of the Arun, on the south of the Wealden, one
branch of which runs almost directly north and south, from a point between Loxwood and Slin-
fold, to the sea at Little Hampton; and the structure of the two rivers is very much alike.
The Arun rises in the centre of the Wealden tract, whence it runs directly to the sea; as does
the Wey from Cranley: but it receives, near Pulborough, at right angles to the main stream,
the copious branch (if it be not rather itself the principal stream,) called the Rother; which,
having risen near the ponds of Wolmer Forest, very near the sources of the Wey, and followed the
curves of the denudation for more than twenty miles, in the trough between the chalk escarpment
and the Lower green-sand, is then carried suddenly out of that direction, and withdrawn from the
valley of the Weald.
(67.) From whatever cause the transverse course of the streams may have
originated, the relative composition of the strata was favourable to their retain-
ing that direction, when once they had made their way across the chalk and
Upper green-sand. For, as the lower beds of the chalk itself, and still more
the Gault, are remarkably retentive, while the upper chalk is permeable by
water,—the slope of all the strata being outwards, or from the central ridge
of the valley, the whole of the waters imbibed by the chalk would be deter-
mined outwards, if any pervious channel were opened at its bottom. And if
a fissure were cut through the whole series, without great vertical displace-
ment, the retentive beds of the chalk-marl and clay, would immediately re-
unite, and close it below; while, the chasm in the chalk above remaining open,
a permanent drainage outwards would be produced, and the break would be
continually enlarged.
* The main stream of the Wey is that which runs direct from Wolmer to Shalford. See the map.
+ It should, however, be kept in view, that the bed of the Blackwater hereabouts is several
feet above that of the Wey.
152 Dr. Fitton on the Strata below the Chalk.
(68.) The following is a list of some of the fossils obtained from the strata
above the Weald clay, within the portions of Kent and Surrey mentioned in
the preceding sections (37. to 67.) :—
List of Fossils of the Gault and Green-sands, in the 1nrerior or Kenr,
and part of Surrey.
Ammonites dentatus. Gault. Brick-field near Westerham. F.
A lautus. Gault. Same place. F.
A splendens. Gault. Bletchingley, Surrey. Mantell.
A tuberculatus. Gault. Brick-field near Westerham. F.
A ? A fragment of a very large Ammonite (or Hamite?), was found by one
of my sons (W. I. F.), among the lowest beds of the green-sand on the south
of Brasted in Kent; which, when complete, must have formed a spiral between
two and three feet in diameter. The separate convolutions are about nine inches
in breadth; and the flutings of the surface, which are simple, are about two
inches across the broadest part, and in depth about an inch. The specimen be-
longs, not improbably, to one of the large species which occur in the Gault
of Yorkshire, (see Phillips).
A Four species occur at Boughton quarries.*
Ampullaria canaliculata. Gault. Bletchingley, Surrey. Mantel].
Belemnites minimus. Gault. Bletchingley. Mantell.
B —. A large species. Boughton quarries. Also at Cold Harbour, near Mont-
real Park, Sevenoaks, Kent. F.,
Cucullea. (Species doubtful.) Lower green-sand. Boughton quarries. F.
Dentalium decussatum. Gault. Brick-field near Westerham. F.
Exogyra conica. Boughton. F.
18; levigata. Boughton quarries. F.
Fistulana. (Species doubtful.) Ditto. F.
Gervillia. (Species doubtful.) Boughton. F.
Gryphaa sinuata. Boughton. Also near Brasted; West Kent. F.
Inoceramus concentricus. Gault. Brick-field near Westerham. F.
_— latus. Ina fragment of yellow quartzose chert, loose on the surface, near
Brasted, Kent. F.
Modiola parallela. Lower green-sand; Near Maidstone. M.C.
Mya. (Species doubtful.) Boughton quarries. F.
Nautilus elegans. Boughton. F.
Nucula pectinata. Gault. Brick-field near Westerham. F.
Pecten quinquecostatus. Lowest green-sand. Riverhill. G.
Pholadomya. (Species doubtful.) Boughton. F.
* All the specimens from Boughton were found in the Lower green-sand: the greater part
in the soft grey calcareous rock, full of green particles, called “ Hassock.”
Dr. Firron on the Strata below the Chalk. 153
Plagiostoma. A small species. Lowest beds of the green-sand: Riverhill, near
Sevenoaks. Mr. Goodhall.
Pleurotomaria striata*. Pl. XIV. f.16. Boughton. F.
Plicatula pectinoides. Boughton. F.
Rostellaria carinata. Gault. Bletchingley. Mantell.
Serpula. Boughton. F.
Sphera corrugata. Lowest green-sand. ‘Trevereux, near Lympsfield, Surrey. F.
Terebratula Gibbsiana. Boughton. F.
T———— oblonga. Lower green-sand. Riverhill. G.
Thetis major? Boughton. F.
Trigonia aleformis. With two or more other species. Boughton. F.
Turbinolia Kenigii. Gault. Bletchingley. Mantell.
Venus angulata? (Cyprina.) Large, flat. Boughton. F.
Wood, Dicotyledonous. Boughton; and near Brasted, West Kent. F.
Hyena. Portions of the bones of the extremities of this animal, and fragments of
the skull and teeth, both molar and canine, with pieces of Album Gracum, have
been found imbedded in brownish sandy loam, at the top of the quarries of
Boughton Mount. F.
Jguanodon. Distinct remains of this reptile, found by Mr. Binstead in the Lower
green-sand at Rockhill, near Maidstone, have been examined and described
by Mr. Mantell. See note on (38).
HampsHire AND WesTERN Sussex.
The south-western portion of the Wealden denudation has been so fully
described by Mr. Murchison and Mr. Martin, that I shall refer to their publi-
cations already quoted, for an account of it; giving here only some additional
facts with which I have been favoured by those two gentlemen: and for a
similar reason I shall leave untouched the territory of Mr. Mantell in Western
Sussex.
(69.) Hampshire —Accumulations of broken chalk flints have been found
very extensively, over the surface of the Lower green-sand, on the newroad from
Petersfield to Midhurst in West Sussex; at Sheet Hill; and several other places
in this part of Hampshire. In the former situation, which is about three miles
from the nearest chalk, the detritus covers an uneven surface of the sand,
which appears to have been acted upon precisely in the same manner as that
* In the list of the fossils of the vicinity of Folkstone (p.131.), this shell has been called a
Trochus: but a very fine specimen obtained from Kent, and kindly mentioned to me by Mr. Charles
Manning, has since convinced Mr. Sowerby that the true genus is Pleurotomaria. See the de-
scriptions of the new species, in the Appendix.
VOL. IV.—SECOND SERIES. x
154 Dr. Firron on the Strata below the Chalk.
of the chalk itself; the sand being eroded into irregular cavities, sometimes
almost tubular, which are now occupied by chalk flints, a great part of them
in small fragments, and all of a rusty yellow colour. Equally abundant accu-
mulations of these are seen also on the hills of white sand (one of the upper
members of the Lower green), at Stedham and Trotton commons, between six
and seven miles east of Petersfield ; but in this case the flints are not dis-
coloured. This latter place is distant nearly three miles from the nearest
point of the chalk, and between nine and ten miles east of that where the
chalk escarpments are confluent. In the angle of the chalk west and north-
west of Petersfield, particularly in the ascent to Alton by Stoner Hill, such
heaps are yet more common. These facts coincide with the observations
already mentioned, near Boughton, Dorking, and Wracklesham (38, 56, and
65); so that it would seem as if chalk flint gravel above the Lower green-
sand was of general and frequent occurrence all around the denudation. Mr.
Murchison, however, adds, that he has still no knowledge of any such debris
beyond the limits of that formation, or within the Wealden properly so called.
(70.) The stiff and retentive marly beds, at the base of the Downs, sus-
taining the water which descends through the chalk, have produced a line of
ponds along the bottom of the escarpment of the South Downs ;—a result pre-
cisely analogous to the breaking-out of the springs above the mar], at Lydden
Spout, upon the coast (8.), and all along the base of the Downs on the north.
(71.) One of the chief characteristics of the tract near Petersfield, consists
in the great relative extent and prominence of the Upper green-sand; which
runs out beyond the foot of the chalk escarpment, like a step or terrace,
throughout the tract from Farnham, by Selborne and Petersfield, to the south
of Petworth, and affords some of the best sections anywhere to be found,
except perhaps in the Isle of Wight. Though in the parishes of Buriton,
Harting, &c., there is an insensible passage from the grey chalk and chalk
marl, into the Upper green-sand, still the whole of the terraces (there at least
two miles broad) are exclusively composed of what is called in the country
Malm-rock*. 'The grey or lower chalk of this portion of the South Downs
is charged with the Inoceramus mytilordes, I. Cuviert, I. Brongniarti, and two
species of small plicated Terebratula, and does not contain any of the cha-
racteristic malm-rock fossils enumerated in Mr. Murchison’s memoir; nor
does the malm-rock contain, so far as his observation goes, a single specimen
of the genera Inoceramus and Terebratula, so abundant in the overlying
* The Malm-land, which is remarkable for the fine crops of corn produced upon it, is, pro-
perly, the soil over the lowest beds of marly chalk, which are carried out upon the tops of the
projecting terraces; the term, ‘‘ Malm-rock,” being confined to the stony beds beneath.
Dr. Frrron on the Strata below the Chalk. 155
chalk : a fact which is the more deserving of attention, as several other genera
and species are found both in the Upper green-sand and the Lower chalk*.
(72.) Vicinity of Pulborough.—I am indebted to Mr. Martin for the section
(Plate X a. No. 5.) across the Wealden district, from Duncton Beacon on the
South Downs, through Petworth, to Cranley; and I have, from my own ob-
servations, continued it in the same direction to the North Downs. This
section shows, what Mr. Martin’s recent observations have fully confirmed,
that the subdivisions of the sands below the chalk, in the north-west of Sussex,
correspond with those above described, in the neighbourhood of Folkstone ;
and that a similar valley distinctly marks, in both cases, the place of the middle
greener and retentive sands, (24.). I have had myself also an opportunity of
seeing, with Mr. Martin, a section parallel to that of Plate X a., in which this
structure is very clearly displayed, on a line about half a mile west of Pul-
borough, passing through the heights of Park-hill farm and Pethenden (with
the valley of the middle sands between), to a detached summit within the
Weald-clay, called Pickhurst Hill; (See Plate X b. fig. 2.). Fuller’s-earth
like that of Nutfield, appears at Fittleworth Church, near Pulborough.
Besides the mass of this intermediate group, a detached stratum, about 40 feet in thickness, of
dark-coloured, greenish grey, retentive sand, including much pyritous matter, occurs above it,
with some feet of ferruginous and yellowish sand between ;—-a subordinate bed, in fact, within the
upper ferruginous mass of the sand: and this ought to be held in view, as in some cases it might
be mistaken for the Gault. It is very conspicuous on the ascent of the London road, from the flats
on the south, to the church at Pulborough; and can be traced thence, almost continuously, for
some miles both to the east and west. No fossils have been found in this stratum, except some
impressions of what may be the branches of fuci. A bed of dark hue, with the same characters,
seems to occupy a corresponding place in the series near Reigate: See note f on (52.).
(73.) This country has been the scene of several upheavings and derange-
ments of the strata, analogous to those above mentioned in West Kent (41.
to 43.), but much more complex and extensive. Some of these have been
described in Mr. Martin’s work already referred to; and of others, more re-
cently observed by that gentleman, I hope he will himself soon publish a
description}.
* See Mantell’s “ Tabular Arrangement of the Organic Remains of Sussex”—Geol. Trans. 2nd
Series, vol. ill. p. 210. Terebratule are there mentioned among the genera common to both
deposits.
t The forces by which such derangements may have been effected, appear to be still in action
in this part of England. In the spring of the present year, 1834, distinct shocks of an earthquake
were felt throughout a tract, of which Chichester seems to have been the principal point. At
Pulborough, they were of such force as to ring the bells at the parsonage. An account of the
phenomena, is, I believe, in preparation, by some members of the Philosophical Institution at
Chichester.
x 2
156 Dr. Firron on the Strata below the Chalk.
(74.) The junction of the sands and clay,at Stopham brick-yard, on the west
of Harwood’s Green, near Pulborough, affords the only indications that have
come to my knowledge, of any interruption or disturbance between the de-
position of the upper part of the Weald clay, and of the incumbent Lower
green-sand. Thesurface of the clay at the place in question is hollowed into
irregular roundish cavities, at the bottom of which portions of green-sand were
found, including several of the characteristic fossils of that formation ; while the
clay, immediately below, is equally characterized by the presence of Cypris. At
the junction, the clay was mixed with sand; and specimens of Panopea plicata
were found even two or three feet within nearly pure clay, along with ferru-
ginous concretions, containing fossils of the Wealden, impressions of Cyclas,
Cypris, and remains of fishes: and this mixture was observable to the depth of
several feet ;—so that both the sand and clay must have been at the time of
mixture in a state of sottness ; or the sand must have been introduced over
a surface of argillaceous mud, before it had consolidated. When | had the
pleasure of examining the place, with Mr. Martin, the circumstances were
unfavourable to observation: and, as the junction of the two formations
here, is on the slope of a hill, it might have been doubted whether the
appearances could not be explained by the effects of subsidence producing
intermixture, during very rainy weather, or under water, before any of the
strata had emerged. Mr. Martin, however, who had seen the place when the
phenomena were better exhibited, is of opinion that this explanation of them
would not have sufficed. In this brick-yard, the loamy sand found near the
junction is used alone for making the bricks; sand being required in the
manufacture, only for sprinkling the moulds.
(75.) List of Fossils from the Beds below the Chalk, in part of Hampsnire
and Western Sussex.
[ Upper Green-sand. |
The following List of Fossils from the Upper green-sand in the vicinity
of Petersfield, in addition to those mentioned in Mr. Murchison’s paper on
that district, (Geol. Trans. 2nd Series, vol. ii. p. 99.) I owe to the kindness
of Mrs. Murchison, in whose collection the specimens are placed.
Ammonites catillus. Fishes. Scales and vertebre.
A—— splendens. Gryphea columba.
Arca carinata. G vesiculosa.
Avicula grypheoides. (See Pl. XI. f. 3.) G sinuata.
Cucullea. Much compressed. Nautilus elegans ?? Much compressed.
Echino-spatangus. (Three new species.) Pecten asper.
~
Dr. Firron on the Strata below the Chalk. | 15
Pecten Beaver. Solarium granulatum. Mantell.
P nitidus. S or Trochus. Another species.
P orbicularis. Thetis major.
P quinquecostatus. Besides one or Vegetable impressions. Like those of the
two other species, indistinct. upper chalk near Lewes. Mantell,
Plicatula inflata. | CE Pe RO Ce
[Lower Green-sand. |
Ammonites dentatus. Stopham brick-yard, West of Pulborough, Sussex ; in a mass of
phosphate of lime. his, with the other fossils from the same place, was found
by Mr. Martin covered by green-sand, in an excavation at the top of the Weald
clay. Martin MSS.
A————.. (Near to Nuifieldiensis, but a distinct species.) Lowest member of the
sands near Pulborough: Martin.
A——_——. (Impressions of one or two other species.) Stopham brick-yard: Martin
MSS. One of these is in a roundish mass of phosphate of lime, precisely like spe-
cimens found near Copt Point, Kent: the outer surface is whitish, and is eroded
in small tortuous grooves, as if eaten by worms: the interior brown.
Auricula (new species). Martin, cbid.
Avicula? Martin, zbid.
Cardium? (New species; delicately striated.) Stopham brick-yard : Martin MSS,
Coprolite. Stopham brick-yard : Martin MSS.
Corbula gigantea. Bowyer’s Common: Mrs. Murchison.
C. striatula. Bowyer’s Common, near Petersfield: Mrs. Murchison. Parham :
Mantell, and Martin.
Cc (new). Near Pulborough: Martin, p. 32.
Crustacea. “‘ At Bognor Common, in Fittleworth parish, there is a vein of friable
“‘ oreen-stone, rich in Pectens, Trigonia, and the remains of a crustaceous fossil
“like a shrimp.”” Martin, p. 34, note.
Cucullea decussata. Parham: Mantell, and Martin.
C glabra? Bowyer’s Common: Mrs. Murchison.
C (Another species—or two?) Stopham brick-yard: Martin MSS.
Cyprina angulata. (Venus, Min. Con.) Stopham: Martin MSS.
Cytherea parva. (Venus, Min. Con.) Parham: Mantell. Bowyer’s Common, and
Lyss near Petersfield: Mrs. Murchison. Upper ferruginous member of the
Lower green-sand, Pulborough Mount: Martin MSS,
Gervillia acuta. Parham: Mantell.
G aviculoides. Parham Park: In concreted masses of fine-grained ferruginous
sand, with several other species mentioned below; all casts: Martin. Also
Bowyer’s Common: Mrs. Murchison.
G solenoides. Parham: Mantell.
G (Another species, probably new.) Upper ferruginous member of the
sands: Martin.
Inoceramus gryphaoides. Lowest group of lower green-sand: Martin, p. 33.
158 Dr. Firron on the Strata below the Chalk.
Lima semisulcata. Plate XI. fig. 10. Pulborough: Martin.
Lucina? Bowyer’s Common: Mrs. Murchison.
L (Perhaps two species.) Lowest member of the sands; near Pulborough:
Martin.
Modiol. lis.
Ae eqalts Parham: Mantell.
M. bipartita.
M— imbricata. Upper ferruginous sands: Mantell, and Martin.
M— bella. Plate XI. fig. 9.
M.- (A new species.) Near Pulborough: Martin, p. 32.
Mya mandibula, Wowest member of the sands. Pulborough: Martin.
M-— plicata. (See Panopeea plicata).
M—. (Two species not figured.) Martin, p. 33. Lowest group of lower green-
sand.
Mytilus edentulus? Martin, p. 32.
M— lanceolatus. Parham: Mantell.
Natica. Parham: Parkinson; Organic Remains, vol. 3. Pl. 6. fig.2. Lyss near
Petersfield: Mrs. Murchison.
Nautilus. Near Pulborough: Martin, p. 31.
Nucula impressa. Parham: Mantell. Lowest member of the sands; Pulborough :
Martin.
N— antiquata. Upper ferruginous member of the Lower green-sand; Pulborough
Mount: Martin.
Orbicula. (Not figured.) In sand rock: lowest member of the sands; Pulborough
and Stopham: Martin.
Panopea plicata. Lower member of the sands; Parham Park, and Stopham brick_
yard: Martin MSS.
Patella. Parham: Mantell.
Pecten obliquus. Parham: Mantell, and Martin.
Ji orbicularis. Pulborough: Martin. Parham: Mantell.
yd quadricostatus. Parham: Mantell.
Je (A new species.) Martin.
Pholadomya. Wowest member of the sand near Pulborough : Martin, p. 32. and MSS.
Pinna tetragona. In sand-rock ; lowest member of the sands: Martin.
P (A cast.) Stopham brick-yard: Martin.
Rostellaria calcarata. Parham: Mantell.
R— Parkinsonii. Parham: Mantell. Upper member of the sands ; Pulborough
Mount: Martin.
R———. (Very like Pes Pelicani.) Parham: Mantell.
helene emialis: j Parham : Mantell, and Martin.
T: inequalis. ‘
p. ? (A species not figured.) Lowest member of the sands, near Pulborough :
Martin.
Terebratula lata.
1 oT,
Parham : Mantell.
|
,
Dr. Firron on the Strata below the Chalk. 159
Terebratula nuciformis. Upper member of the sands; Pulborough Mount : Martin.
ye depressa. Upper ferruginous member of the Lower green-sand ; Pulbo-
rough Mount: Martin MSS.
[T—__—.. (Another species—uncertain.) Same place : Martin.
Thetis major. Lowest member of the sands; Pulborough: Martin.
T: minor. Bowyer’s Common, and Lyss, near Petersfield: Mrs. Murchison.
Parham: Mantell. Upper member of the sands; Pulborough Mount: Martin.
T—— (new). -Stopham brick-yard. Martin MSS.
Trigonia alaformis. eee Common: Mrs. Murchison. Parham: Mantell. Stop-
T—— clavellata? | ham: Martin.
T—— dedalea. Parham: Mantell.
ft spinosa. Pulborough: Martin, p. 33.
Turbo rotundatus. Parham: Martin MSS.
T—. (Another species.) Near Pulborough: Martin, p. 31.
Turritella granulata. Parham, and Pulborough: Martin MSS.
T (Another species.) Near Pulborough: Martin MSS.
Venus angulata. See Cyprina.
: — } Patham Mantell.
V—- ovalis.
V— parva. See Cytherea parva.
V—. (Casts of two other species.) Stopham: Martin MSS.
Vermicularia concava. Parham-park, Parkmount-lane near Pulborough, Chiltington-
common. Martin, pp. 33 and 34.
Tor WeEaLven.
(76.) In adopting this general denomination, proposed by Mr. Martin, for
the formations below the green-sand, in the Wealds of Kent, Surrey, and
Sussex, I have extended its acceptation to the Purbeck strata also, which do
not occur within those counties ; because the whole group abounds in fossils
of the same character. And though the Purbeck strata consist principally of
limestone, which has many indications of lacustrine origin, they include, like
the upper members of the Wealden, distinct alternations of marine fossils
with those of freshwater :—one very thick bed especially, which consists al-
most entirely of oysters,* showing that the sea must have had access to the
waters from which they were deposited. Mr. Martin has ascertained that the
Wealden strata above the Purbeck, consist, throughout, of alternations of
sand, sand-rock, and grit, with clay and marl; so that the separation of the
Weald-clay from the Hastings sands, is in a great measure arbitrary. But as
in the only tracts where this group has yet been observed, the sands rise above
the valley of the clay, into a very prominent ridge, which forms a striking fea-
* Webster: Geol. Trans., 2nd Series, Vol. IL., p. 40.
160 Dr. Firron on the Strata below the Chalk.
ture of the surface, this subdivision is to a certain extent natural, and may be
retained with advantage.
(77.) Valley of the Wealds.—The‘beds of sand, sand-rock, and limestone
subordinate to the Weald clay, have been traced by Mr. Martin throughout
the tract represented in his map of Western Sussex, and I refer to his memoir
for an account of them: their place is indicated in the Section, Pl. X. a.
fig. 5. L have myself observed beds of the same description,—no doubt con-
tinuous with those described by Mr. Martin, though I have not traced their
continuity, on the opposite side of the Wealden and of the forest ridge, about
Ewhurst, and on the east of that village*. And in the course of the valley
eastward, through Surrey and Kent, distinct and almost continuous ridges,
apparently produced by the greater durability and prominence of similar
strata, are observable from the escarpment of the sands, and are in part ex-
pressed in the Ordnance Maps.
Two, if not three lines of these subordinate strata cross the road which descends from the
escarpment of the sands through Ewhurst. 1. The first is at the foot of a height, which runs from
the south of Coneyhurst Farm, through Woodland; the beds consisting of limestone, (Sussex
marble) full of large Paludinz and Cypris. A group, possibly a continuation of this, occurs in
Mr. Turner’s grounds, north of Forest Green, at Atherley, about two miles east of Woodland,
below Leith-hill Place; but there the stone is greenish micaceous grit, in three contiguous
courses, each about 12 inches thick, containing very large Paludinz, Uniones, and stemlike concre-
tions, where the stone adjoins the whitish sand, on which it rests. Above Henhouse Farm also,
about a mile and a half east of Atherley, a range of high ground indicates the presence of firm
bands of stone; and grit is found there, which includes similar Uniones, and a few Paludinz.
2. A second band, composed of ironshot sand, over variegated reddish brown clay, crosses the
road, at the church of Ewhurst, passing thence eastward through Lyefield Farm. The stone-pits
of Forest Green seem to be on this line, but they consist of beds of grit including Uniones and
Cypris, above yellowish sand, reddish clay, and concretional sandstone, with casts of Uniones.
3. At Bowles’s Farm, on the east of Cranley, is a bed of very compact sand-stone, apparently
lower in the series than those above mentioned: and the roads hereabouts are repaired with grit
from Newhouse, between Cranley and Ewhurst. Stone is also found nearly on the same line east-
ward, at Redford and Standling; and again on the south of Capel (on the road from Dorking,
about a furlong north of the 30th mile-stone), is a prominent ridge, with a course of sand, in
beds from 2 to 6 inches thick, in light-coloured clay.
The height last mentioned, near Capel, may probably be the continuation of a ridge which, on
the Ordnance Map, begins about 34 miles to the east of that place, passing from Stand-hill, through
Norwood and Horse-hill; and which (being resumed on the east of the Mole), forms a range nearly
parallel to the escarpment of the Lower green-sand,—by Lady-farm, about two miles south of
Earlswood-common on the road from Reigate to Brighton, Outwood-common, Lostland, south
of Gayhouse-farm, and thence, through Hook-stile, to the stream south of Comfort’s-Place farm,
and Moat farm. On the east of the place last mentioned, the ridges between the Lower green-
* See the eastern part of the Section, fig. 5.
Dr. Fitton on the Strata below the Chalk. 161
sand and the Hastings sand, are not so well defined; but on the south of Boughton, a series of
heights extends from Marden to the east of Staplehurst.
(78.) Coast of Kent. There is, strictly speaking, no section of the Weald
clay and the upper part of the Hasting sands on the coast of Kent; the line
of heights which, at some very remote period, may have been sea-cliffs washed
by the English Channel, being now covered with vegetation, and separated
from the sea by the wide tract of Romney Marshes. Having, myself, some
years ago, observed indications of sand and stone, in the Weald valley near
the coast where it is difficult to find good sections exposed, my friend the Rey.
G. E. Smith was good enough, at my request, to examine that part of the coun-
try; and from his notes I learn that the greater part of the series there must
consist of sand and sandy clay,—the blue fissile clay, which occurs in the
upper part of it, not recurring, or not having been detected, farther down.
The first rise of the clay from beneath the green-sands, is represented in the view Plate VIII.;
and the general section of the coast between Folkstone and Beachy Head, (Plate X. a. No. 6.)
includes the strata on the west of Hythe. The shore beneath that town, which is sometimes
laid bare, when the sea carries away the shingles, during the prevalence of easterly winds, consists
of soft bluish clay, which has the characters of river mud, and differs much from the uniform slaty
clay of the Wealds. But the latter has been cut through in sinking wells above the main street
of Hythe, which, in some instances, have gone to the depth of 75 feet entirely in clay. In one of
these wells, the succession of beds was thus ;—beginning at a point about 60 feet beneath the
bottom of the Lower green-sand.
Upper Part of the Weald-Clay at Hythe.
Ft In.
oe ot ROR OAR Ge rn atest stainleieto vara 2 6
RR RCOMNT CLAY Sates sas oe ew oe vee osnensetnes scenes ne 6 to 7 0
3. Greenish sandy clay, in thin bands, alternately of dark and lighter hues.. 5 to 6 0
4. Blue, uniform, slaty clay, containing Cypris about a foot from the top.. about 5 0
5. A band, composed of argillaceous iron ore, abounding in Paludina elon- .
20 PU eS ie so ee een ne 2
18 0
6. Blue clay continued. Here a boring was made to a depth of about 20 feet :
aUBtantaisUncinverie ci Magee shs Pe PLT Mifesal 20 0
hotahs 0 ote ts. 38 0
Blue clay with Cypris occurs also, according to the Rev. G. E. Smith, immediately below the
green-sand, at Aldington Corner ; but nothing like it, he informs me, in the succeeding parts
of the section towards the south. A bed of limestone, with Paludinz (‘ Sussex marble”) occurs
at Hurst}, beneath Court-at-Street, and seems to be continued in the clay which passes from
that place round the base of Aldington Knoll; and a similar stone is found, in a corresponding
situation in the cypriferous clay, at Daniell’s Water on the south-west, Stanford Bridge, on the
*In descending from the sands at Linton, south of Boughton, and in many other places, the
top of the Wealden is seen to consist of very red clay.
‘| The term Hurst is of such frequent occurrence in the names of places in Kent, Surrey, and
Sussex, that the Ordnance Maps alone afford a List of about 120 such names. Having sent this
List to the Rev. Joseph Hunter, late of Bath, that gentleman has favoured me with some obser-
VOk. IV.—SECOND SERIES. Y
162 Dr. Firron on the Strata below the Chalk.
west of Ashford, and near Bethersden, about 22 miles south of Stanford Bridge. A continuous
range of slightly elevated ground, extending from Lovelace near Bethersden towards Shadoxhurst
(in a direction parallel to that of the other ridges of this country, and to the range of the chalk
escarpment), may also indicate the existence of some stratum of greater firmness than the clay.
Mr. Smith mentions two subordinate courses of sand, with sand-rock, sandy clay and loam, as
occurring in the lower tract, or valley of the Weald, between Aldington Corner and the cliffs of
sand and grit on the north of Rye. (1.) The first of these runs from near Bilsington, through
Orleston ; with which line a range in the interior seems, from the map, to be continuous, for about
four miles more towards the north-west,—through Woodchurch Beacon and Redbrook Street.
It seems to be parallel to the ridge above mentioned between Bethersden and Shadoxhurst;
and sections of the strata are disclosed at Bilsington Priory; on the roads from Bilsington Cross to
High-house; from Ruckinge to Ham Street, and from Ham Street to Orleston; and perhaps near
Warehorn Leaton. (%.) The second course, which consists of red clay with sand and sand-rock,
begins at Brookarm, on the verge of the marshes, and passes through Bench-hill. On the south
of this last-mentioned range, sand and sandy clay appear to abound: concretional beds of hard
vations of so much interest, that, but for the immediate object of these pages, I should willingly
have inserted them in full.
‘“¢ The word,” Mr. Hunter states, “does not occur in Lye’s Saxon Dictionary; but I observe
“ that the modern Lexicographers speak of a Saxon word, hypyz, as synonymous with sy sys and
as TE) it seems, occurs in low Latin, for ‘wood’. Wachter explains Horst, Germ, ‘locus
* “nemorosus et pascuus’; and refers it to dpos, mons. Kilian has Horscht, Teut. ‘ virgultum;
** «sylva humiles tantiim frutices proferens.’
“In England, Hurst appears to signify a small wood; but, in’ Scotland, a barren height or
‘““ eminence, and sometimes a shallow in a river. I do not find the word,” Mr. Hunter continues,
“in any of the provincial glossaries ; and yet I think it is not quite out of use, in its uncompounded
‘« state, to denote a Wood, generally; but I much doubt whether any specific difference can be dis-
‘* covered between the sense of this word and that of many other words, in a language which is
‘particularly rich in terms which designate woods, or woody places: grove, thicket, copse,
“* brake, &c.
“Tf Drayton’s authority (Polyolbion, viii. 2.) were not thought sufficient to prove that in
** England the word was formerly used to signify a Wood, the combinations in which it occurs in the
** names of innumerable places, dispersed all over the southern part of the island (1. e. south of the
‘‘ Tweed), would be sufficient to prove it. There is Oak-hurst, Ake-hurst (a varied form of Oke-
*‘ hurst); Elm-hurst, everywhere ; En-hurst, Hasel-hurst, Ash-hurst, Ashen-hurst, Maple-hurst,
“ Nut-hurst, Beam-hurst (Staffordshire), Brere-hurst, Box-hurst; besides many Hursts without
* any prefix,—of which Hurst-Monceawx is one ; Monceaux being an addition made after the Con-
* quest, from the name of some Norman Lord.
‘“* So many instances in which the names of trees are united with this word, would, I think, of
‘* themselves be sufficient to prove that it was really in use in England, in the sense of ‘wood’; and
“it may be added, that it lies deep in the language,—the woods so designated being older than
** the towns’ which have risen near them, and those towns of Saxon foundation.
“‘ Again, there are other instances in which the adjunct is congruous with this idea of Hurst; such
“as Hawk-hurst, Crow-hurst, Broad-hurst, Buck-hurst, Brocklehurst (Brock-hole-hurst),—the wood
‘‘ where the badger (brock) made his holes. So also Brock-hurst, Park-hurst, Coney-hurst, &c. &c.
“Tt must, however, be admitted, that there are many names of places, into the composition of
‘which the word Hurst enters, of which it is extremely difficult to trace the origin; and when
“ those for which we can account are taken out of the list, it is hard to form even a conjecture con-
** cerning those which remain. In this respect, however, the compounds of Hurst are but in the
“‘ same predicament with the prefixes to -ton, -ham, -field, -by, and many of the local terminals;
‘““and probably they are, in many instances, the names of early Saxon proprietors, detorted
“ from their original forms. Some, however, more skilful etymologist, or one better acquainted
‘‘ with the language of our ancestors of the 6th and 7th centuries, when probably these names first
“ became fixed, might explain :—Shadocks-hurst, Cog-hurst, Bub-hurst, Tile-hurst, Sissing-hurst,
“ Capen-hurst, Desron hurst, &c. &c.”
Dr. Firron on the Strata below the Chalk. 163
grit, with Paludinee and Cypris, occurring in the sands about Stone and Knock-house; and still
more conspicuously in the range of heights further south, which extends from Boons-hill to the
cliffs below Playden, not far from Rye.
(79.) Hastings Sands.—Mr. Webster has described and given a drawing
of the cliffs on the east of Hastings, in a preceding volume of these 'Trans-
actions* ; and a general section of the coast between the chalk downs of Kent
and Sussex will be found in the annexed Plate, X.a, No.6. I shall not,
therefore, here detail the stratification of this portion of the Wealden, espe-
cially as lists of the strata will be given hereafter, in describing the coast of
the Isle of Wight and of Dorsetshire ; but shall confine myself to an account
of the cliffs, on the west of those represented in Mr. Webster’s Sectional
View,—which were uncovered to a great extent during the progress of the
buildings and improvements recently carried on between Hastings and St.
Leonard’s f.
(80.) Shore on the West of Hastings.—The anticlinal line of the ridge
consisting of the Hastings-sands runs inland, from the shore towards a
point about 60° west of north; beginning on the east of Hastings, about
Lee Ness Point, and passing through Battle, and thence along a series
of ridges, to its greatest height at Crowborough Beacon, on the south-west
of Tonbridge Wells. The strike, on the west of Hastings, is not parallel
to the anticlinal ridge, but oblique to it at an angle of about 44°, the strata
running nearly from east to west, and dipping generally towards the south.
The direction of the coast line for a short distance, at St. Leonard’s, co-
incides with the strike, but from Hastings to the entrance of that place,
makes an angle with it of about 10°,—the line of the shore running from
about 14° north of east, towards the south of west; and on the west of
St. Leonard’s, the coast turns a little towards the north of west, and again
makes a small angle with the strike. In going along the shore, therefore,
from Hastings towards Bulverhithe, the strata first appear to be inclined
* Geological Transactions, 2nd Series, Vol. II. p. 31, &c. For additional information on the
Wealden tracts in general, the reader is referred to Mr. Mantell’s publications; Mr. Lyell’s “ Prin-
“ciples of Geology,” (3rd edition), Vol. IV. chap. 21 and 23, pp.165—191, 219, &c.; and to
“ A Sketch of the Geology of Hastings,” 12mo, 1832, by the author of the present paper.
+ This general section is on the same scale of relative height and horizontal distance, as all the
others in Plate X. a.; but asa correct estimate of the elevation is, in this case, important to theory,
the heights are given in true proportion, on the line immediately below, as has been done by Mr.
Lyell, in one of his chapters on the structure of the Wealden.
t The Sections following in the text, from (80.) to (90.), formed the substance of a Notice
read before the Geological Society, in November, 1833 (Proceedings, vol. ii. p. 1.); and are here
introduced by the permission of the President and Council.
y 2
164 Dr. Firton on the Strata below the Chalk.
to the south of west; then to become horizontal; and beyond St. Leo-
nard’s, to rise a little from the sea,—the same beds recurring there in a re-
versed order. The Section, Plate X. b, fig. 2, which is on a much larger
scale than Plate X. a, No. 5, represents the cliffs here referred to, and
will illustrate the structure above described.
(81.) The top of the great stratum of white and nearly pure sand, which
forms the cliff under the castle at Hastings, comes down to the shore at the
White Rock, and disappears under the sea on the west of it. A stratum which
has many of the same characters, and seems to be a continuation of that of
Hastings, rises at the bottom of the cliff, about 350 paces west of the
church at St. Leonard’s ; all the beds in the intermediate space being con-
sequently higher in the series. There is still some obscurity as to their rela-
tions, from the effects of disturbance ; and some points are concealed : but the
following list gives an approach to the order of their succession, descending,—
with an estimate of the relative thickness of the groups, and the places in
which they are found.
Supposed Groups of Strata on the Shore between Hastings and Galley Hill.
Estimated Thickness.
No. Feet. Feet.
I, Sand, and sand-rock, in large proportion ; with clay, in alternate courses .... 15@
a. Heights above and within the entrance of St. Leonard’s, from Hastings ... 50 |
b. From the archway at entrance of St. Leonard’s to Warriors’ Gate...... 50
c. Space corresponding to the vacancy at Warriors’ Gate (thickness it Eo
mated fromthe noxizontal distance): .c\ctsc sees vos + osis'e e eeieae ett
Dl Sand-rock, clay, ane Pmller’s-eartlis/c\cte's clots hots ete clea « ate! ciel ete etenels about 75
a. Heights between Warriors’ Gate and the White Rock ; nearly thus, in detail ;
Me aOLAb YP ClAY petewlelc.-f-rere 8 feet. 7. Dark sand-rock, with lignite.. 2
2, Sand and sand-rock. .20 8. Alternations of sand-rock,
g. Fuller’s-earth ...... 2 sand, and sandy clay, about }
Aim and=rockspryese ier 4 W752
o-Pullers-earthe yf. 2 9. Light blue clay, ae >
Gynsand-Tock reer ae 12 downwards into (III.)....
III. Sand-rock, alternating with grit, slaty clay, and clay iron-ore, and including one or
more layers of Endogenites erosa, with numerous other fossils... . between 50 and 60
a. Ledge under the White Rock.
b. Strata in the cliff behind the new Brewery on the east of the White Rock.
Endogenites erosa in great numbers.
The connexion of a. and b. with the light blue clay, (II 9.) was not dis-
closed: but the whole group seems to be the same with III. e.
c. Ledge of rocks under the “* Marina” at St. Leonard’s.
d. Beds around St. Leonard’s church, and in the cliff on the west of it.
At these places the grit and conglomerate include remains like those of Til-
gate Forest.
Dr. Firron on the Strata below the Chalk. 165
IV. White sand, and soft sand-rock, including thin flakes of light grey clay, and some
PGnenansiO! MMe S) oi cast wa et- Seca alerd ets ani oietls shai als Din wlee ws\\s upwards of 80
a. Cliff under the castle, Hastings.
b. Shore below, and on the east of the White Rock.
c. Bottom of the cliff, near the Sussex Hotel, west of St. Leonard’s.
cs
Or
V. Brownish sandy clay, with much lignite, immediately beneath IV.............
a. Under the Castle-cliff, behind Pelham-place, Hastings.
VI. Yellowish and ferruginous sand, and sand-rock, including nodules of pyrites,
and grains of reddish (pisolitic) oxide of iron............-.0.00004- }
a. Shore, about low-water mark, beneath the town of Hastings.
b. Shore between St. Leonard’s and the Martello Tower, No. 39.
VII. Variegated clay and sand, of various shades of red inclining to purple, and
Vipht Greenish reverent cso: - scien cee ee ee aden ee ne i
a. Heights west of Bopeep.
b. Shore from Bulverhithe to Galley Hill.
ec. Similar beds, with granular oxide of iron, are found on the east of Hastings,
in the bay of the Lover’s Seat, &c.
(82.) The following details respecting the strata just enumerated may be
worth preserving, as the surface of the cliffs will probably soon be concealed.
I. a.—The highest members of this series are partially exposed on the north of the back
street, near the eastern buildings of the Marina and the archway at the entrance of St. Leonard’s ;
from whence down to the shore is a series of strata, which are horizontal on the line of the strike,
but rise in reality towards the north, at an angle between 12° and 15°. The uppermost beds con-
sist of soft grey sand-rock, with some intermixture of clay, and form a total thickness_of about
66 feet above the road. The lower members are visible in the back street, and on the west of
the houses are seen to rise towards the west. The horizontal portion occupies about 150 paces
from west to east, and after that space, in consequence of a change in the direction of the shore
towards Hastings, a rise towards the east begins to be apparent. The strata which connect this
group with the beds of clay around the church hereafter mentioned (III. d.), have been carried
away or are concealed.
I. b.—The group next below is partially seen on the shore between St. Leonard’s and the
White Rock. Between the archway and the vacancy in the range of heights, which is called
Warriors’ Gate, is a low cliff about 250 paces in length, and about 30 feet high, which has been cut
away to admit of the erection of houses. It consists of sand-rock, alternating with clay or marl ;
the beds of which rise and disappear in succession, corresponding altogether to a total thickness
of about 50 feet.
I. c.—The opening at Warriors’ Gate occupies a horizontal space of about 300 paces, and
within it, on the north, is a bank of sand-rock like the strata last described. On the east of this
opening, a low range of grass-covered cliffs, from 40 to about 60 feet in height, extends without
interruption to the beginning of the road over the projecting masses at the White Rock*; and two
* The storms during the high tides of 1833 and 1834, had so shattered the mass which bore the
name of the White Rock, that very few of the interesting appearances represented and described
by Mr. Webster now remain, the face of the rocks which aftorded them having been either con-
cealed or carried away. The destruction had been such in April 1834, that the town of Hastings,
goatee concealed by the prominence of the shore, was then visible from the entrance of St.
eonard’s.
166 Dr. Fitton on the Strata below the Chalk.
remarkable beds of greenish Fuller’s-earth, in general about two feet thick, but in some places
much thicker, separated by about four feet of sand-rock, rise upon the road-side, and are continued
steadily in the face of the cliff, nearly to the White Rock, being, near that place, more than 30 feet
above the bluish clay (II. 9.) at the bottom. The base of the cliffs here is about 20 feet above a
floor of rocks which is bare at low water, and consists of yellowish, firmly concreted sand, or
sand-rock, abounding in granular (pisolitic) reddish oxide of iron*. This granulated rock forms,
hereabouts, a ledge beneath high-water mark, dipping to the west of south, at an angle of about
11°, with a strike towards a point about 6° or 7° south of east.
II.—About 120 paces west of White Rock, where the road formerly began to rise over that
prominence, the cliff behind the new houses, about 40 feet high, consists of a large proportion
of sand and sand-rock, with alternations of clay; and in some places contains so much lignite,
in the form of indistinct fragments of stems and portions of branches, as to have a dark brown
or blackish hue. A bed of light bluish clay (II. 9.) forms the lowest part of this cliff, and seems
to be continued downwards ; it probably corresponds to the beginning of the series of beds of clay
&c., (III. c.) near the church of St. Leonard’s.
On the shore at low water, about 150 paces west of the place last mentioned, is a group of beds
which are curved, so that their dip is divergent, those on the east dipping towards the south, at
an angle of about 10°; they consist of sand-rock, and may possibly be continuous with the sloping
bed at the White Rock, shown in the section, and inferior to the bluish clay of II. 9. Other ap-
pearances indicate that this has been the scene of some derangement, so that the relations of the
beds, above described, to those under the White Rock and on the west of it, are still doubtful: the
whole series, however, is nearly conformable, and almost continuous with the rest of the strata
_ towards St. Leonard’s.
On the east and south of the nook, in which is the light bluish clay, II. 9. a bed of brownish
sand-rock about 10 feet thick, immediately adjoins the road, dipping to the south of west, at a
much more rapid inclination (about 18°) than that of the adjacent strata. This bed, neverthe-
less, may be a continuation of those which form the curve represented above; and its present
position may have been the result either of subsidence, which has caused it to fall away from the
apparently continuous mass of strata within it on the north, or of some more extensive derange-
ment of the coast at this place.
III. a— White Rock Ledge. —The great ledge visible upon the shore at low water, to the solidity
of which the prominence of the White Rock (so long as it remained) was to be ascribed, rises
beneath the sea, about 200 paces to the east of the rock, and seems to be continued for a consider-
able distance in that direction. A series of conformable strata of sand-rock, concretional grit, and
slaty clay, here occupies the whole space between high- and low-water mark, for more than 100
* This stratum I did not see in these cliffs: but granular oxide of iron abounds in those on the
east of Hastings, and seems to be very generally diffused in a lower part of the series. The
grains which I have here called Pisolitic, seem to have existed originally in the form of iron
pyrites ;—of which substance globules of various sizes from that of pistol bullets downwards,
are still found on the sand-rock at St. Leonard’s. The origin of the ore of iron to which the name
of Pisolitic has been applied, is ascribed by Haidinger to the decomposition of pyrites.—Trans-
lation of Mohs’ Mineralogy, vol. il. p. 412.
Dr. Firron on the Strata below the Chalk. 167
paces; with a strike to about 20° east of south, and dip to the west of south: and this remarkable
_ group contains in some places pisolitic grains of reddish oxide of iron, disseminated in yellow
sand-rock, like that which is found in the strata beneath.
III. b.—The beds in the upper part of the cliff behind the Brewery are a continuation of part of
the group upon the shore (III. a.), and, like it, contain great numbers of the singular fossil which
has been called Endogenites erosa. They are probably the same with those of III. c. which rise on the
shore under the Marina at St. Leonard’s, of which an extensive section was exposed in excavating
the site of the church; and both groups are interesting, for their apparent identity with the Tilgate
strata, which have furnished to Mr. Mantell an almost inexhaustible store of extraordinary fossil
remains.
Beds of the Group (III. b.) in the Cliff on the North-east of the White Rock.
Ft. In, Ft. In.
1. Earthy brown sand-rock, about... .......- 2.6. see eee eee eee eee eee ee
2. A group, about 10 feet in average thickness, composed as below.
a. Sand in thin courses, alternating with clay, which includes Cyclades. ]
The sand passes into grit, and in some instances also abounds in
Cyclas media in the state of pulverulent carbonate of lime. From the
different hue of the sand and clay, the cross fracture is perceptibly |
striped in very thin layers; and in the darker beds the surfaces of the f
clay are often dotted with white specks, the sections of very small cylin-
drical cavities, now filled with very fine sand or clay, which seem to
have passed through several of the adjacent folia, vertically or obliquely
6. Thin courses of subcalcareous grit, alternating with bands of clay. The
grit is in small concretional masses, often not more than half an inch
in thickness, which thin off to an edge. On the surfaces adjoining the
lay are very mumerous Cyclades 0.220002. SP J
y. Flat, nodular masses of argillaceous iron ore, containing Cypris. In the
fallen debris are fragments, apparently from this place, which contain |: )
also clusters of Paludina elongata in great numbers ..............
5. Soft argillaceous sand-rock, alternating with thin layers of darker clay, é
and including some portions of iron ore...........-......4.. ae 2)
6
e. Alternate layers of grey sandy clay, and yellowish ferruginous sand-rock,
passing into grit, and including the remains of Endogenites erosa. }
This and the succeeding stratum very much resemble (b.) above ....
as in (6.). This bed contains Paludina fluviorum, and Cyclas media, in
g. Light greenish grey sand, passing into grit, and alternating with clay,
| 0
PUCALNMMOETS Re Pes eae. Ee Ai OS, OAL DAD tt
3. Yellowish sand-rock, with ferruginous stains, passing in some places into grit.. 3 0
4. Slaty clay, alternating with yellowish and brown sand, and including remains
of leaves and stems, in the state of lignite, generally about th of an
inch in thickness. The lignite is divided into rhomboidal portions,
separated by thin partitions of clay, which, when the coaly matter is
removed by decomposition, have a deceptive resemblance to organic struc-
ture. This group passes insensibly into (5.)........... HEISE tare \- ?
4
168 Dr. Frrton on the Strata below the Chalk.
Ft. In. Ft. In.
5. Uniform sand, with alternations like those described above, (2. 6. and 2. e.).
Continued nearly to the bottom of the cliff, where the rock is a fine uniform
white sand-rock, like that of the great cliff at Hastings.
The distance from the bottom of 5. to the base of the cliff, is about ....... 45 0
The total height of the cliff being........ about 65 0
The foregoing divisions are evidently arbitrary. In a general view, this section may be said
to consist of rather more than 50 feet of thinly stratified sand and clay, with grit in concretions;
including, at the upper part, a stratum of darker colour, about 12 feet thick, near the middle of
which the remains of Endogenites are found.
(83.) The rock composed of alternating layers of sand, and darker sandy
clay, No. 2. a. of the preceding list, constitutes a large proportion both of the
Weald clay and the Hastings sands; anda similar alternation of sand and
clay of different hues and consistency, extends upwards beyond the limits
of the Wealden, into the Lower green-sand. When the masses of the rock
are dry, the structure is less conspicuous, but it becomes beautifully appa-
rent when they are moistened. The delicacy and distinctness of the folia
which are then seen in the cross fracture of the beds, are very remarkable ;
the separate leaves being frequently as thin as paper, yet perfectly di-
stinguishable, from their different alternating shades of greenish grey ;
and commonly continued with great regularity for considerable spaces ;
a structure clearly indicating very tranquil deposition, such as might be
expected in a fluid suspending solid matter divided to extreme minute-
ness, yet subject to frequent changes at nearly equal intervals; which
may well be conceived to have taken place in the waters of a lake or estuary,
at different seasons, or during different conditions of the waters,—if it be
going too far in theory to suppose the minuter laminz to have been the pro-
duce of successive tides.
(84.) The continuity of the ledges of rock under the Marina at St. Leo-
nard’s, with those of the shore under the White Rock, is rendered more pro-
bable by the occurrence of the Endogenites erosa in both*. The principal
ledge at the former place is very conspicuous on the shore at low water, and
is one of the most remarkable geological features on the west of Hastingst.
The following are the beds of which it is composed:
* I did not myself see this fossil at St. Leonard’s; but Mr. Woodbine Parish, jun., informed
me that the specimen represented in fig. 8, Plate X1X., was obtained at the foot of the cliff around
the church.
+ These prominent ledges are precisely analogous to those which occur in the Hastings sands
on the south coast of the Isle of Wight, where several reefs of rocks run out almost directly into
the sea, and have obtained separate names from the inhabitants. On the Sussex coast they are less
conspicuous, from the more rapid dip towards the sea, and the obliquity of the strike to the line
of the coast; but many more such ledges do exist, between the flat near Pevensey and Cliff-end,
about midway between Hastings and Winchelsea :—see hereafter, (95.)
Dr. Fitton on the Strata below the Chalk. 169
Beds of the Group (III. c.) composing the Ledge on the Shore beneath St. Leonard’s.
1. Hard, subcalcareous, greenish grit, full of fossils; chiefly Cyclades, with Paludine, } 1 6
and some large Uniones ..+..++++eeeeeeeeeeeecseeeenee iveievorsushé 5 ois bie
A thick and nearly continuous stratum, very like the stone of Hollington about
24 miles north-west from Hastings; its structure, however, like that of the
White rock, is distinctly concretional. The top of the concretions, when ex-
posed and washed by the sea, exhibits beautifully the minute stratification of
the original sand; and the globular masses on the underside project into the
sand (2.) below. The stone is traversed nearly at right angles by veins of cal-
careous spar, and includes portions of trees, converted into lignite. It is asso-
ciated also with patches of a looser conglomerate, consisting chiefly of rounded
grains of whitish, nearly opake, quartz, including the teeth, scales, and bones of
fishes, and of a species of Trionyx?. The strike of this)stratum is about 10°
south of east, and the dip towards the west of south, at an angle of about 11°.
2, Yellowish sand-rock, abounding in impressions of Cyclades, and also resembling } Mtg
part of Hollington group ...+++-.+- Spsisitalefels) ois t.0,.cia en « <jo,shonenelotare ni oho: eieux
3. A band of slaty argillaceous iron ore .......+0. Sicjoieieasiencier sc ctakereee BHD COGOnE 0 «3
4, Slaty clay, with numerous shells, chiefly Cyclades and Cypris....... sjeunie/cleieia'ee! ye) O° 9
e Continuous band of iron ore; like 3, above....... eereratcheraiel aeiere wiehelchetoteseterelay axels OQ
Rotaliaboutec ortetetete sodocupobooo. 81
6. Slaty clay with Cyclades and Cypris............... sieia: slgialeimisteielsietsls)o « sivisie.c's
III, d.—The group last mentioned must be continuous with that in the height to the westward,
although the connexion is at present concealed; for a line from the point where the grit rises from
the shore, would reach the base of the vertical cliff near the church*,—where slaty clay, with grit
and sandrock, occupy a thickness, according to the quarrymen, of more than 70 feet. The same
strata then rise gradually westward, and disappear about 700 paces west of the church. Several
quarries, concealed from below by a terrace-like projection, have been opened for the extraction of
the grit near the top of these western heights: and a hard sparry conglomerate, immediately
beneath the more uniform stone, has afforded many of the Tilgate fossils; a large collection of
which, presented to the Geological Society by Mr. Woodbine Parish, includes specimens of bones
and teeth of the Iguanodon, scales and other remains of Lepisosteus, and shells of the genera Palu-
dina and Cyclas in profuse abundance. The cliff here may be about 90 feet in height, and its
base about 25 feet above low-water mark.
List of Beds composing the Group (III. d.) at the Church, St. Leonard’s.
Ft. In, VM bse
1. Soft sand-rock at the top of the hill (visible) ......... held het stedei stare G a
BPGECMISN Prey SANG. 6. ss ccccccsscess alatotel | <faliclcteicleiy ol cece ZO
* The dip, however, of the strata in this cliff, is not to the south, like that of the ledge under
the Marina, but northwards; so that it is not impossible that there may be here some local
derangement, though I saw no indications of it on the shore. I had, however, an opportunity, in
an early stage of the improvements at St. Leonard’s, of seeing what may have been a fault, in
the rising ground on the west of the Assembly Rooms, which was then opened in preparing the
foundations of some houses. The surface thus exposed was nearly at right angles to the coast,
and consisted of sand-rock, over greenish clay or Fuller’s earth, in regular strata, dipping north,
about 20° east: while immediately without, and separated by a distinct vertical line or crack,
was a mass of clay ;—which, however, may have been brought into that situation by subsidence, as
the place is close to the shore.
VOL. IV.—SECOND SERIES, Z
170 Dr. Firron on the Strata below the Chalk.
Ft. In. Ft. In
3. Reddish, and purple sandy clay ; thickness not ascertained.......... ”
Sub ivevandsgreyaslaby Clay, i Awol iataeteisve)> cic ete sjaielsielel evel olive ects) eerie 20 «90
5. Greenish Fuller’s-earth.......... eferavelorsienste ete ieieel keveles« oncosnace ye oO
Gh WE esihle oohanbcodiocorsouosmonG adcucoDSDGonwbosooO6aoseou) 3
7. Band of iron-stone ..... Sietete oa erwin rie cele cere) etansveversiaterere ster ete sietersveneore a Onmmmes 17 G
8. A band of ‘clay iron-stone and slaty clay ©.0..:02.-.scscecsecene san lOme to
9. Slaty clay approaching to clay iron-stone............-- aoouooucco §=©6 G 20 ~O
10, Firmer slaty clay including small flat nodules of iron-stone with numerous
Maree Gycladesy 66 eM eee eae colt ete ten cee ee ener 10) Oy
jSetlard!grit; about’. ..%0 1... sogass00056 Hrabooeissuaaedouss SovEeD Lis
ee Softesand rock Imi 3 (Or AnCOUNSES meleletel oteleletehetecolelenstelel oleleletcielenerclatsrate 2. 6
13. Firm sandy clay, with Cyclades ; firmer and more sandy at bottom.... $ 6
14, Yellow and reddish sand (or very soft sand-rock), in very thin alter-
nating courses..... e's, clo) 0) elallel ee vias’ s\n ieleVolieiotel(elela/s (olavelo/e\ allele! s/s ieie tes pL iG)
15. Soft sand-rock, resembling the last but of lighter colour. This seems to
go down to the base of the church. Visible, about............-. 9 0
16. A bed of firm sand-rock (immediately on the east of the church), about 2 0O
17. Thin beds of slaty clay; with interposed layers, or thin masses, nearly con-
tinuous, of clay iron-stone, including layers of Cyclades. Visible about 6 0
Total thickness (visible)..... nie eieyonela BARON ae
The strata in the roadside on the east of the church dip towards the east of south, at an angle
of about 10° to the horizon ; but behind the church the dip is 3 in 40 (or about 4°), towards the
north.
The following is an approximate list of the strata in the cliff on the west of the Sussex Hotel,
between the bottom of the group last mentioned (III. d.), and the White sand-rock IV. ; cor-
responding therefore to the strata on the east of the White Rock, beneath the group III. a., which
contains the Endogenites. The measures exceed the truth, but the proportions are probably correct.
ies LO WM SAC KOCK Wretelercuelsioteta clei s\eletsia sisterate shee leted ote fa/e)iofe aj el ojo loreietete let aeletenet el aE 40
2. Sand-rock with clay, including Cyclades, about ........... sb0sn654 oes ss oneal
3. Beds of darker hue, apparently consisting of clay and sand .........-. + one siete
4. Dark yellowish brown sand-rock .......eseeeeeeeee ov 0/6, « elu o)ejcle)s ola)ieiaiel aie
70
5
tom of the cliff, and is continued downwards. The femur of an Iguanodon was
. Very white sand-rock, or slightly coherent sand, occupies about 30 feet at the bot- |
30
found in this stratum ...... asererier sey siieleiieiel eta rereheerewererete eis) a oreteliereretonelenete wane
Totalvabout.-eeree oa | 00
I
n.
0
0
0
0
0
0
I1V.—In the space between the base of the cliff at the Brewery and the Castle-hill, all the beds
have been carried away. But the great white sand bed IV. a. & b. is itself visible at high-water
mark immediately below the middle point of the White Rock; and thence to the place where the
road to Hollington is cut through this stratum.
thick, it is continued with perfect uniformity of character to the top of Fairlight Down*.
From the Castle-hill, where it is at least 80 feet
* The massive beds of scarcely concreted sand around Tonbridge Wells,—on the Race-ground,
at Rusthall-common, and in the heights of Frant and Eridge-park, appear to be a continuation of
Dr. Frirron on the Strata below the Chalk. 171
IV. c.—The white sand-rock above supposed to be a continuation of that on the Castle cliff, pro-
bably rises on the shore under St. Leonard’s church, but is not visible in the cliff, till it reaches
a spot on the east of the Sussex Hotel, where caves have been cut in the mass of almost uniform
sand, not to be distinguished from that of Hastings. It would be very desirable to ascertain by
experiment whether marine salt exists in this deposit.
V.—Immediately below the sand-rock (IV.), at the western extremity of the Castle rock, is a
thickness of about 35 feet, of dark brownish, tough, sandy clay, including lignite in considerable
quantity, some of the continuous pieces being several feetin length. This group goes down to the
level of the road or street ; and thence to low water mark, a space about 20 feet in thickness is
concealed. But under the Parade on the east of Pelham-place, a floor of grey sand-rock, is exposed
at low water, the strike of which seems to be nearly from east to west. It includes crusts and
patches of brown oxide of iron ; and is traversed by two sets of cracks, one running nearly north
and south, the other from the north of east to south of west, which divide the surface into nearly
rhomboidal portions, with angles of 72° and 108°.
VIL.— Cliffs on the West of St. Leonard’s.—The line of the coast at St. Leonard’s coincides with
the strike for about 200 paces west of the arch at the entrance to that place; and the strata at the
water level appear to be horizontal; but about 400 paces west of the Sussex Hotel, the heights
turn inland towards the north of west; so that the strata in the retiring portion of the cliff are lower
in the series than those upon the shore. They agree with those which are visible at low water be-
neath the town of Hastings, and with the lower strata in the cliffs around the shallow bay, or cove,
at the Lover’s Seat.
VII. a.—The cliff west of the Church is continued for some distance at an uniform height of
about 100 feet. It becomes lower in approaching Bopeep; and at a point where it turns inland,
between 200 and 300 paces east of the Martello Tower No. 39, is a floor of sand-rock, at low-
water mark, full of grains of oxide of iron, like that of the coast to the eastward; the strike being
towards the east about 25° south; and the dip east of north, at an angle of about 11°. The upper
part of the cliff at this place, which is about 40 feet high, is composed of brown sand-rock, in beds
from 2 inches to 6 in thickness. A grass-covered height, of less elevation, occurs immediately on
the west of Bopeep, and the rock exposed there to a thickness of about 10 feet, consists of reddish
sandy marl (VII. a.), not distinguishable from the Red marl of Devonshire. A low flat hill about
300 paces west of the Tower No. 40, consists for about 20 feet at the top, of sand alternating with
clay, in beds dipping very gently to east of north.
VII. 6.—At the east end of the cliff at Bulverhithe, on which stands the Tower No. 43, the
beds dip regularly about east 30° north, at an angle of about 1°. Thence, along the shore, to the
Tower upon Galley-hill (No. 44.), strata of reddish sandy clay or marl, variegated with light
tea-green, are very well disclosed, declining, towards the east, at an angle between 2° and 3°:
and above these coloured marls, is brownish sand-rock, about 50 feet thick.
this stratum of Hastings. On the north of those great beds, and above them, is a group com-
posed of thin, alternate beds of sand-rock and slaty clay, in many respects resembling that of the
Brewery near the White Rock. These upper beds are quarried at Huntley’s Farm, about a mile
west of the northern entrance of Tonbridge Wells; where they abound in Cyclades, Paludine, and
Cypris Valdensis (C. Faba of Min. Conchology), and include the remains of several plants, among
which are Sphenopteris Mantellii, and a new species of fern, represented in the wood-cut at p. 181.
The relations of the strata at this place, and in the tract on the north of it, towards the valley of
the Weald, are well deserving of attentive examination: I am indebted to the Rev. Mr. Pope of
Tonbridge Wells, for having pointed them out to me, and for a collection of specimens obtained
there by himself.
z2
172 Dr. Fitton on the Strata below the Chalk.
On the west of Galley-hill, the strata in the banks, which scarcely can be called cliffs, are in-
clined slightly to the west of south; and the flat shore, near Cowden Point, consists of beds of clay
and sandy clay, varying in colour from dark to bright blue, declining very gently towards the
south-west, and extending outwards to some distance under the sea, with a strike towards a point
about 16° south of east. Under the Martello Tower, No. 51, about four miles west from Galley-
hill, is sand-rock, with ferruginous seams, and thin alternating beds of clay, slightly inclined to the
west; from their situation not improbably one of the groups subordinate to the Weald-clay men-
tioned by Mr, Martin.
(85.) Endogenites erosa.—In cutting down the cliff on the east of the
White Rock, immediately within the site of the new Brewery, large sur-
faces of the several strata were successively laid bare ; and I was so fortunate
as to visit the place when one of them was exposed, which contained a great
number of the singular fossil bodies to which the name Kndogenites erosa
has been given, and to see some of them in their original position before
they were disturbed. ‘The workmen assured me that the fossils had been still
more numerous in a portion of the same strata cut away not long before.
The place in the series, of the strata which include these fossils, has been already mentioned
(p. 164—8.). I observed but one line in the face of the cliff which seemed to afford them, about
6 feet from the top of the group ITI. 6. (81.) and (82.), which was about 10 feet in total thickness.
The workmen told me, however, that some were afterwards found at a short distance below, where
the strata were still nearly the same. I did not find any specimens of the fossil upon the shore ; but
fragments are frequently washed up by the sea in the neighbourhood of this place ; and I saw a very ©
large specimen in the face of the bank, on the side of the road over Cuckoo Hill, which joins that
from Hollington to Hastings. Mr. Woodbine Parish obtained one, (Plate XIX. fig. 8.), which was
dug out in his presence near the Church at St. Leonard’s. Their occurrence at Tilgate Forest, where
they were discovered by Mr. Mantell, has been mentioned in the Geological Transactions and in his
own publications*; and Mr. Martin mentions the Endogenites, as having been found near Mulsey,
in Western Sussex, in the first course of sand with reddish clay, subordinate to the Weald-clay,
and above the Sussex marbleft. There can be little doubt that when the corresponding beds in
other parts of the Wealden district have been examined, they will be more extensively discovered.
The rapid change of character in the beds of this formation appears from the fact, that the
great concretions of grit, several feet in length, and 2 or 3 feet in thickness, which are found upon
the shore to the westward, do not occur in this cliff, though not more than 200 paces distant ; their
place being apparently supplied, in the strata above those which include the Endogenites, by nodular
masses of hardened sand-rock. ‘The bed III. b. 2. e. (p. 167.) which includes these fossils, passes
both above and below into the adjacent strata, but has in general a darker hue. ‘The fossils were
closely enveloped in a mass of slightly coherent sandy clay ; and I was enabled, with care, to
preserve some specimens, (one of which is represented in Plate XIX. fig. 4. a. and b.) with part of
the surrounding rock still adhering, as a proof that the coating of coal by which the nucleus was
invested had never been of greater thickness, and that the whole of it was retained.
(85.) All the specimens of this singular fossil which I saw, lay with their
* Geol. Trans., 2nd Series, vol. i., p. 423;—and Mantell’s Fossils of Tilgate, p. 54.
+ “ Memoir” &c. p. 41, note f{.
Dr. Firron on the Strata below the Chalk. 173
longer diameter and their flatter surfaces in the horizontal position. Their
appearance when first uncovered by the removal of the rock above, was
that of elongated and flattened elliptical bodies, tapering at both extremities ;
as represented in fig. 1. of the subjoined wood-cut, ‘They consist of two
distinct portions ; a stony nucleus, of a dark brownish grey colour, with a
very slight tinge of purple; and a crust or case, in the state of lignite,
which has externally a nearly uniform surface, and varies in thickness, in
different specimens, and in different parts of the same specimen, from
about =}; to+aninch. This crust becomes thicker near the extremities of
the nucleus, and, in many instances, extends considerably beyond it, in a sort
of appendage at both ends; but in other specimens of smaller size these
appendages do not appear to have existed. ‘The annexed wood-cut explains
the structure of one of the largest specimens, and shows the relative propor-
tion of the parts ; and the figures in Plate XIX. show some of the principal
varieties of form which the fossil has hitherto presented.
Fig. 1 of the wood-cut on this page represents the external appearance of the entire fossil, as
seen from above ; the situation of the nucleus being indicated by an obscure dotted line. Fig. 2
is a longitudinal and vertical section, on the axis or line a, b; and fig. 3, a transverse vertical
section, on the line c, d; showing the proportion of the coating to the nucleus,
The figures in Plate XIX., which are on a scale of one sixth, in diameter, of the natural dimen-
sions, are intended to represent some of the forms of the complete fossil, and of the nucleus when
divested of its coating of coal. They are, however, from necessity so much reduced, as to con-
vey but a very imperfect impression of the bulky objects which they represent.
Fig. 1 represents the greater part of a very large nucleus, of which only one of the extremities
seems to be wanting. The remaining extremity is of irregular shape, as if it had been broken;
and the specimen is much compressed in the middle. Fig. 2 is a nucleus apparently complete,
tapering towards one extremity, nearly as may be supposed to have been the case in the part
which is wanting in Fig. 1. Fig. 3, a and b, are horizontal and side views of a much smaller
specimen, still retaining its coaly covering, with part of the smooth surface, hereafter mentioned.
Fig. 4 is a larger specimen, with some of the sandy clay in which it was imbedded still adhering,
the laminze of which are curved as if they had adapted themselves to its form. The specimen
174 Dr. Firton on the Strata below the Chalk.
retains the greater part of its covering of coal, which has a smooth outer surface, of a light
brown or drab colour: and at the lower part, a portion of the coal has been drawn away from
the nucleus, apparently by the contraction of the investing matter to which it strongly ad-
heres. One end of the specimen, where a portion has been accidentally broken off at b, shows
P P y
the proportionate thickness of the coating to the nucleus within. Fig. 5 is a smaller nucleus,
nearly complete, very short in proportion to its width. Figs. 6 and 7 are sections of speci-
mens broken across, and exhibiting the flat surface of the fracture in the nucleus, with the
proportion of the coaly covering, and the porous structure of the nucleus. Fig. 8 is the nucleus
of a large specimen found by Mr. Woodbine Parish, in the strata near St. Leonard’s Church.
It is remarkable for the compressed appearance of one extremity, and seems to have been
originally longer in that direction. It still retains a portion of the investing coal, and of the
smooth outer surface of that coating, but the greater part has been removed or disturbed.
Fig. 9 is taken from a specimen from Tilgate Forest, presented to the British Museum by Mr.
Mantell, which is remarkable for its length, its nearly cylindrical figure, and the acute tapering
of the extremity. The superficial furrows also, in this specimen, are deeper and much larger
than in the greater number of the nuclei found near Hastings *; but inthis respect it is approached
by Figs. 1 and 2. Fig. 10 represents rather more than one half of a complete nucleus, of the
natural size: the upper surface of a, of which fig. b is a separate representation, showing the
appearance of a fracture on the line of the longer axis.
(86.) The size of the different specimens varies considerably. The largest
that I saw in its place, and from which the foregoing wood-cut was taken, must
have been in the whole full nine feet long; but there were portions of other
nuclei of greater size, among the fallen specimens previously dug out. The
lignite at one extremity was three feet in length; the nucleus 43 feet; and the
workmen assured me that the coal at the other end extended to about 18
inches. ‘The width in the middle was 12 inches, and the greatest thickness
4 inches. Another specimen, which had been for some time exposed to de-
composition, was about 73 feet long ; the nucleus about 52 feet, with about
12 inches of lignite remaining at each extremity ; and from these dimensions
there seem to have been gradations down to a few inches in length. The
nucleus of the smallest specimen that I obtained, which is represented, of its
natural size,in Plate XILX., fig. 10, is not more than 3 inches long, and about
2 inches wide; yet the external figure is complete, and the internal tubes are
not smaller than most of those in the largest masses.
(87.) The original form of this vegetable was probably cylindrical ; and
that shape is still retamed in a large specimen of a nucleus from Tilgate
Forest, now in the British Museum ; Plate XIX., fig. 9: but in the majority
of the specimens the figure has evidently been compressed, and the section
is now an oval variously modified; figs. 6,7, 10. In those represented in
* Since this sheet has been at the press, I find, on examining several other specimens in
Mr. Mantell’s museum, that the uncompressed figure and greater size of the external tube-like
furrows, are general characters of this fossil at Tilgate Forest.
Dr. Firron on the Strata below the Chalk. 175
figs. 2 and 9, the extremity is more acute than in the greater number of the
specimens. In a few instances (as in fig. 8, and less obviously in figs. 2,
and 1,) the nucleus seems to have been suddenly reduced in thickness near
the broader end; but no specimen of this form was observed zn situ. None of
the specimens exhibited the tapering figure, somewhat like that of a ninepin,
represented in the engraving in the Geological Transactions* ; but many of
the broken and worn fragments washed up on the shore near the White Rock
had acquired some approach to that form. There was not, in any of the spe-
cimens, the slightest indication of lateral branches from the main body ; but
they all lay as if they had been distributed without connexion in the stratum
in which they were found.
(88.) The coaly covering did not, in any instance, show traces of or-
ganic structure; it burned with a slight flame when thrown upon hot coals,
and in the flame of a candle became white, and was reduced in bulk without
losing its form. In some of the fresh specimens it was coated with a thin
crust, of a light brownish or drab colour, with a very slight glistening lustre ;
apparently consisting of compressed clay. This is represented especially in
figs. 4, a and b, and partially shown in figs. 3 and 8.
(89.) The internal structure of this fossil has been partially described and
represented in the Geological Transactions+, by the Secretaries and a Com-
mittee of the Members. I am enabled to add some further particulars to
what is there stated, through the kindness of my friends Mr. Brown and
Mr. Stokes: the former having lent me the specimen represented in Plate
XX., fig. 3., and given directions for making the slices, figs. 1. and 2.; to
which Mr. Stokes was so good as to add a very thin slice, represented in figs.
4.and4.a. The vermicular cavities or tubes, of which a longitudinal section
is represented in fig. 1., and a transverse section in fig. 2. and 4., are all coated
within with transparent quartz crystals, the summits of which are discernible
with a lens; and in some cases the cavity of these tubes was partially oc-
cupied by exceedingly minute crystals of quartz, either detached in the
state of sand, or intermixed witha flocculent coaly matter. The transverse
sections of these tubular cavities exhibit a similar change of form, from circular
to elliptic, to that shown by the entire plant. In the greater number of cases
no trace of truly organic conformation could be detected with the microscope
in these sections ; but in two specimens a distinct indication of the original
vegetable structure was to be seen. These are represented in Plate XX., fig's.
3.and4. The former figure, drawn from the extremity of a solid and opake
* Second Series, vol. i. Plate 48.
t Second Series, vol. i. Plates 46 and 47: and Mantell, Tilgate Fossils, Plates 2 and 3.
176 Dr. Firron on the Strata below the Chalk.
mass, a little decomposed, shows, within a cavity, a somewhat circular band,
exhibiting organic structure, which is probably tubular* ; and the same kind
of structure is indicated in the other figures, 4. and 4. a, which are taken
from a transparent slice belonging to Mr. Stokes; the latter being a more
highly magnified portion of fig. 4.
(90.) Fossils of the Wealden—The catalogue of the organic remains of
Sussex, published by Mr. Mantell in the last volume of these Transactions,
and which he has stated to have been intended to accompany these pages 7,
renders it unnecessary to insert here the fossils of that portion of the Wealden.
The following list, therefore, will contain such species only as have been
found in the tracts described in the preceding pages of this paper, or as do
not occur in Mr. Mantell’s catalogue: and I have been enabled to add se-
veral species to those of my own collection, through the kindness of Lord
Greenock, Mr. Hills, Mr. Martin, and especially of Mr. Mantell.
List of Fossils of the Wealden, in Kent, Surrey, Hants, and Western
Sussex tf.
Bulla Mantelliana. Pl. XXII. f. 3. With Unio antiquus, within a cavity in the grit
of Tilgate Forest: M.
Corbula alata. Pl. XXI.f. 5. Pounceford near Burwash, Sussex: M.
Cyclas angulata. Pl. XXI.f.12. Weald clay: M.
C. maor. Pl. XXI. f.13. Weald clay, in nodules of clay iron ore, with Cypris
Valdensis and Paludina elongata, Hythe (Kent): F. With Cypris, fish-bones, and
pyrites, in iron ore; upper part of the Weald clay, near Pulborough: Martin.
Henhurst, near Ockley, Surrey; in Weald clay. With Paludina fluviorum in
thin bands of very hard ferruginous calcareous grit, passing into ferruginous
sand ; near the top of the Weald clay on the west of Leith-hill, Surrey: F.
Cyclas media. (Cyrena media, Ann. of Phil. Vol. VIII. p. 376. Cyclas media, Min..
Con. Tab. 525. f.2.) Pl. XXI.f. 10. So generally diffused throughout the
Wealden strata that the specification of localities is hardly required. The fol-
lowing are some of the circumstances under which this shell has been found.
In coarse grit near the top of the Weald clay, at Atherley, south of Tanhurst,
Surrey. In very compact uniform grit, with thin carbonaceous vegetable im-
pressions,—shell calcareous : also in very fine-grained micaceous sand-rock, with
* In this figure, from the greater difficulty of representing the opake object, the partitions between
the dark spots which denote the cavities of the tubes, are much too wide: the real proportion of
the cavity to the partition is more correctly expressed in fig. 4. a.
’
t “ A Tabular Arrangement of the Organic Remains of the County of Sussex.” Geological
Transactions, 2d Series, vol. iii. p. 215.
+ In this list the letter M. denotes that the specimen is in Mr. Mantell’s collection; F. in that of
the author.
Dr. Firron on the Strata below the Chalk. 177
Cypris; impressions only, without traces of the shell: Hollington, near Has-
tings. In nodules of clay iron ore: Cliffs west of St. Leonard’s. In shale,
called “Shab,” alternating with beds of limestone called ‘‘ Greys,” (a stone al-
most entirely composed of thin shells): Limestone pits north-west of Battle: F.
With Paludina fluviorum, in bluish compact and sparry limestone, (“ Sussex mar-
ble”); Daniel’s Water, Kent. In sand-rock near Tunbridge Wells: M. At the
top of the Weald clay, mixed with bivalves of the Lower green-sand; Stopham
brick-yard near Pulborough: Martin,
Cyclas media. (Young.) Plate XXI. f.9. Hastings sand, Hollington, in hard grit ;
shell converted into carbonate of lime: F. Etchingham near Robertsbridge,
Sussex: M.
——. (A gibbose variety.) Plate X XI. f.11. Penhurst pits, in a bed of lime-
stone, about 3 inches thick called ‘“‘ Top-greys’’: F.
C——. A wider species than media. Hastings sand, Hollington: F.
C—— membranacea. (Cyrena membranacea, Ann. of Phil. 1824. viit. p. 376.) Cliff west
of St. Leonard’s, in sandy shale, with Cypris: F. Weald clay, Shipley, near
East Grinstead, Sussex, with a spiral univalve (Potamides?): M. Limestone
pits near Battle: F. Penhurst, Ashburnham, and Pounceford: M.
C—— subquadrata. Plate XXI.f.8. Hastings sand, East Cliff, Hastings, in soft,
fine, sandy clay, not effervescent: also cliff west of St. Leonard’s: F.
C——. One or two other species, probably new, occur in the Weald clay, at Ather-
ley, Surrey: F.
Cypris granulosa. Pl. XXI. f. 4. In ferruginous sand, Tilgate Forest: M.
C.
C tuberculata. Pl. XXI.f.2. Frequently black. With Cypris Valdensis and
Paludina elongata, in nodules of clay iron ore, near the top of the Weald clay :
found by Lord Greenock, at Hythe
C. Valdensis. Pl. XXI.f. 1. (C. Faba, Ann. of Phil. 1824, vir. p. 376.; Min.
Con. Tab. 485.) This fossil occurs in such numbers in every part of the Wealden
group, that it may be considered as characteristic of the formation; and being
found in all the places where these strata have been hitherto observed, the speci-
fication of localities would be superfluous. Its profuse abundance may perhaps be
accounted for by the fact, that the animal which inhabits the valves or crusts, sheds
them periodically*. The Cypris to which the specific name of “‘ Faba,” was given
by M. Desmarestt, occurs in strata probably superior to the chalk; and though
the characters of the valves nearly approach to those of the Wealden Cypris,
M. Deshayes is of opinion that it probably constitutes another species{. On these
grounds, I have thought it expedient to adopt a new specific name for the fossil
represented in Pl. XXI. f.1.; and that of Valdensis (of, or belonging to the
Wealden) is intended to indicate both its geological or stratigraphical position,
and the local situation of the tract in which it has hitherto been found in the
* Lyell “ Principles,” &c., 3rd edition, vol. iv. p. 98.
+ Brongniart and Desmarest, ‘‘ Crustacées Fossiles,” p. 141, Pl. XL, fig. 8.
t “ Coquilles Characteristiques,” p. 255, Pl. 10. figs. 4. aud 5.
VOL. IV.—SECOND SERIES. 2A
178 Dr. Firron on the Strata below the Chalk.
greatest abundance. A description of the several species of this genus repre-
sented in the annexed plates will be found hereafter, in the Appendix.
Melanopsis ? attenuata. P\. XXII. f.5. (Melania attenuata, Ann. of Phil. 1824, v111.
p. 376.) Inthe Hastings sands, Hollington: F. Pounceford: M.
—? tricarinata. Pl. XXII. f. 4. (Melania tricarinata, Ann. of Phil. ibid.)
Pounceford near Burwash, Sussex: M.
Mytilus Lyellii. Pl. X XI. f.18. Beds below, or at the bottom of the Hastings
sands, near Battle: F. In slaty clay, near Pounceford: Messrs. Lyell and
Mantell. ;
Neritina Fittonii. (Mantell ; South-East of England, p.248.) Pl. XXII. f.7. Casts
in the grit of Tilgate Forest: M.
Ostrea ? (a thin-shelled species). Sand-rock of the Hastings sands, west of St. Leo-
nard’s: F.
Paludina carinifera. (Min. Con.) Hastings-sands, west of St. Leonard’s; below the
White Rock, Hastings; and at Hollington: F. In Septaria, at Resting-oak Hill,
near Lewes: M.
M.
P elongata. (Min. Con.) This fossil is very generally diffused in the Weal-
den strata. It occurs in nodules of clay iron ore, near the top of the Weald clay,
at Hythe: F. In hard blue grit, with Cypris Valdensis and C. granulosa? In
the grit of Tilgate Forest: M. Near Ockley, in Surrey: F.
P fluciorum. (P. vivipara, Min. Con.) One of the most abundant univalves of
the Wealden. On compact calcareous beds in the Weald clay; Bethersden and
Daniel’s Water, Kent. At Henhurst, Surrey; in ferruginous sandstone. In
concretions of grit in the Weald clay, very large. At Forest-green, and near
Ewhurst, Surrey; near Ockley, Surrey, with Cypris Valdensis, in beds of
“Forest marble.”” South of Den-park, Sussex: F.
yb Sussexiensis. Pl. XXII. f.6. Resting-oak Hill, near Lewes, Sussex: M.
P. two or more other species, probably new, occur at Tilgate: Mantell.
Potamides ? With Cyclas media, in shale, alternating with limestone; pits north-west
of Battle: F. In Weald-clay, East Grinstead: M.
Psammobia? Tellinoides. Pl. X XI. f. 6. With Cyclas in limestone; Pounceford near
Burwash, Sussex: M.
Tornatella Popii. P}. XXII. f.8. Lenthington (pronounced Langton) Green, near
Tonbridge Wells, in dark brown ferruginous sand-rock, with Unio, Cypris, and
Cyclas: Rev. Mr. Pope; and M.
Unio aduncus. Min. Con. Bolney, near Pulborough: Martin. Near Cuckfield,
Sussex: M.
U— antiquus. Min. Con. Weald clay, near Pulborough: Martin. Tilgate Forest,
very frequent: M.
U— compressus. Min.Con. Weald clay, near Pulborough: Martin. Tilgate Forest :
M.
U— cordiformis. Min.Con. Tilgate: M.
U— subtruncatus. Pl. XXI. f.15. With Cypris Valdensis, Cyclas media, and Tor-
Dr. Fitton on the Strata below the Chalk. 179
natella Popii? in dark brown ferruginous stone, Lenthington-green, near Ton-
bridge Wells. Also at Tilgate Forest: M.
Unio Gualterii. Pl. X XI. f.16. Discovered by Mr. Walter Mantell in the dark brown
ferruginous sandstone of Lenthington-green, near Tonbridge Wells: M.
U— Mantellii. Pl. XXI. f. 14. In calcareous grit, passing into ferruginous sand,
near the top of the Weald clay ; Atherley and Henhurst, Surrey: F. Tilgate : M.
U— Martinii. Pl. X XI. f.17. Upper part of the Weald clay, near Henhurst, Surrey:
Martin, and F.
U— porrectus*. Min. Con. Weald clay, near Henhurst and Atherley, Surrey: F.
Large specimens, with Paludina fluviorum and Cyclas media, eccur in the cliffs
west of St. Leonard’s, in firm bluish grit: F. In sandstone, Tilgate Forest: M.
Reprives. The reptiles of the Weald clay and Hastings sands in Sussex, nearly all
of which have been discovered by Mr. Mantell, have been so fully treated of in
his various publications, that I shall refer to those works for an account of them,
and here only enumerate their names, with some of the chief places of their oc-
currence. The remains, however, of oviparous quadrupeds seem to be dispersed
throughout the whole of this formation, though hitherto found principally in the
Weald clay and the upper part of the sands beneath it: it is from this latter
situation, in the grit and sand-rock of Tilgate Forest, that the greater number of
Mr. Mantell’s specimens were obtained.
Trionyx Bakewelli. (Mantell, S.E. of England, p.255.) Tilgate Forest.
Emys, (species unknown.) Same place.
Chelonia. Ditto.
Saurians,—of at least six genera.
Crocodile. Remains of two, if not of four, species. (Ibid. p. 265.)
The teeth, scales, and some of the bones, are mentioned by Mr. Mantell, as oc-
curring at Tilgate. A vertebra, which was considered by the Baron Cuvier,
as belonging to this genus, was found in the strata of shale and limestone at the
bottom ofthe Hastings sands, near Briglitling, Sussex: F.
Phytosaurus cylindricodon. The teeth: Tilgate Forest. (Mantell, S.E. of En-
gland, p. 292.)
Plesiosaurus. Vertebra, teeth, and other remains: Tilgate. (Ibid. p. 281.)
Megalosaurus Bucklandii. The teeth, (supposed) ribs, and vertebra. Tilgate
Forest. (Ibid. p. 260.)
Hyleosaurus. (First described by Mr. Mantell, in a paper read before the Geo-
logical Society (Proceedings, &c. Vol. 1. p. 410.), and since published in his
Geology of the S. E. of England; p.289, &c. Plate V.) The remains were
found in Tilgate Forest.
Iguanodon. (Mantell, Philos. Trans. 1825, p. 179.) The remains of this mon-
Several indistinct specimens of this genus, including probably some new species besides
those above mentioned, have been found at Henfield and Atherley, in Surrey, by the Author;
and near Pulborough, by Mr. Martin.
2a2
180 Dr. Firton on the Strata below the Chalk.
strous reptile have hitherto been found chiefly in the upper part of the Has-
tings sands at Tilgate Forest: but very large bones, belonging, as it now
appears, to the same animal, have been obtained much higher up in the Weal-
den series, at Loxwood, and Headfold wood, in Western Sussex*: and very
recently, even beyond the limits of the Wealden group, among the lower
strata of the Green-sand, near Maidstone, (as already intimated, p. 132; note +):
they occur also as far down as in the Great Sand-bed of the cliffs on the
coast near Hastings, where that stratum reappears on the shore west of St.
Leonard’s. Iam requested by Mr. Mantell to state, that the mass of remains
from Maidstone confirms the appropriation to this reptile, which he had pre-
viously made, of other bones of great size found detached, and in different
places; and that, among other new points in the osteology of this extraordinary
creature, the Maidstone specimen has enabled him to ascertain that certain
phalangeal bones which approach to the mammalian character,—with flattened
claw-like extremities, resembling those of land-tortoises,—belong to the hind
feet of the Iguanodon; while the fore feet of the creature appear to have been
long and slender, like those of the recent Iguana.
In addition to the Saurian remains which can be referred to distinct genera,
there are also in Mr. Mantell’s collection, detached bones, probabiy belonging
to new or nondescript reptiles.
Birps. Fragments of some long bones found at Tilgate, and at first supposed to
have belonged to Pterodactyles, appear to be really those of a bird, probably a
species of Ardea. (Mantell, S. E. of England, p. 283.)
Fisues. The fishes of the Wealden, especially of the two upper members, have
hitherto been imperfectly collected; and it still remains to be determined to
what species of this tribe many of the remains which frequently occur in the
Weald clay are to be referred. All the specimens from this formation in the col-
Jections of the Geological Society, of Mr. Mantell, and Mr. Martin, have been
recently examined by Mr. Agassiz, with a view to his work on Fossil Ichthyology,
now in progress ; and the following are some of the genera to which he has re-
ferred them.
Pycnodus microdon. Teeth. (Represented in Mantell’s Tilgate: Pl. XVIII. f. 26,
and 27.)
Hybodus grossicomis. Teeth. (Ibid. Pl. V. f. 14, and XV. f. 2.)
————-. Two other species, not yet figured.
The dorsal defences referred by Mantell to a Silurus, (Ibid. Pl. X. f. 4,
and f.6.), Mr. Agassiz considers as belonging to an Hybodus.
Lepisosteus. (Lepidotus, Agassiz.) The remains of one or more species of this
genus have long been known, as diffused throughout the Wealden ; in every
part of which detached scales and fragments of the scale-covered surface are
very commonly found. The Teeth are represented in Mantell’s Tilgate fossils,
P]. X. f. 2.; the scales, in Pl. X. figs. 3,4, 15, and 16; and from an examination
* Murchison: Geol. Trans. 2nd Series, vol. ii. pp. 104, 105.
Dr. Frrron on the Strata below the Chalk. 18]
of these, and of some very fine specimens of the head and fore part of the fish,
belonging to Mr, Martin, Mr. Agassiz has been led to divide the genus into
two species, distinguished by the forms of the teeth.
Coprolite,—(or, more correctly, masses of phosphate of lime approaching to the
form, and possessing many of the chemical characters of Coprolite,) has been
found by Mr. Martin in cavities on the surface of the Weald-clay, at Stopham
brick-yard, near Pulborough, but so mixed with fossils of the Lower green-
sand that the whole may probably have belonged to that formation. The re-
cent discovery of the Iguanodon, near Maidstone, forms an additional link of
connexion between those two formations; and coincides with other evidence
which indicates the probable continuity of their deposition.
REMAINS OF PLANTS.
A Cone ofan unknown species, (Pl. X XII. f.10.), remarkable forthe double prominence,
or ridge, in most of the scales; (see Appendix No. 1.) : ina mass of hard, greenish
grit. From a quarry on the estate of Henry Shirley, Esq., at Pippingford in
Ashdown Forest, very near the highest point of the ridge of the Hastings sands.
Endogenites erosa. (Plates X1X.and XX.) Described in the preceding sections (85.)
to(89.). Tilgate Forest: M. Coast west of Hastings: F. In the first course of
sand in the Weald-clay, near Mulsey’s Farm, about 24 miles north-east of Pul-
borough, on the main road to London: Martin.
Sphenopteris gracilis : represented in the subjoined wood-cut. See the descriptive note
in the Appendix A, p.349. From beds of sandrock and slaty clay, in the quar-
ries at Huntley’s Farm near Tunbridge Wells, above the great bed of White
sandroek: Rev. W. L. Pope.
1 BA
iy Y7)
= SN vi i pn | i B, 2 <
Va USS. bio,
182 Dr. Firron on the Strata below the Chalk.
Tae Istz or Wigur.
(91.) The general relations of the strata on the southern coast of the Isle
of Wight, have been described by Mr. Webster* with so much ability, that
little was left to succeeding observers but the task of filling up details, and of
supplying some facts respecting the lower members of the series, which did
not fall within the immediate scope of his inquiries. Having already pub-
lished a general account of these lower strata in another placef, I shall here
give some farther observations on what is commonly called ‘‘the back,” or
south side, of the island.
(92.) As the chalk passes entirely across the Isle of Wight, nearly from
west to east, in a narrow ridge composed of vertical strata, and again
invests a pordon of the southern promontory of the island, with a cap of
almost horizontal beds, at present detached from the central ridge and ex-
tending nearly to the sea,—the result is, that two very distinct sections of the
vertical chalk and inclined strata beneath it are disclosed upon the shore,
at the extremities of the central range; and again, two other sections, in
which the same strata are prolonged from beneath the horizontal chalk, on
each side of the promontory that projects towards the south, so as to meet
the continuation of those which rise from the middle of the island, and with
them form very flat curves. The coast thus exhibits a series of sections of
almost unequalled richness and variety : and though the general characters of
the strata are well known, there is still quite enough to be learned in this
most interesting geological region, to repay such detailed researches as have
been of late years devoted to some other portions of England, but whieh those
only who reside near the place can carry on with complete success.
(93.) The Section, Pl. X.a. No.7. (which is on the scale of the Ord-
nance Survey), shows the general order of the strata on the southern coast of
the island, and, with the aid of a good map, will enable the reader to follow
the ensuing detail. In the lower of the two lines, the heights are on the same
scale as the horizontal distances.
Chalk.—The relations of the lowest beds of the chalk are best seen, on the west, at Compton
Bay ; and on the east, in the cliffs under Bembridge Down; both sections exhibiting admirably
the passage from the white chalk to the Upper green-sand. Large portions of the chalk are pre-
* «Tetters to Sir Harry Englefield,” &c. 4to. 1816.
+ “ Annals of Philosophy,” Nov. 1824, p. 367, et seq.
{ The map annexed to Mr. Webster’s Jetters, in Sir H. Englefield’s volume, (Plate 48.) though
less accurate geometrically, gives many names, and much information useful to the Geologist,
which are not to be found in the Ordnance Survey.
i
|
Dr. Firron on the Strata below the Chalk. 183
served also at the top of the higher Downs, on the south of the island, resting on a plateau of the
Upper green-sand ; and the lower beds of the chalk are in many places visible in descending from
these heights, as from Niton to the undercliff, and above Old Park, on the south-west of Wol-
verton. The gradation of hue and texture, from the whitest chalk,—through various shades
of grey, and various degrees of softness, to the state of bluish marl, resembles precisely what is
observable in the same part of the series at Beachy-head, on the shore near Folkstone, and on
the opposite coast of France, under the cliffs of Blanc Nez.
The central ridge, or anticlinal line of the chalk, it will be remarked, is neither continuous nor
rectilinear ; but is divided, about the middle of the island, between Carisbrook and Shorwell, by a
tract of irregular ground, intervening between two nearly parallel branches of the chalk range about
three miles apart. The first, or southernmost, of these branches runs directly from the Needles to
Brixton-down; the more northern from Arreton-down to Bembridge-down and Culver-cliff. The
course of the principal streams of the island is transverse to that of the central chalk range: the
‘river Medina, which nearly bisects the island from north to south, rising high upon the sands, about
Stroud Green on the south of Kingston, and running almost directly northward to the estuary at
Cowes. The other principal stream, the Eastern Yar, springs beneath the southern chalk, about
Whitwell, not far from Niton; and after a tortuous course, instead of joining the sea in Sandown
Bay, it cuts through the ridges of the green-sands and the chalk, between Yaverland and Brading.
The egress of the streams, therefore, is here analogous to that already described in Kent and
Sussex: and this effect may not improbably be ascribed, in both cases, to fissures, by which the
lines of drainage were in the first instance determined.
Upper Green-sand.—This formation is but partially disclosed along the base of the central ridge
of chalk; but is distinctly seen in the sections at Compton-bay, and on the south of Bembridge-
down, and in several places along the escarpment of the underclitf*; the course of which, it is to
be observed, is not exactly parallel to the anticlinal ridge, but oblique to it, running towards a
point about 17° south of west. The total thickness here, in some places approaches to 100
feet, and on an average is not much less than 70 feet: its step-like projection beyond the
ehalk, as in Western Sussex, is conspicuous in several places, especially beneath St. Catherine’s
Down. One of the most accessible sections is in the ground rising above the ravine at Luc-
combe, where the road from Shanklin to Bonchurch crosses the strata obliquely. About the
middle of Old Park is a continuous section of beds, apparently undisturbed and more than 3 of a
mile in length, rising very gradually towards the south, or west of south, and consisting above, for
between 30 and 40 feet, of subcalcareous sand and stone, alternating with chert in concretions,—
and below of similar sand, with spongiform masses, like those of the upper part of the sections near
Folkstone ; (21.) and (22.). But one of the best sections, perhaps, of the Upper green-sand, is
visible above the road from Niton, towards Blackgang-Chine, over the Sand-rock spring. The
brow of the cliff at that place is about 591 feet above the sea}; and the beds composing the ver-
tical face at top, which is itself more than 100 feet high, may be thus divided :
Alternations of soft subcalcareous stone, with concretional chert. ..30 to 40 feet.
Yellowish grey sand and stone, with some chert......++e+++++++60— 80
Alternations of yellowish grey and bluish stone, and sand........15 — 20
* As above Western Lines; above St. Lawrence, where the road comes down from the interior,
and thence westward; between Rans and Marables. At the place last mentioned the precipice is
about 60 feet high, with gault beneath, and is traversed obliquely by a footpath up the whole face.
+ Englefield and Webster, p. 238.
VOL. IV.—SECOND SERIES. 2B
184 Dr. Frrron on the Strata below the Chalk.
Gault.—This stratum consists, in the Isle of Wight, of dark, bluish grey, harsh, sandy clay, in-
terspersed with minute particles of mica: but I did not discover, anywhere, the beds of light
bluish, plastic clay, like that of Folkstone, which abounds in the characteristic fossils, and which, I
believe, forms the lower part of the formation. The clay here, which seems not to exceed 70 feet
in thickness, contains very few fossils, and these, from their imperfect preservation, are difficult to
obtain. The tract, however, which this stratum occupies has been very little explored. One of
the best sections of the gault which I saw, was at East-End, between Luccombe and Bonchurch,
where the clay contains nodules, and branching crystalline rods of pyrites, some thin shells in frag-
ments, and minute crystals of sulphate of lime, perhaps produced by decomposition. The top of
the sands beneath this stratum, here slopes both towards the west, and outward, towards the sea ;
so that on the melting away of the gault, everything favours the subsidence and ruin of the upper
part of the cliffs.
Loner Green-sand.—This stratum, which forms the principal portion of Mr. Webster’s ‘ Ferrugi-
nous Sands,’ occupies a great part of the surface on the south of the Isle of Wight, and is
everywhere conformable to the chalk; a ridge of highly inclined strata of sand parallel to that of
the central chalk, crossing the island, from the shore on the south of Bembridge Down to the foot
of Afton Down. The sands are then reflected southwards, and form the lower ground in the
interior, from Mottestone, through Brixton, Shorwell, Kingston, Godshill, and Newchurch, to
the coast. ‘Throughout the greater part of the shore at the ‘ back of the island,’ this stratum is either
below the level of the sea, or concealed by the debris of the undercliff; but where it rises,—
westward from Rocken-End, and eastward from Bonchurch Cove, it exhibits the most distinct and
fully developed sections.
When I examined the Isle of Wight, I was not aware of the subdivision of the Lower green-sand
into the groups, which I afterwards found to be so well displayed in Kent (16, &c.), and Western
Sussex (72.); but from the map of the island, and the characters of the strata on the coast, I have
no doubt that it exists also here. A range of heights from Kingston to Walpen, which in the Ord-
nance Map is a very prominent feature, and seems to be continued to the shore between Walpen
and Whale Chines, appears to be the outcrop of the upper member of the formation; and the
heights on the south of Chale seem also to belong to this uppermost or ferruginous subdivision ;
while the darker beds of Shanklin and Blackgang Chines must represent the middle, or more
retentive group: and even among the highly inclined strata of the Red-cliff, in Sandown Bay, green,
mud-like, beds are distinguishable in the corresponding part of that escarpment. A bed at the
bottom of the cliffs, both at Atherfield, and on the east of Shanklin, which abounds in fossils, espe-
cially the Gryphea sinuata, is probably the equivalent of the lowest group of stone at Hythe. The
total thickness of the Lower green-sand in the Isle of Wight may be considered as about 300 feet.
(94.) The Wealden.—The Purbeck strata do not make their appearance in
the Isle of Wight; and the two remaining members of the Wealden pass into
each other by insensibie gradation, the Weald clay constituting but a small
proportion of the whole. A valley or depression, however, corresponding
to the site of the clay, is still a well-marked natural feature : the escarpment of
the green-sands projecting over it on the one hand; while on the other, the
Hastings sands rise into a small prominence, even in the compressed section
of Sandown Bay ; and form, on the west, an undulating, dome-shaped ridge,
between Barne’s Chine and Compton-Grange Chine, the section of which
corresponds to that of these sands on the Sussex coast.
Dr. Firron on the Strata below the Chalk. 185
The affinity in mineralogical composition,—indeed in most of the cha-
racters except the species of the fossils which they contain, between the
strata in this portion of the series in the Isle of Wight, and those above the
chalk on the north of the island, is exceedingly striking ; though the groups
are separated by the entire mass of the green-sands and the chalk. In
both we find reddish and variegated sandy marls, of various and similar
shades of tea-green, purplish, and grey; in both, also, beds of sand and of
erit*; and in both series, too, is an alternation of beds containing marine
fossils, especially Oysters, with strata which abound in Paludina, Cypris, and:
other productions of fresh water. The inferences from these facts are now
so obvious, that nothing, it would seem, but the strongest prepossessions
in geological theory could so long have kept them out of sight f; and the
proof they furnish of the repeated submersion and re-elevation of the land, is
irresistible.
(95.) On the other hand, there is a very obvious resemblance, in mineralo-
gical character, between a great proportion of the deposits, both above and
below the chalk in the Isleof Wight, and the reddish and variegated marly
sands of the new red sandstone (red marl), of England. Nothing can better
prove the insufficiency of mineralogical characters, as a ground of identi-
fication in geology, than this close resemblance in the productions of periods
so distant ; while it demonstrates also the permanence and uniformity, both
of the substances out of which the strata have been composed, and of the
operations which produced their aggregation {.
Weald Clay.—This stratum is visible on the coast, in one of the sections at Sandown Bay, and
in both of those on the west of Rocken-End, forming a narrow band of comparatively low and
flat ground,—encircling, and, as it were, insulating the Hastings sands, which rise from beneath
it into heights of small elevation. In Sandown Bay, the most eastern portion of the clay, which
* Grit, not in itself distinguishable from that of Hastings, and containing Paludine, occurs on
the north-east coast of the Isle of Wight, near Cowes. See Mr. Webster's “ Letters,” &c. p. 321;
—and “ Annals of Philosophy,” 1824, vol. viii. p. 379.
+ Soon after my examination of this part of the Isle of Wight, I had the pleasure of a visit there
from M. Constant Prevost; and the following passage in one of his letters, written on his return
from an excursion to the west of the island, coincides precisely with what is mentioned in the
text :—‘ La succession des couches rappelle tout-a-fait celle de méme nature, que sur une échelle
“‘ moins grande recouvre la craie, ou mieux est posterieure a Ja craie, 4 Alum Bay: c’est la méme
“ disposition générale, le méme assemblage de couleurs, les alternatives de sable et d’argile avec
“lignite, les mémes septaires, &c.; tout est analogue dans les deux series, a l’exception des
“fossiles. On peut retrouver une analogie aussi forte entre les argilo-sables (Hastings sands)
“ inferieurs a la craie, et la grande formation du nouveau gres rouge; les argiles verte, jaune, et
“youge, les gres blancs et bigarrés, les conglomerats,” &c.
} The abundance of the variegated reddish and greenish sandy clays in the upper members of
the Wealden group, both here and in Sussex, is such,—and their proportion to the whole so
great, that the name of the deposit might very well have been taken from them; and if the term
Red-marl be retained as a general denomination, these and the new red sandstone might with
some advantage be called the Upper and Lomer (or first and second) red marl; which would in-
dicate both their mineralogical resemblance, and their relative position in the series. :
282
186 Dr. Firtron on the Strata below the Chalk.
succeeds the sands of Red-cliff, is much obscured by intermixture with the ruins of several
different strata fallen from above ; but it abounds in the characteristic fossils. The corresponding
portion of the Weald clay, on the west of the Hastings sands, between the fort at Sandown
and Shanklin Chine, forms a flat shore, which is visible only at low tides. Beyond Atherfield-
point, in like manner, the clay rises from beneath the Lower green-sand, and exhibits beautiful
sections in the Chines immediately on the north-west of that prominence: thence it passes inland,
through the lower grounds of Sutton, Thorncross, Yafford, Marsh-Green, Mottestone, Brook-
House, and Compton-Grange, and meets the coast on the south of the Lower green-sand ridge, at
Compton-Grange Chine ; where a similar section to that of the west of Atherfield (or rather to
that on the east of Sandown Bay), is exposed: but thereabouts the strata seem to have been
disturbed,—whether by mere subsidence or the presence of a fault, I did not ascertain.
Hastings sand.—The general position and relations of that portion of these sands which is
visible on the coast of the island (for the sections do not go down to the lowest strata), will be
obvious from what has been already stated, with the aid of the section, Plate X.a. No.7. In
Sandown Bay the sands form but a small insulated spot, of an irregular figure, surrounded by the
Weald clay: but on the south-west coast the superior strata of the formation are much better
developed ; occupying an oblong tract, approaching to the shape of half an oval, from the west
of Cowleaze Chine to Compton-Grange Chine.
It will be seen from the Ordnance Map, that two small but remarkable prominences called
Atherfield Rocks, and Brook Point, project beyond the general line of the shore, between Rocken-
End and Freshwater Bay: so that the coast is divided into three shallow recesses, called Chale
Bay, Brixton Bay, and Compton Bay; the last being, in fact, only the eastern portion of Fresh-
water Bay. Atherfield Rocks, and the heights on the south-east of them, belong to the Lower
green-sand, of which they are the outcrop. Brook Point (or perhaps the more obtuse prominence
of the shore between that place and Southmore,) is apparently the central and lowermost portion
of the Hastings sands; the culminating point being much nearer to the chalk in the centre of the
island, than to that on the south, in consequence of the more rapid rise of the strata in the central
range. <A considerable prominence, however (which, in actual elevation, is the highest point of
the Hastings sands), occurs at Barnes’s-high.
The rocky ledges which shoot out from the land in several places along this part of the shore,
form some of its most striking features; and make this coast exceedingly dangerous to shipping-
They all consist of the subcalcareous grit, which occurs throughout the Hastings sands, in con-
cretions more or less continuous and frequently of great bulk. Similar ledges appear also, but
are less prominent, in the section at Sandown Bay ; and, as has been already mentioned (84.), on
the coast near Hastings.
(96.) Sectional Lists of the Strata.—The preceding passages will enable
the reader to connect the subjoined lists of the strata, in which I have availed
myself of the notes annexed to three heautifully executed sectional drawings
of part of this coast, by Sir John Herschel*. I shall here follow the shore
* T should gladly have inserted Sir John Herschel’s sectional drawings, and my own, in
place of the reduced general section, Plate X. a. No. 7.; but this could not have been done without
such reduction as to exclude the greater part of their contents, and such exaggeration of the
heights, in proportion to the horizontal distances, as wholly to destroy their resemblance to
the natural appearance of the cliffs.
In the following list I have adopted throughout Sir John Herschel’s measurement ; and from
the difficulty of estimating the vertical thickness of the strata, in consequence of the varying
Dr. Frrron on the Strata below the Chalk. 187
from east to west: giving, Ist, A section from beneath Bembridge Down
to the middle of Sandown Bay; 2ndly, The opposite side of the curve,
from Bonchurch Cove, eastward, towards the same point; 3rdly, The succes-
sion of beds beyond Rocken-End, north-westward, to the geological centre,
or lowest point, on the south-west range of the coast; and 4thly, The
series from the chalk under Afton Down to Brook Point. This will involve
some apparent repetition, as the strata in all the sections are essentially the
same; but it will perhaps be the best mode of assisting the inquiries of
those who wish to become acquainted with this district.
(97.) Sectional List of the Strata from the south-west of Bemeripcz Down
to the middle of Sanpown Bay.
The Section begins at the bottom of the flinty chalk. Beds very thick and massy.
The flints small and disseminated.
Paces.
O—510. Loner White Chalk, without Flints.
0—255. This part of the beach is occupied by ruined masses from above. The base of the |
Paces oeeupied
by each division.
cliff, where accessible, seems to consist of knobs of white chalk, bedded in a greyer mass.
The stratum is defined by a layer of distant, insulated flints, which separates it from the
flinty chalk above. Dip about 65°. Strike, about 6° north of west; which is very
nearly the direction of the coast .......eseeees ARO SINC Oe 0): ST craete sce ees els's
255—510. The finest and thickest beds of pure white chalk. Dull; not very = tits chalk ;
easily scratched by the nail. Beds, 3 or 4 feet thick ; separated by layers, 5 or 6 inches
thick, of chalk like the rest, but interlaced with a kind of network of very grey matter.
Dip, 60° north. Strike, 74° west, almost coincident with the trend of the shore ......
350. Inocerami, much crushed. At 450 paces, the same, but less oe At 500,
dip, 60° north; strike, 69° west of north......... =O DCE Ope Sytevalsvelovenaeielcreare
*~
on
or
255
510—783. Marly and Grey Chalk.
511. Outcrop of a seam of greyer chalk ...........- ponecdocuoancaduoccascoggoune
526. In the grey chalk a layer of yellow harder knobs........+eeese0- pieieteisicra ts shoe |
540. A bed of very uniform grey chalk, 6 to 8 feet in thickness exposed....... Anco COs
690, A thick bed of grey chalk, as at 540; and the same rubbly yellowish layer as at 526..
650. Grey chalk; thick uniform beds, 3 or 4 feet ....... as oie) Yaherelgielalahe/etataveie) ofata er ofeie aaa
700. Grey and white chalk, in alternating layers. This alternation extends about 20 feet [ ~
imp) the clitt, which, shelves, back)... js.00:00 000540. [OMe Sees os soe abo otaee eeaiereies
750. At a breaking away of the talus, the outcrop of the grey chalk is superbly seen.
Alternating, dark grey, almost blue, layers, and white, like a striped riband. Corals oc-
cupy the lower 5 feet. [The same appearances are very remarkable at the foot of Blanc
Rez ON NCP TERE EDASt MCAT MC MIAIS. [2 ots «ise s o.6 00 6.6 vee ci oisi0 a.0 ain) vloisit nelade os
obliquity of the section to their planes, I have stated the horizontal spaces occupied by the strata
at the base of the cliff, which give at least a comparative view of their proportions. I find, from
the mean of several comparisons, that my own paces (which are somewhat shorter than Sir J.
Herschel’s), are about 43 (strictly 42°77) = 100 feet: and in my section the Upper green-sand
occupies 196 paces on the shore; the Gault 94; Lower green-sand 840; the Wealden, to the cul-
minating point of the Hastings sand, about 2000 ; ;— of which space the Weald- clay may be 600,
and the | Hastings sand about 1400, from their first rise to the middle or top of the saddle.
188 Dr. Fitton on the Strata below the Chalk.
Paces occupied
by each division.
783—900. Upper Green-sand. ........e0 000 Ease Rte Sate ee elec 6 ohaatete olen tees U7
[The rise of this stratum is here very distinct in the section on the shore; and its course
inland is marked in the original Ordnance Map (scale, 6 inches to a foot,) by a distinct
ridge parallel to that of the chalk, passing from the shore close to the little village of
Yaverland, on the north.]........ o} Sig pe.eelsie wie «say stoie)sielg oieiwiere pye'er aie mole ae euress
783. Here the green-sand crops out, in a bed 20 feet thick, of very dark grey, sandy, cal-
careous layers, with concretions of harsh lime-stone .....-.+++++-- Sido bon 20 feet.
787. Fine specimens of coral....... eneeis eheleteld ee abe in| elo wielerelahetetelereteicletatme eiereterel etna oe
800. A thick bed of green-sand, with Stphonie. In 3 feet the fossils change, the corals
disappear, and the Siphonie come in. In this bed is a layer, 1 foot thick, of very black chert.
850. A darker set of layers, 1 foot, rises among the green-sand beds ....... oiacetanereeenes
900—1020. Gault.—A blue-grey marly mass, almost like the lowest beds of the chalk, 120
but more mud, or silt-like. Harsh to the touch............ RepOODOU0D 00 00,00.000¢ ir
[I could obtain no specimens of the fossils, which were few and broken. The slope
above this stratum is covered with grass.—F., |
1020—1767. Lower Green-sand...... Rave ie a (oie J0c.4 'v' av eo 15140 ARES R LOE ee oe A
1020. Reddish brown sand rises; small rolled gravel, and quartzy pebbles. Trend of the
shore, 16° 30! south of west. Dip, 70° north. Strike, 74° west. Thickness, 30 or 40 feet.
1061. Yellowish grey mud; outcrop (presumed) concealed by rubbish; over blue mud,
passing into grey, and much mixed ..........+-. Sieiel ei oleleratey tetereteiet vecccec sevens
1100. Vivid yellow sand, 6 feet. Light grey mud, 8 feet. Blue mud, 15 feet ........ 29
1140. A great bed of dull brown sand. 1st subdivision, = 15 feet. 2nd, = 20—25 feet.
3rd, = 30 feet; brown and green-sand, and quartz pebbles, and bits of iron-stone. } 65
Mhe lowest’S feet very ereen-Sand 2/0. cic /iiee ow oo» woe ele) omels Bdacondnandeuadac .
1200. Deep brown sand, full of bits of oxide of iron, of a strong resinous lustre and high
polish. The upper 3 feet rather less brown. [Like that which abounds in the Lower i 58
green-sand of Western Sussex and Surrey; (59.)|] ..seescessceescves sis Yo lalesia stctokere
1250. The cliff becomes mural.
1258. Presumed outcrop of pale yellow sand. Mere sand; no cohesion: has a few broken 40
shells@eyvcneve ateteranetofe FOdo0d ODOC ODODE DD alia leseuekevoielolelnia chat telebete ote Thickness, 40 feet.
1323. Red sand, but not so dark as at 1200. A vivid stripe of orange and yellow. 7
Thickness, 20 feet.
1541. A continuation of the last, separated by a rather honeycombed line. Apparent
role) =e as Aare goo se seweeee piete)ioiairefake SO SOM OSA ORIG © Thickness, 50 feet. +100
1406. A mere continuation of the last, separated by a dotted line, but same material.
[ The sand-rock hereabouts is divided, by fissures, into masses approaching to rhomboids. |
Thickness, 30 feet.
1470, Outerop of a very thick bed of dark grey mud or silt, contrasting strongly with the ]
red sand which overlies it. Apparently the equivalent of the middle, more cohesive,
greener, and less stony member of the Lower green-sand, like that of Folkstone |
(24—28.)? The darker sand here gives a green streak, when scraped or struck with |
the hammer. ] ,
1600. The cliff loses its mural character, and falls back into an amphitheatre, full of the
rubbish:of the bed *abGvie rectotereite ce clsieieis © oles cr leveleve co ete elev cvelnie'e te eicte hen Tene |
1676. A very red (almost blood-red) seam, a foot thick, visible in the rubbish of the beds |
ANE so0500 ekoetsiotelcvetcl tetstefenetol xab00005004 a) 0) elelle eKelsiols 9)0) ¢10) « s\ejvllols [else eles «lelerelele
1710, &c. Wealden.
[A fresh range of low sectional cliff commences on the beach at 1710; the amphi-
theatre of the higher cliff retiring far back,—perhaps from the rise of the Weald-clay ;
the decay of which, and its efflux in the form of mud, seems to have produced the ruin
and fall of the upper strata. |
Dr. Firron on the Strata below the Chalk. 189
Paces occupied
by each division.
1767—2150. Black slaty clay, with layers of sandy stone 2 inches thick, formed of agglu- ]
tinated leaves, like sheets of paper.
[Apparently the same alternation as that which abounds on the confines of the Lower
green-sand and Wealden group, described (83.), p. 168. ]
1850. The amphitheatre of the retired cliff has again come round to the beach..........
1880. Layers of small flat oysters, agglutinated by calcareous matter, very like one of the
beds between Atherfield and Shepherd’s Chine. [See hereafter, 5580, p.197.]...... ane
1900. The apparent dip of the strata is now much less, = 10° .....+.eeeeeeeeeee wees
2000. The stratum here is like mashed slate; but earthy and incoherent, with stony
layers occasionally .......+.++- noo CODOOBUUNO OU OOOO GUN door (2 COND ON50 sc 00800"
2100. Very clayey: the stony layers, when broken, appear to be very white indurated
clay; but their old cracks, dark blackish brown......cesesceeccreccsecees speheeeiels, =
2132. Like slates; as thin as paper, but friable .........cccesceees sooo Sdaabed .
of the strata 2° or 3°; but they dip back 10°. [Que. Commencement of the Hastings
SANUS] wovovnseveacene Ree Gaia <ivievs SARS SREB e ESE aisle! seis wigleis/axa
2400. A very pale sandstone. Outcrop concealed .......sseeeeeee Socondqouocacue
2520. Mixed red and brown-yellow clay: no fossils. The strata still rise from the east.
Trend of the beach, 19° south of west; and so, forward to the Fort, and back to
the cliffs.
2700. Grey and red clay. No fossils.
2894. Red clay. Strata still rising at an angle of about 12° from the east.
5000. Shore too low to show the strata distinctly.
3240. A layer of tough gritty sandstone ; horizontal, or rising a very little to the south-west.
3300. Another layer of tough gritty sandstone, on the beach.
2150. Sand. Upper 2 feet stony. Red layers of stone and rubble mixed. Apparent =
370
3330. Culminating point of the saddle. Strata almost exactly horizontal. The red clay
is seen resting on the stony layer of 3240 and 3300.
3400. The strata now begin to dip 1° towards the nest.
3506. The first wooden barrier to stay the shingles on the beach near Sandown Fort.
3535. Red clay, resting on stony layers strangely contorted. The same clay also under-
lies them. These contorted layers extend 50 paces.
3617. Third wooden barrier. Here the grass comes down to the beach, and an embank-
ment begins at high-water mark.
3700, the fifth wooden barrier. | 3782, the seventh barrier. }| 3862, the ninth - barrier.
3741, the sixth. 3821, the eighth. Here begin zigzag weirs.
4050. In a line with the eastern edge of the south-east point, or bastion, of Sandown Fort.
(98.) The junction of the Lower green-sand with the Wealden strata is
one of the most interesting points in the sections upon this coast, from the
importance of determining whether the transition from the freshwater to the
marine strata was gradual or abrupt. As far as my own observations have gone,
the change, in all the sections of the Isle of Wight, is unaccompanied by any
marks of disturbance, or any variation in the characters of the strata them-
selves, and can in fact be learned only from the total change of the fossils :
a few feet in thickness, of beds conformable with those both above them and
below, dividing the strata which abound in Cypris and Paludinz, from the
190 Dr. Fitton on the Strata below the Chalk.
lowest members of the green-sand formation, which contains shells of many dif-
ferent marine genera in great numbers ;—Trigonia, Gervillia, large Gryphites,
especially G. sinwata, with others decidedly marine. The bed which contains
these fossils is apparently the equivalent of the lowest stone beds of the coast
near Hythe, and is detached from the ferruginous stone at the top of the
Lower green-sand, by a mass of soft, dark, sandy clay, which seems to corre-
spond to the middle group of Kent.
The strata on the west of Red-cliff are so much obscured by the washing away and ruin of the
clay beneath the green-sands, that no continuous section is observable here. An obvious depres-
sion, however, corresponds to the site of the Weald-clay ; and both the clay and the sands which
rise from beneath it include their characteristic fossils in great abundance and perfection, and
contain the same large proportion of reddish and variegated marly and sandy clays, with occasional
beds of subcalcareous grit, as on the Sussex coast. The following details may be added to what
is stated in the preceding list.
The upper part of the clay abounds remarkably in Cypris Valdensis ; and contains some nearly
continuous bands of clay iron ore, in elongated flattened nodules, two to nine inches in thickness,
including clusters of Paludina elongata. ‘The beds above this clay form as it were the transition
into the green-sand formation, consisting, for some feet, of alternate layers of greenish and grey
sand and sandy clay of different shades, like those described above, (83.). A vertical portion of
the cliff at the top of the clay, which was exposed to a thickness of between 30 and 40 feet, con=
sisted of the following substances :
Feet.
Greenish-grey sand and clay in alternate bands.............- 10 0
Clay and sand with iron ore ....eeeeseeeeeee nis o ahs elelete atte 2 0
A band or course of iron ore, with Cypris...........- atoleueece 0 8
Greenish-grey sand, alternately of dark and lighter hues......
Bluish slaty clay, abounding in Cypris..........e.0eee0e08
Clay ivontoresct s\.c\c1e' craic wy oelotetalet ate olahelotetst ohetetotete «about 0 8
Slaty and sandy clay............). wfelofatsbeleloeb se iol-veyeieteolevate
—= 20 O
A bed of dull, solid, earthy calcareous stone........+eeeeee 0
Greenish-gtey Sandy Clay, science cieisit's ie s/s 6 eis) aac eecertoe ceonp .0 0) tOncRmaae
Sand-rock, in some places very ferruginous............+e00%
Total, about... 40 0
About 770 paces from the bottom of the Lower green-sand, a bed of sand-rock, from 12 to 14
feet thick, makes its appearance: perhaps one of the courses of sand, subordinate to the Wealden,
indicated in Western Sussex by Mr. Martin.
In this upper part of the Wealden is at least one thin bed of limestone, consisting principally of
the shells of a species of oyster (or Gryphea?), of which I could not find any distinct specimens.
It is invested with a thin crust of fibrous, somewhat earthy, carbonate of lime, having the appear-
ance of what has been called “‘ Cone incone.” In one loose specimen of this limestone, I found a
fragment of an Ammonite, evidently derived from some more ancient stratum, washed down and
lodged in the mud of which the whole of this formation is composed. The fragment is too small
to indicate the species, but the genus is perfectly clear.
+-_—
Dr. Firron on the Strata below the Chalk. 191
I did not find among the strata any one containing Paludina vivipara ; but on the beach were
several loose blocks containing that fossil, with Cypris Valdensis, and not distinguishable from the
stone of Bethersden in Kent,—the ‘* Sussex Marble.”
About 1800 paces from the Lower green-sand, a large block of sand-rock on the shore had the
waved surface, or ripple mark, which is common throughout the upper part of the Hastings sands :
and here the alternations of greenish grey sand and sandy clay, so frequently mentioned above,
are again very conspicuous.
About 1950, was a mass of indurated clay iron ore attached to a nodular portion of hard siliceous
grit, containing moulds of large Paludina, filled with sparry sulphate of barytes: a fact which
accords with the supposed continuity of deposition of the Weald-clay and the Lower green-sand ;
sulphate of barytes being found, it will be remembered, in the fuller’s-earth of Nutfield, at the
bottom of the latter formation*.
About 2040, are strong beds of sand-rock including concretions of hard grit; and thence
westward the entire cliff is composed of reddish clay and sand. From this part of the series,
which seems to correspond to the strata near Brook Point, on the south-west coast of the island,
it is probable that the remains of the Iguanodon have been derived, of which Dr. Buckland has
given an account in a paper read before the Geological Society + : and near the same place beds arise
of purplish red and variegated clay, alternating with fuller’s-earth of a clear bluish green colour,
mixed with cohesive sand.
(99.) Strata from Boncuurcy Corr to the middle of Sannowwn Bay.
The direction of the coast on the south of Sandown Bay, from the Fort to
the south of Dunnosef, is about 15° west of south. But on rounding that
promontory the direction changes, and the general trend of the coast thence to
Rocken End, is towards a point between 15° and 17° south of west, which
seems to be generally the strike in the southern portion of the island; the
dip being south 17° east.
The summit of the Downs here consists of Chalk, with the Upper green-sand beneath; and the
subsidence of the Gault has produced very extensive ruin, especially at East End and thence to
Luccombe ; the debris there affording numerous fossils, among which were the following :—Am-
monites Rhotomagensis, A. Seliguinus, A. varians, Gryphea vesiculosa, Inoceramus tenuis, Mya
mandibula, Ostrea spinosa, Pecten orbicularis, Serpulz, Vermetus Polygonalis.
The Lower green-sand rises a little on the west of the streamlet at Bonchurch-Cove, and the
following subdivisions, though in a great measure arbitrary, will give a general notion of its com-
position.
Sulphate of barytes has been found also in the Upper green-sand at Worbarrow Bay, Dorset-
shire,
+ Proceedings, vol. i. p.159: and Geol. Trans. 2nd Series, vol. iii. p. 421.
i The names of the headlands in the Ordnance Map of this part of the coast, are different from
those of the Admiralty chart and of Mr. Webster’s map of the island. In the former, the height
between Luccombe and Shanklin Chines is called Dunnose ; and the greater promontory between
Luccombe and Bonchurch-Cove, (which in the other maps, above mentioned, is named Dunnose,) is
called Chine-head. I have adopted the position assigned to Dunnose in the Admiralty chart. The
top of Shanklin Down, (which is not very different from the general level of the Chalk Downs
hereabouts) is according to the Ordnance Survey, 792 feet above the sea.
VOL. IV.—SECOND SERIES, Qc
192 Dr. Firron on the Strata below the Chalk.
A. Boncnuurcnu Core to a fissure north of Litrrestarrs Point.
a. The top of the first group of sand, about 30 feet thick, may be traced north-eastward, and
thence north, to its outcrop in the shoulder of the cliff, above a point called Horseledge, imme-
diately on the east of Derranew. It is composed chiefly of brownish sand ; but in some places
reddish and yellow. It may be remarked in general of these strata, that the colour seems to
depend on the accident of exposure to moisture; the recent surfaces disclosed by the falling
away of the cliffs, being frequently ferruginous yellow, or even whitish; whilst in other parts of
the same beds the hues are brown and dark greenish grey: the difference arising apparently
from the state of the iron, which the sand contains.
b. The next group, also about 30 feet thick, is composed of dark brownish sand and sandy clays
but is bright yellow in some of its higher points. It rises at a short distance east of Bonchurch
Cove, occupies the shore thence to Steel Bay, and forms the principal portion of the cliffs at
Luccombe Chine, whence it is continued northward to the summit of Knock-Cliff, on the south
of Shanklin Chine.
The bed or group which rises about midway between Steel Bay and Luccombe Chine extends on
the shore to about an equal distance north of the Chine, and goes out beneath the summit of
Knock-cliff. It is about 30 feet thick, generally of a dark grey and brownish hue.
d, Ata place called Derranew, north of Luccombe Chine, a bed rises, of much darker hue, and
more approaching to clay than the preceding. It occupies about a third of Knock-cliff, near
c
the lower part, where it spreads into a terrace; forms the upper part of Shanklin Chine, and caps
the cliff as far as the south side of Small-hope Chine, a detached portion appearing on the top
of the cliff at Little-stairs Point. From this stratum masses have fallen, like those of Parham
in Western Sussex, consisting of highly ferruginous sand-rock, with numerous impressions of
shells (Gervillia — Natica— Rostellaria—Terebratula —Thetis —Trigonia—Turbo—Venus ?).
These are found in nodules loose upon the beach south of the Chine, and i situ, within the
Chine itself, at the upper part; and the debris of these upper strata, at the foot of the cliffs
between Shanklin and Small-hope Chines, afford several varieties of concretional sparry stone,
abounding in green particles, like the blocks on the shore near Folkstene (20.), containing the
remains of an Astacus, Corals, and Spatangi, with shells of the genera Ostrea, Serpula, Spheera,
and Trigonia.
e. A bed or group, not very prominently distinguished from the last, rises immediately on the
south of Knock-cliff. It is in general of a dark greenish, mud-like hue, contains a great pro-
portion of silicate of iron, and seems to correspond to part of the middle group between
Sandgate and Folkstone. This occupies about a third of Shanklin Chine, and forms the upper
portion of Small-hope Chine, whence it declines a little to the chasm at Little-stairs Point, by
which it seems to be cut off abruptly.
f. Appears above the sea on the south of Shanklin Chine ; forming, as it rises, a terrace covered
with the debris cf the upper strata, as far as Small-hope Chine, where its top is about 22 feet
above sea; and then declines to the fissure near Little-stairs Point. It consists of an intensely
deep green, almost black sand, (no doubt a part of the middle group of Folkstone), and in
many places contains very fine specimens of Gryphea sinuata.
Immediately on the north of Little-stairs Point, about 800 pacesnorth of Small-hope Chine (and
about 1600 from Shanklin Chine) is a remarkable break or fissure: and here Sir John Herschel
found reason to suppose that a fault exists, the strata on the north of the chasm not correspond-
Dr. Frrtron on the Strata below the Chalk. 193
ing with those on the south of it, The occurrence of such faults is highly probable, from the proxi-
mity of this place to the great displacement in the central ridge of the island*.
Hence to the end of this cliff, in Sandown Bay, the beds rise more rapidly than in the preceding
part of the section, from Bonchurch; and the order, in Sir John Herschel’s sketch, beginning
at the fissure, is as follows:
B. From the fissure to the middle of Sanpown Bay.
Paces.
0—580. The cliff, about 100 feet high, which forms the north side of the fissure, consists of three
ortions.
Bright yellow sand, which goes out at 400, perhaps a continuation of e, last page? :
2. Deep muddy green, almost black sand or silt, (perhaps a continuation of f?) going out at top
about 580. The beds 1 & 2, together, occupy about a fourth of the cliff, at the upper part.
3. A thick stratum of sand of various hues, cut off by the fissure on the south, but occupying
the shore thence to about 600: the bottom rising rapidly, and going out near 1400 at the
top of the cliff, which is there about 110 feet high. ‘This stratum is subdivided thus :—
a. Sand, dark red and dull brown, with a with red. Dip, about 3° at the bottom,
greenish tinge; entirely cut off by the fis- about 2° at top. Contains Gryphea si-
sure, not coming down to the shore. nuata in great numbers.
b. Athicker bed of sand; at the bottom dull | c. Vivid yellow sand, harder than a and 6;
greenish and dark grey,—but, as it rises, rising on the shore at 420, and extending
of a vivid yellow, in some places tinged thence to 580. Dip, 3°.
580—1100. A great bed of sand, dull dark grey on the shore, but at the upper part lighter, and
near its disappearance bright yellow. ‘This bed is much subdivided as it ascends ; the lowest
subdivision consists of transversely disposed layers ( false stratification), on which those above
rest unconformably, indicating either an inclined beach or some peculiarity of deposition. Goes
out at top at 1750.
1100—1268. Sand; grey at the bottom of the cliff, bright yellow at top. Goes out about 1780.
1268—2000. A very thick bed or group, consisting of sand, and very sandy clay or silt. Goes out
at top, about 2150.
1268—1630. A very dark sand or silt, of a deep dirty green, or almost black colour.
1500. Dark arenaceous clay, with yellow and green efflorescence. Dip, 5°—10°.
[The cliff, from 1780, northwards, declines rapidly in height. ]
2000. Sand, luteous yellow, without cohesion.
2000—2160. A clayey sand, or rather arenaceous clay,—dirty brown silt; yellow at the upper
part: about 20 feet thick. The bottom goes out, at the top of the declining cliff, about 2270.
2160—2300. Yellow sand.
2300. Dull yellowish sand, with thin blackish layers. Apparent dip, about 25°.
2350. Bright yellow sand.
2400. The coast bank is of sand, 15 or 20 feet high. The cliff ends here, and the flat begins.
A low sand-hill commences about 2436. (Que. loose blown sand ?)
* My own section, however, ascribes the more rapid rise of the beds on the north of the
prominence at Little-stairs Point, to the change in the direction of the shore; which brings the
face of the cliff more nearly into the line of the greatest inclination, and makes the dip appear
to be greater than before.
2c2
494 Dr. Frrron on the Strata below the Chalk.
Paces.
2700. The King’s Head Inn, at Sandown, by Sir John Herschel’s measurement, is 2700 paces
from the gap or fissure at Little-stairs point.
The coast, from the end of the cliff above mentioned, to a point about 400 paces north of the
Fort, is a dead flat, occupied by the Weald-clay, which is visible at low tides on the shore
beneath the Inn, and thence southward.
At 364 paces north of the Inn, beds of ferruginous (Hastings) sand first make their appearance,
rising from beneath the clay, which dips to the south-west at an angle of about 5°: this being
the descending side (on the south-west) of the curve, of which the summit is at 3330 of the pre-
ceding list, (97.).
(100.) Strata on the South-west Coast of the Istz or Wicut, from
Biacxeane Caine to Brook CHine.
At the west end of the back of the island, the Lower green-sand makes its
appearance beneath the Gault, a little to the east of Puckaster Cove, where
the sands are ferruginous. I have no sections from that point to Black-
gang Chine, a space much obscured by ruins fallen from above: but thence
westward, the sections, from about the middle of the Lower green-sand to
the lowest beds of the Hastings series which appear above the sea, are probably
the most complete and the best developed that anywhere exist in England. In
the following list, the numbers, as far as Cowleaze Chine, are taken from Sir
John Herschel’s sections, and the descriptions from his notes, with additions
from my own.
A. Brackeane to CowLe4ze CuIne.
In the broken ground above Blackgang Chine, whitish sand-rock is visible immediately beneath
the Gault, above the Sand-rock spring *, which breaks out about 150 feet above the sea, and ap-
parently about 50 feet below the top of the green-sand, from whitish sand, containing much lignite
in small fragments, with a considerable depth beneath of dark and ferruginous sands mixed with
clay. There can be little doubt that these upper beds which form the shore between Puckaster
Cove and Blackgang Chine, belong to the uppermost group of this formation. (See above (16.) et
seq.) The same beds form also the heights about the village of Chale, and seem to extend from
that place from Walpen to Kingston, as already mentioned, (93.) p. 184.
The strata immediately over Blackgang Chine, rise upon the shore at a considerable distance to
the eastt. They consist of the following substances:
* A full account of this spring, by the late Dr. Marcet, has been published in a former volume
of these Transactions, (1st Series, Vol. I. p. 213, &c.). It is remarkable for the extraordinary
quantity of saline matter which the water holds in solution;—no less than 107 grains in 16 ounces;
of which 41°4 are sulphate of iron; 31°6 sulphate of alumina. The saline matter in one of the
strongest mineral waters previously known, at Horley Green, near Halifax in Yorkshire, is only
4.0 grains in the same quantity of water. The water of the streamlet at Blackgang Chine itself is
pretty strongly impregnated with sulphate of iron.
+ The gravel on the beach along this part of the coast consists, in a great measure, of small
rounded fragments of chalk flint; which, from their incessant agitation under the surge, are
worn, and almost polished, to such smoothness and mobility, as to render it extremely laborious
to walk there.
Dr. Firron on the Strata below the Chalk. 195
[Lower green-sand. |
1, 2. Loosely coherent sand and sand-rock. 1, 2, and 4, in blocks about 6 feet thick.
8. Dark sand or silt, like loose black mud. 7. Loose black mud or silt, much like 5.
4, Sand-rock like 1 and 2, in homogeneous | 8. Mere loose sand, without cohesion.
blocks. 9. Black earthy sand, rising on the shore about
5. Black mud-like sand. 900 paces east of the Chine, and forming
6. A great bed of sand, loosely coherent, like the bed over whichthe streamlet falls.
In the following detail of the strata, the distances are measured, in both directions, from the
middle of the Chine, as being one of the most remarkable points of the shore.
Thickness
Paces. in Feet.
850 to 560,—east of the Chine. Yellow agglutinated sand above, passing below into a dark
muddy silt. It has no green earth in it. ‘This bed forms the upper stony-looking layer over
which the water falls at the Chine.
The bottom goes out at 350 paces west of the Chine; 15—20 feet thick.
0. Middle of Blackgang Chine.
560 east, to 240 west of the Chine. Sand, full of green earth. The second or middle stony-
20
20
looking bed of the fall, which has there a convex surface. ........... J dire ered rtion
Bottom goes out at 590 west of the Chine
cauldron of Blackgang ; coloured red externally by the action of water and air on the ferru-
240 east, to 400 west of the Chine. Very dark or almost black sand, forming the base of the
15
ginous matter which it contains. .......... seeeee+s Goes out at 1040 west of the Chine. }
400 west of the Chine, to 520. Black slaty clay or mud, like mashed slates, without solidity],
of ageregation ; decomposes into muddy earth. «....... eee ees Goes out at 1130 west. :
500. Hereabouts are very remarkable stems of Siphoniz.
[This part of the shore, about 500 paces north-west of the Chine, is called Cliff-End. |
520 to 614. Green-sand closely intermixed with ferruginous layers and much pyrites, which],
Bivedt compactness and solidity........secsdecscscccaccencds Goes out at 1420 west.
614—768. Three feet at top, forming a transition from the last stratum, by alternation with
the following. Below, 10 feet consist of deep green, almost black, and very uniform sand ; bis
without fossils........--eeeee. Sieisicjs cc's ¢0.6'4 0 esisietivve’s's sia SOOO Or Goes out at 1520.
768—812. Rugged ferruginous sand, of a brown colour ......... ....Goes out at 1580. 7
812—1090. 1. Mixed green and yellow sand, very dark, including Gryphea sinuata, in very
See NNR UETENEYSS ah a ale fola!"a: distal ofaeetis=\') ahd orayayd\o 2:4 ala cual ojae)ousin, 0:8 916) 0)ei-aie Thickness, 4 feet.
2. A second bed, at the bottom of which is a layer of Gryphea sinuata......... 1 foot. $12
3. Mixed brownand green sand, including detached specimens of Gryph. sinuata..7 feet.
The bottom of this group goes out at 1800.
1090—1360. Very green sand, softer than the last. Cliff mural. Lines of false stratification
at the top............. This bed goes out on the east side of Walpen Chine about 1910.
1360—1590. Brown green-sand, much like the last, but different in cohesion ......... Hide
Goes out at top in the east side of Whale Chine, at 2480.
About 1431, a copious spring has, in its fall, coloured the whole face of the cliff with a
broad red streak. The whole seems to be greenish grey sand, and clay; very dark and
moist. The cliff continually scales off in great flakes, which are washed away, so as
not to form much talus. Red drip frequent............ Wrainscl'e} elo roizacohie Jawuee ayhinicsnis
1590—1800. Sand, with layers of great flattened and oval concretions of very tough calci-
12
ferous stone, 2 feet in diameter. [Que. like the Cowstones of the Devonshire coast*]..
Goes out at 2660.
* See De la Beche, Geol. Trans., 2nd Series, vol. ii. p. 113.
196 Dr. Firton on the Strata below the Chalk.
Thickness
Paces. in Feet.
1800—2200. Very dark sand, which, from 2100 to 2400, forms a mural cliff, standing back
behind the rubbish of the next stratum below, and its own. At 2200 it is cut into a ravine
(not marked in the Ordnance Map) called Ladder Chine: there is, however, very little of
a stream from it. This stratum forms the beach-line of Walpen Chine. Goes out at 3010.
1950. The middle point of Walpen Chine.
2200—2900. Loose dark mud. It contains, especially at 2400, the large Gryphza, us }
smaller than the gigantic specimens of the beds next below. The ruins of the stratum
form a terrace-like projection, increasing in height gradually from 2200. Goes out at 3800.
2570. The middle point of Whale Chine.
2900—2948. A group of sand, the bottom of which goes out at 3710. ...-++--
3070. A bed of fine large Gryphites, over 2 feet of sand, hardened so as to ae out Me
springs, which have stained its exterior a vivid red......eseeeeeeeeee Thickness, 4 feet.
3100. Very large Gryphites, in the same hard, green brown sand. They occur in yee and
are concreted “firmly together. [Clusters also of Serpule and Terebratule.] .........
3146. A layer of fine Terebratula, strongly agglutinated in the darker green sand........
3152. Gigantic Gryphites below the layer of Terebratule, at 3146..... siptoce/byeleie Sere nm!
3170—3400. Brown sand; upper part more compact than lower. The bottom goes out at 4610,
3400 — SaO0 aS andyaetlteeiala\eiiaje a <feicielsiale clei siele =i a ».¢ aleieleteieloleleieioters Goes out at 3410. 10
[This part of the shore, which is called Atherfield High-cliff, strongly resembles that
between Shanklin Chine and the middle of Sandown Bay. |
8560-23 1OOFE Darkeanudeias acters cs aie oor s ses setae 8 chetelalotereta seietenererere Goes out at 4610. 10
3700. Hard tough sandstone, passing into the next division below, which is softer. The }
separation is marked by great concretionary masses, in balls or kidneys, some of them |
6 or 7 feet long, and 4 to 18 inches thick, including Gryphea sinuata and Perna, with |
small Ammonites in pyrites. Similar concretions occur also at the top of this bed, and at
the bottompotathemextemcrelereleteler siete rele creel B000G00000 This division goes out at 6070. |
4010. Passes insensibly into the mud next below: near the junction a small Ammonite...
Goes out about 6080. ?
4010—4725. A loose, incoherent, blue-grey, muddy clay. It is in a state of great ruin, and
has overwhelmed the beach with a vast talus of its mud, which bases the sand-cliff an
Atherfield, and forms a slope, on which are fishing-huts, boat capstans, and a path up to
the Preventive Station, which cannot be seen from the beach. The place where this bed
goes out at top is indistinct, but it seems to form the upper part of the south-east side of
Shepherd’s Chine, about 6100 ......++-+eeees BOGOR S Onan Oa cICm CoD o ofatetenate
[This clay appears to be the equivalent of the fuller’s-earth of Surrey. It is about
15 to 30 feet thick and contains very numerous fossils: Ammonites, Echini, Tere-
bratule and Corals; with crystals of sulphate of lime, perhaps produced by decom-
position. |
4725—4775. Brown and green sand-stone, 2 feet thick, and well defined .........e+e0-
[Apparently the equivalent of the lowest beds of stone very near to the bottom of the
Lower green-sand at Hythe; and here abounding in marine fossils, among which are the
following genera: Ammonites, Avicula, corals, Corbula, Cucullea, Exogyra, Gervillia,
Gryphza (especially G. sinuata), Nautilus elegans, Ostrea, Panopea, Pecten, Pinna,
Plagiostoma, Serpula, Thetis, Trigonia, Vermetus, with others of the Lower green-sand.
Nothing can be more striking than the sudden contrast between such an assemblage and
the fossils of the clay immediately below.] .........-.0. sleie\n/aneletete cafets etateietal Seen secs
The continuation of this fossiliferous stratum is still visible, high up in the ruined face
of the cliff and above the clay, as far as 5700 paces .......0ee- Rima iecejeiese.c cuore anes Fs
Dr. Firron on the Strata below the Chalk. 197
Thickness
Paces. [ Weald Clay. | in Feet.
4775—5700. A mass of incoherent, muddy-brown, grey, and blue clay immediately }
succeeds to the last bed, and goes out in the east side of Shepherd’s Chine about
6100. It has covered the beach with an immense ruin of mud, which contains the
substances under mentioned. ‘The ledge called Atherfield Rocks, which is visible at
low water, about 10 feet below the bed of sand-rock with Gryphites, consists of blue
slaty clay, including Cypris Valdensis in myriads, with thin portions of pyrites......
Between 4800 and 5000 is Atherfield Point; and here the course of the beach alters.
5040. At this point the stratification of the clay is distinctly discernible on the beach.
It is deep blue black, and SMIVOEY Ss sioca'eleie cine ale cls ware Witla e's elelpelelele cis dele eee
5440. Here occurs a thin seam of pyrites in large flat cakes, with rounded outlines, in
great abundance. They seem to form a bed, but are individually discrete, like the
flints in chalk*. The rise of this seam is not visible ....e0-++sseees she blctiouete le ete
5500. Large, well-formed, transparent crystals of selenite, 2 or 3 inches long, lozenge-
shaped, not lenticular...+.+sese secrete cece cece ene eenees aa ae Reed taterc ele
5580. Thin stony layers of very tough limestone, half an inch thick, which seems to
consist of agglutinated small oysters, the flat shells of which are chiefly visible....
About 5700, immediately on the west of Atherfield Point, is a deep and rugged recess,
called Tiepit.
5700—6220. A thick. bed (50, 60, or 70 feet) of black shaly mud, including occasional
layers of tough, hard, shelly limestone, consisting, seemingly of agglutinated bivalves
(Cyclades). The concave surfaces of the shells lie uppermost, and form the whole
surface of the layers. The lower surface of these layers of stone is curiously corru-
gated, (or studded) with short, crossing protuberances, apparently the edges of pro- 50-7
jecting shells. The layers are one or two inches thick. There are also in this bed oat
tough, stony, non-effervescent layers; but the general material is a blue or black clay,
which breaks into thin layers, like mashed slates. [This bed constitutes the bottom
and a great portion of the lower part of Shepherd’s Chine: it rises to the top of the |
cliff, far to the west, about 500 or 600 paces west of Cowleaze Chine.|...... .
6220. About this point is the middle of Shepherd’s Chine.
6220—6440. The whole is yellow sand, but little coherent; the upper part "st |
—_—
compact, including large pyritous balls excessively hard and tough; the lower soft
and shivery. This bed occupies on the shore about half the space from Shepherd’s
to Cowleaze Chine. ‘The top goes out about 900, the bottom at 1200 paces west of
Cowleaze. It crosses Comleaze Chine at the upper part, and thence westward
rises steadily at the upper part of the cliff .......essseeveeees sie Vagbidier sasha wove
6440—6615. Upper 7 feet shaly mud, in thin flakes ; lower 3 feet black, not adhesive 10
mud, which breaks into layers. No fossils. ‘The whole 10 feet thick ...... oa ores
upper 3 feet sand; the lower 3 feet a black shaly clay, passing into the stony stratum
next below. Goes out about 1500 paces north-west of the Chine
6650. Is about the middle of Cowleaze Chine.
6615, to about 20 north-west of Cowleaze Chine. A stratum consisting of two layers : |
6
eeoeoerereeseeeeesees
* Flat, cake-like, nodules of pyrites occur in what I have supposed to be the upper part of the
Weald-clay, at Peasemarsh, near Guildford in Surrey. See above (64.).
t Some of these beds of limestone break into rhomboidal pieces, the angles of which projecting
in the face of the cliff, produce serrated lines remarkably contrasted with the uniform surface of
the clay.
{ It is through this chine that a streamlet, which once made its way to the shore at Conleuze
Chine, now reaches the sea; and the manner in which the alteration was produced, shows the
facility of changes on a coast composed of materials like these sands and clays. ‘Lhe streamlet
im the Ordnance Map is seen to rise near the village of Kingston, probably at the junction of the
ferruginous upper member of the Lower green-sand with the middle retentive group (25.). It was
very tortuous near the shore, and formerly came close to the edge of the cliff near its present out-
let, but made its way to the beach at Cowleaze; till, the soft and narrow barrier at top having been
cut through, the water soon deepened the chasm, and formed anew chine, leaving its previous bed,
with Cowleaze Chine itself, deserted and dry.
198 Dr. Firron on the Strata below the Chalk.
[As the Weald-Clay and its passage into the sands beneath are better displayed here than in any
other place with which I am acquainted, I shall subjoin a more detailed enumeration of the beds,
collected from the successive portions of the ruinous cliff, which, when I examined the place, were
well exposed on the shore at Zvepit, thence to Shepherd’s Chine, and within that Chine itself and
Cowleaze Chine. This list is still no more than an approximation; but time and labour only
are required to carry the enumeration to any extent of detail: it begins almost immediately be-
neath the remarkable bed above mentioned as abounding in fossils (4725—4775), which may be
considered as the lowest member of the Lower green-sand. ]
Ft. In. Ft. In.
A group of beds, full of crystals of sul- Similar beds, including pyritous wood
phate of lime, perhaps produced by and pyrites, with a band of siliceous
exposure :—detail thus : limestone, curiously embossed at the - 7 0
a. Clay, with much pyrites .... Aig Wy bottom with Cyclades converted into
b. Greenish and blue slaty clay . carbonate of lime (see 5700; p.197).
c. Clay and sand, in thin alternate Similar bedsie7.iats alse «ctotsteats Boon Ss 8 0
Sore, IAT STS a Shale with Cyipris Valdenss.<.. | a
Dark bluish grey slaty clay, with thin
courses of very fine light greenish 8 0 pons g pe pe Oana he 15 6
sandy clay .< 219 0c sdovasniognd ; i
A bed of limestone, with thin oyster- gee Se ans : Ayla
shells (or Gryphites ?) indistinct .. \ 0 8 Sandy clay and shale..... 2 +.¢ 0s + anne
see : Ditto, of lighter colour......... Le 0
Shale, as above, abounding in Cypris
Valdensis, and including a bed of} Ty 8 Beds of sand and clay, ae nord 4 0
pyrites with Paludina elongata.... dules of iron-ore ......+.+- viaee
A course of limestone, with Eselate| eee Greenish white sand in Loe soe. 2-4 0
ARNE ING Soo Qoda ns oa Dba ae Apparently light greenish sand — 12 0
Thin, paper-like courses of sand, alter- | brownish sandy clay «+++...
nating with slaty clay ........
Biuish grey shale, with small bones of 4 0 Greenish grit, containing numerous | 3 0
fishes and some crystals of sulphate empty moulds of Cyclades <piclalets J
Onley -ieccae hot eae URES Yellowish sand-rock, with lines of false
Sandy clay of a lighter hue........ Ope stratification ...... ay): 2 a
: : ; 20 0
Bluish grey shale, with Cypris and fish{ | [A line of darker hue occurs in the
Ones Mepesnitectetichecs apie Sect : \ group. Que. Remains of bones ?|
Greenish grey shale; the folia pene- [The preceding group of grit and
trated by cylindrical and retical prs} len sand-rock, which is not improbably
tions (likestems) of lighter grey sand the equivalent of one of Mr. Martin’s
Flat nodular portions of very poor clay Nae pee sone re ing Weald-clay,
HOW ago ahosdcgncgpbeanood } Esse peers onthe enor aaa
2 opening of Shepherd’s Chine; and
Greenish, very sandy, clay ........ 2 0 rising thence gradually westward, oc-
Greenish grey sand and clay in thin } cupies about 20 feet in the side of Cow-
courses, alternating with dark,tough, leaze Chine, near the middle. |
slaty clay, containing clusters or (10 0 Beds of greenish grey sandy clay, of
patches of Cyclas media with Cypris two shades of colour, alternating with |
Valdensis ...eseeeececessveuee specks of mica. A range of nodules of $15 0?
iron-ore is within a few inches of the
top, containing Paludine and Cyclades.
Lighter coloured slaty clay, “prey and |
10 0
Total thickness about 140 feet.
Cypris; alternating with grey and
whitish, somewhat sandy clay ....
I sought here, but without success, for remains of the large Saurians like those of Loxwood and
Tilgate forest. Nor were there visible upon the shore any continuous masses of subcalcareous
grit. |
{
!
}
}
|
Dr. Firron on the Strata below the Chalk. 199
B. Cowxesze to Barnes’s Co1ne; about 2150 paces.
The strata on the west of Cowleaze Chine afford little variety and no very prominent features.
The Chine cuts through the bed, or group of sand-rock above mentioned ;—which goes out on
the north-west of a prominence called Barnes’s Hill (or Barnes’s High), and probably is the
cause of its durability and elevation.
0—75. At the foot of the cliff, where Cowleaze Chine opens upon the shore, a seam of hard
yellowish grey sand-rock arises, which is slightly effervescent : it goes out at the top of the cliff
about 1800 north-west of Cowleaze Chine. If it were necessary to assign any strict boundary
~ to the formation, this might be considered as the beginning of the Hastings Sands.
75—900. A mass of reddish and variegated tenacious sandy clay next comes in, much interspersed
with pyrites and containing wood-coal. It rises about 75 paces from the Chine, and occupies
more than 800 paces on the shore, the top going out about 1800, and the bottom about 2000,
very near to Barnes’s Chine. The proportion of red and greenish variegated clay, like those of
this great bed, to the sand-rock, is henceforward so great in the cliffs, that the name of sands is
misapplied to this part of the formation. The general resemblance of the strata to the va-
riegated marls of the new red sandstone, (keuper of the Germans,) has been already mentioned.
900—1050. A group of sand-rock, including in several parts of its course large nodular masses
of hard grey grit, next occupies about 150 paces on the shore. It is about 15 feet in vertical
thickness.
1050—1800. This space on the shore seems to be totally occupied by dark reddish, marly and
sandy clay, variegated with greenish and grey, which form a large portion of the upper and
middle portions of Barnes’s Chine.
1800 to about 1950. A bed of sand-rock, called by the inhabitants ‘“‘ Barnes’s Sand-rock”, rises
about 1800. It is cut through by the lower part of Barnes’s Chine, and goes out far to the
north-west of it.
1950. Dark reddish and variegated clay again comes in, and is continued towards the north-west.
2150, from Conleaze, is the middle point of Barnes's Chine.
C. Barwnes’s Cu1veE to Grance Cu1ne£E,; 2300 paces.
The cliff throughout this space also is very little varied. The bed of sand-rock above men-
tioned (1800 to 1950) rises steadily in the middle and upper part of it, crossing Chip’s Chine, and
going out at top near Ship-ledge, hereafter mentioned.
The dark red and variegated clay, 1950, occupies the shore on both sides of Barnes’s Chine,
and extends far to the north-west. The coast here is throughout a range of low, nearly uniform
cliffs, of a dull reddish hue.
500, north-west of Barnes, is the place of Chip’s Chine.
1000. The place of Ship-ledge ; a group of sand-rock beds, which runs out far into the sea, and
is rendered more solid by concretions of subcalcareous grit.
2300. The place of Grange Chine.
D. Grayee Caine to Brook Cu1neE; 5600 paces.
635—660. A bed of sand-rock rises at 635 from Grange Chine, and at 800 is very near the
top of the cliff.
790, is nearly the place of a chasm in the cliff, perhaps Jackman’s Chine ?
1500. The middle point of Chilton Chine. Hence to Bull-rock-ledge, reddish and variegated
marly sand and clay appear to form the shore.
VOL, IV.—SECOND SERIES, 2D
ah b btn Tag [iO gev) Ng AC ee Oe h ae
200 Dr. Firron on the Strata below the Chalk.
1900—2000. A bed or group of sand-rock, beneath reddish and variegated marly clay and sand,
here occupies the shore for about 100 paces, forming before it rises one of the principal ledges
of the coast, which stretches far into the sea, and is called Bull-rock-ledge. This bed in its pro-
gress westwards is a remarkable feature in the cliff. It is from 15 to 20 feet thick, and rises
gradually to the north-west; attaining its greatest height above the sea near a gap or chasm
at Southmore, and then declining very slowly, till it comes down to the shore between 1000
and 900 from Brook Chine. It seems therefore to form a curve; which, however, is only |
apparent, resulting from the general rise of all the strata from the interior towards the sea,
combined with the curvilinear prominence of the coast between Chilton and Brook Chines.
The true relation of the beds here is explained in the transverse section, Plate X. b. fig. 4.
This sand-rock bed, in its progress through the extensive space just mentioned, is of nearly
uniform character, the chief difference arising-from the frequent concretion of the sand into
subcalcareous grit. In several places, the fallen blocks contain cylindrical stems of Siphonia,
with shells, occasionally, of the genera Cyclas, Paludina, and Unio; and the grey sand-rock
includes small patches or specks of greenish clay.
The cliff beneath the apparent curve formed by the sand-rock bed, consists throughout of
dark reddish and variegated marl, or sandy clay, which seems to form all the lower portion of
the prominence at Southmore; the greatest height which it attains being about 30 feet above
the sea.
In approaching Brook Chine, from the spot where the sand-rock bed above mentioned sinks
below the shore, the cliff is low and partially covered with grass, but seems to consist of red-
dish and variegated clays.
A bed of firm grey sand-rock rises at a small angle from the south-east, about 300 paces
from Brook Chine, which it crosses, and forming a very slight but really existing curve, goes
down about 320 paces beyond it, on the north-west ; the highest point being near the middle of
the Chine. All below this curved sand-rock bed consists of dull red and greenish variegated
clays: these are seen especially in the north-west side of the cove, or bay, which leads to Brook
Chine; and the floor beneath high-water mark is composed of them.
(101.) Strata on the South-West Coast of the Istz or Wieu7, from the
Shore under Arron Down to Broox Cuine.
The line of the coast immediately under Afton Down cuts the strata very obliquely. The Upper
green-sand does not offer any important difference from that of the section under Bembridge Down
on the east of Sandown Bay. The following measurement commences with the rise of the Gault,
which is distinctly marked, this stratum occupying a valley or depression between the upper and
lower green-sands.
0Q0—170 is the width of the oblique section of the Gault.
170—725. Lower green-sand :—affording nothing so different from the other sections in this f
island already described as to require detail.
512. The middle point of Compton Chine.
725—1076. The Weald clay (which appears on the beach below the cliff about 710), first rises
distinctly above the beach at 725; and thence for a considerable space the shore is occupied 1a
by mud and fallen ruins, the remainder of the original cliff being thrown back. Blue clay,
however, is visible, apparently in situ, at several points along the shore, and fragments of a thin
bed of limestone full of Cyclades, are frequent.
CN, Oe Oe eae,
Dr. Firton on the Strata below the Chalk. 201
1066. At this point a few regular beds of limestone, six to nine inches in thickness, composed
in a great measure of Cyclades, and alternating with shale abounding in Cypris, are dug out of
the cliff to be burnt for lime.
1076. Here beds of reddish clay or marly sand, (like those which occur below the Weald Clay on
the coast from Atherfield to Brook Chine,) make their appearance, and occupy the shore to
about 1850, where blue clay and shale are found again*.
1100. Shore much obscured by the fallen ruins of the strata.
1200. In the remoter cliff, beds of dark bluish shale are seen, above the reddish clay.
1200—1224. Very red clay on the shore.
1276. A bed of reddish and variegated sandy clay rises, evidently in situ; and thence to 1500,
all the nearer and lower part of the cliff is composed of it, in ruins. Above, in the more distant
cliff, is the blue clay of the Wealds.
1450. Reddish and variegated clay appear in situ on the shore.
1500. A bed of sand-rock of a yellowish grey colour rises. Immediately over it, at 1530, is
dark mottled clay, with much pyrites and coal.
[1600—1850. An under cliff on the immediate shore. ]
1630. A group of beds of sand-rock rises, about 10 feet thick.
1710. Thin beds of sand, with lignite, on the shore in the under cliff. In the remoter cliff is a
small chasm or chine at the top onlyf.
1886. Bluish beds of slaty clay again rise on the shore, in which Cypris Valdensis occurs abun-
dantly. Strata hence to the next Chine much contorted.
1980. A small opening or chasm, called “ Twenty-acres Chine,” on the east of which the cliff is
about 40 feet high. At the upper part, immediately below the diluvium, are beds of bluish
shale in situ.
[At the top, all along the cliff, from about 1850 to Brook Chine, is a coating of diluvial
' Joam and gravel of a very red colour, and 10 or 15 feet thick.
All the strata in the cliffs hereabouts, from 2000 onwards, rise towards the south-east.
They are visible also very distinctly on the shore beneath high-water mark. Compare these
with the strata on the west of Hastings (80.) to (84.).]
2073. A strong band of sand-rock, 4 feet thick ; thin shale 2 feet below.
2090. A bed of iron ore, about six inches thick, with Paludine.
2100. Sand-rock 6 feet thick ; false stratification remarkable.
2140. Stony bands, in shale, with Paludina elongata.
2173—2185. A strong band of firm sand-rock, about 4 feet thick rises ; nodules of grit at the
lower part, immediately above the dark red clay.
2190. Dark reddish clay, apparently continued to 2400.
* The weather was so bad during my examination of this part of the coast, that it was out of
my power to ascertain the cause of this recurrence of the Weald-Clay, after the appearance of the
sands and variegated marl. It may be no more than the effect of subsidence ; and the second mass
of clay, the beds of which are contorted, may have fallen from the heights above; the remoter
undisturbed cliffs consisting apparently of sand at the bottom, and at the top of blue clay and shale.
But, on the other hand, the existence of one or more faults might be expected in this part of
the island; for it is not probable that the great mass of strata, which are nearly vertical in
the central range, should return so soon to the slight inclination in an opposite direction, which
they exhibit on the south, without the formation of cracks, The question is locally interesting,
but does not affect the general order and proportion of the formations. ; ¥
f This remote cliff was not examined, for the reason given in the last note.
2p2
202 | Dr. Firron on the Strata below the Chalk.
2370. Biddlecombe’s Chine; cliff‘on the east of it, about 25 feet high.
2400—2410. A strong sand-bed rises to the middle of Compton-Grange Chine, on the north-west
side.
2410—2552. All reddish and variegated clay; diluvium still at top.
2462 Middle of ‘ Compton-Grange Chine.”
[On the shore, at the mouth of this Chine, are large masses of angular, grey and yellowish,
flint fragments, cemented by ferruginous matter. The coast from hence to Brook Point runs
out uniformly in the same direction. ]
2552. A strong band of reddish sand-rock ; goes out at 2615.
2582—2658. Reddish and greenish clay and sand.
2658. A bed of sand-rock rises ; under it is reddish matter, but concealed on the shore.
2694—2700. A bed of sand-rock rises, about 4 feet thick, with reddish stains and spots, like those
of the new red sand-stone.
2700—2822. Dark red and variegated marly clay seems to occupy all this space.
2843—2855. A bed of fine-grained sand-rock, which forms a ledge in the sea, (the first from
Compton-Grange Chine) rises about 2845, and goes out under the diluvium at the top of the
cliff, about 3000, very near to Brook Point. It may possibly be the same with that which re-
appears on the other side of the point, and crosses the upper part of Brook Chine.
2855—2952. Variegated, wine-red and greenish, cohesive sand, not effervescent, occupies this
space on the shore, and forms the upper part of the Point and nearly the whole of the cliff below
the diluvium thence to near Brook Chine.
2952—3030. A group, consisting of sand and sand-rock, with concretions of subcalcareous grit.
This forms the base of the Point; and the upper beds of the group seem to go down, beneath the
variegated sand of the last-mentioned stratum, between the Point and Brook Chine. The boat-
men informed me that some of the ledges of sand and sand-rock run out several miles into the
sea from this part of the coast. The lower part of this group includes, in great numbers, large
trunks of petrified coniferous wood*, frequently of a dark brown colour, penetrated by car-
bonate of lime and effervescing abundantly with acids; the cracks by which they are traversed
being filled with the same substance. At very low tides, compact variegated sand, like that
which abounds on other parts of this coast, appears below the sand-rock of the Point, and
seems to be the lowest visible stratum of the island.
The extremity of Brook Point is about 3060 paces from the rise of the Gault under Afton
Down, measuring along the shore ; thence to the Chine the shore turns inwards a little towards
the east, and the distance is about 830 paces; of which about 250 are occupied by the sand-
rock of the Point, beneath the variegated clay. About 320 paces from the Chine a bed of firm
sand-rock rises, and crossing the upper part of it, forms a slight curve: it is, in fact, a con-
tinuation of that already mentioned, which rises about 300 paces on the south-west of the Chine.
3890. The middle of Brook Chine is about 3890 paces, reckoning round the Point, from the top
of the Gault under AftonDown.
(102.) Fossils of the Beds below the Chalk in the Istz or Wreurt.
[Upper Green-sand. |
Ammonites cinctus. East End. In grey marly chalk, with few green particles.
A — Mantellii, Western Lines. Some of the specimens compressed into
ovals.
* See Webster’s Isle of Wight, p. 153—4.
Dr. Firton on the Strata below the Chalk. — 203
Ammonites Mantellii? A variety without tubercles. Western Lines. Sandrock near
Niton. ‘
A—_—— Seliguinus. Fast End.
A— varians, East End. Bonchurch. Grey chalk marl. Western Lines.
Belemnites. Western Lines.
Cardium. Western Lines.
Cucullea glabra. Western Lines.
C decussata? Western Lines.
Exogyra undata. Western Lines.
Gryphea canaliculata. Western Lines?
vesiculosa. Kast End and Western Lines.
Nautilus compressus. Western Lines?
Pecten orbicularis. East End: some specimens very large.
P quadricostatus. Kast End. Western Lines.
Plagiostoma Hoperi? Western Lines.
Plicatuia inflata. Western Lines.
Siphonia Websterii. Parkinson, Int.Org. Rem. Western Lines. Figured by Mr.
Webster, Geological Transactions, 1st Series, vol. ii. pl. 27—30.
Solarium conoideum. PI. XI. f.14. Western Lines.
S ornatum. PI. XI. f.13. Western Lines.
Spatangus. Near the Sandrock Spring.
Terebratula depressa? Western Lines.
T. — pisum. Western Lines.
T————- (new). Western Lines.
Trochus. Western Lines. St. Boniface. Upper Green-sand, or Chalk Marl.
Turrilites tuberculatus. Near Bonchurch.
Venus? Western Lines.
Vermetus umbonatus. (Vermicularia umbonata, Min. Con.) Western Lines. Large
specimens ?
V——— polygonatus. Bonchurch and Ventnor Cove.
[ Gault. |
Ammonites Seliguinus (syn. A. Beudantii.) East End.
Gryphea. East End.
Myamandibula. Kast End.
Pecien orbicularis. Compton Bay: In harsh gritty Gault.
Dig quinquecostatus~ Compton Bay.
Fisues. Obscure impressions of. East End.
Puants. Fucoides Targionii. (Ad. Brongniart, “ Végétaux Fossiles,” Pl. IV. fig. 6.;
and Mantell, “S. E. of England,” p. 166.) East End.
204 Dr. Firron on the Strata below the Chalk.
[Lower Green-sand. |
Ammonites furcatus. Pl. XIV. fig.17. Atherfield.
Astacus. East of Shanklin.
Astrea. East of Shanklin Chine, and Atherfield Point: in fuller’s earth.
Corbula striatula. West of Shanklin Chine, in ferruginous nedules, with many other
fossils. Near Atherfield.
Exogyra conica? Atherfield Point.
Gastrochena. In Coral, near Atherfield Point.
Gervillia aviculoides. West of Shanklin Chine. Atherfield Point.
G— solenoides. Same place: in ferruginous nodules.
Gryphea vesiculosa? Sandown Bay: in a mass of yellowish sand, with polished
fragments of brown iron ore.
sinuata. Kast of Shanklin Chine: in ferruginous sand, with dark particles
and fragments of iron ore. Frequent on the east of Atherfield Point. Near
Niton: very large.
Inoceramus concentricus. Near Atherfield: in fuller’s earth: in sandy stone, with
vegetable impressions (Fucoides Targionit ?).
Lingula. Barnes’s Chine. Isle of Wight?
Modiola depressa? Near Atherfield: in fuller’s earth.
Mya plicata. (See Panopea.)
Natica. In ferruginous nodules, West of Shanklin Chine.
Nautilus radiatus ?. Near Atherfield. This and other specimens from Kent very much
resemble N.radiatus, from Malton, Yorkshire. It is very distinct from N. elegans.
Ostrea carinata. East of Shanklin. Atherfield Point: in green sand and in the
fuller’s earth.
O macroptera. Near Atherfield.
Panopea plicata. Atherfield Point. East of Shanklin: with Serpula.
P. (new). Atherfield.
Pecten obliquus. Atherfield Point, with Terebratula Sella.
Perna quadrata? Fallen masses on the shore east of Shanklin Chine.
Pinna tetragona? Atherfield Point : in fuller’s earth.
P__ (new species?). Near Atherfield: in green sand, like the middle bed of Sand-
gate, Kent.
Plagiostoma elongatum. Atherfield Point: in fuller’s earth.
Rostellaria calcarata. Shanklin, top of the cliff, west of Chine: in ferruginous no-
dules, with many other fossils.
G
Rostellaria Parkinsonii. Shanklin: in ferruginous nodules. Same situation.
Serpula antiquata? Atherfield Point: fuller’s earth.
PS) Another species, with Ostrea. Atherfield. Cowleaze Chine.
Spatangus. Kast of Shanklin. Atherfield. Cowleaze Chine? fuller’s earth.
Sphera corrugata. Shanklin, (large specimens.) Sandown Bay.
Siphonia. Near Atherfield Point: in green sand.
Dr. Firton on the Strata below the Chalk. 205
Terebratula biplicata. Chale Bay.
T——— Gibbsiana. Atherfield Point.
T: latissima. Near Atherfield.
T- — nuciformis. East of Shanklin.
T— Sella. Sandown Bay. Atherfield Point: in greens and, and in fuller’s
earth. With Pecten obliquus; Chale Bay.
T———— parvirostris. Pl. XIV. f.13. Debris on the shore east of Shanklin.
Thetis major. Atherfield Hill. Blocks loose on the shore.
T— minor. In ferruginous nodules, west of Shanklin Chine.
Trigonia alaformis. East of Shanklin; of unusually large size : and in ferruginous
nodules, west of the Chine. Atherfield Point; large, in sand very like the
middle Sandgate bed.
Turbo conicus. West of Shanklin Chine: in ferruginous nodules.
T— rotundatus? Shanklin.
Turrilites? Near Atherfield.
Vermetus concavus. With Terebratula Sella: Atherfield ; and east of Shanklin.
[| Wealden. |
Ammonites. A fragment imbedded in a portion of Sussex marble, with Cyclas, Ostrea,
and Paludina elongata. This Ammonite probably formed part of a foreign mass
accidentally brought into the Weald clay, during the progress of its deposition.
Cyclas major. Atherfield Rock, in Sussex marble and Weald clay: also forming
singular prominences on thin layers of stone; see p. 197 line 24, and p. 198.
Cowleaze Chine. In ironstone, west of Skepherd’s Chine. Barnes’s Chine, very
large. Compton Bay.
media. Sandown Bay. Atherfield Rock, about 2 inches thick, in a bed al-
most composed of these shells, incrusted with fibrous carbonate of lime. West
of Shepherd’s Chine: in coarse ferruginous sandrock, probably one of the sub-
ordinate beds of the Weald clay: in pyrites. Cowleaze Chine. Barnes’s Chine.
membranacea. Sandown Bay : large, preserving its iridescence. Near Ather-
field. Shepherd’s Chine. Barnes’s Chine.
C (A thick and gibbose species.) Sandown Bay in ironstone.
Cypris Valdensis. Pl. XXI. fig. 1. Occurs throughout the Wealden. At Sandown
Bay ; Atherfield ; Shepherd’s Chine ; Cowleaze Chine; Barnes’s Chine ; Under
Barnes’s High; Brook Point; Compton Bay.
Cypris tuberculata. PJ. X XI. fig.2. Near Atherfield and Cowleaze Chine.
Modiola (new). Sandown Bay.
Ostrea. A bed of limestone nearly composed of oyster shells occurs in the Weald-
- clay at Sandown Bay; near Barnes’s Chine; and on the west of Compton-
Grange Chine.
Paludina acuminata. Near Atherfield. Near Barnes’s Chine (young).
P elongata. Occurs throughout the Wealden. Sandown Bay : in ironstone.
Atherfield Rock: in clay. Tiepit, near Atherfield. Cowleaze Chine: in no-
C.
C.
206 Dr. Firton on the Strata below the Chalk.
dular masses of ironstone. West of Shepherd’s Chine. Near Barne’s Chine:
in stem-like masses of pyrites. Under Barnes’s High. West of Compton Chine.
Paludina fluviorum. Sandown Bay, with Ostrea, Cyclas, and Paludina elongata: in
a course of stone, about 2 inches thick : also with Cypris Faba, in similar stone.
Potamides? In clay, Sandown Bay.
Remains or Fisnes. Scales of one or more species of Lepisosteus, (Lepidotus of
Agassiz,) apparently the same with those which are frequent in the Wealden of
Kent and Sussex, are found in the Weald-clay at Sandown Bay: as are also the
teeth, vertebra, and other bones of some small species of fishes, at Sandown
Bay ; near Atherfield Point; and at Cowleaze Chine.
Large concretional masses with small tubular erosions on the surface, much
resembling those of Sandgate in Kent (13.), containing a large proportion of
phosphate of lime, and affording during solution the smell of Coprolite, have
been found at Atherfield.
Rerrtites. The tveebone of a very large Igwanodon, found under the cliffs of the
Wealden strata on the shore of Sandown Bay,—and fragments of other bones,
probably of the same animal, found near Brook Point?, have been described
by Dr. Buckland, Geol. Trans. 2nd Series, vol. iii. p. 421.
Portions of the teeth of another Saurian, probably a Crocodile, have also been
found at Sandown Bay.
Puants. Impressions of the leaves of a species of Fern: in the Wealden sand-rock :
at Sandown Bay, and on the east of Barnes’s Chine.
DorsETSHIRE.
(103.) Isle of Purbeck.—The principal additions which I have to make, to
what Mr. Webster has published on the Isle of Purbeck*, are the distinction
of the ferruginous sands below the chalk, which contain marine fossils, from
the representative of the Hastings sands; and the indication of a stratum
between the Portland stone and the Kimmeridge clay, which I propose to
distinguish by the name of the Portland sand.
The section, Pl. X.a. No.8. represents the coast on the east of the Isle of
Purbeck, from the chalk at Ballard Down to Durlstone Head; and No. 9.a
section near the middle of the peninsula, from the Chalk to the shore of Kim-
meridge-bay, of part of which Plate X. b. fig. 6. is an enlarged illustration.
In the coast section on the east of Purbeck the whole series from the chalk
down to the Portland stone is disclosed}: the Upper green-sand, Gault,
* Letters to Sir H. Englefield ; and Geol. Trans. 2nd Series, vol. ii. p. 37—41.
+ A beautiful view of this section of the Isle of Purbeck is visible with a telescope, from
the heights on the west of the Isle of Wight; and reciprocally, the transverse section of the latter
Dr. Firron on the Strata below the Chalk. 207
Lower green-sand, and Weald clay, in strata highly inclined, occurring in a
nook or recess called Punfield, at the southern foot of Ballard Hill; and the
Hastings sands, occupying the whole of the long range of cliffs thence
to the town of Swanage; the section of which is so distinct, that with
sufficient labour all the details can be made out. The strata correspond,
however, precisely with what I have mentioned in the preceding accounts
of the Isle of Wight and of the coast near Hastings*, and, as at those places,
consist of sand and sand-rock, including concretions of calcareous grit, and
alternating with a very large proportion of reddish and greenish cohesive
sandy clay. Detached portions of lignite are frequent also throughout the
series here. Fragments of the trunks of silicified coniferous trees have
been found in dark brown masses; and detached bones of the Iguanodon
sometimes occur loose on the shore beneath the cliffs near the town of
Swanagey.
The Hastings sands can be traced entirely across the peninsula to Wor-
barrow Bay, in a range of heights passing through Godlingston, south of
Westwood, Steeple, North Egleston, and Tineham: but the subdivisions
between the sands and the chalk become indistinct on the west of Punfield ;
a slight difference only in the hue of the vegetation on the surface indicating
in some places the presence of the Weald clay. The junction of the sands
with the Purbeck strata is concealed, at Swanage, under the level tract which
separates the sand cliffs from the hill above the town: and the only place
among the numerous sections westward, in which the connexion between the
Hastings and the Purbeck strata is visible, is on the south side of Worbarrow
Bay. At the time of my examination, the appearances there were not distinct,
but I shall here insert what I observed, as these beds are supposed to represent
the strata on the north-west of Battle, which have been considered as the
lowest in Sussex.
island forms a very striking object from the hill above the town of Swanage. Views thus seen
from a sufficient distance have all the abstract clearness of a geological outline; while the mi-
nutest features are preserved without any departure from the true proportion of height to hori-
zontal distance.
* For this reason I have thought it unnecessary to insert here the list of these strata to which
I have referred above, (79.). The spaces which the several formations occupy, measured along
the foot of the cliff, are thus: Upper green-sand, about 250 paces; Gault, 200; Lower green-
sand, 240?; Weald-clay, 46?; Hastings sands, 3,500 ;—Total distance from the chalk to the
bottom of the sands, about 4,250 paces. A flat of about 200 paces intervenes between the sand
cliffs and the rise of the Purbeck strata. Compare these spaces with those at Man-of-war Cove,
hereafter (110.).
ft See Dr. Buckland’s paper, Geol. Trans. 2nd Series, vol. iii. p- 421,
VOL. IV.—SECOND SERIES, 25
208 Dr. Firron on the Strata below the Chalk.
Beds on the confines of the Hastings sand and the Purbeck strata, at Worbarrow Bay*.
Paces. Paces.
Grey sand, occupying on the shore .... 8 Clay and limestone, including the ‘‘ Lean-
Welfowish sand 22/20 auc ss tee ee sees 5 ing vein ” of the quarries on the east of
A space concealed at top; where visible Purbeck. [ Que. the ‘ Lane-end Vein”
the beds consist of grey clay, bitumi- of Mr. Webster?) c'> ste sete’ ojcletsteme ?
nous or carboniferous, which includes at
the bottom concretions of quartzose Here the ground rises into the promi-
grit, and contains Cyclades.......... 9 nence called Worbarrow Knob; and the
A group including beds of stone com- back on top of a very extensive mass of
posed of small Paludinz, in a cement stone is waved, like the ripple-mark on
containing much green matter :—the the sea-shore. In the little cove between
“marble” and “marble-rag” of the the “knob” and Gad Cliff, a thickness
Swanage quarry-men .........-...- 16 of about 50 feet consists of clay, alter-
Brownand grey clay,alternating with bluish nating with beds of limestone very much
grit, and thin beds of stone .... About 25 contorted.
(104.) Purbeck strata—The ridge of the Purbeck and Portland strata
runs nearly from east to west, entirely across the peninsula; but the dip is
not uniform, and the strata form a curve, or a portion of a dome-like promi-
nence, of which the highest part is between Acton, St. Alban’s Head, and the
heights above Kimmeridge, and thence to Tineham Hat; the culminating
point being about Swyre Head, which seems to be about 700 feet above the
sea,—nearly on a level with the chalk down at the western extremity of Pur-
beck Hill, and perhaps 100 feet higher than the summit of Ballard Downy.
The whole of the Purbeck series is exposed in the ruinous cliffs of Durl-
stone Bay, where the strata have been enumerated in detail by Mr. Webster.
At the upper part they consist of compact limestone, alternating with clay,
and abounding in freshwater shells, especially of the genus Cyclas: but in-
cluding also a thick bed called “ cinder” by the quarry-men, which is almost
entirely composed of oyster-sheils. At the lower part, the formation consists
principally of fissile limestone, the junction of which with the Portland strata
exhibits some very remarkable appearances.
All the stone which is quarried at present, occurs in the upper part of the
series; and from Mr. Webster’s list it appears that in a thickness of about
125 feet, 55 consist of beds of useful stone ; 12 feet of the “cinder’”’ composed
of oyster-shells ; and the remaining 58 of slaty clay, and thin beds of unpro-
fitable stone. I was informed that about 150 feet more, of what the work-
* This is the spelling of the Ordnance Map, and the word is so pronounced in the country. It
is sometimes printed War-borrow, and by Mr. Webster, Worth-barrow.
+ The top of the Down between Acton and Bottom, (about the place of the final s in “ Down-
shay’s Farm”, in the Ordnance Map), is much higher than St. Alban’s Head, and not much below
Swyre Head. It seems to be nearly level with Encombe Head (Hound’s-Tout), and the east
end of Ballard Down.
t Geol. Trans. 2nd Series, vol. ii. pp. 38, 39.
“
Dr. Frrron on the Strata below the Chalk. 209
men call “rubbish ” and “slate ’’, intervene between the lowest of the courses
(or “ veins’’) of good stone, and the top of the Portland formation ; so that
the total thickness of the Purbeck formation here is about 275 feet.
Ft. In. Ft. In.
Workable stone, and “rubbish”..........+..00. 99 O
EOIN Chik Vorers fo al's7a (slots. oi bie aie ete) steuthe@iaerabiesches op LZ of 124 8
Workable stone, and “rubbish”........c00ces+e- Lo 8
RIOR IRD AISA” GLACE 5 cterare cles vines Kio] a x/ofala: ayalatate’e! epeterare;e 6° 150770
HOO dence ace Gas sonore db coucoe nde 274 8
The high ground between Peverell Point and Durlstone Head is divided by a depression or
ravine, on the north of which, in addition to the flexures and contortions seen in all the sections,
and well represented in Mr. Webster's plates, the strata are traversed by fissures, produced by
upheaving, or subsidence, or both. The effect of these disturbances can be traced by means of
the “cinder” bed; disjointed portions of which are still visible, inclined at different angles, in
three or four successive falls, the first throwing down that bed more than 100 feet, and others 40,
15, and 3 feet. The fissures which separate the disjointed masses are widest at the top, and are
filled with fragments of the dislocated strata. The place where these derangements occur is
called “the Gulley”: on the south of it the strata are much less disturbed, and the “ cinder ” can
be traced almost continuously in its proper situation, till it disappears near the face of the hill,
not far from Durlstone Head.
The groups at the top of the formation called the ‘‘ Marble” and the “‘ Marble rag”, consist for
the greater part of small Paludinz, cemented by carbonate of lime with a very large proportion
of green matter. ‘These beds are exposed on the shore at Peverell Point*, and were quarried
many years ago at Langton, from which place it is said the pillars in the interior of Salisbury
Cathedral were obtained. Another stratum, also containing a large quantity of green matter, but
of a conglomerated or coarse sandy texture, is found at the top of the formation in some of the
sections westward,—as near Worbarrow Knob, and on the east of Lulworth Cove. It includes a
large and thick species of Unio; the shell, as Mr. Webster has remarked, being so abundant as to
constitute a very large proportion of the whole mass.
A characteristic of the upper part of the Purbeck series, both on the coast and in the interior,
is the occurrence of seams of fibrous carbonate of lime, frequently more than two inches thick,
and either detached within the beds of clay, or adhering to the limestone beds, like the thinner
crusts attached to the limestone of the Weald clay.
The bivalves, principally Cyclades, of which a great part of the Purbeck stone is composed, are
not less numerous, and commonly much more distinct, in the slaty clay of the “‘ rubbish” between
them ; which cannot be distinguished from the clay with Cyclades (‘‘ Shab”) of the limestone pits
on the north-west of Battle in Sussex. The “Slate”, a coarsely fissile limestone at the lowest
* A very remarkable appearance, which I am at a loss to explain, was observed by Mr. Bab-
bage and myself in 1824, on the back, or top of the Purbeck strata, at that time exposed on the
shore between the town of Swanage and Peverell Point. The surface there, which dipped at an
angle of 7° or 8° towards the north, was depressed in some places into nearly circular pits or
cavities, from 4 to 7 feet in diameter, and about a foot deep in the middle,—as if the beds had
been forced in by a violent blow; the depressed surface being divided by irregular but nearly
concentric cracks, which were filled with white sparry carbonate of lime. Three of these
depressions were visible ; two of them about 6 feet apart, one of which was 74 feet, the other
about 43 in diameter at the outeredge. A third, about 10 paces to the west of these, was of
smaller dimensions.
2E2
210 Dr. Firron on the Strata below the Chalk.
part of the Purbeck series, was formerly much quarried for roofing, in the hill above Tillywhim,
and near the south coast of the peninsula: and there, as well as in the corresponding beds of
Portland and the north of Weymouth, I have found in it casts in calcareous spar of one or more
species of Cypris.
(105.) Portland Stone.—This formation first appears upon the coast be-
neath the Purbeck strata at Durlstone Head, and rises slowly in the rocky
cliffs on the west of Tillywhim to a point about midway between Winspit
and St. Alban’s Head, where it is succeeded by the Portland sand. The stony
strata there retire as they rise from the shore, and occupy the margin of an
irregular space thence to Gad Cliff, where they return to the coast and sink
under the sea: so that between the extreme points of Durlstone Head and
Gad Cliff (or rather Worbarrow Knob, a rocky hummock on the west of that
place), a real curvature combined with the general inclination of the strata
towards the north, which is in some places very rapid, has caused an extensive
disclosure of the lower beds, excellent sections of which are visible on the
west of St. Alban’s Head. ‘Phe component strata of the Portland stone in
Purbeck, agree with those of the Isle of Portland, which have been described
by Mr. Webster.
(106.) Portland Sand.—I propose to give this name to a group of strata
which holds the place of that mentioned by Mr. Conybeare as occurring
beneath the equivalent of the Portland stone at Shotover Hill in Oxfordshire,
and in Bucks; and which in the interior contains a large proportion of
sand, including green particles, ascertained by Dr. Turner to be of the same
composition with those of the green sands beneath the chalk*. I have found
a similar group abounding in green matter, and containing, as at Shotover,
very large concretions of grit, in a corresponding place in the lower Bou-
lonnoist, where a great part of the formation consists of sand. But on
the Dorsetshire coast, and I believe, in the Vale of Wardour also, the beds
are generally of a dark grey colour, more coherent, less sandy, and the
calcareous matter which they contain, is more uniformly diffusedt. The
group is certainly of sufficient importance to require a separate name, and
that of Portland sand, while it expresses the more usual character, indi-
cates also its intimate connexion with the Portland stone. On the other hand,
it graduates into the Kimmeridge clay beneath; and its position seems to be
* See above, (10.) note §. t Geol. Soc. Proceedings, vol. i. pp. 9 and 27.
t{ On the west of Upway, however, near the coast of Dorsetshire, nearly half the substance of
this stratum is made up of grains of green earth; and along the whole line of the formation in
that quarter, the prevailing character is that of siliceous sand and green earth.—See Dr.Buckland’s
and Mr. De la Beche’s Memoir, in the preceding part of this volume: p. 20, and note.
Dr. Pyios on the Strata below the Chalk. 211
analogous to that of the sand and subcalcareous grit which occur between
the Oxford oolite and Oxford clay,—the inferior oolite and the lias clay : ??
The whole mass of strata deposited in the first instance, having been in all
these cases, sand and mud; the upper part of which abounding more in calca-
reous matter, was subsequently converted into stone, and the lower more or:
less concreted into nodular masses of calciferous grit, in proportion to the
quantity of carbonate of lime diffused through it.
In the Isle of Purbeck, the Portland sand first rises above the sea about midway between
Winspit and the point of St. Alban’s Head, and is disclosed by denudation on the north of that
remarkable promontory, in a ravine called Pier Bottom, near which place the Kimmeridge clay
appears to rise on the shore. A good section of the sand is visible at Emmet’s Hill, a ridge
capped with Portland stone, between Pier Bottom and Chapman’s Pool; and the group may be
traced thence, beneath a capping of stone, all round the inflections of the high ground from
Bottom Farm, by the prominences called Encombe Point (or Hound’s Tout), and Swyre Head,
through Kimmeridge, to Gad Cliff, where it declines along with the stone and sinks again under
the sea. Its relative place and its effect in modifying the surface, are well seen in the amphi-
theatre of high ground which nearly encircles Kimmeridge Bay ; of part of which Pl. X. a. No. 9,
and X. b. fig. 6, are illustrations: the summits all around consisting of Portland stone, and
the rapid grass-covered slope beneath of this sand, resting upon a tract comparatively flat and
uniform, which is occupied by the clay of Kimmeridge. The sand again makes its appear-
ance on the coast west of Purbeck, in a small portion distinguishable by its bluish grey colour,
beneath the rocky cliffs called Horsewalls, which form the most prominent part of the shore
between Lulworth and Durdle Cove. In the complex and disturbed tract on the north and west
of Whitenore, the Portland sand is found wherever the superior strata rise high enough to dis-
close it; and in the Isle of Portland it everywhere accompanies the stone, and has the same
characters as on the coast of Purbeck.
The following is a List of the strata at Emmet's Hill, immediately on the north of St. Alban’s
Head :—PI. X. b. figs. 5 and 6.
Feet.
1. Portland stone, with layers of flint near the bottom, forming a shattered and inac-
cessible precipice at the top of the cliff .............-. ‘ geacdsare 50 to 40 feet
2. Portland sand. Soft stone, or marly coherent sand, with a rugged external surface ]
of a yellowish grey or brownish colour; but in the recent fracture, of a dark bluish
or greenish grey. It includes concretions of firmer consistence. In a bed of stone 25 to 80
uv
of the same description at the cross-roads above Kimmeridge Farm, which seems to
belong to the same place in the series, Trigonia clavellata, Ammonites giganteus,
RNR AE ERIE SATE MNO iol ««) Scie: a) + <a =, cio aie, 0igila.s eivic ois 6 uo aveleiale o Seas 0 eles
3. Bluish grey, inclining to green, sandy clay and marl, including ranges of con-
cretions approaching to stone: the whole effervescing with acids. The more stony |
portions acquire by exposure a yellowish brown tinge, and are in some places
coated with a crust of white pulverulent carbonate of lime. A bed of this group
dug for building near Bottom Farm, consists of bluish grey sandy stone, but t about 60
slightly effervescent, and is streaked or mottled with portions of a darker hue. In
some other places the strata are divided by fissures into nearly vertical flakes,
two and three feet in thickness, and include occasionally nodules of much more
CUT UAE USSD A Gen COC ODOT COO OCOR OTH OO CO OONOMC OO Er sere evcces eons
212 Dr. Firron on the Strata below the Chalk.
Feet.
4. A rugged platform at the foot of the cliff above described, is covered with }
debris, and partially clothed with shrubs and vegetation. The beds appear to
be :—
a. Soft, dark bluish grey, effervescent sand-rock, or indurated marl, including a
band of firmer consistence, which contains casts of Panopea depressa and other
bivalves. | 40 to 58
6. Brownish marly sand-rock, softer than a.
c. A firmer stratum, including, about 20 feet from the bottom, large subglobular,
but nearly continuous concretions of greater firmness, which also contain casts of
Panopea depressa and other fossils.
[These concretional masses, not improbably represent the great nodules of
Shotover Hill in Oxfordshire. ]
Total estimated thickness of the sand....... Beco ar ona seeseesee 120 to 140
Springs break out at the bottom of this group, where the Kimmeridge clay might be ex-
pected. The total height from the top of the cliff may be between 250 and 280 feet.
(107.) Kimmeridge clay.—The clay which has obtained its name from the
farm and bay of Kimmeridge, rises from beneath the beds last mentioned,—on
the east, near the point or southern prominence of St. Alban’s Head, and
on the west, immediately under the lofty precipices of Gad Cliff. It occupies,
apparently, the whole of the low undulating tract which intervenes between
these extreme points ; and is capped, about the middle, by the projecting mass
of Portland stone and sand which forms the summit of Swyre Head. The
bituminous strata which characterize this formation are seen with greater
distinctness on the shore of Kimmeridge Bay, as the coarse sand, grit, and
limestone found between them and the Oxford oolite on the north-east of
Weymouth, do not come up to the surface in the peninsula of Purbeck.
The little promontory of Hen Cliff may be considered as the centre of an
almost semi-circular space, which is continued in a narrow slip or platform,
along the shore to Pier Bottom: Plate X. b. fig. 6.
The strata on the shore at Kimmeridge Bay form a low dome-shaped prominence, the cul-
minating point of which is at some distance from the ridge of the Isle of Purbeck. At Broad-
bench, where they are very well displayed, they rise with a very slight inclination from the south;
and rise also from beneath Gad Cliff on the west; but at Hen Cliff the dip is towards the south-
east, conformably to the general disposition of the strata beneath St. Alban’s, and thence to Durl-
stone Head; while it is obvious that under the main ridge of the peninsula they must dip to the
north, along with Portland and Purbeck strata. The rise of the beds from the sea, where the
shore is cut into by the circular erosion at Kimmeridge, has produced an apparent curve in the
cliffs around the bay; so that the strata seem to rise from the sea near Broadbench, and to de-
cline again as the line of the coast returns toward the south in approaching Hen Cliff. The
natural sections hereabouts are very distinct; and a considerable surface also of some of the
strata is exposed upon the shore, consisting apparently of the lowest beds in the Isle of Purbeck.
The coast at Kimmeridge Bay is probably not less than 400 feet below the bottom of the Port-
land stone; and if 100 feet of that interval be assigned to the Portland sand, it will follow that
Dr, Firron on the Strata below the Chalk. 213
about 300 feet of the bituminous Kimmeridge clay are disclosed on the coast of Purbeck;
which probably, is not far from the total thickness of the formation.
The beds here consist in general of bituminous fissile clay in a large proportion, alternating
with thin courses of brown subcalcareous stone, or bituminous limestone. The clay in some
cases contains so much bituminous matter, as to be used for fuel under the name of “coal*”; in
others it contains a large proportion of carbonate of lime, alternating with the laminz of the clay.
To these more calcareous and whiter beds the name of “ White Lias” is given in the neigh-
bourhood.
The connexion of the Kimmeridge clay with the Portland sand and stone is visible, though the
section is in some points inaccessible, at a place between Gad Cliff and the commencement of the
lower cliffs of the bay, where the following was the order :—
1. Dark sandy marl (Portland sand) about 100 feet. A specimen taken here about 100 feet
below the Portland stone, consists of light grey, soft, caleareous matter, including minute green
particles in very large proportion; the whole very much resembling some portions of the
Upper, and of the middle strata of the Lower green-sand.
2. A series of beds about 30 feet in thickness, composed of shale, in part so bituminous as to
serve the purposes of fuel; in other places passing into a very bituminous soft fissile limestone
(“ White lias”) of a light brown or grey colour, which on decomposing becomes almost white.
The dark surfaces of the fissile beds are spotted with numerous light grey specks, probably the
remains of organized bodies.
Another form in which calcareous stone alternates with the bituminous shale above mentioned,
is that of a dark brown stone,—sometimes of the consistence of indurated marl, effervescing
freely, sometimes acquiring a flat conchoidal fracture and greater hardness, and but slightly
effervescent.
The strata around Kimmeridge Bay, which seem to belong to a lower part of the series than
the second group above mentioned, include a remarkable bed of brown, bituminous, and some-
what gritty limestone, about two feet thick, which is divisible into rhomboidal fragments. This
is succeeded by a considerable thickness of shale, less bituminous than the “ coal”; which in-
cludes with other fossils, great numbers of Ammonites biplex much compressed, and alternates with
thin beds of the limestone. At Hen Cliff three or four such beds occur in the shale. One of the
same character is conspicuous in the arch or curve of the cliff at Kimmeridge Bay, and another
about 30 feet below, seems to be the lowest stratum of the Isle of Purbeck.
The Kimmeridge clay, sinks into the sea at Gad Cliff, and does not again
appear till after an interval of seven or eight miles, where a very good sec-
tion is visible in Ringstead Bay on the west of Whitenore. The beds which
occupy the shore thence to Weymouth Bay form the transition from this
clay into the Oxford oolite; and as a full account of them will be given by
Dr. Buckland and Mr. De la Beche+, I shall only mention here that the
* It burns with a bright flame, emitting a very disagreeable smell, and leaves a grey, light, and
spongy cinder.
t+ The country around Weymouth had been previously illustrated by a paper of Professor
Sedgwick, in the Annals of Philosophy for 1826, vol. xi. p. 339, &c.; where its resemblance to
the cliffs near Scarborough was pointed out, and the relations of the beds between the Port-
land strata and the Oxford oolite, in different places, explained. The Memoir of Dr. Buckland
214 Dr. Fitron on the Strata below the Chalk.
whole of this series, including both the bituminous strata of Kimmeridge,
and the more complex group beneath, is fully developed in the Lower Bou-
lonnois, of which I have given an account in another paper read before this
Society *; and that the coast of Yorkshire near Scarborough is composed of
similar strata t.
(108.) On a general view from the heights in Purbeck or Portland, of the
great bay or excavation of the coast, of which the Isle of Purbeck forms the
east wing, and that of Portland the western promontory, it is natural to
suppose that the strata in both places are the remaining portions of a wide
plane, which at one time passed continuously through both places, and formed
the reflected portion of that which rises from beneath the chalk and runs
in a nearly uniform direction from Ballard Hill to the heights near Lulworth
Cove. This ridge, if continued, would pass through Weymouth: but the
chalk is suddenly interrupted at Whitenore Cliff, and its main outcrop on the
west of that place, being directed towards a point about 15° or 16° north of
west, makes an angle of about 20° with its previous range through the Isle
of Purbeck. On a close examination, this change is found to be attended
with some very remarkable circumstances ; the coast on the north and west
of Whitenore having been the scene of great disturbance, by which a very
complex series of faults has been produced. The general disposition of
the strata, however, is still that of a saddle ; the northern side of which dips
to the east of north, while the beds in the Isle of Portland, (the only re-
maining portion of the slope on the south side,) dechine towards a point about
48° east of southt. The upper beds of Portland are therefore but a part:
of the mantle-shaped covering which once enveloped the lower strata both
in Portland and in the intermediate space from thence to Kimmeridge Bay,
where indications of the mantle-shaped arrangement are still visible; the
strata on the east of the bay sinking into the sea between Tillywhim and
Durlstone Head, very much in the same manner as they do at the Bill of
and Mr. De la Beche, so often referred to in the text, has been printed in the beginning of the
present volume of the Geological Transactions.
* Proceedings, vol. i. p. 6.
+ Sedgwick; Ann. of Phil. 1826. J. Phillips; Geology of Yorkshire, 4to, 1829.
+ The strike in Portland is well determined by the position of the two points on the opposite
side of the island, where the beds beneath the stone rise from the sea. ‘These are,—on the west
coast, a spot almost due west of the words “ H™. Light” in the Ordnance Map; and, on the east
coast, the place where the shore is cut by a line passing through the letter ¢ in “‘ Church-hope,”
and the bottom of the letter £ in the word “iste”. The line joining these opposite points,
makes an angle of about 48° with the meridian; the dip being consequently directed to about 48°
east of south. See the Map, Plate VIII.
Dr. Firron on the Strata below the Chalk. 215
Portland. The structure in this case is, in fact, analogous to that of the
Isle of Wight; except that the top of the curve has in that place been car-
ried away, and that what remains of the upper strata on the south of the
island is much less inclined.
(109.) Coast west of Purbeck.—The sections west of the Isle of Pur-
beck, as far as Whitenore on the coast of Dorsetshire, have been generally
described and represented by Mr. Webster with his usual clearness *, but
have not yet been examined in detail. The Purbeck strata especially are
disclosed there under a great variety of aspects, no fewer than nine sections
of the beds between the chalk and Portland stone being visible, on the shore
of the small bays by which the coast is indented, within the short space of five
miles +. One of the most remarkable circumstances in the structure of this
part of the coast, is the rapid convergence of the strata in proceeding west-
ward from the Isle of Wight; the total distance from the top of the green-
sand to the beginning of the Portland stone, which, between Ballard Downs
and Durlstone Head is about two miles and a half, beg reduced to about
150 paces at Durdle Cove. The sectional sketches Pl. X.a. Nos.8. to 10’,
which are drawn to the same scale, exhibit the proportion of this reduction ;
and PI. X. b. figs. 7. and 8., show ona much larger scale, the detail of the beds
in the east side of Lulworth Cove, and on the east of the isthmus connecting
the ridge of Portland stone with the chalk, at Man-of-War and Durdle Coves;
beyond which some detached vertical masses, standing out in the sea like
walls, and successively coming nearer to the main cliff, are the last indica-
tions of the beds below the chalk upon this part of the coast.
In these western sections of the groups immediately below the chalk it is impossible to recog-
nise all the subdivisions of the coast of Kent, and the adjoining counties ; the separation between
the upper and lower green-sands having in a great measure disappeared, and the latter being
greatly reduced in thickness, or wholly united with the upper sands. In the Wealden, likewise,
the clay can scarcely be separated from the strata representing the Hastings-sands, which occupy
a considerable space ; and here, as in the Isle of Wight, the proportion of red and variegated
sandy clay to the ferrugimous sands is very great, one distinct group of such clay being observ-
* Letters, &c., pp. 185-6, 193-7.
+ These sections are: 1. Worbarrow Bay. 2. Mewp Cove, not named in the Ordnance Map.
3. Bacon Hall, a nook on the west of Mewp. 4. and 5. Lulworth Cove, east and west sides ;
Pl. X.a. No. 10.; and X.b. fig. 7. 6. Stare Cove. 7. West of Horse-walls. 8. Man-of-War Cove;
Pl. X.a. No. 10!., and Pl. X.b. fig. 8. 9. Durdle Cove. The coast hereabouts being difficult of
access, and the adjacent country thinly inhabited, I believe that the best stations for a geologist
who wishes to examine it with ease, would be Swanage, for the eastern part of the Isle of Purbeck ;
and East Lulworth, for the coast westward. A good boat should be taken in calm weather, at
Lulworth Cove or at Worbarrow, to view the cliffs from the sea.
VOL. IV.— SECOND SERIES. 2F
4
216 Dr. Firron on the Strata below the Chalk.
able at the top and another at the bottom of the sands. The curves and contortions of the. a
limestone beds in the Purbeck strata, where they alternate with clay, are strongly contrasted a
with the parallelism and regularity of the more uniform parts of the series, both in the sands
above, and the Purbeck and Portland formations below; the difference being probably ascribable 1
(as Mr. Conybeare, I believe, has remarked,) to the effect of lateral pressure, upon a mass con-
sisting of folia which differ so much in their power of resisting flexure and compression, as the
limestone and the clay.
Lulworth Cove.—The relative space occupied by the different groups below the chalk, on
the east side of this Cove, is as follows: (See Pl. X.a. No. 10.; and X.b. fig. 7.)
Ft. In.
1. Upper Green-sand, including large concretions of chert.....-eseeseeececececs aoe SCENE
2. Blue Clay (Gault), occupying a depression, in part covered with grass......... oosiele 9 (GOT
3. Wealden, Clay and sand :— Feet.
@rekveddish sand vanduclayir ser (ere eretesteletelelcleiele.s ote iale ole) o\eleier nicl eisai 122
b. Sand of various shades, yellowish and brown: about the middle are beds
of coarse conglomerate, consisting of fragments of translucent quartz and
of iblackish fine oi. nseia/eteloseteteyais aeba@bieley Kel siaibis) =, (opalo) 4 ef-ole ole Bdseope 281
[A coating of diluvial gravel extends from the chalk to about the mid
of this space, where the cliff is about 40 feet high. |
c. Reddish sand and clay. [The cliff is here 10 or 12 feet lower.]........ 80
d. Dark-brown sand, including fragments of lignite and of fossil wood. 4
{Large Unios and a small Paludina (elongata?) are found near this place. |
e. Grey‘ and whitish sand/7. cs. cc ccc cc cs cc cercrvsreresacce 15 0 Al
Greenish clay and sand. [Cliff about 30 feet high.].........- 26 0
f. A band of red clay and of dark-brownish matter....... soya ciefeli ais Sn ae 2
g-. Yellowish Sand. 2..6.0)..5 1c ones “uo como o Ponoedado dd «mie sheieisys
kh. Dark carbonaceous sand. .25..0.--2.+5 00% She Soosoooneaoos acces cae |
i. Variegated sand and clay, greenish and reddish. [A depression here in |
the outline of the cliff. At the lower part beds of compact grey lime- i 66 :
and clay. Surface in part concealed and covered with grass.|] ...... —~
Total, about.... 600 0
4. Purbeck strata: estimated at 150 yards ; cliff about 80\feet high. [Distinct ledges of
coarse sand-rock, including much green matter and a thick species of Unio, are 450 0
quarried near the top of the formation. On the shore were fragments of beds of
fibrous carbonate of lime, 7 to 8 inches thick] ..........eeceeceeceere wie otteelhs .
5. Portland-stone (estimated at 80 yards) ....... claldlstalolaleteletels. elelolale ce eeees sesesee 240 0
The Upper Green-sand is very distinct in this section. ‘The place of the Gault is indicated by
a slight depression, which is continued in the grassy hills on the east of the Cove. The Lower
Green-sand may, possibly, be included in the general mass of sand, 3.a.; but the Weald clay is
not distinguishable. Below the mass of yellowish and ferruginous sands, 3. b., is a considerable
extent of variegated clays, comprising beds much charged with carbonaceous matter; the whole
clearly referrible to the Hastings sands. The transition thence to the Purbeck strata is not
distinctly seen; but some of the beds, 3.7., of grey uniform limestone, alternating with clay, near
the junction, resemble those of the “ Jime-works” on the north-west of Battle, which are sup-
posed to be the lowest members of the Hastings series. ‘The top of the Purbeck on the east of
the Cove contains very numerous Unios in coarse green sand-rock: and on the west side a bed |
of greenish slaty stone, in the upper part of the series, consists of oolitic particles, and. contains
Cypris. Near the junction of the Purbeck with the Portland stone, the site of the “ Dirt-bed”,
which in the Isle of Portland contains silicified trees and Cycadez, is very distinctly seen.
|
|
|
|
|
Dr. Firron on the Strata below the Chalk. Q17
Man-of-War Cove, Pl. X.a. No. 10!.; and X. b. fig. 8.—In the isthmus here, which connects
with the main land a wide peninsular mass of Portland stone rising towards the south, many of
the beds are inclined backwards, and lean towards the chalk hills. A coating of reddish
gravel, from 3 to 6 feet thick, extends to some distance from the chalk along the top of the
isthmus, and is shown by the dotted line in fig. 8. The following are the strata at this place :
Paces.
1. Chalk.
2, Green-sand ...0.ceesevvesvens APR ioe Hie Pieters « Pisetntets feiss ce 0/0 a oa.0.s. 6 aul ele pe oe
3. Wealden-clay and Sands.
a. Dark clay, much mixed with sand; and including a mass of ieee sand-
rock, 4 to 6 feet thick: seems to represent the Weald clay .....+see0e005 u
b. Light grey, and white sand............. Be ape elochiey Sialt olek ect Ad'si5 ha elas caerts
c. Red clay, nearly vertical ; but inclining a little towards the chalk............ ¥
d. Grey, and brownish sand, including at top a conspicuous bed, of dark hue, which
contains much lignite in large pieces. [The breadth of the isthmus here, at « }
the bottom, is about 150 paces from west to east; at top about 40 paces.] .
e. Dark red and variegated clay. A considerable depression here in the outline of 10
RIM crs falai nicl nial cicliegsisialsivighs)oiets'u|siaiols <'c'ele sate" Pistols cele! s ole / ale = e/aincatstareneeaes
Total, about......... 74
4. Purbeck strata. Upper calcareous beds much distorted. About the middle a bed of
oysters is conspicuous, which, as it rises, is divided like a Y, and one of the portions re- - to
flected back towards the chalk. Estimated thickness (probably less than the true).....
5. Portland stone (estimated) ..... B-tidpisllebisi-trisiety -bieadecr> dhe shite ls Ate yee» . -80—90
(110.) Isle of Portland *.—The coast of Dorsetshire, from the promontory
of Whitenore to Lyme Regis, forms the subject of a memoir by Dr. Buckland
and Mr. De la Beche, which is printed at the commencement of the present
volume: I shall not, therefore, give any general description of it ; but having
been favoured with a perusal of that valuable paper, I find it necessary to
mention some details respecting the appearances observable near the junction
of the Purbeck and the Portland formations, with a view to a comparison
of this part of the series in the interior, with that of the coast in England,
and in the Boulonnois.
Mr. Webster, in his account of the strata above the Portland stone, has
described a remarkable bed, called by the quarry-men the “ Dirt” or “ Black
dirt’, which he found to contain portions of the trunks of silicified trees;
one of which he himself saw standing upright, and divided at the lower part,
“so as to give the idea of roots”. He states that these trunks were not found
in any other part of the series ; but not having seen any fossils in the beds
above the Portland stone, he expresses liimself with caution as to the place
of the boundary between the Purbeck strata and the oolitic group beneath
* The substance of this and the following sections, to (116.) inclusive, was read before the
Geological Society on the 13th of May, 1835; and is inserted here by permission of the Pre-
sident and Council.
T Geol. Trans., 2nd Series, vol. ii. p. 39, &c.; read Nov. 1824.
I
218 Dr. Firron on the Strata below the Chalk.
it ; intimating, however, that it will probably be found at the top of the chert
or flint in the upper part of the oolite. Some years afterwards Dr. Buckland
described specimens of a new family of fossil plants from the “‘Dirt-bed” above
mentioned; to which, at the suggestion of Mr. Brown, he gave the name of
Cycadeoidee *, but which M. Adolphe Brongniart, adopting a different system
of nomenclature, soon after formed into a genus which he called Mantellia Ff.
Dr. Buckland was subsequently led to infer that the “ Dirt-bed”’ was actually
the soil in which both the silicified trees and the Cycadeoidee had grown:
and in a paper read before the Society in 1830 {, now published in this
volume, he and Mr. De la Beche have stated several facts respecting that
remarkable bed ; adding in a note§ that Professor Henslow had ascertained
the existence of two other beds of dirt (or of clay with carbonaceous matter)
below it; one of them about seven feet beneath, the other about two feet
still lower down.
On visiting the Isle of Portland last summer, with a knowledge of these
facts, I found that the clay, or “dirt”, below the Cap, (the upper appa-
rently of the two additional clays described by Professor Henslow,) itself
contains Cycadee, in an upright position, and to all appearance in the places
where they had grown; and I obtained also some new evidence respecting
the character of the beds immediately above.
(111.) The following are a sketch and enumeration of the strata exposed
at the time of my examination, in the quarries about the middle of the island,
and westward of that point ; which I was enabled to revise during a second
visit to Portland, when I had the satisfaction of being accompanied by
Mr. Brown.
The whole mass of the strata which now form the Isle of Portland must have been subjected
to great disturbance long before the surface acquired its present configuration; by which
the vertical rifts, from a few inches to some feet wide, were formed, which are now observ-
able in the face of the quarries, passing indiscriminately through both the Purbeck and
Portland strata, and having in many instances produced displacement in the separated portions:
and this at such distances from the present coast of the island, as to prove that no recent
disturbance or subsidence of the sea-cliffs has had any share in producing them. Yet it is
remarkable that the surface over these disjointed beds is now perfectly uniform; the inequalities
occasioned by the sinking and fracture of the slaty Purbeck strata near the top having been com-
pletely filled up to a level by rubble and vegetable soil. In one place a fissure between two
and three feet wide cuts down, almost vertically, through about thirty feet of stony strata,
* Geol. Trans., 2nd Series, vol. ii. p. 395; read June, 1828.
+ Prodrome d'une Histoire des Végétaux Fossiles, 1828, pp. 92 and 96.
+ Proceedings of the Geol. Soc., vol. i. p. 217. et seq.
§ Page 16. of the present volume.
Dr. Frrron on the Strata below the Chalk. 219
and still retains its width at the bottom. The thin slaty beds of the Purbeck are in this instance
disturbed and bent, downwards and towards the fissures, to some feet on both sides ; but the soil
above is perfectly level; and in some other cases, where two or more cracks are near each other,
the intermediate masses are still more contorted and displaced. It will be shown hereafter that
appearances of the same kind are observable in the Portland-stone quarries in Wiltshire, Oxford-
shire, and Bucks.
Section of one of the PorTLAND Quarrizs. 1834.
1. Vegetable Soil ...ccsccsscseenereceeeeeees BRU
DMCUSIGLE.: \icsddededes's Ue. lade birds dds seis
. Clay, or “ Dirt” ...... ceereecss soou0banS —
. © Bacon-tier’’...cccecccveccceresess ae. tee
Soft Burr” ..csccoceoeeee Peussecenas cote
© Black Dirt”? scsccsecessseseveseeceesers =
SM Ao
S
>
Purbeck Strata (Freshwater).
©
2
aS}
oe
eeeeees
10. “ Dirt”, with Cycade@ .......sseeree.
11. “Shull-Cap” .....+.. Seecseecs scnes nome
NORMAN GU seal loses te omestens sens shecsiiecereas.
14. “ White-Bed”’........ Bae eaicsislvieves nas
Bottom of the Quarry.
Portland (Marine).
2. The “‘ Slate” of the preceding section is nothing more than the coarsely fissile limestone
which pervades the whole of the Purbeck formation, but at the lower part less frequently alter-
nates with clay. Its thickness varies in different parts of the Isle of Portland, from about
fifteen to less than six feet. In some places it includes small veins of rhombic carbonate of
lime in minute crystals; but has commonly the general aspect and flat conchoidal fracture of
freshwater limestone. On a close examination these beds are found to contain the remains of one
or more species of Cypris*; and I saw a few traces of small Modiolz, like those which abound
in the corresponding strata in the Vale of Wardour and Buckinghamshire. The Cypris, in fact,
is found in all the beds above the oolite (13. of the Sketch above); so that no doubt remains
respecting the boundary between the Purbeck and the Portland formation below. Nothing can
i with few exceptions, casts only of the interior of the crusts are obtained here, it is difficult
to determine the species of these fossils. Mr. Sowerby is disposed to refer most of them to a
ri Bperics, C. tuberculata, Pl. XXI. fig. 4.; and a few perhaps to the C. Valdensis, Pl. XXI.
g.1.; both of which abound in the corresponding part of the Purbeck formation in the interior.
220 Dr. Firron on the Strata below the Chalk.
be more remarkable than the immediate contact of these two groups; the upper consisting of
freshwater limestone with few fossils; the lower distinctly oolitic, with fossils in great number
and variety, and all of them marine*.
3. Besides the “* Black Dirt” (No. 8.), or, as it is usually called by the quarry-men, “ the Dirt”,
two or more thin courses of clay occur above the Cap: one (No. 3.), about two inches thick,
between the Bacon-ledge and the Slate; another (No. 5.), about an inch in thickness, dividing
the former from the 4sh. The number, however, of these thin beds of clay varies in the different
quarries ; and, in general, it may be said that such alternations with the limestone are not unfre-
quent. They all bear the name of “ Dirt”, and are more or less mixed with fragments of stone
and with carbonaceous matter; but contain commonly much more clay than either of the two
beds hereafter mentioned, which include the remains of plants.
4. The Bacon-tier consists of calcareous slate alternating in some places with thin beds of sand.
It is from 2 feet to 25 feet in thickness.
6. The Ash is a soft fissile limestone, like the last-mentioned bed, from which it is easily sepa-
rated in working. In general it is from eighteen inches to two feet thick, and is closely connected
with the Soft Burr, 7. When the incumbent beds are removed, it generally exhibits an uneven
surface, with numerous bosses or prominences, enveloping the broken tops of the trunks, which
stand upright in the dirt-bed below, as described by Dr. Buckland and Mr. De la Beche.
Oblong depressions also are frequently observed on the surface of the Ash, called by the quarry-
men “graves”, the origin of which it is not easy to explain.
7. The Burr of the Ash, or Soft Burr, is between two and three feet thick. It has obviously
been deposited around the lower part of the petrified trunks, and is always separated from them
by a small space, at present occupied by the carbonaceous matter produced by the decomposition
of part of the tree: and this is the case also where the Ash envelopes the top of the broken
stumps. The junction of these two beds, around the trunks, is often attended with some very
interesting appearances, for an account of which I refer to a note by Professor Henslow in
the preceding part of this volume t.
8. The “ Dirt”, or “‘ Black Dirt”, in Portland is separated from the stone, both above and
below, by well-defined surfaces; while some of the other beds of clay, or dirt, pass by gradation
into, or adhere closely to, the stone which adjoins them. It is from twelve to eighteen inches
thick, and differs from all the other beds alternating with the slaty limestone, in containing
large worn fragments of stone {, from three to nine inches im diameter, in such numbers that
the whole deserves the name of coarse gravel. With these are mixed coarse carbonaceous
matter and minuter fragments of stone ; but seldom, in the Isle of Portland, any continuous or
cohesive clay :—the carbonaceous matter arising, no doubt, from the remains of vegetables, and
being most abundant immediately around the trunks and Cycadez, which this bed includes, or
supports.
At Upway, on the north of Weymouth, the representative of the “‘ Black Dirt” likewise con-
tains petrified trees: but the pieces of stone which it includes are few and much smaller, and
it approaches more nearly to the usual form of vegetable mould, or of clay. On the north-east
of Weymouth its place can be distinctly recognised in the cliffs between Lulworth Cove and Wor-
* Compare what is here stated, with the account of the junction of the marine beds with the
top of the Wealden, at Atherfield in the Isle of Wight (supra, p. 196, last lines).
+ Pages 16. and 17.
{ In these fragments I could find no fossils ; Mr. Webster considers them as belonging to the
lower beds of the Portland stone.
Dr. Firron on the Strata below the Chalk.
barrow Bay; and in the Isle of Purbeck, beneath Wor-
barrow Knob. In the loftier cliffs at Gad Cliff it is not
accessible; but among the fallen ruins on the shore were
some portions of silicified trunks. Between Tillywhim
and Durlstone Head a cavity can be perceived in some
places, in the part of the cliff where this bed might be
expected.
Petrified Trees.—The portion of the trees left standing
above the dirt-bed in Portland, is frequently more than
three feet in height: and one instance was mentioned to
me in which six feet of a trunk stood thus in the up-
right position. I did not see any case in which the roots
penetrated into the Cap below; but observed several fis-
sures in the top of that bed, some of them coated with a
crust of stalactitic carbonate of lime. In one instance a
prolonged branch of the root had evidently been bent out
of its course by meeting the Cap, and was continued ho-
rizontally along its surface for several inches: the quarry-
men said that such cases were not uncommon, and that
the roots sometimes ran along the top to a much greater
distance, but never penetrated the Cap itself.
Some very fine specimens of the silicified trunks had
been found not long before I saw them ; one of which had
been judiciously restored, by joining the fragments and
placing the whole erect against the wall of a house. The
total height from one extremity to the other was above
205 feet; the diameter of the stem where the roots went
off, about113 inches. The trunk was nearly straight and
undivided for about 17 feet, and the branches slight in
comparison with the main stem.
A still finer specimen, found, I believe, near the same
place, in Dungeness Quarry, and at the same time with
that just described, has been brought to London for sale;
and I am enabled, through the favour of Mr. Freeman, in
one of whose warehouses the specimen was deposited, to
insert a representation of it, from a drawing made by Mr.
Sowerby, after careful admeasurement, as it lay horizon-
tally, the fragments which had been separated appearing
to fit exactly. The total length, from the extremity of the
roots to that of the branches, was about 234 feet, and to
the bifurcation nearly 20 feet. The roots and undivided
portion of the stem to the first crack, occupied about 2
feet. The situation of the other cracks, of which there
are fourteen or fifteen, is expressed in the figure. The
trunk is compressed throughout ; the branch on the right, *
especially, having been much flattened near its extremity.
SSS=s
—S
~ —s"
—<——=
———S—-=
= =
222 Dr. Firton on the Strata below the Chalk.
At 2 feet from the extremity of the root, the greatest diameter is 183 inches, the transverse
diameter only 125; at 4 feet, the diameters are 165 and 114 inches; at 11 feet, 143 and 112;
and at 18 feet, 15 and 93 inches. The right branch at its extremity, 11 and 43 inches.
The specimen here represented is much like that which is preserved in the Isle of Portland,
in general aspect and proportion; but many of the stumps which I saw standing in the quarries
were much larger. One that I measured,—of which 5 feet stood upright from the lowest point
of the roots to the top of the broken trunk,—was 2 feet in one of its diameters, and 6 feet 9 inches
in circumference. Another, 5 feet 10 inches in total height, was about 2 feet 10 inches in diameter,
and 9 feet 4 inches round; and I was assured that others had been found of much greater thick-
ness. All the larger trees that I saw were in the quarries on the north-west of the church; one
of which afforded also the specimen represented in the wood-cut, with several large Cycadez. In
many places I saw large branches lying prostrate, and partially immersed in the Dirt;—one of
them, above 3 feet long, within 2 feet of another portion, about 10 feet in length, and in the
same direction with it*.
From the evidence afforded by thin transparent slices, both of the transverse and longitudinal
sections, which have been examined under the microscope+ by Mr. Brown, the fossil trunks of
Portland are found to possess the characters uniformly belonging to coniferous wood: but it must
be observed that these characters are not absolutely confined to Conifere.
The Cycadee found in the “ Black Dirt” are generally from 9 inches to a foot in diameter,
and about 9 or 10 inches high. I myself saw but one specimen, which had been recently taken
from its place, in this bed; and it was stated by the quarry-men that on the west of the main
road from Chiselton to the church, they have been found, or noticed, only in the Dirt above
the Cap; while on the east of the road, as I shall presently mention, they are certainly found
below that bed. In the eastern quarries, indeed, the workmen, who had not seen them elsewhere,
asserted that the Cycadez were never found above the Cap ; but this I found afterwards to be
incorrect. In both situations, they are much less common than the coniferous trunks.
9. The “ Cap” is the thickest of all the strata above the Portland stone ; the average thickness
being about 8 feet, the extremes 6 and 9 feet; of which, in some cases, about 18 inches at the
top are easily separable from the rest. When recently exposed, the whole of the remaining mass
is continuous, and consists chiefly of uniform limestone of a light brownish or drab colour, with
a flat conchoidal and splintery fracture ; but it cannot be used for building, as, in the workman’s
phrase, “ it will not square.” About the middle and towards the lower part it is spongy, or
cavernous, including tortuous cavities surrounded with botryoidal carbonate of lime; and it has
* It would be desirable to ascertain the direction in which the prostrate stems lie, with respect
to the meridian, and to the roots and portions of the trunk remaining upright, in order to deter-
mine whether they were overthrown by an uniform current of wind or water.
+ One of the longitudinal slices examined by Mr. Brown was broken from the extremity of the
left branch of the tree represented in the annexed wood-cut.
The process by which these slices are prepared for the microscope has recently been carried
to great perfection by Mr. Nicol of Edinburgh. It consists in attaching a thin polished slice of
the fossil, separated by the ordinary method, to a piece of plate glass, by means of a uniform
cement; and then grinding it down as far as possible on the lapidary’s wheel. In this way tran-
sparent slices have been obtained, which exhibit the internal structure of fossil wood with beau-
tiful distinctness, and show the extreme delicacy with which the original vegetable structure
has been preserved during the petrifactive process. ‘Two papers by Mr. Nicol on the structure
of the recent and fossil Coniferze are published in the Edinburgh Philosophical Journal, vol. xvi.
1834, pp. 137 and 310; and a third in the Report of the Fourth Meeting of the British Asso-
ciation for the Advancement of Science, 1834, p. 160.
Dr. Firron on the Strata below the Chalk. 223
altogether a very strong resemblance to the Z’ravertine of Italy. The top is sometimes penetrated
by conical and nearly vertical cavities, encrusted with a yellowish stalagmitic coating. In the
Isle of Portland it is compact and continuous at the bottom ; but in other places the lower part,
and in some cases the whole, is resolved by decomposition into slaty strata.
At Upway, on the north of Weymouth, the lower portion of the Cap consists of a series of
thin beds of limestone alternating with very thin courses of clay. In Portland, even where
most compact, it contains a few casts of a small species of Cypris; and these seem to be
more frequent (perhaps because more easily detected) in the more fissile representatives of the
bed at Upway and Bacon-hall. In one or two instances I found in it obscure traces of small
univalves like those of Garsington and Combe Wood near Wheatley in Oxfordshire.
In a nook or recess, called by the boatmen Bacon-hall*, upon the coast about a mile east
of Lulworth Cove, the section of this part of the series was as follows:
a. “Black Dirt” of Portland.
b. Cap, consisting of:
i. Slaty limestone, divided by dark lines of stratification; which at the lower part become more
distinct, and at last take the form of ii.
ii. Dark grey indurated slaty clay ; one bed of which is nearly 2 inches thick.—Beneath it is
iii. A thin flake of soft whitish limestone.
e. Dirt. An indurated bed, of a light brown colour, 4 to 5 inches thick; composed of argil-
laceous (and carbonaceous) matter, and including small fragments of stone.
d, (Skull-cap?) Limestone, somewhat botryoidal ; the more compact portions having a flat con-
choidal fracture ; 2 to 6 inches thick.
e. Portland stone, abounding in the characteristic fossils, and including, about 6 feet from the top,
a band of flint, in detached masses, about 4 inches thick.
10. “ Dirt” below the Cap. Immediately below the Cap in the Portland quarries, and conse-
quently separated from the “Black Dirt” by a thickness of about 8 feet, is another bed, also
called “ Dirt” by the quarry-men, from 2 to 6 inches thick, but more uniform in its texture than
the former, resembling coarse silt or indurated loam, and containing in some places small frag-
ments of stone, but never such large masses as the ‘“ Black Dirt”. This lower bed deserves especial
notice, from its affording specimens of Cycadez, in an upright position, and partially immersed in
it, as if they had grown there. Of these I myself saw two in their original place at a quarry
called “‘ the Wheat-croft ”, on the east of the ‘‘ Traveller’s-rest” ; one of them about six inches
high, surrounded with the Cap, into the lower part of which it projected above the Dirt for about
half its thickness, so that it was necessary to cut away the stone to take it out; and from the
existence of many other specimens in the debris of the same quarry, which the workmen assured
me had all come out of this bed, I believe them to be of frequent occurrence. Among the latter
was one of unusual size, larger indeed in its horizontal dimensions than any other specimen I have
seen, either from this bed or the Dirt above the Cap{. This, from its flatter form, may possibly
* Notwithstanding the apparent firmness of this rocky coast, great changes are constantly in
progress there. An old boatman who conducted me, without having been asked a question,
expressed in very strong terms his surprise at the alterations produced, to his own knowledge,
within the last thirty years.
+ The specimen is now in the museum of the Geological Society. It is of an irregular figure
approaching to an oval, and measures 20 inches by 19 in its horizontal diameters, the vertical
thickness varying from 63 to 9 inches. Another less perfect specimen which I saw in the same
quarry, was about 9 inches thick, and its diameters not less than 34 and 30 inches. Of the Cy-
cadez from the Upper Dirt-bed very few exceed 10 inches, in height and horizontal diameter.
The largest I have seen is nearly 10 inches high, and about 12 in diameter near the bottom.
VOL. IV.—SECOND SERIES. 26
224 Dr. Firron on the Strata below the Chalk.
belong to the species nidiformis of Adolphe Brongniart (Cycadeoidea megalophylla of Dr. Buck-
land): but it deserves inquiry whether the specimens in the lower bed agree in all respects with
either of those found in the upper one.
In the Isle of Portland, no trees have hitherto been found in this lower dirt; which, from its
smaller thickness, might seem to have been less adapted to their production than the upper one.
But if I can rely upon a single observation, part of a prostrated trunk exists in the Dirt below the
Cap, in a section exposed on the west of the road leading from Upton (on the main land of Dor-
setshire) to Poxwell. T came to this conclusion from observing that the inclined stratum of lime-
stone over the bed including this specimen was distinctly botryoidal, and of great thickness,—two
characters which accord with those of the Cap; while the stone below it contained Portland
fossils. But I saw no Cycadez in the bed at this place.
11. “ Skull-Cap.” The thickness of this bed in Portland varies from one to three feet, and it
frequently swells out suddenly from 15 or 18 inches to double that thickness, and returns as
rapidly to its previous dimensions. It is less uniform than the Cap, and sometimes has an
obscurely conglomerated appearance, but, like that bed, consists of freshwater limestone, and is
in some places botryoidal. It includes also, as Mr. Webster has stated, small cavities coated with
minute rhomboidal crystals of carbonate of lime, like those found in the slaty beds above.
12. At the lower part, the “‘ Skull-Cap” is closely attached to, or passes into, a seam of argil-
laceous matter, sometimes not more than half an inch, and seldom more than 24 inches thick, by
which it is separated from the Portland stone. ‘This seam appears never to be wanting in these
quarries, and is much more uniform than the Dirt immediately above the Skull-Cap, which is very
unequal in thickness : in some instances it is incorporated with, or adheres very closely to, the
top of the Portland stone *.
13.and 14. The top of the Portland series consists of very fine-grained oolite, resembling the
roe of fishes, and of a very light brownish hue. With the oolitic particles, other rounded frag-
ments, less regularly shaped, are mixed and united by a calcareous cement, so that the whole
compound is very like the recent conglomerates which abound on the shores of New Holland, of
many of the Indian Islands, and of Bermuda; especially resembling the newly-formed masses of
the last-mentioned islands, described by Lieut. Nelson in a paper lately read before this Society +.
This oolitic portion is seldom more than four inches thick, and passes at the lower part into dark
grey flint, in irregular concretions, which form an interrupted range near the top of the bed, and
include the same petrifactions (but silicified), with those which abound in the limestone imme-
diately around and below them. The stone below the flints, to a distance of from two to four
feet from the top, is called ‘* Roche” by the quarry-men, and is essentially continuous with the
lower part of the bed; but it contains so many casts of shells (of which, indeed, it is almost
entirely composed), as to be useless for the purposes of building, and is therefore always sepa-
rated in the quarry. The remainder of this stratum, about 8 feet thick, is known in the island as
the ‘‘ White-bed”, and is that which is now, almost exclusively, quarried for the market under the
name of Portland stone. This and the lower strata of the formation, which are not worked at
present, have been already described by Mr. Webster.
Among the fossils of the White-bed in Portland, are a Corbis ?, Cytherea parva, Lithodomus,
Pecten lamellosus, Perna quadrata, Plicatula, Terebra Portlandica, Trigonia gibbosa, T. incurva.
* The existence of Cycadez within three feet of the Portland beds being certain, it deserves
inquiry whether they may not occur also in this lower and thinner Dirt-bed immediately above the
stone.
¢ Proceedings, vol. ii. p. 81.
Dr. Frrron on the Strata below the Chalk. 225
At Upway, this bed, or one of those immediately below it, is beautifully white, like chalk, and
contains nodules of dark grey flint, frequently hollow and lined with quartz crystals, which it
would be impossible, without attending to their fossils, and their geological position, to distin-
guish from those of the chalk. One of the characteristics of the best Portland stone, both of this
and other beds, is that the blocks ring very distinctly under the hammer, giving out a clear and
agreeable note.
(112.) It appears, therefore, that on the Dorsetshire coast the Portland
strata are everywhere succeeded by a series of beds of freshwater limestone,
alternating with beds of clay, or of a compound called “dirt”, which con-
tains carbonaceous matter and fragments of stone; and that two at least
of these “dirt’’ beds, the first about three feet, the second about twelve
feet above the top of the Portland series, include the remains of plants, which
grew in the places where they are found ; nor is it wholly improbable that
similar remains may hereafter be discovered in some of the other and thinner
beds of “dirt”’.
A point which Mr. Brown considers as well deserving of remark is, that the
only remains of vegetables hitherto found in these strata, under the circum-
stances above described, belong to two nearly related families, Coniferee and
Cycadex, which have lately been regarded as forming a distinct class, cha-
racterized not only by the greater simplicity of the parts of fructification, but
also by some peculiarities of internal structure, and thence have been con-
sidered as intermediate between Phanogamous, and Cryptogamous or Aco-
tyledonous plants.
Another striking fact connected with the remains included in the “ dirt
beds” is, that they are composed almost entirely of silex, though surrounded
either by limestone or by the mixed components of the dirt itself. The
cavities in the petrified trunks are lined with minute crystals of quartz; and
Dr. Prout, who has been so kind as to examine specimens of the coniferous
wood taken from the confines of the Purbeck and Portland formations, in Port-
land, and other places to which I shall refer hereafter,—finds them all to consist
almost wholly of siliceous matter, with very slight traces only of carbonate of
lime and of iron; some of the darker parts of a specimen, from the Vale of
Wardour containing also bituminous matter. The Cycadeew likewise are
described by Dr. Buckland as being almost entirely siliceous, “‘varying from
“coarse granular chert to imperfect chalcedony” *.
(113.) The great abundance of small, worn, fragments of shells and stone
at the top of the Portland formation, is what might have been expected
on the surface of an island of small height, just protruded from‘ the sea,
* Geol. Trans., 2nd Series, vol. ii. p. 398.
262
226 Dr. Firron on the Strata below the Chalk.
perhaps so gradually as to have been near the surface for some time before
its emersion. The next step, in the series of revolutions which produced
these strata, must have been the diffusion of fresh water over the new land,
from which the “Skull-cap” was deposited; and this was followed by a
drying up or retirement of the water, so as to disclose and convert into dry
land the lower of the two beds of clay, or dirt, which now contain the Cy-
cadee. Iam not sufficiently acquainted with the habits of the recent plants
of this family, to form any opinion as to the length of time necessary for
their acquiring the size of the specimens now found petrified, nor to judge
how far the rapidity of their growth would be modified by climate: but
all the known species are said to be of slow growth; and being found at
Japan, as far north of the equator as 40°, and at the Cape of Good Hope
and Port Jackson, in the southern hemisphere, about latitude 34°, they cannot
be considered as strictly tropical productions.
A second submersion of the surface in fresh water must have followed the
production of the Cycadez in this lower bed, from which the “‘Cap”’ was accu-
mulated, to a thickness of between seven and ten feet, and the ‘* Black Dirt”
deposited above it; anda third, and apparently more durable submersion, still
in fresh water, must afterwards have taken place, by which the “slate” and
a great part of the Purbeck strata were produced. In this last case the water
seems to have been at first unmixed, but to have become after a time ac-
cessible to the sea; since not only does the Purbeck formation contain a
thick bed of oyster-shells, but thence upwards, throughout the Wealden,
oysters are found, in strata which in several instances alternate with others
abounding in freshwater shells.
(114.) Mr. Lyell has pointed out the resemblance between the geological
events which produced the strata of Portland Island, and those which are
known to have occurred at the mouth of the Indus, from the effect of suc-
cessive earthquakes connected with volcanic eruption*; and it is clear that
all the changes above supposed to have taken place,—depression and elevation
of the land, through comparatively small depths and at different periods, with
alternate though irregular submersions both in salt and fresh water,—have
been produced in that region, not only within the period of tradition, but
many of them so recently as in 1819. Among other facts, it is stated, that
for some years after the earthquake of Cutch, which happened in that year,
“the withered T'amarisks and other shrubs protruded their tops above the
“‘ waves, in parts of the lagoons formed by subsidence, on the site of the
* Principles of Geology, 4th edition, vol. ii. p. 237-242.
Dr. Firron on the Strata below the Chalk. 227
“village of Sindree and its environs. Every geologist,” Mr. Lyell justly
remarks, “will at once perceive, that forests sunk by such subterranean
“movements may become imbedded in subaqueous deposits both fluviatile
“and marine, and the trees may still remain erect ; or sometimes the roots
“and part of the trunks may continue in their original position, while the
“currents may have broken off or levelled with the ground their upper
“ stems and branches*.”
(115.) It is very desirable that the examination of the Portland quarries
should be repeated from time to time: for as the valuable stone lies deep in
the series, and it is necessary, for the purpose of obtaining it, to remove the
whole of the incumbent matter, the features described in this paper are con-
stantly undergoing a process of destruction ; while, on the other hand, new
facts are continually brought into view, which are lost if not observed at the
moment. ‘The greater part of the phenomena described by my predecessors
had thus disappeared when I visited the island, and a few hours might have
removed the fossils which I observed in the bed below the Cap. Geologists
may assure themselves that the trouble of a journey to Portland will be most
amply rewarded ; since few places, it is probable, in the world, exhibit with
such distinctness and in so small a space, phenomena of more extraordinary
interest, or of greater importance to theory.
_ (116.) The strata, abruptly cut off by the sea on the west coast of Port-
land, are found no more in that direction in England f ; nor do they occur on
the opposite coast of France immediately on the south, which consists of the
primary masses of Guernsey, Auvigny, and the main land about Cherbourg.
On the east of the last-mentioned promontory, where they might be expected
to appear among the beds beneath the chalk between the mouth of the Seine
and Bayeux, their presence, I[ believe, has not been distinctly ascertained.
And on the north of the Seine they must be far below the level of the
English Channel, at least as far as Etaples, where the rocks upon the shore
consist of chalk with flints i sitw. The Portland beds, with a thin covering
of the lowest Purbeck strata, rise from beneath the chalk and green-sand on
the south of Equihen in the Lewer Boulonnois, and are found all along the
cliffs thence to the north of Cape Gris-nez, where they again give place to
the superior strata. They have not yet been discovered, so far as I am in-
formed, further to the north in Europe.
* Principles of Geology, 4th edition, vol. iv. p. 274.
+ The most western point where the Portland strata have been found in England, is on the
main land near Portisham, twenty miles west of Lulworth Cove. See p. 15. of this volume.
228 Dr. Fitton on the Strata below the Chalk.
(117.) List of Fossils from the Beds below the Chalk, on part of the Coast
of DorseTsHiRe.
[Upper Green-sand. |
Cirrus depressus. Worbarrow Bay.
Exogyra conica. Face of the Hill top, W. of Osmington Mill.
E: levigata. Worbarrow Bay.
Gryphea vesiculosa. Swanage Bay, under Ballard Hill. Hill top, W. of Osming-
ton Mill, with stems of Siphonia.
Ostrea, new. Between Ham Cliff and Osmington Mill.
Pecten asper. Swanage Bay. Hill top, W. of Osmington Mill.
Je orbicularis. Swanage Bay. W. of Osmington Mill.
P— quadricostatus. Swanage Bay. Worbarrow Bay.
P quinquecostatus. Swanage Bay.
P A very convex variety (young ?). Worbarrow Bay.
Serpula antiquata. Swanage Bay
Siphonia. Stems. Worbarrow Bay. Hill top, W. of Osmington Mill.
Terebratula pectita. Swanage Bay.
Vermetus concavus. Swanage Bay. Osmington Mill.
[ Gault. ]
Mya mandibula. Punfield*, Swanage Bay.
[ Weald Clay. |
Cyclas media. Punfield. In thin beds of bluish limestone, encrusted with fibrous
carbonate of lime (‘ cone in cone’’).
C. membranacea. Punfield.
Cypris tuberculata. Pl. X XI. f.2. Punfield.
C Valdensis. (C. Faba, Min. Con.) Pl. XXI.f. 1. Punfield.
Exogyra? Punfield. In brown clay.
Melanopsis? attenuata. Pl. XXII. f. 5. Punfield. In blue clay.
M- ? tricarinata. Pl. XXII. f.4. Punfield. In blue clay.
Ostrea. A plicated species. Punfield. Ina bed of stone subordinate to the Weald
clay, the greater part composed of shells; with a striated bivalve (a Cardium ?).
O——. Asmooth species. Punfield. In greenish sandy stone, coated with fibrous
carbonate of lime.
Paludina acuminata. Punfield.
Pp. elongata. Punfield. With Cyclas media, in greenish grey sandy clay.
Unio. Punfield. In thin, slaty, dark bluish clay.
Saurian Rertites. Fragments of bone of a Saurian; and the teeth apparently of
a Crocodile. Punfield.
Woop. Coniferous, silicified, in fragments. Punfield.
* Punfield is a small nook or recess on the north of Swanage Bay, between the ridge of Bal-
lard Down and the sand-cliffs.
Dr. Firron on the Strata below the Chalk. 229
[Hastings Sand. }
Cyclas media. Sand-cliff between Swanage and Punfield. In nodules of clay-iron-
ore, with Paludine; also in hard subcalcareous grit.
Paludina elongata. Same place and situation.
Unio. One or more species occur in the concretions of grit within the sand-beds, be-
tween Punfield and the town of Swanage.
Saurian Rerrives. Large bones of the Iguanodon have been found loose on the
shore at the foot of the sand-cliffs near Swanage, by the Rev. T. O. Bartlett;
(see Dr. Buckland’s Notice, already referred to*;) but their precise place in
the cliffs is still to be ascertained.
Woop. Large portions of the stems of silicified coniferous trees have been found on
the shore under the sand-cliffs in Swanage Bay, by the Rev. T. O. Bartlett.
The stone into which they are converted is of a very dark brown colour, re-
ceives a fine polish, and does not effervesce with acids.
[Purbeck Strata. ]
Corbula alata. Pl. XXI.f.5. Numerous in slaty limestone, at Upway, on the north
of Weymouth, with Cyclas media. Durlstone Bay: Isle of Purbeck.
Cyclas media. Pl. XXI. f.10. This fossil occurs throughout the series of Pur-
beck strata, and is one of the most abundant fossils of the formation, some of
the beds being almost entirely composed of it. Upper beds of the series, at
Peverell Point, and Durlstone Bay, At Upway, west of the road, 50 feet above
the “ Cap”.
angulata. Pl. XXI1.f. 12. In “ Quarry vein”, one of the strata worked for
stone, near Swanage. In hard stone resembling the lower chalk, when indurated ;
Durlstone Bay. Of large size, in slaty stone, at Upway, N. of Weymouth.
Cypris.. Casts, in transparent carbonate of lime, of the interior of one or more small
species of this genus, occur in great abundance in the beds of slaty limestone,
which frequently includes rhombic crystals of carbonate of lime, at the bottom of
the strata above the “‘ Dirt bed”’, as well as in the “ Cap” over the Portland stone :
but it is difficult to determine the species, as the external surface is commonly
wanting. Ina few instances an exterior spine or prominence, like that of Cypris «
spinigera, P|. XXI. f. 3., is perceptible ; and in others the protuberance at the
end of the valves, represented in the figures of C. Valdensis, Pl. X XI. f. 1., was
observed. It is not, however, improbable that some of the casts may belong
to species different from both of these. Isle of Purbeck, and coast thence to
the west of Lulworth Cove. Quarries at Upway, north of Weymouth. Isle
of Portland : in the “slate”’.
Exogyra bulla. Pl. XXII. f. 1. Durlstone Bay.
Ostrea distorta. Pl. XXII. f. 2. Durlstone Bay. The bed called “ Cinder ’’, about
the middle of the strata which are worked for stone, consists almost entirely of
this and other species of oyster.
C.
* Proceedings of Geol. Soc., vol.i. p.159.; and Geol. Trans. Second Series, vol. iii. p.421. et seq.
230 Dr. Firtron on the Strata below the Chalk.
Ostrea. A new species? Durlstone Bay. West side of Lulworth Cove, in bluish .
sandy stone. Durdle Cove, in a bed like the ‘ Cinder”’.
Paludina carinifera. W. of Lulworth Cove, with Unio compressus, and a pearly
oyster, in the uppermost of the Purbeck beds, some of which are almost entirely
composed of shells of Paludine. Also, with bones of fishes, in very blue com-
pact and sparry limestone.
P. elongata. Peverell Point. Abundant in the uppermost beds of the Pur-
beck stone, with much green matter. Durlstone Bay, with Cyclas media.
P- Sussexiensis. Pl. XX. f.6. Peverell Point; in splintery limestone, with
disseminated calcareous spar. Durlstone Bay.
Unio compressus. Durlstone Bay ; in oolitic stone, with Cypris.
U— new species? At the upper part of the series; in beds composed of carbonate
of lime, apparently derived from the presence of these shells, with a large pro-
portion of green matter (silicate of iron). East side of Lulworth Cove. Wor-
barrow Bay. [The occurrence of bivalves in this place is mentioned by Mr.
Webster, Geol. Trans., 2nd Series, vol. ii. pp. 39, 40.]
Reprtites.—Turtles. Fragments of the shell and bones of Turtles are not unfre-
quent, and even entire skeletons are sometimes found in the Purbeck strata.
Saurians. Fragments of bone, and teeth.
Fisnes. Palatal bones: Durlstone Bay. The scaly remains, also, of different spe-
cies, are frequent in the slaty strata of the Purbeck stone.
Puants. Near the junction of the lower slaty beds of the Purbeck with the
Portland stone, large trunks and branches of coniferous wood are found in great
abundance in the “ Black Dirt” above the “ Cap’’, in the Isle of Portland, and
on the coast east of Lulworth Cove ; and in the dirt below the “‘ Cap”? between
Upton and Poxwell.
A Cone, represented in Plate XXII. f. 9., and stated to be “ from Purbeck”’, is
in the Museum of the Geological Society. It has some slight resemblance to
the cone of a Dammara of the Moluccas.
Cycadeoidea (Mantellia of Adolphe Brongniart, ‘“ Prodrome”’, &c.). Remains of
at least two species of Cycadee occur in the Isle of Portland, along with the
trunks of coniferous trees, in the “ Black Dirt” above the “Cap”; and those
of at least one species, also in the dirt or clay, between that bed and the “ Skull-
Cap”.
[Portland Stone. |
Ammonites biplex. Isle of Portland.
A new. Isle of Portland.
Cerithium? excavaltum (Turritella excavata, Min. Con.). West of the Isle of Port-
land.
Cytherea parca (Venus, Min. Con.). West of Portland, in the flint of the “ Roche”.
Lithodomus. New. Upper part of the “ White Bed’’, Portland.
L —. Another species? Same situation.
Dr. Frrron on the Strata below the Chalk. 23]
Monodonta. New. Lowest beds of the Portland stone. Near Blacknore, Isle of
Portland.
Pecten lamellosus. Lowest beds of the stone. Same situation.
Plicatula? Casts of the interior, numerous in the “‘ Roche” immediately over the
“ White bed’’. Portland.
Terebra Portlandica. Pl. XXIII. f.6. Very numerous in the “ Roche”
the ““ White bed”. Portland.
Trigonia incurva. PI. XXII, f.14. (Miss Benett*: Pl. XVIII. fig.2.) In the
“White bed”. Portland.
T——— gibbosa. Frequent in the “ Roche’’. Portland, and elsewhere on the coast.
T: A variety, approaching to incurva, but less oblique. Portland.
Venus parva. (See Cytherea.)
: also in
{Portland Sand. |
Ammonites giganteus. Cross-roads above Kimmeridge Farm, on the north-east.
Isle of Purbeck.
New species. In concretions of splintery indurated marl, or soft lime-
stone. Lowest beds of the Portland sand. Emmet’s Hill: Isle of Purbeck.
Cucullea. (A small species.) Portland.
Exogyra nana. West side of Portland Island, on an Ostrea.
Ostrea levigata. Kast side of Portland.
Panopea depressa. (Mya depressa, Min. Con.) In concretions of dark bluish grey
indurated marl. Lower part of the sand. Emmet’s Hill: Isle of Purbeck.
Pecten. A new species? Upper part of the sands. Blacknore, Portland.
Serpula tricristata. Pl. XXIII.f.3. East side of Portland. Qua. in Kimmeridge
clay?
variabilis. P]. XXIII. f.7. East side of Portland. Qua. in Kimmeridge
clay?
A
Ss
Trigonia clavellatat. Cross-roads above Kimmeridge Farm on the north-east. Isle
of Purbeck.
Fisnes. Scales of fishes are found in strata apparently belonging to this formation,
under Gad Cliff, in the Isle of Purbeck.
Rays of dorsal fins (see the abstract of a paper by M. Agassiz, Pro-
ceedings of the Geological Society, vol. ii. p. 101.) occur in nodules either of
this formation or of the Kimmeridge clay, on the east coast of Portland.
[Kimmeridge Clay. |
Ammonites biplex. Numerous in the bituminous shale of Kimmeridge Bay, with
transparent sulphate of baryta: sometimes along with an Ostrea.
* “A Catalogue of the Organic Remains of the County of Wilts;” 4to, with 18 plates.
Warminster, 1831.
t Besides the shells mentioned above, two or three other bivalves, of which the genera are
indistinct, have been found in the Portland sand, at Emmet’s Hill and other places, in the Isle of
Purbeck.
VOL. IV.—SECOND SERIES. 2H
232 Dr. Firron on the Strata below the Chalk.
Ammonites mutabilis. Young.
Astarte cuneata? In firm brown shale. Kimmeridge Bay.
Panopea depressa. Kimmeridge Bay ?
Ostrea deltoidea. East of Portland. Que. in Portland sand ?
Fisues. Teeth.
Rays of dorsal fins.
[ Weymouth Strata and Oxford Oolite*.}
Ammonites circularis. Pl. XI. f.20. In reddish sandy beds above the pisolite. Ab-
botsford.
Astarte cuneata. In ferruginous sandy stone. Near Weymoutht.
Belemnites fusiformis. North of Weymouth.
Clypeus clunicularis. (Smith, “ Strata Identified’”—Coral Rag, fig. 6.) Weymouth;
in oolitic sand.
Exogyra nana. In whitish oolitic stone, between Ham Cliff and Osmington. North
of Weymouth.
Gervillia aviculoides. In the coarse grit between Ham Cliff and Osmington Mill.
Melania Hedingtonensis. In oolitic sand, near Weymouth. In reddish sand-rock,
above the pisolitic clay, near Abbotsford.
Modiola bipartita. In hard reddish clay. Osmington.
Ostrea. A thick-shelled species, near Abbotsford, in oolitic sand, at the top of the
oolite.
O Species? Between Ham Cliff and Osmington Mill.
Nerinea Goodhallii. Pl. XXIII. f. 12. Cliffeast of Osmington Mill ; in coarse
rag. Mr. Goodhall. 4
Pecten annulatus. n sandy beds, near Osmington ?
Pullastra? Yn marly pisolite at the top of the Oxford oolite, near Backwater, going
from Wycke Church; Weymouth.
Terebratula inconstans. Near to Osmington, in blue clay. Boat Cove.
T————. New? Oval: reddish beds above the pisolite. Abbotsford.
Trigonia clavellata. Abundant on the shore between Ham Cliff and Boat Cove. In
ferruginous sandstone near Weymouth, with Astarte cuneata.
T. costata. Osmington.
Trochus Sedgwickii (olim T. reticulatus). From the reddish beds above the pisolite.
Near Abbotsford. Upper part of the Coral rag, and lower of the Kimmeridge
clay. Near Weymouth.
* As the sands and clays of the Weymouth group pass insensibly into the Oxford oolite, it is
difficult, and perhaps unnecessary, to distinguish them by a definite boundary. The fossils
appear to be the same.
+ Most of the specimens here referred to, from the neighbourhood of Weymouth, are in
Mr. Goodkall's collection.
Dr. Firron on the Strata below the Chalk. 233
DeEvonsHIRE.
(118.) The coast on the west of Portland as far as Sidmouth has been
described by Dr. Buckland and Mr. De la Beche* in these Transactions ;
where also the former has published a map of the coast between Teignmouth
and Portland, with views from Sidmouth to Bere Head, and from Lyme Regis
to the vicinity of Weymouth and Portland +. The coast of Devonshire,
therefore, requires no additional illustration ; and for the local extent and
distribution of the strata in the interior of that county, it is now in my power
to refer to the beautiful Geological Map recently completed by Mr. De la
Bechet, and to be followed by an explanatory memoir and sections.
As the beds between the chalk and the bottom of the lower green-sand on
the west of Purbeck appear to have coalesced, and are no longer marked by
the previous subdivisions, the green-sand of Devonshire may be regarded as
the equivalent of the whole series. The lower green-sand seems especially
to have been reduced in bulk, in its progress westward. The gault has
wholly disappeared ; but some of its characteristic fossils are found in the
sand and grit of the cliffs on the west of Lyme. At the bottom of the
sands the boundary is everywhere distinct: and the plateau which shoots
out to the west of Dorsetshire is found successively in apposition with the
lower oolite, the lias, and new red sandstone ; while its remotest portion rests
on grauwacke slate. Throughout the greatest part of the tracts thus occu-
pied, the green-sand forms a flat-topped, uniform cap, investing the hills, as
far west as Sidmouth on the coast, and the Blackdown range on the north
of that place, nearly to Wellington ; and finally, it constitutes an exten-
sive outlier, from the north-west of Teignmouth to Penhill, about six miles
south-west of Exeter, which caps the heights of Great and Little Haldon,
and is detached from the more continuous tract above mentioned by an
interval of more than twelve miles, occupied by the new red sandstone.
Several insulated portions of chalk, however, still remain above the eastern portion of the
green-sand platform, especially upon the coast between Sidmouth and Lyme, and along the line
from Beaminster through Chard and White Stanton. The transition from the chalk to the sands
is well seen at some of the junctions, especially on the south-west of Axmouth, where the strata
* See their joint memoir at the commencement of the present volume; Geol. Trans., 2nd
Series, vol. i. p. 40, &c.: and a separate paper by Mr. Dela Beche, vol. ii. p. 109, &c.
T Ibid:, vol.i. p. 95, &c.
t “Ordnance Geological Map of Devon, and of portions of Cornwall and Somerset, by H. T.
“De la Beche, Esq.,” in eight coloured sheets.
2H
234 Dr. Firron on the Strata below the Chalk.
rise a little towards the north from the point of Bere Head, so that sections of the subjacent
beds are exposed in the cliffs on both sides of that promontory. The beds immediately below the
chalk are best seen on the shore towards Branscombe, and have been described by Mr. De
la Beche, who has also mentioned the quarries near that place, from which stone corresponding
in situation to the firestone of Surrey is extracted *.
The section at Whitecliff, on the east of Bere Head and of the village of Bere, is thus :
Feet.
1. Chalk: white at top, yellowish below; very sandy, containing throughout numerous }
small nodules of flints, both in bands and irregularly disseminated,—more numerous at
top.) Vermetus is a frequent fossil here... 200.6000 c0sdesnicevecscenscevccvnsesus 0
[At the bottom is a course of very sandy chalk, including concretions or lumps of { —
greater firmness, produced apparently by the unequal diffusion of the siliceous matter. | |
Total, 60 or 70 feet.
2. Yellowish grit, with green stripeS ». nese cene secs ceen cn eers re ceccsscnss selene
3. A conglomerate of lumpy concretions, and apparently of fragments also, of hard matter ;
with green particles between the lumps. Petrifactions numerous ..............About
4, Beds of chert; both continuous and in irregular concretions, alternating with bands of
xc 2 : : 2 50
siliceous grit ; from 3 or 4 feet down to a few inches in thickness .... Total, about 40 or
5. Bluish green and grey sand, with bands of more solid texture, increasing gradually in 40
number towards theibottom .). 03 J. cls ve sie ole © wiecle’ ibimcitia ts eicls ele ble clic tN DOME ONE
6. Bluish moist sand, in some places almost black, abounding in petrifactions, and becoming }
darker in colour downwards, the hue apparently depending on the degree of moisture.
This bed contains Gryphites, traces of large Ammonites, Vermetus, and numerous stems of
Siphonia «i100. tie ele cles e so sieciee ec cee vee sisie vais of si 2/5 +96» About 50) or 60tect ama
[This darkly coloured sand contains at the lower part large nodules, consisting of
greenish grit, in courses from 3 to 6 feet apart. The stratum is in immediate contact
with the red marl. Springs come out at the junction. |
7. Red marl. At the top containing gypsum in nests; throughout including spots and
patches of a light greenish grey, and alternating with beds, of irregular thickness, of the
same hue. (‘ Bunter sandstein ”?)
I have inserted the preceding list from notes taken during the summer of 1825, as its coinci-
dence with that since published by De la Beche, shows the correctness of both. It will be
evident, upon comparing these lists with each other, and with that of the sands near Lyme, that
the group which here succeeds the chalk is the equivalent of the Upper green-sand ; the local
variations in this formation on the Devonshire coast not being greater than those of the range
which extends from Folkstone into Surrey; in the course of which the Upper green-sand is
in some places almost wholly wanting, while in others it acquires great thickness, and often
contains beds almost suddenly developed, no trace of which is to be found in the intermediate
spaces. The grizzle of Sutton quarry, and the Beer-stone, are varieties of the siliciferous
stone on the confines of the chalk and Upper green-sand, which under various denominations,
“ Fire-stone”, ‘‘ Totternhoe-stone”, &c,., occurs very generally in that part of the series, and is
everywhere in request for building. The total absence of blue clay is remarkable in the section
at Bere. The place where it might have been expected is immediately beneath the cherty groups
of Mr. De la Beche’s figures 1 and 2+; and if the gault were added to those sections, estimating
* Ina large pit or quarry at the bottom of the chalk, near Sutton and Widworthy, a stone,
called Grizzle by the quarry-men, is dug in the situation of the firestone. The beds are altogether
about 5 feet in thickness. It contains green particles, and does not burn to lime. Among its
fossils is Catillus Cuviert.
t+ Geol. Trans., 2nd Series, vol. ii. pl. 16.
Dr. Firron on the Strata below the Chalk. 235
its thickness only at 100 feet, the total thickness of the whole of the green-sand group would not
be more than 300 feet: the actual thickness of the sands being nearly 200 feet at Lyme Regis ;
and at Whitecliff, according to my own measurement (it is not stated by Mr, De la Beche),
about 160. The beds below this cherty group represent Mr. De la Beche’s “ Fox mould” (No.6.
of the above list); and are apparently the equivalent of the upper and more ferruginous group
of the lower green-sand: the lower, moist, and dark-coloured sands, with the ‘‘ cowstones” at
the bottom, being probably the equivalent of the middle, dark, cohesive sand of Sandgate (24.),
Shanklin (192.), and Black-gang Chine (195.);—the ‘ cowstones” representing the calcareous
group of Hythe, &c. This occurrence of nodules dispersed in sand is frequent wherever calcareous
strata are near their termination ; as in the cases of the Portland stone, the lower oolite, &c.
I have stated these resemblances that the whole case may be before the reader: butin the vale
of Wardour,—where the distinct occurrence of a bed of blue clay with the characteristic fossils
of the gault, leaves no doubt as to the place where the sands are divided,—the inferior beds
of the Upper green-sand acquire a character very like that of the Lower in other places; and
the latter is either wholly wanting, or very imperfectly represented.
(119.) Blackdown Hills.—In approaching the hills of green-sand, their
aspect on every side is the same, precisely resembling that of the long’ flat-
topped ranges of this formation, and of the Bagshot sands, in Kent, Surrey,
and Hampshire. The surface is barren, and the chief products, at present,
seem to be furze and heath ; though in former times, it is reported, extensive
woods were here. 1 ascended first from Wellington on the north of the
Blackdown Hills, and found red mar! for more than two thirds of the height,
so nearly resembling some of the sandy and variegated clays of the Wealden,
especially of the Hastings sands, that but for the presence of sulphate of
lime in crystalline nests, it would be difficult to distinguish them; while the
greenish varieties of the marl also very much resemble some of the beds above
the chalk in the Isle of Wight. From Beacon Hill, on the south-west of
Wellington, the uniform level of the summits is very striking, the eye being
carried over the whole range without interruption, and the ravines quite lost
sight of. The absence of the remains of chalk from the debris on the top of
these hills is remarkable : I searched long, but did not see a single fragment
of flint, all those which I could find being chert, easily distinguishable from
chalk flints. In the yellowish sand near the surface, at the Barnscombe side
of the hill, brown iron ore is found, in polished fragments of very high lustre,
resembling those of the lower green-sand at Sandown Bay in the Isle of
Wight (1200; p. 188.), of Surrey (59.), and Western Sussex.
Although the strata forming these hills are in a general view continuous, the whole country is
divided by fissures, attended in some cases with considerable dislocation; for an account of
which I refer to Mr, De la Beche’s Map of Devonshire, and his essays on Theoretical Geology *.
* « Researches in Theoretical Geology,” 1834, p. 185, &c.
236 Dr. Fitton on the Strata below the Chalk.
Three nearly parallel lines of fault, running about north and south, are especially remarkable in
Mr. De la Beche’s Map; one on the east of the county, passes from about a mile north of
Combe Beacon, through the hill which bears that name, along the valley of Wambrook, and the
streamlet west of Chardstock, across the Axe, to a point about two miles east of Axminster ; the
total extent to which it has been traced being about ten miles. A second fault extends from
Balay Down on the north of Challenge, through Membury, to the bed of the Yart south of
Yetlands; the lias being thrown up into immediate apposition with the green-sand through a
great part of its course, as is also the case in the preceding fault near Wambrook. A third and
shorter fissure, about three miles in extent, reaches from the north of Wilmington to Stockers,
about two miles south of Widworthy, crossing the main London and Exeter road, and skirting the
eastern slope of an outlying hill of chalk on the south of that village.
(120.) The hills which have furnished the greater number of the Black-
down fossils form the western range of the group between Honiton and
Wellington, about six miles to the south of Beacon Hill above mentioned.
Their escarpment, between Punchey Down on the north, and Upcot Pen on
the south, is distinguishable at a great distance by the white line produced
by the refuse thrown down from the openings of the sithe-stone pits; the
heaps thus formed constituting an almost continuous horizontal stripe in
the face of the hill.
The whole thickness of the sandy strata above the red marl in this part of
the country, seems to be about 100 feet. ‘The contrast between the barren-
ness of the upper sands, and the comparative fertility of the marl beneath, is
everywhere very conspicuous ; and it would seem from the unequal ascent of
the hedge-rows and cultivated ground that the surface of the marl is very
uneven.
The strata which afford the whetstones are about 80 feet below the top of the hill, to which
they are parallel. The mines (or “pits” as they are called) are driven in direct lines into
the hill, almost horizontally, and in some cases to considerable distances. The stony masses
from which the sithe-stones are cut, are concretions of very irregular figure, imbedded in looser
sand, nearly resembling those which occur in the upper division of the Lower green-sand near
Sandgate (21.): and though very irregular in shape, marks of the stratification of the sand can
be traced on their outside. The masses of which the sithe-stones are made, vary from 6 to
about 18 inches in diameter, and the beds which afford them would form a total thickness of about
7 feet, of which about 4 are fit for that purpose; the looser stone at the top and bottom being
employed for building.
The following is a sectional list of the beds in one of the principal sithe-stone pits at Punchey
Down, which, I was informed, was a fair representative of the whole:
Ft. In. Ft. In.
1. Reddish sand rock, extending upwards to the top of the hill.
2, “ Fine vein”. Concretions of firmer consistence; the best for sithe-stones.
[Shells are found in all the strata here, but abound remarkably in this one, jo 2 .to Vee
and inthe ‘frock beneath iti) <0)... ee cea. SOA 05 Sa ASRS nics oe
3. “ Top sand rock”; sand with irregular concretions; of no use.......... 5 0 to 4 0
Dr. Frirron on the Strata below the Chalk. 237
Ft. In. Ft. In.
4. * Gutters”; concretions of stone in 4 or 5 courses, in the sand, This bed is S268 tos
that most commonly used for sithe-stones ........+eeeeeeecerreeeeeees
5. * Burrows”; stone and sand of the same kind, but used only for building... 2 0 to 3 0
6. “ Bottom stone”; a range of concretions, affording excellent sithe-stones.... 0 2 to 0 6
[These concretions sometimes extend downwards, even to 5 feet, in the sand. |
7. “Rock sand”; chiefly sand, with fewer concretions; of no use ........-- 4 0
8. “ Soft vein”; concretions which afford excellent sithe-stones ............ O 2 to O 6
0
The strata below are not known to the workmen. ‘The total thickness, therefore, of the strata
which furnish the material for sithe-stones, including the rejected sand and rubbish, is from 12
to 18 feet; the whole of which is removed in cutting the drifts or galleries.
Sithe-stones.—As the manufacture of these stones occupies a great number of the inhabitants
of the country, and is of some commercial importance, a large proportion of the whole quan-
tity used in England being supplied from the Blackdown pits*, I shall here describe the method
of preparing them.
The sithe-stone men take from the owners of the soil the privilege of digging for stones,
leaving 40 yards on each side between the drifts (or “ pits” as they are called). There is no
limitation as to depth, and the drifts are commonly pushed to about 500 yards inwards, greater
distances not repaying the labour of bringing out the sand. When first taken out, the stone is
greenish and moist, and can be cut or chopped with ease. The tools employed are a sort of axe
or adze with a short handle (fig. 2.), called a “basing-hammer”, which is ground to a sharp
edge. These are made at the adjacent village of Kentisbere.
The other tools are “ picks”, without any peculiarity of struc-
ture, and “ hollowing-shovels” (fig. 1.), for digging the masses
of stone out of the sand.
For the purpose of cutting the stones, a vertical post of wood,
or “anvil”, is so fixed in the ground as to stand between the
knees of the workman, who sits upon a sort of bench built of
stone, with some strong pieces of old leather attached as a de-
fence to his left knee. He first, with the edge of his “ basing-
hammer”, splits from the blocks, upon his knee, long portions
approaching to the shape of the sithe-stones f ; and then cuts or 12 inches
chops them down, nearly to the required size, upon the anvil and his knee,—just as a carpenter
cuts timber with an adze. After being thus rudely shaped, the stones are “ hewn” to the proper
dimensions with a larger “hammer”, and then rubbed down with water by women, on a large
stone of the same kind; and when dried they are fit for sale.
The stones when finished vary from about ten to twelve inches in length; some have the
shape of a portion of an almond, with the ends and sides cut square, and about 2 inches by 14
in thickness; others are almost cylindrical, but smaller at each end, with the sides a little
curved ; the diameter in the middle about 2 inches.
* Sithe-stones are also manufactured in great numbers in Derbyshire from the sandstone of
the coal formation. (Farey’s Derbyshire : 8vo, 1815; p. 437-8.)
ue The masses of stone, I believe, split best in the direction of the lines of stratification of the
sand,
238 Dr. Firton on the Strata below the Chalk.
A good workman can cut out of the blocks about seven dozen of the stones per day *. They
are sold by the makers chiefly to one merchant at Honiton, who supplies the retail dealers. The
prices (in 1825) varied from 2s. per dozen, for the finest stones, 11 to 12 inches long, down to
8d. a dozen for the coarsest, 10 inches in length.
(121.) Between the sand and the red marl beneath it, I did not observe
any perceptible valley, nor any indications of an intermediate bed of clay.
In a lane at Standhill, between Wellington and Bryants, about half a mile from the latter place,
the strata were thus; belonging to what is, here, the upper part of the new red sandstone.
Ft. In.
. Dusky red clay, or marl, adhering to the tongue ........ sfeloke okshexeagte lip orpiets vie oloipin
. Light greenish clay, with glittering particles (mica) .......++22eeeeeeee ++ -about
o.o ©&.o
2
1
. A band of greenish sandy clay, in part concreted and sparry, irregular in thickness .. 0
sutoreenish clay, like NOj2.. o/s: ajeltetensestare teat leialcretetaccle /ovele ican. teteteletatetatareieta +« ADOUt NS
cor B® GO tO =
. Reddish clay, like No. 1., in part concealed at the bottom........... bi sieee @elele atone
These beds are scarcely distinguishable from those at the top of the Hastings strata, at the back
of the Isle of Wight.
At Kentisbere, about 15 mile west of the escarpment of the hills which contain the stone pits,
the strata of red marl appeared to dip to the south-east. They consist of coarse gravel and con-
glomerate of a dull red hue, under firm, red, marly sand: and here there is a distinct alternation
of yellow sand with the red marl, the former appearing below the marl in thick stony beds at
Jeast 50 feet thick. A rough section at this place is given in Plate X. a. No. 12,
(122.) Fossils —The great numbers and variety of the Blackdown fossils
may be ascribed in part to the extent of the quarries, which have been
dug for sithe-stones during a long series of years ; but the beds themselves
must be more than commonly fertile in these productions, since the entire
thickness of those from which almost all the specimens have been obtained,
does not exceed twenty feet. Their beautiful preservation arises, in some
measure, from the loose sandy character of the matrix in which they
are imbedded, and from which they are easily detached: but the compo-
sition of the fossils themselves has also contributed to this effect ; for, with
very few exceptions, the shells are converted into chalcedony, and the
* Mr. Meade, of Chatley near Bath, has favoured me with the perusal of a letter from the
Rev. Mr. Steinhauer, dated in 1813, in which, after an account of the whetstone pits at Black-
down, it is stated that the preparation of the sithe-stones is so injurious to the health of the work-
men, that in the little village of Punchey Down, which is inhabited exclusively by the stone-cutters,
the writer saw but one elderly person, and was informed that few reached the age of forty. The
complexion and figure of the greater number he describes as striking and interesting in a high
degree; but it was the hectic aspect, and itself a proof of disease. When I visited the place about
twelve years afterwards, I did not meet with anything that called my attention to the health
of the quarry-men: but the facts described by Mr. Steinhauer are analogous to those which prove
the frequency of consumption among the grinders of needles, and the workmen at some other
trades, where minute particles of solid matter are diffused in the air, and taken into the lungs.
Dr, Frrron on the Strata below the Chalk. 239
whole of their calcareous matter has disappeared*. This is the more
remarkable, as in many other places, indeed generally, the fossils of the
green-sands consist of carbonate of lime; the absence of which, however,
is prevalent throughout the sand of the Blackdown Hills, which seldom
effervesces with acids ; and to this circumstance, probably, the excellence
of the concretions which they contain, as a material for whetstones, is to be
attributed.
A very extensive collection of fossils from the Blackdown pits was formed
by the late Mr. Miller, of the Bristol Institution ; and is now in the museum
of that establishment. The Managers were so good, at my request, as to allow
the whole of this valuable collection to be sent to London, where it was
examined by Mr.Sowerby, by whom the subjoined list, and the annexed
plates, have been prepared: and I have great pleasure in expressing my
obligation for this mark of their confidence and favour.
(123.) List of Fossils from the Sands of Bracxpown, and of some other
places in DevonsHiRet.
Ammonites auritus. M.
A— denarius. A thin crust of hydro-
phanous chalcedony, over spongy sili-
ceous stone. M., Min.Con., F.
A— dentatus. M.
A— falcatus. M.
A— Goodhallii. Blackdown. M., F., Min.
Con. Near Lyme. D.
A— Hippocastanum. Dowlands cliff,
near Lyme. Min. Con.
A— lautus. M.
A— splendens. Pinhay, in hard green
sparry stone. F.
A—triserialis. Pl). XVIII. f.27. Mr.
Sowerby’s museum.
A— tuberculatus. M.
* See Conybeare ; “Outlines,” &c., p. 128.
Ammonites varians. A gibbose variety.
M. Pinhay. F.
A— varicosus. M., F.
A— Another species, probably new.
M.
Amphidesmatenuistriatum. M. P1.XVI.
f. 7.
4rca rotundata. M. Pl. XVII. f. 8.
Astacus, Portions of. Pinhay. Miss An-
ning. Near Lyme. D.
Astarte concinna. Pl. XVI. f.15. M.
Mr. Sowerby’s museum: D.
A— cuneata. F.
A— formosa. M. Pl. XVI. f. 16.
A—impolita. M. Pl. XVI. f. 18.
A— lineata. ¥F.
+ All the Fossils in this list are from the Whetstone Pits at Blackdown, except those to which a
different locality is assigned: and all the specimens from the Blackdown pits, where a different
composition is not mentioned, are casts in chalcedony.
The letter M. denotes that the specimen is from the collection of the late Mr. Miller, now in
the museum of the Institution at Bristol: Min. Con. refers to Mineral Conchology : D. to a paper
of De la Beche, on the chalk and sands in the vicinity of Lyme Regis and Bere; Geol. Trans.
2nd Series, vol. ii. p. 109 et seq.: F. to the Author’s Collection.
VOL, IV.—SECOND SERIES.
240 Dr. Frrron on the Strata below the Chalk.
Astarte striata. M. Min. Con.
A— multistriata. M. Pl. XVI. f. 17.
Auricula? incrassata. M.,F. Min. Con.
A—? Two species, not figured. F.
Aviculaanomala. M. Pl. XVII. f. 18.
Cardium Hillanum. ¥F., M., and Min.
Con.
C— proboscideum. M. Min. Con.
Corbula truncata. M. Pl. XVI. f. 8.
C— elegans. ¥., M., Min. Con.
C— gigantea. M., Min. Con.
C— levigata. Min. Con.
C—. Two other species, probably new.
M.
Cucullea carinata. M.
like stone. Min. Con.
C— costellata. M., F. Min. Con. Col
lumpton, Devon: near Lyme. D.
C— decussata. Pinhay or Bere? F.,
Min. Con.
C— fibrosa. M., F. The sand-rock of
this specimen is very like that of Ris-
borough, near Hythe. In red jasper-
like stone or chalcedony. Min. Con.
C— glabra. Pinhay. In firm sparry grit.
M., Min. Con. Near Lyme. D.
C— formosa. M. Pl. XVII. f 7.
Cyprina angulata. (Venus angulata. Min.
Con.) The shell about one third filled
with chalcedony, as witha liquid. In
some specimens the shell, the place
of which is now occupied by chal-
cedony, had been bored through, as
represented in the Plate: in others
the shell is covered by a thin outer
crust of chalcedony, opake and hydro-
phanous ; and the cavity is nearly full
In red jasper-
of very fine siliceous sand, over which
in some places is a thin crust of flat
botryoidal translucent chalcedony. M.
Teignmouth. Min. Con.
C—cuneata. M. PI. XVI.f.19. Drawn
from a specimen in Mr. Goodhall’s
collection.
Cyprina rostrata. M. Pl. XVII. f. 1.
Cytherea caperata. (Venus. Min. Con.)
M., F. Variation in the depth of striz.
Min.Con. Blackdown, and near Lyme.
C— lineolata. (Venus. Min. Con.) M
Min. Con. Berehead. F.
C— parva. (Venus. Min. Con.) M., Min.
Con. Pinhay? F.
C— plana. (Venus. Min. Con.) M., Min.
Con. Pinhay? F.
C— subrotunda. M. Pl]. XVII. f. 2.
Dentalium cylindricum. Near Exmouth.
Min. Con.
D— ellipticum. F.
D— medium P\.XVIII. f. 4. M., Min,
Con.
Echinus, portion of an. Bere: In white
calcareous sandstone. F.
Exogyra conica. (Chama, Min.Con.) M.,
F. Ware, west of Lyme Regis. Pin-
hay. Bere. F.
E— conica: var. Ridge high and sharp.
Berehead. F.
E— halyotoidea?
Blackdown. F.
E— levigata. (Chama, Min. Con.) Low-
est part of the green-sand at Bere-
head: In soft agglutinated sand,
abounding in green particles. F,
E— undata. (Chama, Min. Con.) M.
and Min. Con.
Fusus clathratus. M. Pl]. XVIII. f. 19.
F'— quadratus. (Murex, Min. Con.) M.
Pl. XVIII. f. 17.
F—rusticus. M. Pl. XVIII. f. 18.
F— rigidus. M. PI. XVIII. f. 16.
#— another species? M,
Gervillia aviculoides. M. Lyme. Min.
Con., F.
G— solenoides. Min. Con.
Gryphea canaliculata. (Chama, Min.
Con.) M. Outer surface calcareous
and effervescent, chalcedony within.
F.
Me}
(Chama, Min. Con.)
Dr. Firron on the Strata below the Chalk. Al
Gryphea canaliculata: a broad variety.
In yellowish effervescent sand, with
green particles. F’,
G— vesiculosa. Berehead? M.
Hamites spinulosus. M.
Inoceramus concentricus. M. Iniridescent
chalcedony: Pinhay. In green hard
stone. Min.Con., F. Near Lyme.
D.
I— gryphaoides. M. Near Lyme Regis:
In concretional masses of hard green-
ish grit, including very small scales of
mica, and some minute black specks,
under Dowland’s Cliff. Miss Anning;
and F,
J— sulcatus. Berehead. M.
Tsocardia? ¥.
Lima semisulcata. (Plagiostoma semi-
sulcatum. Nelson.) M. PI. XI. f. 10.
L—? subovalis, M. Pl. XVII. f. 21.
Littorina pungens. M. Pl. XVIII. f. 5,
I— gracilis. M. Pl. XVIII. f. 12.
Lucina? orbicularis. M. Pl. XVI. f.13.
T— Pisum. M. Pl. XVI. f. 14.
Lutraria striata. Pinhay near Lyme.
Min. Con.
Mactra angulata. M. PI. XVI. f. 9.
Modiola reversa. M. PI. XVII. f. 13.
Murex Calcar. M., F. In iridescent chal-
cedony. Min. Con.
M— quadratus. (See Fusus.)
Mya leviuscula. M. Pl. XVI. f. 6.
M— mandibula. Pinhay Cliff. In firm
green micaceous sparry grit. F.
M— plicata. (See Panopea.)
Mytilus inequivalvis. M. PI.XVII.
f. 16.
M— lanceolatus. Min. Con.
M—prelongus. P]. XVII. f. 15.
M—tridens. M. Pl. XVII. f. 14.
Nassa costellata. M.? Pl. XVIII. f. 26.
N— lineata. M. PI. XVIII. f. 25.
Natica (Parkinson, Geol. Trans.). F.
N—? carinata. M. Pl. XVIII. f. 8.
Natica granosa. M. PI. XVIII. f. 7.
N— canaliculata. (Ampullaria, Geol.
Suss.) M. Pl. XVIII. f. 6.
Nautilus elegans. M. Also in the sand
near Lyme Regis. D.
Nucula angulata, M., F., Min. Con.
N— antiquata. M., F., Min. Con.
N—apiculata. F. Pl. XVII. f.10.
N— impressa. M., F., Min. Con.
N—lineata. M. Pl. XVII. f. 9.
N— obtusa. M. Pl. XVII. f. 11.
N— pectinata. Pinhay. In hard greenish
stone. F.
Ostrea carinata. M. Near Lyme Regis. D.
O— macroptera. Berehead. F.
Panopea ovalis. M. Pl. XVI. f. 5.
P— plicata. (Mya, Min. Con.) M. Pin-
hay. F.
Pecten Stutchburiensis. M. Pl. XVIII.
f. 1.
P— asper. M.
P—compositus. M. Pl. XVII. f. 20.
P— Millerii. M. Pl. XVII. f. 19.
P— orbicularis. M. Pinhay. F.
P— quadricostatus. M. A cast in grey
chalcedonous chert. F. Haldon Hill,
Devon. Min. Con.
P— quinquecostatus. Pinhay. F.
P—,(new.) Bere. F.
Pectunculus umbonatus. Blackdown. F.
Haldon, Devon. Min. Con.
P— sublevis. Min. Con.
Perna rostrata. M. Pl. XVII. f. 17.
Petricola canaliculata. M. Pl. XVI. f.11.
P— nuciformis. M. Pl. XVI. f. 10.
Phasianella pusilla, M. Pl. XVIII. f. 13.
P— formosa. M. Pl. XVIII. f.14.
P— striata. M. Pl. XVIII. f. 15.
Pholas prisca. M. In silicified wood.
The shell is chalcedony.
Pinna tetragona. M., Min. Con.
Podopsis striatus. M., F. Effervesces.
Pollicipes levis. M. Pl. XVI, f.1. (See
also Pl. XI. f. 5.)
212
242 Dr. Fitton on the Strata below the Chalk.
Psammobia? gracilis. M. P). XVI. fig.12. Thetis minor. Large. A castin firm sparry
Pyrula Brightii. F. Pj. XVIII f. 21. grit. Pinhay, or Bere. F. Black-
P— depressa. M. PI. XVIII. f. 20. down, and near Lyme. Min. Con.
Rostellaria calcarata. M., Min. Con. T—(new.) Pinhay. A cast. F.
R— macrostoma. M. PI. XVIII. f. 23. Tornatella? affinis. M. Pl. XVIII. f. 9.
R— Parkinsonii. M., Min. Con., F., Pl. Trigonia affinis. M., Min. Con. Blue
XVIII. f. 24. mammillated chalcedony.
R— retusa. M. Pl. XVIII. f. 22. T— aleformis. Blackdown. M.:—Ridges
R— Another new species. F. very sharp. F. Near Lyme. D.
Scalaria pulchra. M. Pl. XVIII. f. 11. T— dedalea. M., Min. Con.
Serpula ampullacea? M. T— eccentrica. M. Hembury Fort,
S— antiquata. M. Pinhay. Calcareous. Devon. Min. Con.
S—carinella. M. Min. Con. T— pennata. Teignmouth. Min. Con,
S— filiformis. M. Pl. XVI. f. 2. T— quadrata. M. Pl. XVII. f. 12.
S— plexus? M. Effervescent. T— spectabilis. M., Min. Con.
S— tuba. (M.. Pl. XVilies. T— spinosa. M., Min. Con. Near Lyme.
S—vermes. Pl. XVI. F. f. 4. D.
Siphonia pyriformis (Goldfuss). PI. Turbo conicus. M., Min.Con.
KGa: T— moniliferus. M., Min. Con.
Solarium conoideum. (Cirrus plicatus, T— rotundatus. M., Min. Con.
M.C.) M. Turrilites costatus. M. Not chalcedony.
Spatangus Bufo. (Goldfuss, Pl. XLVIT. Turritella costata. M., Min. Con.
£73) Mi. T— granulata. M., Min. Con., F.
S— Portion of another species, proba- Venus angulata (see Cyprina.)
bly new. M. V— caperata (see Cytherea.)
Tellina inequalis. Pinhay; M. Black- V— Faba. F., Min. Con.
down; Min. Con. V—?immersa. M. PI. XVII. f. 6.
T— striatula. M. Pinhay; F. Black- V—?sublevis. M. Pl. XVII. f. 5.
down; Min. Con. V— lineolata (see Cytherea.)
Terebratula biplicata. M., F. Calcareous. V—? ovalis. M., Min. Con., F.
T— dilatata. M. Pl. XVIII. f. 2. V— parva
T— dimidiata, Haldon, Devon.; Min. V— plana (see nC ythenca®
Con. V—? truncata. M. Pl. XVII. f. 3.
T— latissima. (T. lata, Min. Con.) M. V—?submersa. Pinhay. F. Pl. XVII. f.4.
Z— megastrema. M. PI. XVIII. f. 3. V—. (‘Twoother species ; probably new.)
T— Pisum. M., Min. Con. Vermetus concavus. Pl. XVIII. f. 10.
T— striatula. M. Pinhay. Berehead. M.
T— Lyra. M. V— polygonalis. Calcareous. Bere. F.
Thetis major. Blackdown. M. Berehead; | V— radiatus. (Planorbis radiatus. Min.
Min. Con., F. Con.) M.
In addition to the species mentioned in this list, there are several others in
Mr. Miller's collection, apparently new ; but being too indistinct for figuring,
they have been omitted.
Dr. Firron on the Strata below the Chalk. 243
(124.) Blackdown to Shaftesbury.—The great range of the chalk escarp-
ment in the interior of England, which stretches, like the shore of a sea or
lake, from Crewkerne in Dorsetshire to the north-east of Dunstable in Bed-
fordshire, is perfectly analogous in structure and appearance to the downs
of Surrey and Sussex. It is interrupted by three or four indentations or
gulfs ;—one of great width, opening towards the west, between Crewkerne
and the heights about Stour-head in South Wiltshire; another expanding
to the north-west and terminating in the defile where the Thames cuts
through the chalk, in its course to the south-east from Buckinghamshire and
Oxfordshire. The vales of Pewsy and of Warminster are intermediate
bays of the same general structure but of smaller dimensions ; and all these
valleys are apparently the result of denudation, aided by previous disturbance
of the strata,—which has carried away the chalk, and laid bare to various
depths the strata beneath it*.
The Green-sand hills range nearly from west to east for about ten miles on
the south of Wellington and Taunton, and are then broken through irre-
gularly, retiring towards the south to join the north-western extremity of the
Dorsetshire chalk, of which some large outliers exist in the vicinity of Chard
and Crewkerne. The chalk escarpment is thence continued in a direction
parallel to the northern range of the Blackdown hills, to an opening on the
north of Blandford, through which the Stour makes its way to the sea at
Christchurch ;—the tributary branches of that river, before it cuts through the
chalk, winding extensively over the country around Sturminster, from whence
the waters of the whole bay are conducted to the south-eastern coast. From
the opening of the valley of the Stour the escarpment turns nearly north
towards Shaftesbury, between which place, or rather between the promi-
nence of the Upper green-sand on the north of it, and Mere, is the opening
of the vale of Wardour. The beds immediately below the chalk from Crew-
kerne to Shaftesbury, have not yet been examined in detail, but the general
distribution of the strata is represented in Mr. Greenough’s Map.
Sourw WiTsHiRre.
(125.) Vale of Wardour.—This tract may be considered as an eastern
prolongation of the first of the great gulfs above mentioned, which being
suddenly reduced in width between Shaftesbury and Mere, is continued east-
* The principles of structure in these tracts, are ably discussed in Dr. Buckland’s well-known
paper “On the Formation of Valleys, by Elevation of the Strata that inclose them,” (Geol.
Trans., 2nd Series, vol. ii. p. 119, &c.,)—where the vales of Wardour, Warminster, and Pewsy
are expressly mentioned in illustration of the author’s views.
244 Dr. Firron on the Strata below the Chalk.
ward as a valley surmounted on both sides by hills. It will be seen from
the Map, Plate IX., that the anticlinal line by which this lower tract is tra-
versed coincides in direction with that of the great Wealden denudation of
Hants, Surrey, and Sussex; and is parallel also to the line of upthrow on
the coast of Dorsetshire and the Isle of Wight, and to other shorter lines
of elevation, the connexion of which is not at present visible, on the north of
the Weald,—through Burgh-Clerc, Ham, Shalbourne, and Burbage, to
the Vale of Pewsy. One of the anticlinal lines of the lower strata, beneath
the new red sandstone, from Frome to the Steep Holm in the Bristol Channel
also runs nearly from east to west; whilst, on the contrary, another line of
fault by which the lower beds are intersected, beginning near Portishead-
point on the west of Bristol, runs northward, across the Severn, through
Newnham, and thence to the north-west of Gloucester *.
(126.) The Vale of Wardour has the general form of a triangle, the base
of which extends from the chalk hills on the south of Shaftesbury to those of
Mere, the apex being a little to the west of Harnham Hill on the south-east
of Salisbury : for it is deserving of observation, that the stream of the Nadder
escapes from this valley, not directly through the angle at its geological sum-
mit, but through the north side; ma manner perfectly analogous to that of
the egress of the streams from the Wealden denudation in Kent and Sussex.
The heights which bound the vale consist at top of chalk, the inclination
of which, like that of the strata beneath it, on the north of the anticlinal
line, is in many cases more than 20°; while on the south, it is seldom more
than 3° or 4°, apparently deviating but little from the general disposition of
the strata in the South-east of England ; and this anticlinal line itself is
throughout much nearer to the north than to the south side of the vale.
The strata from the chalk down to the gault inclusive seem to be continued
all through, and to be nearly uniform in thickness ; but the surface between
the chalk hills is very irregular, and is divided by a ridge or bar formed
by the escarpment of the Portland strata, on the east of which the ground
is hilly, but on the west comparatively flat and low :—the appearances being
altogether such as would arise from the deposition of the green-sands and
chalk, over a tract partially occupied by the Purbeck and Portland forma-
* The anticlinal lines near Bristol, on the Map, Plate IX., are taken from Messrs. Buckland
and Conybeare’s paper on that district. For a full account of their reiations to those in the South-
east of England, the reader is referred to a paper since published by the Rev. W. Conybeare
(London and Edinburgh Phil. Mag. for 1832, vol. i. p. 122, &c.), who states that one of the great
lines of fault, by which the transition strata of the Quantock Hills in Somersetshire (beyond the
range of the Map, Plate IX.,) are traversed, runs also nearly east and west.
Dr. Frrron on the Strata below the Chalk. 245
tions, so as to overlie the latter, and beyond them come into immediate
contact with the subjacent clays.
The small map, Plate VII. fig. 3, gives a plan of this valley on a larger
scale than that of Plate 1X., and the Sections as to Gu, Pl. X.a., No. 13.,
further illustrate its structure:—the strata being the Chalk,—Upper green-
sand,—traces of the Lower green-sand, and of the upper members of the
Wealden; beneath which the Purbeck and Portland formations are more
fully disclosed.
(127.) Chalk.—The beds at Harnham Hill, immediately on the south of
Salisbury, are inclined to the north ; and about a mile to the west of that hill
a curved ridge, or horseshoe, formed of the upper chalk, seems to be the first
divarication of the strata which bound the Vale of Wardour*. It therefore
deserves inquiry whether the continuation of the fissure produced by an
upheaving on the east of this point, may not be discoverable in the space
between Salisbury and the head of the Wealden denudation. The southern
limb of the chalk forms a continuous and lofty ridge from Harnham,
through Compton Hill and Chiselbury, to White Sheet Hill, around the base
of which the Upper green-sand occupies the whole space from Berwick
St. John’s to Shaftesbury, the escarpment of the latter formation, which
is the immediate boundary of the vale, being continued all along the foot
of the chalk range, and rising from beneath it towards the north.
On the summit of the ridge at Chiselbury, the chalk includes black flints in spongiform nodules:
the Down slopes northward at an angle of upwards of 26°; and at its foot there is a depression
or trough. The lower and marly chalk form a ridge at Hoopside, about 200 feet above the
stream at its base, and perhaps 100 below the summit of the highest range, which as the name in-
dicates is curved, and nearly parallel to the curve of the upper chalk at the Race-course. The
hill in Wilton Park belongs to the upper chalk, which there crosses the stream of the Nadder,
passing through North Burcombe and thence towards the north of west, to form the higher downs,
on the north of the valley, at some distance from the ridge of the sands. The lower chalk and
chalk marl constitute an intermediate tract, in several places outtopped by the sand ridge. In
the height above South Burcombe, is chalk with veins and nodules of flint; and nearly on a
level with the river, north-west of Hoopside, the Upper green-sand comes in.
The succession from the flinty chalk to the Upper green-sand, on the north of the valley, is
well seen in the road from Hindon to Fonthill Gifford. The ridge on which the archway stands,
at the entrance to Fonthill Park, being chalk with large flint nodules, exposed in a pit imme-
diately without the plantations, dipping north about 12°, and separated by a depression from the
ridge of the Upper green-sand, which is here very low.
* The Map, Plate VII. fig. 3, unfortunately, was engraved before I had observed the structure
described in the text, so that the points here referred to are not included in it: but the features
are well represented in the Ordnance Map; the aid of which, indeed, is almost necessary through-
out these pages, to understand what is stated respecting the structure of the country.
246 Dr. Firron on the Strata below the Chalk.
(128.) Upper Green-sand.—The effect of the unequal inclination of the
two sides of the valley is remarkably shown by the great difference in the
extent of the spaces occupied by this formation. On the south, the upper
beds are concealed at the foot of the chalk hills; but the lower strata shoot
out into plateaus, which form the tops of the hills all the way to Shaftes-
bury ; but on the north the whole series of the Upper green-sand rises ab-
ruptly and forms a very narrow ridge of unequal height. The Map and Sec-
tions, Plates VII. fig. 3.and X.a., No. 13., sufficiently explain this structure.
Some of the best sections of the transition from the chalk into the Upper green-sand are
visible near Barford St. Martin and thence to Baverstock. In the lane over Baverstock Hill
(called in the country Cloudles) the series consists of alternate beds of chalk and sand with
green particles, succeeded by a thick bed of green-sand abounding remarkably in Gryphea vesi-
culosa, which can be traced almost entirely round the valley. The ridge of these sands over
Dinton House is full 200 feet above the bottom of the depression between it and the lowest
chalk.
The greatest superficial extent of this formation occurs in the vicinity of Shaftesbury, where
the upper part seems to have been better preserved than in the continuation of it eastward. The
sections vary from 50 to 60 feet in thickness; of which about a third at top contains beds of
chert like those of the Isle of Wight: but the lower beds only are found in the plateaus which
project beyond the chalk.
Several good sections of the upper strata are visible in the lanes about Shaftesbury ;—at Lud-
well, Hernsham Street, in the ascent from Brookwater, and thence to the foot of White Sheet
Hill, where some of the quarries include chert and veins of chalcedony.
From Castleditches,—-an ancient fort or encampment on the summit of a remarkable promi-
nence, the sand which composes the top declines uniformly towards the foot of the chalk range, but
extends with an even surface, westward to Shaftesbury, and eastward to Barford Heath. The beds
have many points of general resemblance to the sands of Blackdown;—with this important dif-
ference, that a very distinct stratum of bluish clay (Gault), which is wanting at Blackdown, is
here found, everywhere, below the sand.
The relations of these strata are well shown in a large quarry at the top of the hill east of
the valley of Fovant and of the Pembroke Arms, where the following was the order :—
Fovant Quarry. ron
. in.
Soil and Grass.
1. Greenish sand, alternating with gray, including stone which passes into chert, in irre- 16 0
gular concretional bands and masses :—very like the sands of Blackdown .... 14 to
2, Sand of a much darker hue, below passing into ston€.......sseeseeeceecees about 5 6
3. Stone called “Greenstone”, in firm beds, whichare quarried for building; upper surface 9 0
irregular; contains Gryphea vesiculosa, Pectens, and shark’s teeth ........ about
This stone is valuable from its not being affected by frost. It can therefore be dug
at any season, and stands well in water, as the foundations of bridges, and in
exposed situations, as in copings, &c.
4. Stone; but not good ......-cccsceesscne Sinlaisle.c/atetoc/elsials) stolo/eiateleuaerar: cocccens) tn
5. Sand; depth unknown.
On the north of the valley, the Upper green-sand appears likewise to consist of two portions;
Dr. Firron on the Strata below the Chalk. 247
that which immediately succeeds the chalk, the equivalent of the fire-stone of Surrey, and the
Malm-rock of Western Sussex, abounding in chert. To the lower portion the term Green-sand
is strictly applicable, as it is composed of sand, and abounds in green particles.
About two miles west of Ridge the sands suddenly expand and occupy a large space from the
north of Fonthill Abbey to Stop Beacon, where the surface is strewed with fragments of chert,
the remains, probably, of the higher beds which have disappeared. But further west, between
the Abbey and East Knoyle through Middlemore, the ridge again is narrow and highly inclined ;
but so much reduced in height, that the chalk of Hindon can be seen over it from the flat country
at the mouth of the vale. The sands again expand a little on the west of East Knoyle; but at
Upton their dip is not much less than 40°; so that the horizontal section occupies but a few paces,
and on the north the chalk is seen at a lower level, connected by insensible gradation with the
sands,
(129.) Gault.—The clay beneath the Upper green-sand seems to be co-
extensive with that formation. It forms on the south of the Vale of War-
dour a rapid slope; on the north, a depression, immediately below the
sand; and is identified in several places with the gault of the eastern coun-
ties by the characteristic fossils. At Lower Donhead, under Lidhurst, it
contains Ammonites with coproid masses of phosphate of lime; and at
Ridge, where one of the most distinct sections is exposed, many other fossils
have been found, the clay having been long used for tile-making. The beds
all dip to the north, between 6° and 7°; anda well has been sunk through
the clay, and a thin bed of sand beneath it, down to the Purbeck strata ;
the order being thus :-—
Section at the Tile-pits, Ridge.
South. Purbeck Upper Green-sand. North.
Stone-pit. Sand. Gault. Tile-pits. Well. QE
|
=) Feet.
coe j ——— 100
715
=e 15
= SS =
Ft, In
1. Upper Green-sand, at the upper part of the hill, consisting of—
a. Green-sand.
b. Green sand-stone, full of Gryphea vesiculosa at the upper part......8to 10 ft.
PPCRPEEMASIU SANG: 6 ole\e seine sencle selec nes clsisteeecisiene cs cces --more than 30
d. A bed called by the workmen “ malm-rock ”; sand with stems of Siphonia
and impressions of Ammonites ....0-eseeceesscrecceccessees -about 100 0
2. Gault, including near the top a bed of pyrites, shot through with veins of calcareous
spar, of which some large crystals are found here. The rest is clay* containing 75 0
Ammonites, and other characteristic fossils, with Septaria and ovoid concretional
magaces Of phosphate OF ME ....-secneccesscesrecvesscnsecscesvascesscccs
* About 3 feet of clay, which occurs on the north-west of Ladydown, may belong either to
this stratum, or to one of the beds subordinate to the Purbeck formation.
VOL. IV.—SECOND SERIES. IK
248 Dr. Firron on the Strata below the Chalk.
3. Sand; (perhaps the representative of the Lower green-sand) said to be like that of 15
the hill top. Masses of a calcareous conglomerate in the upper part ..+..+-seee- 0
4, Fissile stone ; some of the upper beds of the Purbeck series :—
a. Slaty limestone, abounding in Cypris and Cyclas, with smooth Paludinz, and
another acute spiral univalve.
b. Fine-grained oolite in uniform globular particles, like the roe of fishes.
(130.) Lower Green-sand.—This formation is nowhere prominent in the
Vale of Wardour, and scarcely observable throughout the greater part of it.
The ferruginous sands below the gault in the eastern portion of the valley
may not improbably be referable to some of the Wealden sands; but on the
road descending from the Pembroke Arms to Catherine Ford, a bed of
greenish sand occurs below the gault, which seems to be superior to the
Wealden strata; and if this be continuous with a bed of sand which appears
at Penthurst and Fovant, it must belong to the marine beds; as I found at the
former place a Pecten and the stem of a Siphonia. Ochreous sand, with some
blue clay, to a total thickness of five or six feet, occurs likewise above the
Purbeck strata at Totterdale (Totteridge of the Ordnance Map),—a height
on the south of Tisbury, to which I shall hereafter have occasion to refer.
On the north side of the valley, sand of the same doubtful character occurs
immediately below the gault ; but a bright ochreous clay, in a corresponding
place between Apsell and Chicksgrove, is in my notes referred distinctly to
the Lower green-sand ; and a part of the sands from Fonthill Abbey to Stop
Beacon, may also belong to the same formation. On the whole, however,
the difference between the bulk of the Lower green-sand here, from that
which it exhibits in Kent, Sussex, and the Isle of Wight, is very remarkable,
and accords with the rapid thinning out of the formation westwards, on the
coast of Dorsetshire and Devon.
(131.) Wealden.—The indications of the upper members of this group in
the Vale of Wardour are likewise indistinct, nor did 1 find here any of their
fossils ; but where the strata rise slowly from beneath the gault on the east,
under Fovant Wood, and thence by Catherine Ford and the sloping ground
towards Dinton and Teffont Magna, (PI. VII. fig. 3; and Pl. X.a., No. 13.)
are traces, probably, of the Weald clay and Hastings sands; the pond at |
Dinton Parsonage, especially, resting on a bed which answers well to the
site of the Weald clay. ‘These indications deserve notice, as they furnish
the only instance with which I am yet acquainted, of the occurrence of
the upper members of the Wealden in the interior of England. The place
where these strata may be looked for with the greatest chance of success,
is on the descent from the plateau of the Upper green-sand to Catherine
Dr. Firron on the Strata below the Chalk. 249
Ford; and their existence is rendered more probable, by the distinctness
with which the connected strata of the Purbeck group are developed ; the
whole series apparently thinning out towards the west.
(132.) Purbeck Formation.—The Purbeck beds rise from beneath the sand
and clay at Dallard’s Farm, near the eastern angle of the Vale of Wardour ;
and from that point they can be traced,—on the south of the Nadder, at
least as far as Totterdale, south of Tisbury ; and on the north, to Ashley
Wood, west of Ladydown, or perhaps to Stop Street, a hamlet above the
village of Fonthill Giffard ; occupying also the greatest part of the inter-
mediate heights between these extreme points. The strata throughout agree
with those of the coast ; their fossils, with the exception principally of oysters,
belonging to freshwater genera ; and at the lower part near their junction
with the Portland stone, they likewise include beds of clay alternating with
limestone ; one of which at least contains the trunks of silicified trees. The
abundance of marine shells in the Portland beds immediately below, is here
as remarkable as in the Isle of Portland.
The Map and Sections, PI. VII. fig.3., and PI. X.a., fig. 13. aB &c., show the
general relations of the Purbeck series. The principal quarries open, in the
upper part of this formation, when I examined the country, were at Dailard’s
Farm above mentioned ; at Dashlet on the south of the Nadder, about mid-
way between Catherine Ford and Chicksgrove; and on the opposite bank
of the river, at Teffont Evias and near Legh-barn. ‘The junction of the
Purbeck and Portland strata was best seen in a quarry at Wockley, on the
south-east of Tisbury, the counterpart of a much larger one, worked some
years ago at Chicksgrove (or Chilmark) Mill, but now obscured by decom-
position from long exposure.
At Dallard’s Farm, the beds first seen, on the west of the upper green-sand and gault, were
thus :—
Ft. In. Ft. In.
1. Soil and Grass.
2. Yellowish brown ferruginous loam, or clay......-cceccccercceccvccrers bo56
3. Slaty stone and clay, including seams of fibrous carbonate of lime :
a. Slaty limestone, containing Ostrea distorta, Pl. XXII. fig. 2. ......000. 0 6
b. Fissile whitish calciferous clay, called “ Spangle” by the quarrymen, in- onic
cluding great numbers of a small Modiola ........eeeeeeeseeeesecs
ce. Whitish uniform limestone, including Corbula alata, Pl. XXI. fig. 5., like aLt9
Benmmenr thecoash at Upwayie tie ists ciels O25. £101 safe ois whisicle elsiew werele ois
d. Fissile clay..... Rateithls will hes jota vie atktal s Slaieiiara\uiatele)a cis »'owletdialdiditidie 6a ly 0
e. Clay ; somewhat like d, but more approaching to stone ......s.+..04- 0 6
J. Fissile clay, like ‘‘ Spangle ”, with Modiolz, like those of b. ........0+ e510 4 6
Ke?
250 Dr. Firtron on the Strata below the Chalk.
Ft. In, Ft. In.
4. Slaty limestone in firm beds, alternating with blue fissile clay :
a. Rough and irregular above ..... eoe vane a)ieisle)6 6101 s)is\¢ 0010 6 coeee-6in.toO 9
b. Stone; firm and durable, abounding in Cyclades;—within the valves of
which are deposited beautiful casts of a small species of Cypris. See } 3
LAGOON ly Ha, 7/5, ei area Bobo BUH OUD OOCT OO Oma OO Nd GUC" Soc amaoae z 8
5. Alternations of very blue fissile clay, with thick slaty stone, containing Ostrea Le
ABSLORLG tra) atten Hele) ste s foliniole sl vie o: = slelstetekclolercheieinicysley = miei ict heii
Os Stones contac! Gowen GAdoaoc5 60 4g05064cs0000000050005 visible 2 0
These lower beds are of different tints of blue and gray ; the gray by exposure becoming white,
and the blue portions graduating into a hard, somewhat splintery stone, which in some spe- —
cimens might be taken for limestone of the carboniferous series ; some of the slaty strata alter-
nating with clay (3 above), consist of worn, rounded, fragments of shell and of stone, and are
very like some of the upper beds of Bermuda. The outer surface of the more uniform lime-
stones is here much eroded by the weather; and when the masses are split, the natural partings
are frequently found to be furrowed or eroded with tortuous irregular channels, from half
an inch downward in diameter.
The pits along the south bank of the river, where the Purbeck series emerges from beneath
the heights of sand, afford several good sections ;—very much alike, and fairly represented by the
following detail of one at Dashlet. (See the Map, Pl. VII. fig. 3.)
Section of the Stone-pits at Dashlet.
1. Brown, loam-like clay, including, or passing into 2. ........ee seve eeeeee ie
2. Concretional, but nearly continuous masses of soft stone, with layers of Cy- 0 6
clades and Cypris, and oolitic particles .......sessseesseeeescvons about
The oolitic particles, when decomposed, leave empty cavities in the firmer
cement, which might be mistaken for casts of Cypris.
3. Fissile stone, in irregular beds, almost entirely composed of Cyclades and 1 3
OniretMreigu gue sooeaddcuoddn cdcd Udad 860s 55 SoC eR MOBMenED SSou goo
4. A group of clay and limestone :
a. Thin slaty, calciferous clay, including b. ........+e+seeeceeees cstce) Ob Re
b. Delicately fibrous carbonate of lime, with impressions of Cyclas media 0 2
on the surfaces adjoining the clay ; the beaks unusually sharp ........
Cc. Clay Pee eer weer cree reese reser sess rereesessesesesesssssses Op 1. 3
d. Flattened roundish masses of uniform white and gray stone, imbedded 0 4t- ue
in the clay of c. and d.; vertical cracks within, as in Septaria ........ 1 6
FAI OWINS WEAF oa d045 qopoouc cod OnODBOIIBA saoUoGdoOOKI ODDS lin. to. 05 2
J. Fibrous carbonate ’ordumerrerysc): +/<'<). + 87 sie iohep sis « pista yt Geta ele 0,1
ie. Fissilevclay, caleticroussbelowsmoenel-\>micfacsis,c%)-feise cists = eyelet ete lin, to J0556
5. Compact limestone, in some places bluish, containing very large Cyclades 1 4
(C. major); a large flat bivalve (Unio?); small bones and palates of fishes ; } to
and fragments of Ostrea distorta, Pl. X XUN. fig. 2.0... cane « occ clecie scissile 1 6
The slaty limestone in the pits hereabouts affords the same beautiful casts of Cypris as are
found at Dallard’s, frequently inclosed within the valves of Cyclades, of which, in fact, the beds
are almost entirely composed. In other cases the surfaces of the strata are covered with im-
pressions of a small Modiola. The clay is often divisible into fragments, which are polished,
as if by friction under strong pressure.
Dr. Firron on the Strata below the Chalk. 251
Some of the beds of uniform whitish limestone, to which the workmen give the name of “ Lias”,
very much resemble the stone of Monte Bolca; and where most compact, are so like the stone
used in lithography, that their application to that purpose seems to be well deserving of trial.
The exposed edges of the thicker folia are eroded deeply into spongiform cavities. In some of
the pits, the limestone, alternating with clay, has the appearance of united concretions or lumps;
but within the stone is uniform, the aspect that of freshwater limestone, and the fracture
splintery or very flat conchoidal, resembling a rock found in a corresponding place at Gar-
sington near Oxford, which is there called “‘ Malm”. The masses split into irregular flakes at
right angles to the surfaces, not more than a twentieth to an eighth of an inch thick. Both the
clays and limestones in this part of the Purbeck series have sometimes a bluish colour; and
both inclose large specimens of Ostrea distorta.
On the north side of the valley, as the Purbeck strata rise more rapidly, the sections are not
so much expanded; but about Teffont Evias slaty limestone, alternating with clay and fibrous
carbonate of lime, is seen not far from the gault, dipping about north 15° west, at an inclination
between 2° and 4°. A thick coating of these strata invests the heights thence to Ladydown,
(see the section, Pl. X.a., fig. 13. aB.); but about midway to that place, it is cut through by a
natural ravine, which runs from Chilmark to the Nadder at Penthurst Bridge, and not impro-
bably may have originated in a dislocation. The Portland beds which form the lower part of
the ravine have been extensively quarried on both sides.
At Ladydown, near the highest ground occupied by the Purbeck formation, quarries have long
been worked to great extent, chiefly for the sake of the fissile cycladiferous stone, like that of
the Isle of Purbeck, which here bears the name of “Tilestone”. Among these beds is a group
which abounds in the remains of fishes.
On the south of the Nadder, near Benston, a prominence, like a step at a lower level, extends
beyond the sands and clay which form the upper part of the hills, and is continued to Wockiey
and the west of Anstey Water, capping the height occupied by Totterdale Farm, where the Pur-
beck beds run out. In the lower part of this projection, a large quarry was for many years worked
at Chicksgrove Mill, and another more recently at Wockley ; the bottom of the former is nearly
level with the river; the top about 50 feet above it, and about 30 feet lower than the top of
the prominence above mentioned. The total thickness of the Purbeck strata indicated by these
data does not exceed 60 feet.
A few beds occur in the upper part of the section at Chicksgrove, which do not remain at Wock-
ley ; but the rest are so nearly the same at the two places as not to require a separate detail.
List of the Beds at Chicksgrove Mill, and Wockley Quarries.
BE ine) Eitsain,
Chicksgrove.—
Fn a yl all «gol gama he Deeg dh: Sa Ree Meh IE about 0 9
1, Loam; including fragments of stone, like the “lias” of the pits above men- Ris
Ge Peale da ioteys vial helenae SE SOONOOL POETS ASSN about
=» bluish clay, passing into 3..........-...- capotovee he sesey OU to Om. (OO
3. Yellowish brown, tough clay, very uneven at the bottom; filling up the ir- 6
Lop RE CT a ie on hair ale I a i a a B56 ges ot Oita
2 0
nearly continuous ; in many places having the aspect of magnesian limestone,
4. A bed of coarse, somewhat gritty limestone, very irregular in thickness, but
and containing nests of carbonate of lime in rhombic crystals.....1 ft. to 3 ft.
or
Sc
252 Dr. Fitton on the Strata below the Chalk.
Ft. In,
5. A bed, likewise very irregular, consisting of—
a. Brownish clay, at the upper part.
b. Cavernous concretions or crusts of carbonate of lime, in the form of irre-
gular flakes ; which in some places have a deceptive appearance of or-
ganic structure. This bed accommodates itself to the inequalities in the
surface, both of 4 above and of 5 below it; and seems to be a mass of
loose loamy clay, shot through by stalagmitic carbonate of lime....... .
6. A bed much decomposed, and very unequal in thickness: apparently consist-
ing of soft, calciferous clay, with some portions of firmer limestone ........
All the preceding beds seem to be above those of the Wockley Quarry.
7. (Apparently the same with 2. and 3. of Wockley.) Irregular portions of
limestone, very indistinct from decomposition ; sometimes wholly wanting;
sometimes in the form of thin slaty beds waving over the inequalities of the
Clay (8:) below 222 ss silat eflelelsleieleles lelele clsivivie o'eisie 1 ft. to 1 ft. 6 in.
The whole thickness from 4ft. to 7ft. inclusiveis........ about
8. Tough clay, (seems to be the same with 4. of Wockley).
Wockley.—
Grassy surface.
1. Ferruginous loam and sand, filling the irregularities in the top of 2.....6 in. to
2, Compact limestone, much decomposed, but in the fresher pieces mottled,
grey and bluish. At the bottom this bed is divisible into flakes or thin strata,
curved, or waving; very like the lower part of the “slate” of Portland,
and the fissile beds above the Portland stone at Bacon Hall, (p. 223.) (Que. |
thet Soft Burr,: or “Bacon-ledge |’)s.c' sie 1 « -\<1-'+ <6 ws+» 1 ft. Gin. to 2 ft. J
is)
. Decomposed whitish, fissile limestone ; passing at the lowest part into 4.,
and very nearly resembling the “ Cap” at Bacon Hall .............. about
4, (8. of Chicksgrove Quarry.) Tough dark clay, in some places very like
Fuller’s-earth : seems to represent one of the “ dirt beds” of Portland and the
coast near Lulworth, but is more uniform, and does not contain fragments of
SEOME Wafetets lolol elect tele oiskeye fav oleh re feteteictetehofer<hetots FOOd BOOP CORED OO aba eros
or
. (9. of Chicksgrove.) Fissile stone and clay.
Gy Eland SEONG se iete tere lcle'e « wioteler chet oheoterchetelevel of olistera elect ss. « c\letolsieneienerreeeeete 0 5
b. Thin slaty stone, in some places sandy, abounding in casts of Cypris, and
in Cyclas elongata, P). XXI. fig. 9. This bed very much resembles the
decomposing ‘‘Cap” of Upway (p. 223.) and may perhaps correspond to
the “Ash” of Portland (p: 220.)):.av.-.es+oe- pie oieielehe tecciatereye terse vetete
The beds of this part of the section, at Chicksgrove, include also a
minute spiral univalve. They are intersected by veins of stalactitie car-
bonate of lime, like those in the “ Cap”, &c., of Portland.
lower part over the masses of d.; precisely like the bottom of the
‘Cap’ 2 at bacon dal. (p42 259) meciscislelcei sine </> «6 BbddocgoadHosdn
d. Irregular concretional masses of black flint, rugged without anew de-
tached ; not in themselves distinguishable from chalk flints ......... —
c. Fissile calcareous matter, in beds of unequal thickness, curved at |
0 10
o>)
. (10. of the Chicksgrove section.) Fissile, somewhat gritty limestone; at top }
enveloping the flinty masses 5.d.; below adheringto7. This bed at the upper |
part contains casts of Cypris in great numbers. ‘The proprietor of Chicks-
grove Quarry told me that fishes, like those of Ladydown, were found in this r
part of the series, both there and at Wockley; but the specimens which I |
could obtain were much smaller than those of that place...........00..00+ J
Ft. In.
6 0
1 0
heag
2 6
2
Dr. Firron on the Strata below the Chalk. 253
Bein, «Et. Its
7. (11. of Chicksgrove.) Uniform, soft, very white limestone, here called
“chalk”; but abounding at the upper part in Portland fossils: Pecten la-
mellosus, Cardium dissimile, Trigonia gibbosa, Ostrea expansa. This bed is
not fit for building, and is burnt into lime: it seems, nevertheless, to represent |
the “ white-bed ” of Portland, though without oolitic structure .....
8. (12., &c., of Chicksgrove.) From 7. to the bottom of the quarry, a depth of
about 25 feet, in 8 or 9 beds, is called ‘* Freestone ”: the detail as follows :—
a. Whitish stone, called ‘‘ chalk”, of uneven, subconchoidal fracture ; con-
taining great numbers of Pecten lamellosus and Cytherea ..... a eevee Z
b. Cream-coloured, somewhat sandy stone, also with Pecten lamellosus.... 2 6
o
ce. Similar stone; T'rigonia gibbosa, Cytherea, Pecten lamellosus. Sometimes 3 6
this bed includes 5 to 8 inches of sand ..... setolelhetetetiol oreheveharahets 2 ft. to
d. Concretional stone and sand.
MIEIICIDN 72°52 cidoierstel(ete sta clalass Avia sidlisi ais aierleaingan,d 0 0 tol 8
iil. Sand, separating and surrounding the concretions of i. 4.0 .t0.2.96
about — 4 0
e. Stone and sand :—
MAC ONCKEHONALSEONE: «4, < 6,sj0 0/2, 6 « <psi;s.0 eee! siete ee 1. O. torsee0
ii. Sand around the concretions..........ssseeees acu, 2) G6) etolORmON SiG
BPUONE «2.2.06: + cptoo 66.60 SooooGGoods06 pO BDOOUOOOOOOOd Obl dé 4 0
B. Ditto 0... ccc ee cs ccnesees eesesecees vee eens oe dvlatevele edie wletw ong 3 6
REED aha old's afew wclen cis Se eels ot Sretuletet ciehele ates charalel eta state olebantels 250
OO
These lower beds (which afford the best stone) contain Ammonites
giganteus of great size: they are more like the form of the Portland stone
which occurs in the Isle of Purbeck than that of Portland Isle itself.
Bottom of the Quarry.
At a new quarry near Chicksgrove Mill, the dip was east 25° south, at an angle of 2° or 3°.
(133.) Junction of the Purbeck and Portland formations.—It is obvious that
the preceding strata, down to 7, represent the lower part of the Purbeck se-
ries, which in the Island of Portland includes the petrified trees and Cycadee ;
and the section here is valuable, as it exhibits some variation in the form of
those lacustrine deposits. One of the principal points of difference between
the sections at the two places is, that the freshwater strata here rest, imme-
diately, upon a bed containing marine fossils, without the intervention of any
clay or dirt. Another difference is, that no flinty masses are found here, at
the top of the Portland formation, like those immediately above the white
bed in the Isle of Portland; but, on the contrary, a range of irregular masses
of black flint occurs distinctly within the freshwater series, and is separated
from the Portland stone (No. 7. of the preceding list) by a bed of freshwater
limestone (No. 6.), including casts of Cypris. As the flint, in this latter
case, does not contain fossils, its presence immediately above the junction,
while it is wanting in the usual place below, might at first sight mislead: but
the occurrence of flinty masses is by no means unfrequent in other parts of
the Purbeck group; and in the quarries north of the Nadder, opposite to
254 Dr. Firron on the Strata below the Chalk.
Dashlet above mentioned, where some of the beds partially composed of
dark-coloured flint, are full of Cyclades and other freshwater fossils.
(134.) Petrified Trees.—I saw no traces of trees or Cycadee either at
Chicksgrove or Wockley, nor could I learn that any specimens had been
found there; but I had the satisfaction of finding, on the road from Totter-
dale towards Walmead*, at a point nearly on a level with the top of the
quarry at Wockley, several fragments of a silicified coniferous trunk, with
cavities encrusted with quartz crystals, as in Portland and the Boulonnois#,
which had obviously come from a stone-pit just then filled up, on the road-
side: and soon afterwards, the workman who had dug them out informed
me, without being asked a question, that all the fragments were portions of
one large mass, “thicker than a man’s thigh,” which, he said, stood up-
right among the strata, “ like a gatepost,—and did not lie flat like the beds
“of stone. He had quarried,” he said, ‘“ many a piece near this place,
“as much as a man could heave up, and all standing upright.”’ This testi-
mony leaves no doubt that trunks in the erect position have been found here,
—precisely in the geological place where they might have been expected ;
and it is highly probable that further examination will lead to their dis-
covery 2m situ.
A bed or beds, of clay, near the junction of the two formations, in which silicified trees may be
expected, comes to the surface at several points along the river, between Ham Cross and Ashley
Wood on the west of the Ladydown Quarries. In one place on this line, at a streamlet which
crosses the road from Chicksgrove to Ham Cross, a bed or beds of clay, apparently belonging to
the upper part of the Chicksgrove section, comes down to the level of the road, and well deserves
to be examined ; and on the descent from Totterdale, above mentioned, towards Anstey Water,
is another spot where fossil trunks might be sought for with great probability of success,
(135.) Portland Strata.—The general disposition of the Portland beds in
the Vale of Wardour will be understood from the map and sections, PI. VII.
fig. 3., and Pl. X.a., No. 13. a8 &c. The upper strata are best seen in the
sections at Chicksgrove, Wockley, and Chilmark.
The stone is found in the bed of the river at Chicksgrove Mill, and continued without inter-
ruption on the south of the valley, beneath a covering of the lowest Purbeck strata, which cap the
height at Totterdale, to the vicinity of Wardour-castle, beyond Bridsor. On the opposite side
of the river the strata soon begin to dip towards the north; but they rise also slowly west-
* The names in the Ordnance Map here require correction. The word Totteridge ought to be
Totterdale, and should be transferred to the present place of the word Highgrove; the former
being the name of the farm.
+ Some of the specimens from this place, of a brownish hue, were found by Dr, Prout to
consist almost wholly of silex, with slight traces ef bituminous matter.
Dr. Firton on the Strata below the Chalk. 255
ward, to their final disappearance near Pyt-house. The remoter portions of this formation, on the
north-west, form some of the highest ground within the surrounding ranges of green-sand,—
as at Higher Lawn, Newtown, Pythouse, Linley, and Summerleaze; rising at the first two of
these places, nearly as high as the summit of Stop-Beacon, and out-topping the chalk immediately
on the north of the valley. The hill at Newtown is higher than the top of Castleditches.
The disposition of the beds on both sides of the Nadder westward, accords with that in the eastern
portion of the valley; the dip at Chicksgrove Mill being about east 25° south; and at an old quarry
near the syllable -ton in the word Hazelton of the Ordnance Map, south about 40° east. On the
south of the road from Newtown, immediately below the letters ho in the word Pythouse, the dip
is likewise nearly south, at an angle of about 22°, but this rapid inclination may be, in part, the
result of subsidence. On the north of the anticlinal line the beds dip rapidly in an opposite
direction. Thus, at Linley on the west of Lower Lawn and Summerleaze, and on the north of
Ashley Wood east of the line of Ponds, where the Portland strata come very near to the ridge of
‘Upper green-sand, the dip is almost directly north. In a quarry west of the road from Tisbury
to Fonthill, it is north 30° east, at an angle of about 20°, and the beds are much shattered by
fissures.
Excellent sections of the upper Portland beds are displayed in the quarries on the ravine
between the village of Chilmark and Penthurst Bridge (See Pl. X. a., No. 13, line A B.); where
the strata are inclined to the east 10° south, between 3° and 4°. Among the loose matter at the
top of these quarries is botryoidal carbonate of lime, passing into compact freshwater limestone,
—like the “Cap” of Portland, and the stone called “ malm”, at Garsington in Oxfordshire.
The uppermost Portland beds here afford beautiful specimens of a fine-grained oolite like that
of the “roche” in Portland: but the stone in some places alternates with sand, and has, in
general, a very sandy character.
The principal quarries of the Vale of Wardour are in the vicinity of Tisbury ; and some of the
best, when I was in the country, were near the road from that village to Fonthill Gifford. The
stone is more like that of this formation in the Isle of Purbeck, than in Portland itself, and
of a darker hue. A continuous bed of flint, about 2 inches thick, in. one of these quarries
(Bevis’s) had supplied, I was informed, the beautiful specimens of corals in chalcedony, which
are found in collections from this part of England. Among the fossils I obtained at Tisbury are
Astarte cuneata, Ammonites biplex in chalcedonic flint ; Ammonites giganteus of great size, Nerita
sinuosa, Terebra Portlandica, Turritella excavata (Cerithium? excavatum). A full enumeration of
the species found here, and generally of the fossils of the Vale of Wardour, was drawn up by
Miss Benett for Sir R. Colt Hoare’s History of Wiltshire; separate copies of which, illustrated by
plates of some of the new species, have been presented by that lady to her friends *.
The continuity of the strata hereabouts is frequently interrupted by chasms, locally called “lets ”,
like those of Portland (supra, p. 218.) and of Oxfordshire; in which the beds are abruptly
broken off, and the intervals filled with rubble and looser materials, to a perfectly level surface,
covered with a uniform coat of vegetable soil.
Portland Sand.—I saw no place in the Vale of Wardour in which the beds immediately beneath
the Portland stone were exposed; but I believe that the Portland sand occupies a great part of
the descent from Pythouse to the plain on the west of it; and in crossing from Newtown to Ha-
zelton this group seems to be disclosed immediately below the latter village, springs breaking out
along the line of contact. If this be correct, the bluish gray strata, occasionally visible in the
* “ A Catalogue of the Organic Remains of the County of Wilts,” 4to, Warminster, 1831.
VOL. IV.—SECOND SERIES, 2L
256 Dr. Firton on the Strata below the Chalk.
streams on the north and east of that point, must be referred to the Portland sand ; which, there-
fore, seems here to be more like that of the coast than of Oxfordshire and Bucks. At Tisbury,
I was informed, sand is found, but not more than 18 inches thick, beneath the lowest beds of
the Portland stone.
Kimmeridge Clay.—The whole of the level tract on the west of the opening of the vale seems
to be occupied by clay; and this I have referred to that of Kimmeridge, on the following
grounds, which, it must be acknowledged, are not very satisfactory. The gault and this clay
come into contact, on the north of Shaftesbury, and beneath the heights of green-sand at East
and West Knoyle,—in consequence of an overlapping of the whole cretaceous group, analogous
to what is observable in Devonshire. The lower clay, which is used for brick-making on the west
of Shaftesbury, contains Panopea depressa, and casts of Ammonites like those of Kimmeridge,
with other fossils, and includes a band of Septaria, there called “ Turtle-stone”. I myself found
a Pullastra? about a mile south-west of Pythouse, at the brick-field of Great Mead (or Moat)
on the north of Semley; and Miss Benett states that clay with the Kimmeridge fossils occurs at
Binley Farm (Que. Linley of the Ordnance Map?), on the west of Pythouse. I did not hear of
any bed of stone between the heights of Shaftesbury and Knoyle. It is not, however, impro-
bable, that outliers of the gault or Upper green-sand may exist within that tract. But whether
the Oxford clay also does not occur in the remoter part of the low country on the west of the
escarpment,—the Oxford oolite as well as the Portland strata being wanting there,—I could
not ascertain.
(136.) Stourhead.—I regret that it was not in my power to examine the
heights on the west of Mere, which, according to Mr. Greenough’s Map,
consist of the green-sands projecting beyond the chalk escarpment ; since,
from the information of a friend, to whom I am indebted for the subjoined
sketch and list of the strata, the Lower green-sand may be more conspicuous
there than on the confines of the Vale of Wardour; which would prove
that this group, like the Upper sand, is alternately expanded and again re-
duced in bulk and development.
The subjoined section extends from the chalk on the east of Stourhead, to the clay beneath
the hill on which Alfred’s Tower is placed, which is said to be 817 feet above the sea.
A Wise Sher Hill.
ae we bake Tales ge “Ys VV y" ya Chalk.
re
. sere oort or v camo Pate YY) a V/s Chalk-Marl,
= YONA se >
oe. es SA ss WE Z = OG Chert.
\\ o> CX ee aa
1. Represents the Upper Chaik. Feet.
2. Chalk Marl, here called ‘“‘ Malm”. In this a well had been sunk, which afforded the
following strata, by report of the well-sinker :—
a. “Malm”; like the chalk-marl of Lewes in Sussex, full of the characteristic
: 5 ‘ 100
fossils: ‘sharks’*teeth in great abundances)... <2). «<c0.s + «sie» «alee siereisie sie
b. “ White Stone” ; so called, but in reality rather gray or green: full of Ammonites, 4
many of which preserve their iridescent coats......seccesccvsscereces omyediale
Dr. Firron on the Strata below the Chalk. Qo7
Feet.
S. “Chert”. At the lower part rubbly; and there the water rose ........-++ 5 30
This stratum is visible in immediate contact with the sand (4.), above the Temple,
on the brow overhanging the lake.
4. Sand; constituting the whole of the elevated platform on which Stourhead House
is placed, and extending westward about two miles, to Alfred’s Tower. It is a loose
sand, with huge concretional masses of stone of similar composition. [Que. the
“cowstones” of the Devonshire coast ?] Fossils are abundant in the upper beds: the
lower are more ferruginous.
5. Clay; probably that of Kimmeridge ?.—(or Gault ?)
From a comparison of this list, with the sections in the Vale of Wardour, of which the beds
here represented are a prolongation, I should have been disposed, but for the opinion of my
correspondent, to regard the series as coinciding with that of Ticklepath Hill (Pl. X.a., No. 13.,
line G H), and East Knoyle: the Lower green-sand being indistinct or wanting ;—which is pro-
bable from the absence of gault between the “ chert” (3.), and the sand below it. In this case,
the gault would be inferior to the sand (4.), and perhaps a portion of the “clay” (5.). If
the clay be exclusively that of Kimmeridge, the gault must be looked for above; and a part
of (4.) might then represent the Lower green-sand, which, we shall find, occurs distinctly in the
vicinity of Devizes, about twenty miles from this place.
(137.) Vale of Warminster.—The relations of the strata here are shown
in the section, Pl. X. a., No. 14., on a line nearly from north to south. The
denudation in this valley having cut less deeply than in the Vale of War-
dour, the Gault is the lowest bed brought into view; and this only in the
deeper parts of the streamlets. Excellent sections of the Upper green-sand
are visible around the town of Warminster ; the beds which contain chert
being, in all cases, near the top, and the lower part almost pure gray or
greenish sand.
The Gault, at Crockerton, is a somewhat micaceous bluish clay, affording many of the cha-
racteristic fossils; and along with these Miss Benett has obtained masses of a gum or resin,
supposed to resemble that found in the London-clay at Highgate, which has obtained the name of
Fossil Copal*. I refer to the subjoined list, for the fossils which I myself obtained here; and
to Miss Benett’s Catalogue already quoted, and that annexed to Mr. Lonsdale’s paper hereafter
mentioned t, for a much more complete enumeration.
(138.) List of Fossils of the Vales of Wardour and Warminster, in
South Wiltshire.
[Upper G reen-sand. |
Ammonites monile. Vale of Wardour, at the contact of the Upper green-sand and
the gault; in conglomerate of green-sand.
varians. Ridge; in a compact fine-grained rock, approaching to what is
called “ marlstone”’ at Dean’s Farm, west of Farnham in Surrey (page 150, line
10, &c.). East Knoyle, between Upton and Chapel Farm, in the lowest chalk.
A
* Aikin’s Manual of Mineralogy, 2nd edition, p. 44.; W. Phillips’s Mineralogy, 3rd edition.
+ Geol. Trans., Second Series, vol. iii. p. 276.
2L2
258 Dr. Firron on the Strata below the Chalk.
Exogyra conica. In great abundance. Vale of Wardour: Castleditches Hill:
Norton Bavant; and Hernsham Street. Vale of Warminster.
Gryphea vesiculosa. Vale of Wardour: between the Bull Inn and Sutton Mande-
ville ; between Barford Street and Baverstock Church; Castleditches; Fovant,
lowest beds; Ridge; Dinton, upon Turritella granulata?.
Inoceramus? Between Upton and Chapel Farm. East Knoyle ; in the lowest chalk,
with green particles.
Natica? In green-sand rock ; somewhat slaty: Fovant? or Teffont.
Ostrea. Between the Bell Inn, and Sutton Mandeville.
Pecten orbicularis. Vale of Wardour: Hernsham Street; Fovant Quarry: Castle-
ditches ?
P. quadricostatus. Vale of Wardour: Hernsham Street, in soft green sandrock.
Spatangus Bucardium? (Goldf., Tab. 49, f.1.) Vale of Warminster.
S—— granulosus? (Goldf., Tab.45. f.3.) Vale of Warminster.
Turritella granulata? Vale of Wardour: Dinton.
Vermetus umbonatus. Ridge.
[ Gault. |
Ammonites auritus. Wale of Warminster: Crockerton ?
A — Benettie. Vale of Warminster. Crockerton. A large specimen sur-
rounded with branched vermicular stems, composed of greenish sandy shale:
preserving its iridescence.
A —- Beudantii. Vale of Wardour: Ridge.
A— dentatus. Ridge; with nodules of phosphate of lime. Crockerton; in
a mass composed of phosphate of lime.
A—— new: allied to dentatus. Crockerton.
A——— lautus. Crockerton.
A —monile, Crockerton. Interior occupied by chalcedony ; the thin coating
which remains in the place of the shell itself is opake, white, effervescent, and
has the pearly lustre. by
A—— planus. Crockerton: shell iridescent.
A———— Rhotomagensis. Ridge.
A————_ Selliguinus? Ridge.
A——— tuberculatus. Ridge.
A— varicosus. Ridge.
Astacus. The abdomen, and portions ofaclaw. Ridge.
Auricula inflata. Pl. XI. f. 11. Ridge?
Belemnites attenuatus. Ridge?
Caryophyllea. Ridge.
Cytherea parva? (Venus, Min.Con.) Ridge.
Dentalium decussatum. Ridge.
D—— ellipticum. Vale of Wardour.
Hamites attenuatus. Vale of Wardour.
Inoceramus concentricus. Vale of Wardour.
Dr. Firron on the Strata below the Chalk. 959
Inoceramus sulcatus. Vale of Wardour.
Natica. Two indistinct specimens, probably of different species. Vale of War-
dour.
Nucula pectinata. Crockerton.
Pecten orbicularis. Crockerton.
Pectunculus umbonatus. Ridge. Crockerton : bottom of the clay.
Pentacrinus, joints of. Pl. XI. fig.4. Vale of Wardour: same species as at Folk-
stone.
Plagiostoma elongatum. Ridge.
Rostellaria carinata. Pl. X1. fig. 19. Ridge.
Serpula. Crockerton: filled with phosphate of lime, in clay.
Solarium conoideum. PI. XI. fig.14. Vale of Wardour: preserves its iridescence.
S. ornatum. PI. XI. fig.13. Vale of Wardour: prebably from Ridge.
Terebratula ovata? Crockerton: in pyrites.
T —. Ridge: ina Septarium of phosphate of lime, with thin veins of calca-
reous spar.
Trigonia aleformis. Vale of Wardour: below Fovant? in clay, with numerous
green particles.
Venericardia tenuicosta. Pl}. XI. fig. 7*. Vale of Wardour: in Crockerton.
Venus parva? (See Cytherea.)
Fisn. Teeth: Vale of Wardour. Vertebre and rays: Ridge.
[Purbeck Strata. |
Cardium? Castleditches: Purbeck (or Portland ?) stone.
Corbula? Between Dallard’s Farm and Catherine Ford: with Cyclas.
Cyclas angulata. Pl. X XI. fig. 12. Between Dallard’s Farm and Catherine Ford :
with Cypris granulosa, Pl. XXI. fig. 4. in slaty Purbeck stone ; with Corbula
and Ostrea. Lane above Benston, near Chicksgrove : with Cypris and Modiola.
C— elongata. Pl. XXI. fig. 9. Teffont: with Cyclas membranacea.
C— major? Between Dallard’s Farm and Catherine Ford. Purbeck ;—or Has-
tings sand?
media. Pl. X XI. fig.10. Between Dallard’s Farm and Catherine Ford: in
slaty limestone; some specimens of which are almost composed of this shell.
Dashlet, between Teffont and Penthurst, with Cypris. Ladydown Tile-pits,
composing nearly the whole of the slaty stone. Between Ham-cross and Chicks-
grove, with Cypris Valdensis. Fovant Wood. Teffont: in slaty limestone, ap-
parently the top of the Purbeck, with Cypris Valdensis.
C— media: A gibbose variety; as at Penhurst, near Battle in Sussex, (supra, ’
p-177.) Pl. XXI. fig.11. Vale of Wardour, with Cypris Valdensis.
C—— membranacea. 'Teffont : with Cyclas media and Ostrea.
C— parva?. P|. XXI. fig. 7. Between Ham-cross and Chicksgrove : with Cypris
and Paludina elongata. Dallard’s Farm, where many of the Cyclas casts are full
of the valves of Cypris.
C.
260 Dr. Fitton on the Strata below the Chalk.
Cypris granulosa. P]. XXI. fig: 4. Between Dallard’s Farm and Catherine Ford :
with Cyclas, in slaty Purbeck stone; also with Cyclas and Modiola, in gray
freshwater limestone. Dashlet, between Penthurst and Teffont.
C—— Valdensis. Pl. XXI. fig.1. Vale of Wardour. Ladydown Tile-stone
pits: with a variety of Cyclas media. Between Teffont and Penthurst. Be-
tween Ham-cross and Chicksgrove; Teffont; and stone pits south of Ridge;
with Cyclas media.
Modiola. Dashlet ; between Penthurst and Teffont: in decomposed slaty limestone.
Between Dallard’s Farm and Catherine Ford: with Cypris, in gray freshwater
limestone.
Ostrea distorta. Pl. XXII. fig. 2. Quarry, below Fovant; in very compact stone,
like mountain limestone. Between Dallard’s Farm and Catherine Ford: with
Cyclas. Teffont: with Cyclas media, and C. membranacea.
Paludina elongata. Between Ham-cross and Chicksgrove: with Cyclas media and
Cypris Valdensis.
a minute species; as at Combe-wood, Oxfordshire. Stone-pit south of
Ridge.
P
Fis. Remains of the following species of Agassiz :—
Lepidotus minor. Wadydown Tile-stone pits: some very fine specimens, like
those of the Isle of Purbeck.
Pholidophorus ornatus, 4g. Imperfect remains of a new species. Chicksgrove-
mill Quarry : In white slaty limestone, full of fragments of shells.
[ Portland Stone. ]
Ammonites biplex. ‘Tisbury: in chert; the shell chalcedony.
A——— Brodiei. Fonthill Gifford.
A——— giganteus. Vale of Wardour: in chalcedony. Chicksgrove-mill Quarry :
in gray limestone like chalk. Same place: in stone coated with rhomboidal car-
bonate of lime. Tisbury: in chert; the shell chalcedony.
Astrea Tisburiensis (Madrepora Tisburiensis of Miss Benett). In dark chalcedonic
chert: a concretional bed subordinate to the Portland stone, near Tisbury.
Astarte cuneata. Chicksgrove-mill Quarry. Chilmark Quarry. Tisbury: with
Cerithium ? excavatum.
Buccinum naticoide. Pl. XXIII. fig. 4. Vale of Wardour.
Cardium dissimile. Vale of Wardour. From the lane above Berston: with Trigonia
gibbosa. Tisbury: in white uniform chalk-like stone.
Cerithium? excavatum (olim Turritella). Vale of Wardour. ‘Tisbury: with Astarte
cuneata and Trigonia gibbosa. Ladydown.
Cancer? or Astacus?. Claw, with Trigonia gibbosa. In slaty limestone. Lane above
Benston.
Cytherea? rugosa. Pl. XXII. fig. 13. Chicksgrove-mill Quarry.
Echinus. ‘Tisbury.
Dr. Frrron on the Strata below the Chalk. 261
Exogyra (new). Vale of Wardour. Portland-stone?
Lucina Portlandica. Pl. XXII. fig.12. Luawn Quarry: in sandy Portland stone.
Modiola. Vale of Wardour: in compact sandy Portland stone, Bevis’s Quarry near
Tisbury ; with Ostrea, Serpula, and palate bones of fish.
Mytilus. Ashley Wood, near Fonthill Gifford: in compact Portland rock.
Natica elegans. Pl. XXIII. fig. 3. Miss Bennett's collection. Vale of Wardour.
Nerita sinuosa. Chilmark Quarry and Tisbury.
Ostrea expansa. Vale of Wardour; Chicksgrove-mill Quarry; in white chalk-like
stone.
O— falcata. Pl. XXIII. fig. 1. Chicksgrove-mill Quarry :—Top of the Portland.
O— undulata. Vale of Wardour: in white chalk-like stone.
Pecten lamellosus. Vale of Wardour. Chicksgrove-mill Quarry. Shaver’s Bridge,
Tisbury Parish: with Ostrea, very young. Fonthill. Lawn Quarry; with
Lucina Portlandica, in sandy Portland stone.
Serpula. Bevis’s Quarry, near Tisbury: with Modiola, and pileie panes of fish ;
in compact sandy Portland stone.
Terebra Portlandica. Pl. XXIII. fig.6. Tisbury: casts of interior, not effervescent.
Trigonia gibbosa. Vale of Wardour: Castleditches; with a minute Turbo. A lane
above Benston, near Chicksgrove ; with Cardium dissimile, crab’s claws, and an
Ostrea, in white chalk-like limestone. Chicksgrove-mill Quarry. Teffont. Tis-
bury. Fonthill Gifford: in chalcedony.
T incurva. (Miss Benett.) Vale of Wardour.
Turbo(minute.) Castleditches: with Trigonia gibbosa.
Turritella excavata. (See Cerithium.)
Fish, part ofa palate. Tisbury.
[Portland Sand (or Kimmeridge Clay ?).|
Ammonites biplex. Chicksgrove Mill: in sandy clay at the bottom of the quarry.
A—_ Cast. Brickyard near Shaftesbury.
Panopea depressa. (Mya, Min. Con.). Pl. XXIII. fig. 9. Near Shaftesbury : in clay.
Some specimens very large.
NorrH WittTsHiRre.
(139.) Devizes, Calne—My knowledge of the country from the Vale of
Wardour to the vicinity of Calne is due to my friend Mr. Lonsdale, with
whom I had the pleasure of going over a part of it, in the year 1827.
Mr. Lonsdale himself has since published a very important paper on the
oolitic district of Bath, which is accompanied by sections, three of which in-
clude the strata under consideration in this paper*; and he has been so kind
* Geol. Trans., 2nd Series, vol. iii. p. 243, Plate XXXII. The course of these sections is ex-
pressed in the Map, Plate IX., by the dotted lines adjacent to No. 15. and 16.
262 Dr. Firton on the Strata below the Chalk.
as to furnish me with two additional sections, Nos. 15. and 16. (Plate X. a.)
which may be considered as supplementary to those above mentioned ; the
first, No. 15., running east and west, from Etchilhampton Hill south-east of
Devizes, to the Kimmeridge clay beneath the green-sand which caps the
heights of Poulshot Green: the second, No. 16., from the lower chalk at
Beacon Down, through Sandridge Hill, which is capped with the Lower
green-sand over Kimmeridge clay and Oxford oolite, to the Oxford clay
around Melksham, where the canal is about 154 feet above the sea*. The
sections themselves sufficiently explain the general relations of the strata ;
and for an account of their composition I refer to Mr. Lonsdale’s paper;
regretting only that his colouring of the Ordnance Maps of that part of
England still remains unpublished.
The town of Devizes stands upon a platform of the Upper green-sand, which is there about
430 feet t above the sea, and is overlooked by the chalk of Etchilhampton Hill and the
adjacent heights. And here, as throughout the tract from hence to Swindon, the contrast be-
tween the upper and lower chalk is very remarkable, both in external features and agricultural
character.
The ground near Westbury rises with such rapidity, that the distance between the outcrop of
the upper chalk and of the Upper green-sand is less than a mile; and on the north-east of that
town the slope is still more rapid. But, thence towards the north and east, a great superficial
extent of the lower beds is exposed in the Vale of Pewsey, which consists of the Upper green-
sand surmounted by detached portions of the chalk-marl and lower chalk, the latter, in some
cases, rising into summits of considerable elevation.
The outcrop of the Upper green-sand and Gault has, in general, though irregularly, a northern
direction, from about Great Cheverell, through Pottern,—to Heddington, about three miles north
of Devizes. On the south of the Vale of Pewsey, the Lower chalk is disclosed by denudation, on
a line almost due east from Easton Hill,—through St. Ann’s Hill, Milk Hill, Golden Ball, Hewish,
Martensell, and Terrace Hills; and thence westward through Easton, Milson, Pewsey field, Up-
avon, Cleeve Hill, and the slope thence towards Urchfont, and southward to the upper part of
West Lavington. ‘The outcrop of the Upper chalk, after forming a bold escarpment, between
Westbury and Cheverell Hill, is thrown back towards the east, forming the heights, along which
the Ridgeway is conducted, between Gincross by Bushton Down to Wivelsford. The Ridgeway,
which runs on the verge of the ridge bounding the wide tract of Blackheath, is first directed
* This and’some other heights mentioned hereafter, are derived from Bradshaw’s map of the
canals of England, and are counted from low-water mark at Liverpool. (See Appendix C.)
+ 429 feet 6 inches above low-water at Liverpool. At this level the Kennet and Avon canal is
continued in a direction nearly parallel to the heights of chalk, as far east as the vicinity of
Wooton Rivers, where it rises to 462 feet 6 inches (the summit level) to surmount a narrow neck
of elevated ground on the north of Burbage :—and thereabouts the streams divide; one group
running west, throug Pewsey, to join the Avon near Upavon; the other north-eastward, along
a valley descending rapidly from north to south, through Great and Little Bedwin; and thence
through Salisbury to the sea at Christchurch,
Dr. Firron on the Strata below the Chalk. 263
to the east of north, between Gore Cross and Bushton Down, but turns suddenly eastward im-
mediately on the south of Urchfont. On the east of the Avon, the range of the upper chalk is
less distinct ; but it is directed towards the parting of the streams on the south of Burbage.
The difference between the upper and the lower chalk is very well expressed in the Ordnance
Maps, especially in the more recent sheets, which are engraved with more lightness and deli-
cacy of expression than some of their precursors. The great natural district of Salisbury
Plain, more than twenty-five miles in extent from west to east, and twelve miles from north to
south, though diversified by numerous irregularities, is almost wholly destitute of streamlets ;
and would be without running water, but for the presence of the more considerable rivers, which,
in many cases, do no more traverse the surface of this region, the greater part of their supplies
being derived from a different soil, and remote situation. This point of structure is known to
be so characteristic of the Upper chalk, both in England and France, that good maps alone,—such
as that of the Ordnance, or even of Cassini’s map of France, would be sufiicient to indicate the
space occupied by this stratum. In the tracts, on the contrary, occupied by the Lower chalk—
and still more decisively in the Chalk marl, few, even of the smaller valleys, are without streams;
and hence, as well as from the difference in soil, the vegetation also is different, and the fertility
of the lower regions forcibly contrasted with the naked and barren aspect of the higher downs.
Were it not that the colour is so nearly alike, these two groups would no doubt have been
distinguished in geological maps by different hues; and they ought to be so, wherever the scale
is sufficient to express the distinctive features above mentioned.
(140.) Vale of Pewsey.—The general structure of this tract is fully de-
scribed in the excellent paper of Dr. Buckland to which I have already re-
ferred. It is, in fact, a valley of elevation: its eastern and narrower portion
being a continuation of the anticlinal ridge, which Dr. Buckland has described
as extending from the south-east of Inkpen in Berkshire to the west of Shal-
bourne and Ham; where the Upper green-sand has been brought to the sur-
face by subterraneous force, but is separated by a sort of bridge of the Lower
chalk, about Burbage, from the portion of the former stratum which has been
elevated in the same manner within the Vale of Pewsey itself. At the open-
ing of the Vale, however, between Great Cheverell, Urchfont, and Devizes,
no derangement is apparent, though it is very probable that the surface is
disjointed by less perceptible fissures ;—the Lower green-sand, continuously,
occupying the whole of the entrance of the vale; as is expressed on the map,
and more distinctly shown in fig. 4. of Mr. Lonsdale’s sections. It will be
observed that the beds immediately below the chalk are here more fully de-
veloped than in the Vale of Wardour, the Lower green-sand being’ per-
fectly distinguishable; as might have been expected, from the proximity of
this place to the great expanse of that stratum in Surrey and Hampshire :
and these subdivisions continue to be distinct through the nerthern counties
as far as the coast of Norfolk. The small number of fossils which I could
obtain, in addition to those enumerated in Mr. Lonsdale’s paper*, are men-
* Geol. Trans., 2nd Series, vol. iii. p. 266, &c.
VOL. IV.—SECOND SERIES. 2M
264 Dr. Firron on the Strata below the Chall.
tioned in the list subjoined. One of the most remarkable is the Diceras
Lonsdalu, P\. XIII. fig. 4, for some very fine casts of which I am indebted
to Mr. Goodhall.
No trace of any member of the Wealden group, nor of the Portland series,
has yet been observed in this quarter; and it will be seen from the Section,
No. 16., that the Kimmeridge clay and Oxford oolite thin out rapidly in
rising oii de the west at Sandridge Hill.
(141.) Swindon.—I am indebted also to Mr. Lonsdale for my fe infor-
mation as to the existence of the Portland stone and sand at this place,—and
the occurrence there of large nodular masses of stone identical with those of
Shotover in Oxfordshire, and of the French coast near Boulogne. The Section,
Pl. X.a., No.17., explains the succession and general relations of these strata.
It will be remarked, that the Lower green-sand is distinguished from the
Upper by the interposition of the Gault*: but though the Portland stone
forms one of the most prominent features of this Section, no trace either of
the Weald-clay or the Hastings-sands has yet been observed above it, and
the indications of the Purbeck strata are inconsiderable.
Chalk.—The remarks above stated on the contrast between the spaces occupied by the Upper
and the Lower chalk, apply with even greater force to the tract between Calne and Swindon,—or
more properly between Cherhill and Liddington,—than to Salisbury Plain. The heights from
Hackpen to Barbury Hill, that of Liddington Castle, and the high range thence to Polton Down,
forming prominences above the lower chalk on the west and north-west, and bounding an extensive
district, distinguished by the absence of streamlets and other characters from the more fertile
regions of the lower chalk and chalk marl.
Between Barbury and Liddington Castle, the Upper chalk retires to the south and east towards
Ogbourn St. George, so as to form a sort of amphitheatre. ‘The outline of the higher summits
when seen from sufficient distance, is in many cases almost rectilinear and horizontal; of which
the ridge between Ogbourn St. George and Ogbourn St. Andrew affords a good example.
The Lower chalk forms a lower and uniform escarpment from Compton Basset on the east of
Calne to the village of Liddington, and thence northward nearly to Little Hinton and Bishop-
stone. From the lower beds at Liddington a copious spring breaks out, in a position analogous to
that of Lydden-spout on the coast near Folkstone (8.), and of the range of springs which every-
where appears at the foot of the chalk downs (70.)
Enormous masses of siliceous grit (Grey wethers), like those which occur in profusion near
Marlborough, and in several places over the great chalk district on the south of that place, are
sometimes found here beyond the chalk escarpment. One of these, about 12 feet by 8 in its
diaineters, was about a mile from the chalk-hill at Burdrop Wood ; and with these, in some instances,
are masses of siliceous conglomerate,—the Hertfordshire pudding-stone.
* In the first edition of Mr. Greenough’s map, the spaces assigned to the Chalk and Green-
sands here, are erroneous : the boundary of the latter on the north-west being really that of the
lower chalk ; and that of tle Chalk, as expressed in the map, being truly the limit of the upper
chalk only.
Dr. Firron on the Strata below the Chalk. 265
The Upper green-sand, from Wroughton to Warborough, includes dark-coloured siliciferous
stone, containing mica and green particles. The formation occupies a slightly prominent step
beneath the sloping escarpment of the lowest chalk. Its thickness is probably between 30 and 50
feet (see the Section, Pl. X. a., No. 17.) ; and it may be traced throughout a space of very irre-
gular outline from the road at Burdrop Wood to Liddington.
Gault.—Bluish clay, of a smooth plastic texture, with numerous specks of mica, succeeds the
Jast formation, and occurs at considerable heights in the sloping face of the escarpments. It can
be recognised in the lower ground, on the roadsides, from Swindon to Burdrop Park, and to
Liddington ; but does not here form so distinct a valley or depression, as in Kent and Sussex.
- Lower green-sand.—This, though perfectly distinct, can scarcely be said to form a ridge, as in
‘the south-eastern counties, after rising from beneath the gault. It does, however, occupy a
slight wave or inequality of the surface, about midway between Liddington and Coate (see the
Section, P]. X. a. No. 17.); and then suddenly thinning off, caps the heights at the latter place
and at Swindon. The sand at the upper part is very tough, either from the presence of clay,
or a great abundance of oxide of iron. In some other places it is loose and white ; and among
the substances found within its range is Fuller’s-earth.
This ferruginous sand, as it approaches Swindon, rests, in several places immediately upon
another sand of a very different character, at the top of the Portland series, and the junction is
deserving of notice, the surface of the latter sand being very irregular, as if from erosion by
water, and the inequalities or prominences often of such tenuity, as to indicate a very tranquil
condition of the fluid beneath which they were formed, as well as of that which deposited the
ferruginous mass by which they are at present enveloped :—which is the more remarkable, when it
is considered that the interval between the deposition of these two sands must have been, in point
of time, sufficient for the accumulation of the whole of the Wealden group.
In one of the quarries, near the top of Swindon Hill, the Section was thus. The boundary
/ We ; ;
TW SG WAGES ANY Wi A q {
0. WG ASUS ARES PEN DANN Ss ss Wah)
Z Z MLL Lh WLLL:
i
i ‘ Sito j Ferruginous Sand.
®* ..9u » oa
ps s Eye Be *syiat (Lower Green-sand.)
“S| ae
%,
itd
J
3.
4. Whitish calciferous
Sand; with concre-
tions in which arePort-
2D.
between the two kinds of sand being perfectly distinct and sharp; and the contrast was the more
striking, from the lower being composed, in a great measure, of minute fragments of shells, which
are wholly wanting in the incumbent matter *.
* In Mr. William Smith’s Geological County Maps of Kent, Sussex, Wilts, Oxfordshire,
Bucks, Berkshire, and Bedfordshire, the stratum now known as the Lower green-sand is de-
scribed as ‘‘ Sand, in the lower part of which the Portland stone is found.” ‘To understand the
source of this error, it must be recollected that at the period of those publications, the existence
2m 2
266 Dr. Firron on the Strata below the Chalk.
Purbeck strata.—The only indication of this member of the Wealden which I found at
Swindon, were detached masses of botryoidal limestone, like the middle of the ‘‘ Cap”, in Port-
land (p. 222.), and fragments of dark brownish silicified wood,—fallen, I have no doubt, from the
top of the quarries, though supposed by the workmen to occur amidst the stone itself. In the
looser matter also, near the top of the quarries and above beds of the Portland stone, are masses
including very numerous casts of marine shells (apparently Lucina and Cytherea), in which the
cementing substance has the aspect of freshwater limestone, and is scarcely to be distinguished
from a stone of the same yellowish hue, within the Purbeck series near Ridge in the Vale of
Wardour ;—but in the latter the casts are those of freshwater species, especially Cyclades. In
the subjoined sectional list, it will be found that clay occurs in detached portions above the Port-
land stone, in the great quarry at Swindon; but I was not enabled to determine the formation to
which it ought to be referred.
Portland stone.—The upper part of this formation at Dayhouse farm, east of the Reservoir, and
at Broom farm on the west of that place (Section No. 17.), abounds in the characteristic fossils,
and isimmediately subjacent to ferruginous sand. In many of the quarries here, especially
in the east of the town, even the uppermost beds contain a large proportion of sand; pre-
senting, in this respect, a striking contrast with the top of the series on the south-east coast,
but much resembling that of the Lower Boulonnois, especially of the quarries at Mont Lambert.
The stone is generally dispersed throughout this sand, in rugged and irregular concretional
masses, which, as well as the sand, contain numerous obscure remains of shells, frequently in
the state of a calcareous powder.
The following is a sectional list of the strata in the great quarry on the south-west of Swindon,
which occupies a space of no less than fourteen acres; the beds rising from a point a little east
of south, at an angle between 1° and 5°*.
Section of the Great Quarry at Swindon.
Ft. In,
Le SOE oo sis. 0 ssafoiw sicip » Nina Site minal 9 « ilolele vince els) n'e/eieieie @ » ininve\eie'te nie leliate ie) ee
2. In some places, immediately below the surface is clay, occasionally 23 feet thick, with
a slight covering of ferruginous (Lower green) sand. But in several places the thick-
ness of this‘sand wasyas mulch! asia Meet <i. 2 2-1 ols os s6 «lee sleele ieee) eng tenn
S., Loose rubbly stone \ iiee-9 5, siwi6inisw sole v,S)eiw) eh aioe sleye oe «6.0 eis. 'e iwlersis Bini ete een
4, A group, as follows :
a. Limestone full of petrifactions. Cardium dissimile; Cytherea? rugosa, P\.XXII.
fig.13.; Gastrochena?; Lucina Portlandica, P|. XXII. fig. 12.; Perna quadrata ;
Pleurotomaria; Terebra Portlandica, P\. XXIII. fig. 6.; Trigonia gibbosa; T. in-
curva; locehonsofStime oe 5 8
b. Bluish grey HMmeStONe . cones fe s0d th ne sasdene ones oa
d. Soft limestone, abounding in casts of shells .2:25 </si.% s\o:01 «10 ee = piel sie
of the Wealden group was unknown; and that in point of fact, the Portland stone is found in many
parts of the counties above mentioned, at the bottom of the Lower green-sand, and in a group
which is itself in part composed of sand :—so that where the latter sand is not well distinguished,
as in the section represented in the woodcut on the last page, the whole might easily be mistaken for
one continuous stratum. What is stated above, explains, I believe, the true relations of these
sands, to each other and to the Portland stone.
* A mill on the north of the hill was deprived of water in consequence of the springs which
appear at the junction of the Portland sand with the clay, having been opened on the south-west
side of it,—so as to tap, as it were, the summit, and draw off the whole of the water; the reten-
tive surface of the clay being inclined towards the south. This fact proves also the continuity of
the beds which form the top of the hill, and the absence of fissures—of such depth, at least,
as to penetrate the clay.
Dr. Firron on the Strata below the Chall, 267
Ft. In,
5, Alternate ranges of sand and stone.
a. Sand, in many places cream-coloured, abounding in fragments of shells, which
decompose into a white powder. This includes [bean Tope Cor ee
b. Stone, resembling that of the Portland formation in the Isle of Purbeck, evidently
nothing more than sand consolidated by calcareous matter. ‘The masses, when +20 0
discrete, are of very irregular figure. The stone becomes more abundant in
descending; and near the bottom contains very large Ammonites, 4. biplea, J
Mio taltercteetets, Ae. ah etre pyethns altace 30 0
A depth of about six feet below the bottom of this quarry is said to consist of similar sand and
stone.
Portland Sand.—The lower part of this formation is well displayed in an old quarry on the
northern brow of Swindon Hill, near the letter B of the word Bowling-green in the Ordnance
Map. The rock consists of rough sandy stone, of a dull bluish grey colour, like that of the
upper part of this formation in the Isle of Purbeck, in which are included traces of several fossils
converted into carbonate of lime ;—Ammonites biplex, Perna quadrata, Trigonia gibbosa, Trigonia
clavellata; with numerous dark particles of silicate of iron, and worn fragments of black chert or
flint, many of them evidently the remains of casts of bivalves (some having the outline of a
Venus or Lucina ?), and of Ammonites.
Another form which the Portland-sand assumes here, is that of great nodules of hard greenish
and grey calciferous grit, precisely resembling those of Shotover Hill, and of the French coast,
especially near Cape Grisnez,—and, as at those places, imbedded in grey sand: above which,
is another bed of sand without nodules, containing green particles and numerous fragments of
black chert. Mr. Lonsdale had long since mentioned to me these great masses, several of
which were then visible on the east of the road from Oxford, close to the town; but when I
visited the place, the greater part of them had been broken up and removed. Immediately
below the nodules were about four feet of grey sand.
The Portland-sand extends westward from the town of Swindon, and occupies a part of the
descent of the hill at Okus and Westleaze, where the high ground overlooks the canal. In the
farm-yard at Okus were several large nodules, like those above mentioned *.
Kimmeridge clay.—At the Bowling-green the sand with concretions appears on the surface
as the hill descends, and is succeeded abruptly by dark clay, in which I found fragments of
oyster-shells ; and this is the case also beneath the great nodules near the road from Swindon
to Oxford. Ihave no evidence of the identity of this clay with that of Kimmeridge, but the
facts here stated.
(142.) Last of Fossils from the Strata below the Chalk, in part of North
Wiltshire.
[Upper Green-sand. |
Ammonites dentatus. Rowde Hill, near Devizes.
A— varians. Near Swindon; (in the Chalk marl).
Mya mandibula. Devizes Canal.
Panopea plicata? Rowde Hill.
* Toothill,a small eminence, which is conspicuous from this place, consists of clay, as also the hill
at Eleomb-house. That of Chaddington, still further west, is said to be capped with sand.
268 Dr. Firron on the Strata below the Chalk.
Terebratula nuciformis. Rowde Hill.
Vermetus umbonatus. Rowde Hill.
[Lower Green-sand. |
Arca? Lockswell Heath, near Bowood: in ferruginous coarse sand-rock.
Corbula? Wockswell Heath: in ferruginous sand-rock.
Cardium striatulum? Lockswell Heath.
Cucullea. Wockswell Heath: in ferruginous sand-rock.
Diceras Lonsdalii. Pl. XIII. fig. 4.a.—d. Near Calne. Mr. Goodhall.
Modiola. Wockswell Heath.
Mytilus. Wockswell Heath.
Pecten obliquus. ockswell Heath: in ferruginous sand-rock.
P
Plagiostoma rigidum. ockswell Heath.
Terebratula latissima. Lockswell Heath: in ferruginous sand-rock.
T: — nuciformis. Lockswell Heath: in ferruginous sand-rock.
T—— oblonga. Lockswell Heath.
Thetis minor. Lockswell Heath: in ferruginous sand-rock.
Trigonia gibbosa? Lockswell Heath.
Turbo moniliformis. Lockswell Heath: in ferruginous sand-rock.
Venus? lLockswell Heath.
quinquecostatus. Lockswell Heath.
(Portland Oolite. |
Ammonites biplex. Swindon.
A——— giganteus. Swindon.
Buccinum angulatum. Swindon. Pl. XXIIT. f. 5.
B naticoide. Swindon. PI. XXIII. fig. 4.
Cardium dissimile. Swindon.
Cytherea rugosa. Pl. XXII. f.13. Swindon. The predominant shell in the upper
bed of the great quarry.
Gastrochena. Swindon.
Fiucina Portlandica. Pl. XXII. f.12. Swindon: in stone very like freshwater
limestone; full of moulds and casts of this shell.
Nerita angulata. Pl. XXIII. f.2. Swindon.
Ostrea falcata. Pl. XXIII. fig.1. Swindon.
ecten. Swindon: in stone, very like the Forest Marble.
Perna quadrata. Swindon.
Terebra Portlandica. Pl. XXIII. f.6. Swindon. In great profusion, in the stone of
the great quarry. Some specimens stained with oxide of iron; with Lucina.
The impressions of the interior sometimes beautifully preserved.
Trigonia incurva. (Miss Benett.) Pl. XXII. f. 14. Swindon. Tuberculated ridges.
TD. gibbosa. Swindon.
Trochus? Swindon.
Dr. Firron on the Strata below the Chalk. 269
Woop. Silicified specimens of coniferous wood, in fragments, the cavities of which
are lined with minute crystals of quartz, are found in the debris of the great
quarry at Swindon: they are supposed by the quarrymen to have been found
within the solid stone; but there can be scarcely a doubt that they have fallen
from the beds above, the place of which corresponds to that of the group which
affords the silicified trunks in Portland.
[Portland Sand. |
Ammonites biplex. Swindon.
Ostrea (deeply concave). Swindon.
Pecten. Swindon.
Perna quadrata. Swindon: with Mya?
Pullastra. Swindon.
Trigonia clavellata. Swindon: in bluish sandy clay; with pebbles of black flint or
Lydian stone.
gibbosa. Casts in dark flint, with Pecten or Lucina?
T
Bone. Portions of a long bone of a Saurian.
[Kimmeridge Clay. |
Ammonites. Near Steeple Ashton: in slaty lignite, like the Kimmeridge “Coal’’,
Berxsyire, Oxrorpsarre, BockincuamsHire, BevrorDsHIRE.
(143.) The tract between Calne and Bedfordshire derives its exterior cha-
racter in a great measure from the very slight inclination of the strata, which
in their progress towards the north-west from the anticlinal line of the Vale
of Wardour, are comparatively undisturbed: no conspicuous faults, at least,
have hitherto been detected between South Wiltshire and the northern coast
of Norfolk, though it is probable that this region is not more exempt from
slight disturbances, than the greater part even of the more uniform tracts in
England is found to be, when examined with sufficient attention. One effect
of this very gradual rise of the strata is, that some of the beds, shooting
out successively to great distances, have been the subject of extensive de-
nudation ; so that outliers occur in several places at the distance of some
miles from the general line of the escarpments : and on the confines of Berks
and Oxfordshire a large tract, entirely denuded of chalk, appears, along the
course of the Thames between Abingdon and Reading, breaking in upon
the almost uniform and linear course which the outcrop of that formation
would otherwise have followed from Calne to the fens of Cambridgeshire.
It is not improbable that this wide denudation, and the course of the Thames
270 Dr. Fitton on the Strata below the Chalk.
itself, may have originated in a preexisting fissure, by which the direction
of the principal stream may have been determined, and the effect of the
denuding waters subsequently modified.
My observations were resumed, on the north of Swindon, in the tract
around Hazeley and Garsington ; and the country thence through the con-
tiguous counties of Oxfordshire, Bucks, and Bedfordshire, as far as Wo-
burn, is so much alike in geological structure and composition, that the
whole may with advantage be considered together. I shall therefore first
state generally the order and composition of the strata, and then illustrate
the sections Pl. X. a., Nos. 18, 19, 20, and 21, with some details derived
from points where the beds are best exhibited. The recent sheets of the
Ordnance survey, Nos. 13, 45, and 46, are so well executed as to furnish all
the assistance that can be desired in the examination of this part of England:
and their aid will be almost necessary in perusing these remarks *.
Chalk.—The most striking feature in the outline of the chalk, north-east of Swindon, is the
sudden retreat of the Downs above referred to; by which the escarpment is thrown back towards
the south between Woolstone, on the west of Wantage, and Watlington, not less than eight miles.
The subsequent direction of the outcrop is nearly parallel to that of Marlborough Downs, and
through its whole course thence into Norfolk, the lower chalk and chalk-marl run out far
beyond the escarpment of the upper strata, which, near Nuffield, on the main road from London
to Oxford, through Nettlebed and Abington, is more than two miles from that of the chalk-
marl at Gould’s Heath. On the lines through Stoke Talmage and Tetsworth, the distance is
nearly four miles; and the space varies between one and four miles all along the range, thence
to the north-east of Dunstable, becoming still more considerable in the lower tracts of the
east of Bedfordshire and Cambridgeshire, where the beds are less inclined.
The angle at which the strata in this part of England rise, in general towards the west of
north, in many cases does not exceed 1° or 2°; and the contiguous beds are frequently so mixed
at their junction, as to render it very difficult to define them. An additional source of obscurity
occurs between Aylesbury and the road from Dunstable into Bedfordshire; where large accumu-
lations of superficial gravel (comparatively recent, since it includes fragments of chalk,) mask
the substrata, or totally conceal them. A remarkable deposit of the same kind in the south and
south-west of Oxford, is mentioned by Mr. Conybeare}; and Dr. Buckland has made the trans-
ported matter of the Valley of the Thames, the subject of a paper in these Transactions, in which
his views of the Theory of its production are fully explained.
Upper green-sand.—This formation is not generally so prominent in this tract, as in the coun-
ties near the coast; but its representative is found along the base of the chalk marl in all the
places which I myself examined. Thus, on the line of the Abington road to Oxford, it appears
on the descent from Gould’s Heath towards Bensington ; and firestone, I was informed, is obtained
* The authorities connected with this tract are, the general maps of Mr. Smith and Mr.
Greenough, and the Sections and County Maps of the former. The only published description
of the strata is that of Mr. Conybeare in the ‘‘ Outlines of England and Wales”, p. 170.—183,
from which I have throughout derived most valuable assistance.
‘+ Outlines, &c. p. 190. { Geol. Trans., 1st Series, vol. v. p. 516—544,
Dr. Firton on the Strata below the Chalk. 971
by mining in the lower ground on the north-east of that place, between Rumbold Copse and
Whitehouse Farm. The formation is much less distinct at Tetsworth, but is obvious on the south
of that village; in the descent of the hill from Chinnor towards Emington; and beneath the lower
Icknield-way, at Chadwell Hill on the north-west of Risborough; at North Lee, between Tur-
wick and Bishopstone; and probably in the vicinity of Aston-Clinton. On the north of Tot-
ternhoe, great quantities of a soft variety of firestone were formerly obtained from mines of
ancient date deeply seated at the foot of the lower-chalk escarpment, between the village and
the hill on which is the mound of ancient encampment, called Maiden’s Bower. In this latter
direction, also, an outlying portion of the Upper green-sand is visible, on the road between Kate’s
Hill and the Turnpike near the beginning of Hockliffe, forming the base of an outlier, or penin-
sular portion of chalk, which shoots off from the main body about Chalton, and bears upon it
the village of Wingfield ;—not improbably crossing the road and forming part of a flat-topped
range of heights, which extends westward on the north of Tilsworth and Stanbridge.
Gault.—The gault in this part of the country is very irregularly diffused, in many places forming
a distinct valley or depression beneath the Upper green-sand, in others spreading itself towards
the west, and thinning off gradually over the top of the Lower green-sand.
Lower green-sand.—This formation, which is indistinctly seen in the lower ground, is best
observable near the summit of the heights between Garsington and Shotover on the south-west of
Oxford (No. 18.),—and of the corresponding ranges, from Long Crendon to Brill (No. 19.), and
from Quainton to Whitchurch, on the north-west of Aylesbury (No. 20. & X. b. fig. 11.) Thence
towards Leighton Buzzard, the Lower green-sand is more obscurely seen: but it becomes con-
spicuous in approaching Woburn, and is found in immediate apposition with the Kimmeridge
clay, at Little Brick Hill (No. 21’.), where the whole of the intermediate strata, from the
Wealden to the Portland sand, are wanting,—having been either originally deficient, or partially
carried away before the deposition of the sand.
The greatest extent of continuous surface which this formation occupies here, is between
Leighton* and the west of Woburn. But there can be little doubt that it once extended con-
tinuously from its rise beneath the gault to its final outcrop in the heights above mentioned ;
the greater part having been subsequently removed by denudation.
On the main road from Tetsworth to Wheatley, Section No. 18!., a portion of the gault and
of this sand still remains between the 44th and 47th milestones ; while on the south-west of the
road, a great part of these strata having been removed, the surface is so much lowered as to
disclose the subjacent Portland stone, throughout a space which includes the villages of Great
and Little Milton and Great Hazeley.
Several outliers of the Lower green-sand in this part of England still remain to be examined;
among which the heights near Faringdon seem to be especially deserving of notice. Another
detached portion (which, if the chalk range had been unbroken by the chasm of the Thames,
would have been nearly at the same distance from the escarpment as that of Faringdon), caps the
hills at Bagley Wood and Cumnor, on the south and south-west of Oxford. These have been
generally described by Mr. Conybeare (Outlines, p. 190.), who states that the Portland beds do
not extend so far: but as the relations of the Wealden group were unknown at the time of his
* A large tract around Leighton, including Wing, Cublington, Aston Abbots, Mentmore, &c.,
has not yet been described geologically. The late Mr. Bevan of Leighton was thoroughly
acquainted with it; and I am not without hope that some of his observations may be published
by his son.
VOL. IV.—SECOND SERIES. 2N
272 Dr. Firron on the Strata below the Chalk.
publication, it may perhaps deserve inquiry, whether some portions of it may not exist beneath
the sands in that quarter.
Wealden.—The traces of the upper members of the Wealden, are here so rare and indistinct,
that nothing has yet come within my knowledge which can be referred to them, except on the
summit of Shotover Hill, where shells, supposed to be of freshwater species, are found above
the Portland strata, in a ferruginous sand or clay ;“and at Quainton and some other places in
Buckinghamshire, where grit like that of Hastings, contains Paludine.
The lowest of the Purbeck strata are here fully characterized by their fossils, and precisely
resemble the lower beds of this formation in the Vale of Wardour and on the Dorsetshire
coast. They consist of slaty limestone, like the “ tilestone” of Ladydown in the Vale of War-
dour, and the “Slate” of the Sections in the Isles of Portland and Purbeck. With this stone,
beds of clay alternate, which become more frequent in approaching the Portland strata, and
clearly represent the “ Dirt-beds” of that island and the adjacent coast. One of the lowest of
these clays, contains thin layers of a species of Mytilus (7. Lyell?) which is found in several
detached points of the tract now under consideration. I did not, however, find in any of these
beds either silicified trunks of trees, or of the remains of Cycadez ; but in the corresponding
place at Garsington in Oxfordshire, were detached fragments of silicified coniferous wood, like
that of Portland. In several cases the more uniform freshwater limestone in this lower part of
the Purbeck series is “ Travertine”; and like the ‘‘ Cap” of Portland it includes cavities incrusted
with botryoidal carbonate of lime.
The fossils which this formation affords here, as in the Vale of Wardour, are Cypris and Cyclas
in profusion, and of two or more species; Mytilus and Modiola; with, more rarely, Astarte
and Paludina of two or three species, and some minute spiral univalves.
The Portland strata have been found in this part of England, throughout a tract between six
and ten miles in extent from south-west to north-east, on the line of its rise from beneath the
superior strata, (Pease Farm, near Great Hazeley, in Oxfordshire, to Bierton near Aylesbury,
Bucks),—and about five-and-twenty miles, on the course of its outcrop, (from Garsington in Ox-
fordshire to near Stewkley, Bucks). They, no doubt, constituted at one time a continuous group,
but having been cut through by irregular denudation, now exist principally in the upper part
of the detached heights, which are separated by low ground excavated in the Kimmeridge
clay.
The Portland-stone makes its first appearance north of Swindon, on a line directed from
about south-east to north-west, through Easington, south of Little Milton and Garsington,
towards Oxford. On the south of that line no stone is found ; the villages of Chalgrove, Ascot,
Stadhampton, and Chiselhampton being supplied with it from the Milton pits. Among the points
where I have seen the Portland beds near their first rise from beneath the superior strata, are—
a spot near the brook between Peg’s Farm and Standhill, on the south-east of Great Hazeley
(Section No. 18.) ; near Cotmore Walls, about a mile west of Thame (No. 19.); near the windmill
at Towersey, Bucks; east of Kingsey ; Haddenham Field, about half a mile west of the church;
about midway between Ford and Moreton’s Farm; near Bishopstone; Pistol Hill,—the vicinity
of Walton, and of Broughton, near Aylesbury; and the summit of the heights at Bierton.
Beyond this last-mentioned place, I could not learn that stone has yet been discovered; though,
as it occurs at Church Farm on the road from Wing to Cublington, it may probably be found
to rise between the chalk, at Ivinghoe and Totternhoe, and Wing. ‘The Portland sand has been
quarried between Tinkershole and Stewkley, and about a mile north of Dunton; and the out-
Dr. Firron on the Strata below the Chalk. 273
crop of the stone and sand, can be traced along a very irregular line, from the heights at Gar-
sington and Shotover, by Brill and Muswell Hills, Ashendon, Waddesdon, Quainton, and Whit-
church, to the points last mentioned, near Stewkley, which seem to be their limit in this direction.
The Portland-sand goes out beyond the stone, on the north and north-west sides of the heights
just mentioned. The sand is in some places loose, grey, and yellowish; but in general it abounds
in green particles, and is often almost wholly composed of green matter: the bluish half-concreted
mass, intermediate between stone and sandy clay, which is the predominating component of this
stratum on the coast, being here of rare oceurrence*. Near the bottom, the sand includes
great nodular concretions of hard greenish grit, like those of Swindon, Shotover, and the Lower
Boulonnois; and it contains sometimes worn, polished, fragments of very dark-coloured chert or
flinty slate.
The Portland stone and sand are found between the principal ranges of Brill and Whitchurch,
(Sections 19. and 20.), and nearly at the same level, in the heights of Ashendon, Lodge Hill,
Chearsley, Over-Winchendon, Coney Hill, Cuddington, Dinton, Stone, and Hartwell. But on the
north-east of the road from Aylesbury to Winslow they are rarely visible, being deeply seated,
and concealed, especially in the vicinity of Leighton Buzzard, by large accumulations of gravel.
The intermediate and lower tracts between the lines of section and the heights above men-
tioned appear to be occupied by clay, and the whole district is in general undisturbed; no
derangements at least, at all comparable to those of the Wealden tract, or of the Dorsetshire
coast having yet been observed within it: but in many of the Portland quarries the beds of stone
are traversed by fissures, produced by violence long antecedent to the present condition of the
surface. An elevation comparatively inconsiderable, but analogous to that which has raised
the anticlinal ridges of the south, occurs at Wheatley, between the range of Shotover and that
of Brill,—both of which are capped by nearly conformable strata of Portland sand and stone,
rising gradually to the north-west; while the beds of the Oxford oolite, which appear in the
village of Wheatley, on the main road from London to Oxford, rise more rapidly northward,
from beneath the stone and sands of Garsington and Combe Wood. (See and compare the Sec-
tions, Pl, X.a. No. 18. and 18’, and Pl. X.b. fig. 10.) A small portion, therefore, of the space
between the heights of Shotover and of Brill may be occupied by an anticlinal ridge, or curve,
of Oxford oolite.
Kimmeridge Clay.—This is found everywhere, in these sections, beneath the Portland sand; and
is conformable to the superior strata. It is best seen on the west of Shotover Hill, where the
series of the strata is complete ; but near Leighton it seems to come nearer to the Lower green-
sand; and in the descent from the village of Little Brickhill, (Section No.20.) it appears within
a few feet of the sand, which forms the upper part of the hills there.
The whole of this stratum is disclosed, on the line of Section No. 18, at Headington; and its
characters there are described by Mr. Conybearet. It seems to increase in bulk in advancing
northwards, but does not anywhere attain the thickness which it exhibits near Weymouth, in the
Boulonnois, and near Scarborough. Its predominant fossil here is Ostrea deltoidea: near Ayles-
bury are found Gryphcea virgula, and Aptychus.
Professor Sedgwick has remarked that on the south-east coast near Weymouth, sone of the same
fossils pervade this clay, the mixed beds near Weymouth, and the oolite beneath them; and it
* Bluish stone, somewhat like that of the sands in Purbeck and Portland, is found near the top
of this formation, at Hartwell near Aylesbury.
t Outlines, &c. p. 185,
2n2
Qi4 Dr. Firron on the Strata below the Chalk.
graduates upwards also into the Portland sands. He supposes, therefore, that certain beds of
the series are wanting between the freestone of the Headington quarries and the incumbent
Kimmeridge clay ; an inference confirmed by the condition of the surface of the freestone,—
which Mr. Conybeare describes as exhibiting the appearance of having been marked by the
action of water upon it, before the deposition of the clay ; ‘ presenting occasionally small cup-
‘¢ shaped cavities, and perpendicular rents of various breadth, into which the clay had insinuated
“ itself*.” It is not, however, improbable that some of the intermediate strata exist on the line
of section from Garsington to Langcombe. See hereafter, p. 278.
Ozford Oolite (Coral Rag of Smith).—The characters of this group have been described by
Mr. Conybeare. Its general course is nearly conformable to that of the upper strata, and is
represented in Mr. Smith’s and Mr. Greenough’s maps. On the east of Islip a narrow inter-
rupted ridge passes north-eastward, for about nine miles from Woodeaton, as far as Stanhill near
Marsh Gibbon, and is separated from the escarpment of the Portland stone and sand at Muswell
Hill (Section No. 19.), by a uniform flat, apparently occupied by clay. Blackthorn, a place upon
the ridge, affords a bluish oolite, which Smith refers to the Coral Rag. This ridge appears to
separate the Kimmeridge from the Oxford clay ; but the continuity of the former so far westward
from Muswell Hill, where it ascends considerably, implies a thickness much greater than that
in the Headington quarries.
The regular course of the Oxford oolite is interrupted by the offset mentioned in the last page,
which extends a little eastward of its general direction to Wheatley (see the Transverse See-
tion, Pl. X. b. fig. 10.); the strata there rising towards the north, at an angle of about 9°. The
previous dip about Garsington is much less ; and that of the general range of this formation in
Oxfordshire, according to Conybeare t, not more than 1°. This upheaving seems to be continued
eastward for some miles, so as to bring up the Portland sands at a point much closer to the
chalk near Thame, than on the north-east of that place.
(144.) Section Pl. X.a. No. 18,—from the Chalk through Hazeley, Gar-
sington, and Shotover, to Oxford ;—and No. 18'. from Stokenchurch, through
Tetsworth, to Wheatley—The upper strata between the Gault and the
Portland stone on the line of Section 18, are best seen near the summit of
the range-from Combe Wood to Shotover Hill: and I am indebted to Mr.
Hugh E. Strickland, for the following account of the ferruginous sand at
that place, which I have not examined myself.
SHorover Arxxi:—{ Lower Green-sand, and Wealden. |
“* The bed which crowns the hill and rests on the supposed equivalent of the Portland stone,
“consists of a series of sands, mostly ferruginous, but frequently assuming various shades of
** yellow, white, grey, and even black, according to the proportion of oxide of iron which they
“contain. The sand occasionally graduates into marl and clay ; and seams of yellow ochre also
** occur, which afford considerable supplies of that article. The stratification of the sands and
‘‘ marls is often very tortuous and irregular, which seems rather to be owing to the circumstances
“ of their deposition, than to any subsequent action. In some cases the oxide of iron has been
* Outlines, &c., p. 189. } Ibid., p, 192.
Dr. Firton on the Strata below the Chalk. 275
“ so abundant as to concrete the sand into shapeless masses of great hardness, which occur in
* Jocal strata a few inches thick. Except in these masses of ironstone, no organic remains have
* been noticed throughout the deposit. Taken as a whole, this formation bears a great resem-
* blance to the Lower green-sand of Sussex; and the masses of ironstone are almost identical in
“ appearance with some which exist there: but the fossil shells lately found in it appear rather
* to show that it forms a part of the Wealden group. These shells occur only in the nodular
masses of ironstone, which are scattered near the old sand-pits on the west end of the hill; and
“ were first noticed there by the Rev. H. Jolly of Bath.”
[The shells here referred to by Mr. Strickland, appear to belong to five species: three of
Paludina; a small bivalve, like a Cyclas; and a larger bivalve, like a Unio. But the specimens
hitherto found are all too imperfect to admit of precise determination, and are none of them so
unlike some of the species which occur in the Lower green-sand, as absolutely to exclude them
from that formation. ]
* A small pit had been sunk in quest of ochre at the side of the old London road, about 150
“ yards to the east of the old quarry, where the large globular concretions of the Portland sand
“occur. This spot may be about 50 feet above that quarry; and the pit presented the following
** Section :—
[ Wealden? | Ft. In.
PRHOWISIN CLAY ne a.e oso olen cds encis ects o's Ba oo aeta ah Mets insalauststalaisioeeleys visterctaree. Alo
MEDIC 5 5.faaxd!s sla tal ct ncTalsieiailelale ajblaroieres/aia'clei@ielsle > sin vfelvieeeinsisinin cd stsnce O 4
See sami PUDBIy WaTl SL ee ee tielele a ncelscacsscpeieisccvgissiceslessseseces & O
[ Portland. |
4, Very hard brown sandstone, with a few Trigoniz, anda bone of a crocodile ........
1 0
“5, Rubbly stone, with numerous casts of Trigonia, the shells having decayed into a 1 0
SECT HOWL: « 5 055 10+4,'nrp ie} 4501 0p \010! oe 00:0) 450 5a apeloieie ia, 0 Djayaye ways werbie weicile 3.0 2 b,9.0m,0.0\0
SOI Totals Ai Ree he hes kislatetarel steve steers umvate 10 0
The first three beds exactly resemble the sandy strata which extend from this point to the top
“ of the hill, a height of about 50 feet, and which I am disposed to regard as belonging to the
“ Wealden group. The nodules of ironstone containing the supposed freshwater shells, occur at a
“height of about 30 feet above No. 4.”
Purbeck Strata.—What remains of the Purbeck strata in this part of the country is best seen
in the pits in the southern part of the Shotover range, at Combe Wood and Garsington. The
junction of the incumbent strata with the Portland beds, is first disclosed in the quarries at Great
Hazeley.
The section at Comzz Woop consists of,—
1. Reddish loamy soil, passing into 2.
2. Ferruginous sand (Lower green).
8. A thin bed of very tough clay (Fuller’s earth?); which, with 2, enters into, and follows the
deep erosions and irregularities at the top of 4.
4. Purbeck.—Stone, and soft rubbly matter ;—(the ‘“‘Malm” of the pits at Garsington); containing
freshwater shells, like those of that place:—Cypris; Mytilus, two species; Modiola; Paludina
elongata, and perhaps another species?; Planorbis/?. Some portions of the stone are compact
and uniform, with the usual characters of freshwater limestone ; others, though containing the
same fossils, are composed of grey and brownish, fine-grained, oolite, in which a very small
276 Dr. Frrron on the Strata below the Chalk.
univalve—perhaps a Paludina—occurs in such numbers, as in some places to form nearly
the whole mass.
5. Portland stone; with numerous Trigoniz and Perne.
Great Hazeley.—In the principal quarry at this place the strata dip to about 20° east of
south, at an angle of about 4°; and are traversed by joints nearly in the same direction. The
order is as follows :
Stone-pit at Great HazeELey.
WUHTE di er we all Ge WME ws , ny Mp veal
5.
STEN ial
15.
20.
1.. Soil, forming a level and uniform surface 2... +000 e0cncsescesccevscs se ce cle iE
2. Loam, brown and red ; containing fragments of ferruginous conglomerate, (carstone) 6 on
and ofa brown substance, like umber; passing below into ferruginous sand. . 3 ft. to
8. Thinly stratified firm clay or marl, of a light grey colour, approaching to stone, not
effervescent, containing between the folia impressions of plants, and including portions
of reddish sand, in horizontal masses of very unequal thickness. It breaks down 6 6
rapidly in water, like Fuller’s earth, and its place corresponds best (so far as my
observations went) to that stratum) feist «nla sic loinie «> = +\0\lc «01s ois! 010) ofe) oleo)=teln leita
4, Dark brown clay; like the Fuller’s earth of Tilburstow (p.139.), and of the pits near
Aylesbury. Some of the masses into which it is easily divided, are polished, by
sliding on each other under pressure. At the bottom ferruginous sand alternates
With) the Clay. are isi< tals oletelolaler= iain wleielarele aiwiclolalefolole\'e aus oiels e/einjeicleiteheielr<mialeemnty
[All the preceding beds are much disturbed, and bent irregularly, so as to ac-
commodate themselves to a chasm in the strata below,—here called a “Gull”
(gulley?), and quite analogous to those in the Isle of Portland mentioned at
p-218. The manner in which these “ gulls” are filled, proves that they must
have been excavated before the deposition of the matter which now occupies them.
But the surface of the ground above the opening shows no indication whatsoever
of disturbance. ]
The Purbeck strata seem to be wanting here?
[Portland Stone. |
5. Stone, called “Curl”; grey calcareous grit. Often blue, in the interior of the eo ¢
masses ; containing thick oysters, and Pern .......sesseeeeeceeeseees about
6. Sand and clay, containing fragments of shells, and including at the bottom concre-
tions of calciferous sandy stone, which abounds in petrifactions, especially Pema b 4 0
GUAATALAN Mei elateh ojelo lols cleveolm eielors'e eoleislelsleteve eine x (elsllolailsio'sts (o(alekeietnteretale eaten
7. Uniform whitish sand, and sandy stone, with Perna quadrata, and numerous Serpule. 2=6
[In another large quarry, 6. and 7. unite to form one bed about 7 feet thick. |
Dr. Firron on ihe, Strata below the Chalk. 277
Ft. In
8. ‘ Stone”, commonly in two beds; that for which the quarries are worked. It is like
the Purbeck-Portland, and contains disseminated spots of pyrites. The under
surface is often covered with petrifactions,—Perna, Trigonia, Venericardia, and
Trochus. Bones have been found in it, and sometimes lignite .........+.eee000. .
Bottom of the Quarry.
9. Below is sand: precise depth and relations unknown ...... Mea sin: aidiel ele ame eabout ~ 12 6
Total about.... 35 (0
The principal stone-pits at Garsington, are in the western escarpment of the hill north of the
village, overlooking the low ground about Langcomb and Cowley. One of the largest gave the
following Section :—
Stone-pit at Garstncton.—[Lower green-sand, Purbeck, and Portland.]
MUMMY SOU ow ccc e cece nec d dele valde Gi Warres Siete eter aa roe eaves) oc keenentne about 2.0
a a. Ferruginous brown sand, including portions like umber, and irregular
seams of clay, like that of the bed 3. at Great Hazeley, (Fuller’s earth?).
It contains also patches of greenish sand.
b. A band of yellow ochre, about half an inch thick.
c. A thin bed of uniform tough clay (Fuller’s earth), in wax-like pieces,
polished by motion under pressure
eeceeeree ee ee eee eee eres eeeeeen
[These, like the upper beds at Great Hazeley and Cite Wood, follow all
the irregularities of the mass below. |
3. “ Malm”; an agglomerate, composed of stone and softer marl-like matter, much de- }
composed. Among the components are,—
a. Light greenish-grey marl, like some beds of the lowest chalk; con-
taining at the upper part detached fragments of silicified coniferous
wood, like that of Portland, and portions of bone.
b. Firmer pieces of stone, with some oolitic particles, including small
spiral univalves,—Paludina, perhaps of two species? ; a Planorbis? ;
Pegcilas ; and Oypristisen-sce-cccesccece ee
c. At the lower part, the mass consists of larger pieces of uniform lime-
stone, in some places like the “ Pendle” of the pits at Whitchurch
hereafter mentioned, and including small Paludinz, with other small
spiral univalves, Mytili and Cypris. Some of these pieces have the
botryoidal structure of part of the Portland “cap” (Travertine); of
which bed (or of the “ Skull-cap”) they seem for the greater part to be
the representative: but others consist, as at Combe Wood, of fine-
grained oolite, passing, however, into the compact stone, ‘and. con-
taining the same fossils ........-- Sone optonsens - +--+ Lotal about
[The irregular cavities and waves at the top of this mass are very remark-
able, resembling the erosions at the top of the chalk. ]
4. The Portland stone of these pits requires no particular description.
The upper part of another pit, about half a mile east of that which furnished the preceding
list, was nearly the same, but still more like that of Great Hazeley. A third pit close to it con-
tained a “ gull”, as at p. 276.
The Portland sand is not visible in the descent from Garsington, but is very well seen in the
escarpment of Shotover Hill; where the order, at the lowest part of the Portland series, is as
follows :—
278 Dr. Fitton on the Strata below the Chalk.
Escarpment, Suorover Hi xt.
Ochre; about 8 feet above the sand, 1. | 6. Great nodules of grit, with Perna qua-
1. Greenish-sand (Portland). drata, &c.
2. A bed of concretional masses of grit. 7. Greenish yellow sand.
3. Greenish sand.
4. Beds of clay, about 3 feet thick. Below is Kimmeridge clay.
5. Sand.
(145.) The beds connecting the Portland strata with the subjacent Oxford
oolite are exposed, in detached places, on the descent of the hill from Gar-
sington to Langcombe and Gasson’s Barn, where the following strata occur,
beneath a considerable thickness of whitish sand, which, however, is probably
a part of the Portland group.
Pits near LANGCOMBE.
Ft. In. Ft. In.
1. Soil, including carstone. the quarries at Langcombe, the di-
2. Rubbly stone (Portland) stance of which from Garsington is
: é about a mile.
8. Yellowish sand, with er inter |
tions and calcareous matter inter- ¢ 1 0 Afieriathickness'of between Aone
Spersed.-.see revere receerencs 50 feet of clay as above mentioned,
4. Sand, with Trigoniz; concreted there were, at Gasson’s Barn, the fol-
atithe HOftoMi si. eielen --)n)s S 60000 lowing beds, abounding in Pectens and
5. Sand, including at the bottom 6.. 1 0 other smaller shells.
oft ioe 1. Rubble full of broken shells .... 1 0
6. Stone, in irregular concretions. . 0 9
: 2. Rubble, somewhat slaty....about 10 0
7. Sand; continuous (except where} 4 4 : : =
there is stone) with 5.and9. .... &. Coarse yellowish sand, with whitish
é ‘ ranges, containing numerous fag | i
8. Concretional stone.... 6 feetto 8 O ments, of shells; aan
9. Sand, as above. 4. Stone in concretions .......
Total thickness ...... 15 to 20 0 5. Sand nearly as above, but ine, om
[The preceding part of this section somewhat concretional........
represents the Portland atonenian’ 6, Stone; a congeries of shells, ae
sand of Mont Lambert in the Bou- with sand concreted by calcareous
lonnois. | matter, and containing black flint
10. Clay, (Kimmeridge) ...... about 12 9 pebbles, Pernze, numerous small
11. Blue grit in irregular concretions, B Gryphites and Pectens, and large
with shells and stems of Siphonia? flat bivalves.
12. Clay continuous with 10.; when 7. Sand connected with 5. ...... oe 9 ae
dry, it is yellowish brown, ap- i 40 0 The lower part of this group seems
proaching to ochre yellow .. about to represent the Weymouth beds, or
This clay rises slowly towards the upper part of the Coral rag.
(146.) Kimmeridge Clay.—In one of the quarries at Headington, the
clay over the Oxford oolite was thus :—
Clay-pits, HEADINGTON.
1, Gurface) “Loam” oo.0.0:¢ 6 +0 sim ssins ole o solmelns sie oe 0a) a0e/s)0\s » +) «stein ere sis amen
2. * Brick-clay,” with fragments of Oysters and Gryphites :—about 3 feet from bottom,
6 6
fullot small sirellsiy.ie. 27. efaieyele se =r ine ea leteboialeatctsjelotolele elon (aes) e.s eee
3. “ Blue-stone,” in concretions, on an average about a foot in thickness.........-
Saas”. Se
Dr. Firron on the Strata below the Chalk. 279
Ft. In.
Bee clay, dark muddy blue ... Mi usiciees ce nseaion (Ms OTE 0 altogether about 11 0
At top containing Terebratulee and Gryphites.
About 2 feet from top, a bed of Ostrea deltoidea.
At 4 feet from top, a second bed of the same.
About 7 feet, Ammonites and several small bivalves.
In some places Belemnites, at the lower part.
5 “ Rock;” reddish yellow sandy limestone :—( Oxford oolite).
(147.) Oxford Oolite——The section No. 18' shows the manner in which
this group comes in, after the gault and green-sand, on the great road from
London ; and the transverse section, Plate X b. fig 10., further explains its
relation to tne Portland stone and sands, which, in the eastern part of Sec-
tion 18’ are either wanting, or concealed by a prolongation of the gault and
green-sands. ‘The Oxford oolite is seen, in the transverse section, to rise
from beneath the heights, towards the west of north, at an angle of about 9° ;
and it is probable that all the strata here, from the Portland downward, decline
more to the south than the chalk and the upper members of the series: they
seem to form the southern slope of a curve or saddle, the opposite side of
which would descend towards the north, somewhere between Wheatley and
the Briil-hill range. ‘The lower beds here are much harder than the rest ;
they consist of sparry limestone, including oolitic grains, and the masses are
blue in the middle: I obtained from them an Ostrea; Terebratula media ;
Melania Heddingtonensis ; and a Spongia.
(148.) Section, Pl. X.a. No.19. From the chalk, through Thame and
Long Crendon, to Brill and Muswell Hill.—The characteristic of the sec-
tion on this line, is the distinctness with which the Portland sand is exhibited,
almost throughout its course. The superior strata are best seen in the
quarries around Brill, and at some points on the ridge between that place
and Long Crendon.
The tract on the north and east of Chinnor, on the line thence to Thame, has very obviously
been at one time the bottom of a sea or lake, over which the chalk impended as a lofty shore ;
and near which the tides or currents acted with such uniformity as to level down the ridge of the
lower green-sand ;—while on the west, the ranges of Brill, Quainton, Whitchurch, and other less
prominent summits, stood out as banks or islands, at a short distance from the land. These re-
lations are all very well seen from the ground about Barley Hill, on the north-east of Thame.
Gault.—At a point on or near the section, between Black Ditches Hill, Cotmore Walls, and
Sydenham-hurst, a well had been sunk forty feet, and then bored to fifty more, entirely in tough
dark blue clay, beneath which was sand rock.
Lower Green-sand.—In a great number of the quarries in this part of the country, the ferruginous
sands at the upper part are separated from the rubbly stone beneath, by dark tough clay, 4 to 9
inches thick, which follows the irregularities of the mass below, and coats the bottom of cavities
like the “ Gulls” of Hazeley, (p. 276.). The stony matter seems to be either the “ Malm” of
Garsington and Combe Wood, or the representative of some other portion of the Purbeck series,
VOL. 1V.—SECOND SERIES. 20
280 Dr. Firron on the Strata below the Chalk.
Sections at BRILL.
A.—In a pit at this place, open in 1827, the following beds were visible above the Portland
strata :—the whole (perhaps from subsidence) inclining towards the north-west.
[Lower Green-sand. | Ft. In-
i (Grey and tyellowasand tla steele peiciels icine alesse occ ceccecsececs cess AD0Ut JGumG
2. Alternate layers of ferruginous sand, and of clay used for making tiles. Near the 1s 0
bottom the seams are oblique to the stratification .......... eUalshele ois ele elevpdetevers
3. Black and grey, alternating with whitish and ferruginous, sand, and including flakes 0 2
ofyellow Ochre .-4,..- 25-06 ac godsout AAoooon eileieliels! ois] ctaloisle (=| oie clo falinaieentee
4. A thin course of clay (Fuller’s earth), of various colours, green, wax-yellow, and red-
dish, with a subconchoidal fracture, and a wax-like, almost resinous lustre exter-
nally, like jasper. The polish of the pieces is evidently the result of movement under 0 6
strong pressure.—See the description of a similar clay at Tilburstow in Surrey,
Seti Ws WD, poaconaccao8o0c000 206 aoeoondodsasognoc aVelolels «tele ate e UOULE
5. ‘Sand, increasing , in firmness’ as It Gees owns). « 1). 62,69. neie5 oc ieee na)o cis ole 4 0
[No indication here of the Purbeck strata. |
6. Portland stone,—containing Trigoniz and other characteristic fossils, among which
Pecten orbicularis is one of the most abundant.......... solo tno d MOUS Bidin.cin Jee
B.—At a clay pit about 20 feet below the road on the south-west of Brill, the beds, declining
to the west and south, were thus :—
[Loner Green-sand. |
. Sand; white at top, yellow, and ferruginous below .......+0.++0.. oes eee) 0) tone
2. Gravel, with concretions of “ Carstone”; coarse quartz sand, cemented by oxide oy 6
ATOM brosecouctebaneta eter aloaaieie cere coteverercrstotniene oreterenetelatehatayelets atone eis o's wisieie oteieteiete GRAN
—
Yellow ochre, of very good quality, much used in commerce...... seesceeesel 8 tol 10
Clay; containing thin bands of oehre, a quarter of an inch and less in thickness...about 1 0
Clay ; light bluish grey, uniform: here visible to a depth of .............+..about 5 0
No shells of any kind are known to occur in this bed; but about six feet down an
entire tree was found, converted into lignite much mixed with pyrites. The trunk,
about a foot in diameter, and full 40 feet long, lay almost horizontally, nearly east
and west; and branches extended to about 10 feet beyond it on both sides, be-
ginning about 25 feet from the extremity. It was preserved and shown in an adjoining
house as an object of curiosity ; and though in a state of ruin, when I saw it, from the
decomposition of the pyrites, was one of the finest fossil specimens I had ever seen.
Beneath the tree, it had been ascertained by boring, that clay, but of darker colour,
extended to about 12 feet in depth.
i G2
C.—In another pit, on the outside of the inclosure where the tree was found, the strata
were :—
Grey: sand)? styctaieictel-. aia etetstorttoretetdee sooo rece enn ce cient snes eneccsce sys «ei UOnIn————E
(5.) Clay, said to be the same with (5.) of the list above ; but darker and of more slaty
structure. It is very like 4. of the List A. above, and breaks into pieces with po- yee
lished surfaces: the lower part for about two feet alternates and is mixed with yellow
OUNe saga css aoesod Seren Sop 00.0010
The place of this clay in the series seems to correspond best to that of the Fuller’s
earth at the bottom of the Lower green-sand; and it falls to pieces slowly, in water,
like that substance: but I could not determine its relations to my own satisfaction. |
6. Yellow ochre, of a duller hue than (3.) above; some Fuller’s earth at the lower part..about 0 4
Dr. Firron on the Strata below the Chalk. 281
Ft, In.
7. Under the ochre are irregular flattened ovoid masses, about 18 inches thick, consisting
of stratified matter which contains shells. These masses were divided thus :—
a. Thinly stratified, greenish grey, Fuller’s earth, decomposed. The lowest part
sometimes including thin seams of coaly matter, the remains, apparently, of 1 6
highly compressed stems of plants; with fragments of shells.
b. Thinly stratified, dark grey, alternating with lighter-coloured, sandy clay. Like |
the alternation which is frequent at the bottom of the lower green-sand, and in
the Wealden, described above at p. 168. (83.)
8. Greenish matter, often stratified ;—coarse Fuller’s earth... .....0ccceceecccceecs 3) 0
[Portland stone :|—
9. Whitish rubbly stone, not unlike freshwater limestone, but containing Perna bon ata,
16
with ribbed and tuberculated Trigonize ..........+- heotOSvooontouor 3 to
10. “ Pitching-stone*’’, consisting of—
a. Hard compact grit: sand concreted by a very large Bae of cal-
CaxeOus Matter .\.).\.. 6.6 01 hoodogooane my avatet siete: aay oP 20 a see SAUGHEN OD
f Fuller's earth, yellowish-green 2.2... cece crevcccsccsccccsce Gin: to 0 8
c. Compact grit ;—more siliceous than @.....seeesecoeceees vets alone nal 6 6
memorey clay, in about three layers ...+.sdeccecnececenersccvccccccscnccesesses O 6
12. Limestone in two beds, including Perne .........+.+-- cleleiebsohe soovcceseo,about 2 6
13. “ White limestone”; as below. Pecten orbicularis abundant................3ft. to 4 0
D.—At a pit on the south-west brow of Brill Hill, (a continuation downwards of beds above
enumerated), the following is the order :-—
(13.) “ White limestone” (like the “Chalk” of Chicksgrove, 7. p. 253.) used only for making
lime’; sometimes harder and bluish. It occurs in irregular masses, and has the aspect ott 3.0
freshwater stone, pu Contains, numerous Prigonice...cvcewssccecevccecesess about
14. “ Cap of the Greys”. Brownish clay, full of fragments of shells....... aereiete tales
15. “ Greys”. Good stone for building, full of Pernee. Some of the beds contain stems, ¢!
like those of Siphonize ...... ete pas aid, 6a, ais o/ufotiniu,s ofnictats otelolal eter] stars
eter ee ee eres
Below the “ Greys” are about 9 feet of alternate courses of indifferent stone and of
yellowish grey sand, with Portland fossils—Cardium dissimile, Pecten lamellosus,
Trigonia gibbosa. These are succeeded by sand charged with green particles, which,
in the following list, is referred to the Portland sand; in which Ammonites giganteus
is frequent, in some specimens with Oysters attached.
In some places here also, are erosions or cavities in the upper part of the stony strata, like
the “Gulls” of Great Hazeley, (p. 276).
Portland Sand.—Good sections of this group are to be found in all directions around the
village of Brill; in the descent of the hill from Long Crendon towards Thame; and on the north-
east of the latter village.
Sections at Lone Crenpon, and thence on the Descent towards TH ame.
One of the principal quarries at the upper part of the hill at Long Crendon exhibited the fol-
lowing beds :—
Mecem ldamy clay... cciele as scccoseeces aie ioe ot sicuet sketeverere wyaueleuses acate TedeeieaaDOuteas. O
* T have, in these lists, inserted the names in use among the quarrymen, as they may assist
in identifying the strata in other parts of the country; the same pits seldom remaining open more
than a few months.
202
282 Dr. Firron on the Strata below the Chalk.
[Lower Greensand. |
3 a. Ochre and ferruginous matter .........ceceees ceccssccccsvcsecssessO0 9
bs Wark orey claw itcciel ae /ein/-10 avefe claievelsialele aielsict= US eaarwcors ooe00 4 tolOug
These substances, as at Great Hazeley &c., vary much in thickness, filling up
eroded cavities in the top of 2, next below.
[ Purbeck. |
2. Rubble (the “ Malm” of Garsington and Combe Wood); passing at the lower part into
firm, slaty, cream-coloured limestone, in which green matter is diffused,—but not in
grains; as in some of the upper Purbeck beds on the Dorsetshire coast.
3. Clay :—uniform, without the stony fragments of the Portland “ Dirt.” I could not
4
5
learn that any petrified wood had been found here in this situation.
[Portland stone. |
. Stone, with Portland fossils, beneath which is sand .......... sAhetouoere -here about
[Portland sand. ]
. Below the foregoing beds, on the descent towards ‘Thame, are,—
a. Sand, with very numerous green particles, about 18 inches; enveloping
coarsely concreted nodules, about 9 inches thick............e00. sro lovenele
under which are knobby concretions, of a marly stone with green particles,
b. Rubbly, somewhat sandy, grey stone, with green particles,—like Kentish rag: |
containing clavellated Trigoniz ................ Beouopoosoc 12 0 to
6. Greenish grey sand, At its junction with 5, and for about 6 or 8 inches downwards,
7
are worn fragments of black flint; with Trigonia, Perna, and an oblong bivalve—a }
Panopza ....... aledereictsette whaleleyelievals e/ole loiels chapaserers, « afar alte) set eb atet etait about
The whole thickness of the Portland-sand here is about
. Beneath is clay.
Ft. In,
hi
2
18
30
50
6
0
The greatest superficial extent of the Portland sand in this part of the country occurs near
the village of Thame; extending from Scotsgrove and Scotsgrove Hill on the north, to Priest-end
and Morton on the south; and from Dropshot, near Cotmore Walls, west of Thame, to the flat
between the river and Long Crendon. The apparent range of the formation thence, by North
Weston, Rycote, and Albury, to the heights above Wheatley, I did not examine.
1
ws
Pit at Barley Hiil, cast of Toame.
The strata dip at an angle of about 5°, towards a point about 10° south of east.
. Sollvandjloam).=... shavape coke etexs eieLehonere hele Sete whe tare ste. ne 2ft. 6 in. to 2 ft. 9 in.
[Portland Sand.]
. Irregular concretional lumps of calcareous stone with green particles, interspersed in
sand. Petrifactions numerous:—Pernz, with Lithodomi, and Ammonites -Pla=
giostoma rusticum, (near Towersey)........ aiide ichoveroretcedo PAT ty Ho: IRDA:
[This is evidently a continuation of the group at Long Crendon, on the Opposite
side of the valley of the Thame. It precisely resembles part of the cliff immediately
north of La Creche, on the French coast near Boulogne. |
the bottom, the whole consists of greenish matter, not to be distinguished from that
Sand ; becoming greener as it descends. At the top, few concretions of stone. At
of the Lower green-sand near Folkstone. Serpule very numerous }
Coarse stone interspersed in sand; with numerous fossils, especially Ammonites, and
Trigonia gibbosa ......--. stile xcVeite eae enone rete SOn On Be oe ;
eee ee reve seoe
- More compact and uniform greenish or bluish rock, with green particles; like soft
Kentish rag. In some of the quarries it is fit for building....... sio.e \
eeeeeservee
_
_
Dr. Firron on the Strata below the Chalk. 283
Ft. In.
6. Sand; 30 feet (at least). The top only is visible here, but in other pits nodules of ee
great size are scattered in it irregularly, close to the stone 5.....60.+.-+++
These nodules are distinctly seen at an adjacent place called Dropshot. They are
from 2 to 4 feet in length, and about 18 inches thick, and consist of large sub-
globular masses of hard, bluish green, sometimes highly calcareous, crystalline, grit,
(here called ‘ Bluestone”), like that of the concretions at Shotover. In some
cases it is remarkable that they are flat at the top, while the form beneath is sub-
globular, (fig. 1. of the subjoined cut); pebbles of dark brown or black flint ad-
hering to the upper surface, in a gravel-like crust. They are sometimes traversed
by vertical cracks and veins, as in the quarries at Mont Lambert in the Boulonnois ;
and when broken, these exhibit flat surfaces,—as in fig. 2, which represents a large
nodule, inverted, to show the form of the lower side*.
Muswell Hill.
This hill, which forms the extreme promontory of this range, was one of the principal Ord-
nance stations, and is 744 feet above the sea. The summit, I was informed, is composed of :—
1, Lower green-sand. Reddish sand, including concretions of a dark brown ferruginous
conglomerate (‘ carstone”), which occurs also in large masses, and in thick beds, i 10 0
under a very reddish and ferruginous soil ......... Pa crate eee Ruta gaa . 8 ft. to
[The Portland stone appears to be wanting here. }
2. Portland Sand, with green particles; Perne, Trigonia, Sphere, &c.
3. Kimmeridge clay: springs breaking out at its contact with the sands. No stone, I
was informed, occurs between this place and Blackthorn: that which is employed
in all the flat country on the south-west of the range, coming from Muswell Hill
and Brill.
From Muswell Hill there is a fine view to the west and north-west, of the great plain occupied
by the clays; and westward over Otmoor, which is crossed by a Roman road from Oxford to
Bicester.
Oxrorp Oorite.—The stone of Blackthorn, about 33 miles west of Muswell Hill, is a variety
of oolite or pisolite, consisting of oolitic grains disseminated through sparry limestone of a bluish
colour.
(149.) Section, Pl. X. a. No. 20.—From the Chalk near Wendover,
through Aylesbury and Whitchurch in Buckinghamshire.—The two great
roads from London into Buckinghamshire cut through the chalk, one by the
vale or defile of Amersham and Wendover, the other and more northern,
by the Vale of Berkhampstead and Tring, the general altitude of which above
the sea is about 350 feet; that of the adjacent heights of the chalk rising to
* Fig. 1. is intended to represent a vertical section of a concretional mass of stone imbedded in
sand; of a subglobular or kidney-like form below, but flat at the top.
Fig. 2. is a sketch of another nodule, with a vein at right angles to the mass; through which
a part has been broken off.
Q84 Dr. Firron on the Strata below the Chalk.
more than 600 feet. The summit level of the Grand Junction Canal at the
opening of this vale to the north-west, is 40435 feet above the sea: and a
branch of the canal is conducted at the same level along the foot of the
chalk range to Wendover. The line of Section No. 20. runs from a point
about two miles west of that town, above which Combe Hill, or (as it is called
in the Ordnance Map) Wendover Hill, rises to 905 feet above the sea; and
thence the ground descends rapidly towards Aylesbury, the height of that
place being about 380 feet above the sea*, and a few feet above the flat
occupied by the Kimmeridge clay on the north-west of the town. The slope
and undulating ground from the chalk range to Aylesbury are occupied by
the strata between the chalk and the Portland stone ; and the corresponding
tract, from Thame on the south-west towards Leighton on the north-west,
which is emphatically called “ the Vale of Aylesbury ”’, consists of the same
strata. The Portland stone forms a distinct ridge from Hartwell to Scots-
grove, on to the road from Aylesbury to Thame, of which the highest point
near Dinton Castle is not much inferior in elevation to many parts of the
chalk range. Between Aylesbury and Leighton the first rise of the Portland
beds is obscured by accumulations of superficial gravel.
The Vale of Aylesbury in general has been lowered and levelled by the
agency of water; but several detached portions of the beds between the
Gault and the Portland stone, are still found on the higher parts of the ridge
about Stone, and on the summits of the insulated heights beyond it. The
strata seem to increase in thickness in approaching their outcrop, but this
enlargement is probably no more than apparent, and produced by their
better preservation near the most elevated points. If these places were once
detached summits, or islands, in a shallow sea, of which the chalk escarp-—
ment formed the shore, the waves would naturally wear down and carry
away the strata in the lower ground, while the portions above the reach of
their action would remain.
(150.) The members of the series illustrated by the sections visible in this
country, near to the line of No. 20, are:—1. The Lower green-sand; 2. The
strata thence to the Portland-stone,—including some doubtful traces of the
Hastings-sand, and the Purbeck strata; 3. The Portland stone itself, with
the usual fossils ; 4. In a few places, the Portland sand; 5. The Kimmeridge
clay. The following details could not be arranged in exact succession, as por-
tions of many different groups are frequently found in the same pits ; but the
ists are as far as possible disposed in the descending order of the strata,
beginning with the Lower green-sand.
* The top of the church tower at Aylesbury is, according to Mr. Bevan, 425 feet above the sea.
Dr. Firron on the Strata below the Chalk. 285
Lower green-sand.—A considerable thickness of sand occurs at the top of the ridge above men-
tioned, in the space between Stone, Dinton, and Cuddington. It attains its greatest height near
Stone, where there is a knoll apparently composed of sand; near which the following beds were
found ;—
Sand-pit at SToweE.
Ft. In
BEANIOH ANG SOU... sc eee pce newsesancacscenneesicvcceees. About 1 ft. to 3 0
J. Greenish clay, like Fuller’s earth.......... slelclenstsidia eucithcletic ec sic a ees'cs seO lls 40° OF 9
MIG CIAY occas te cc cavens cen weees cu cic Meeeecis tess s sete ss ed in. to 1
$. Rust-coloured sand, passing downwards into grey: the lower boundary is ill defined] ,
BMBMECOUNAY 6. ccc se nc evervensines sis cleo « sie oveie dacsiste’s wsjelv vcs e eal TOM tO
4, Whitish uniform sand, marked by nearly horizontal but irregular lines, of darker hue, 8
exey, yellow, brown, and nearly black ...5..20se0ceecsvwecoees ss veces dbout t
Total depth...... oa.) oferta Sere 1S 0
Some remains of the Lower green-sand appear also at the top of most of the sections following,
which are only a selection from a great number of lists. The series in all parts of the country is
very nearly alike: but the pits being worked for the sake of the Portland stone, have not, gene-
rally, been opened in the places most favourable to the display of the superior strata.
The circumstance most deserving of notice in the sections at Ford, and thence towards Dinton,
is the occurrence, near the bottom, of dark clay which includes a layer of iridescent Mytili, cor-
responding precisely in its character and situation to that at Bishopstone, Whitchurch, and other
places hereafter mentioned.
Dinton Quarries.—One of the most remarkable quarries in this part of the country, is on the
south-west of the cross-road from Dinton to Cuddington, where the works have been carried on
for more than 200 years, the stone being of excellent quality. The Section was as follows :—
Stone-pits at Dintown.
All the beds inclining a little to the east.
Meveretable soil, and reddish loam.........ccccscccccccusccorsessceseesss about 2 0
2. Ferruginous sandy loam .....cccceccssccccccsrssccccensccsercecers cae OC
Meperreemish Grey Clay ....ccsscccscccccccccccccsccssccrsssccsessesescress fe2- 10°19
4, Brownish and grey clay.......sseeesseseees Sioldandls Gh: aidlteide steletels 5's 1ft.3in.to 3 0
[The great variation in thickness of this bed arises from its entering at the bottom
into the irregularities on the surface of 6. which are coated throughout with the in-
termediate thin bed of clay (5.)]
5. Dark, umber-brown, tough clay, with much oxide of iron.......+.+eeee0+++2in. to O 4
At the bottom of the bed are Mytili, and decomposed fragments of other shells.
[Purbeck Strata. }
6. Grey clay and soft stone (freshwater limestone) becoming white at the bottom by de-
composition : at the lower part more continuously laminated, but including through-
out irregular masses of stone, in some places penetrated by minute tubular cavities,
slightly bent and of uniform diameter,—probaby the work of lithophagous animals,
or such as might be produced by the removal of slender twigs. ‘The decomposed
parts of this stratum pass into the firmer masses; as in the ‘‘ Malm” of Garsington.
It contains a few spiral univalves like those of that place and Combe Wood, including
Paludina (elongata ?), with small Modiole, and a Cyclas? ....-.++eeeeeeeeceeees
(3 feet thick in an adjacent pit)....
7. Between 6. and 8. is a thin bed of tough, dark, somewhat ferruginous? clay, with iri-
descent Mytili (M/. Lyeliii?) at the bottom ....sscccccsssccecccesvevecvcreees
A
os
Mae
286 Dr. Fitton on the Strata below the Chalk.
Ft. In.
8. Whitish beds of nearly uniform aspect. oie
a. Soft fissile marl or limestone in about six beds; the divisions, paiatn my
ae 3 f
seem to be the effect of decomposition ....++++++eeereeeeae Dit, to
b. Uniform hard grit or sandstone, consisting of quartzose sand in a ah 1%
CATEOUS CEMENE .. eee ee seer se cereereecresreressrscereeercrecce 5 0
9. Stony concretions, in greenish very fissile sandy clay ;—3 to 5 beds ; passing into, e 1 8
COontinuOUS With 10...... cc cece cece ce ceeceecrrcccncecrcccccsseencs oieleeseeld .
10. Fissile sandy matter; and grey, sandy clay, passing into 11 ......e+eeeeeeeeeeee 1,
11. Fissile, tough, yellowish, sandy clay, containing much calcareous matter, and naa
Cypris, Mytili, and Modiolae .......-sesececscerccercccsescssccvecce ee
[ Portland Stone. |
12. Beds of good stone; grey without, blue within.
a. “Capping,” full of shells ; like the “ Roche” of Portland...... 8in.to O 9
buSolidistone, the sbest tcepornarvere severe tetetore ele) cve)ove' eile icleovoicciensiel eleheree toners
c. Soft stone, bluish, full of remains of shells; Ammonites giganteus; Exogyra
nana; Ostrea, two species; Plicatula .......e.seeceecsccevcscsccs
Bottom of the (Quarry ieee rate te cleieinoletevoteleita ela) efel(e elms clatale¥s (-lny= o¥=1 ous) nt atten nat
The proportion of sand to the stone, in these quarries, is much greater than in those of the
coast, the Portland stone here appearing generally in the form of concretions in the sand: and this
is the case also in the Boulonnois. Near! Dinton Castle the stone assumes the form of insulated,
subglobular, or potatoe-shaped concretions, containing great numbers of Oysters, with other
fossils.
(151.) One of the most prominent circumstances in the upper part of the
preceding’ sections, is the contrast between the arrangement of the sands and
Fuller’s earth, or ochreous clay, and that of the beds which represent the
Purbeck formation immediately below ; the upper surface of the latter being
commonly indented or eroded into cavities and inequalities, froma few inches
to four or five feet im depth, which are generally coated with a thin stratum
of clay, and then filled up with sand and gravel. ‘These appearances, which
are perfectly analogous to that represented at p. 276, in the cut of the “Gulls”
of Great Hazeley, and to the discordance of the two sands at Swindon, p. 265,
are observable in all the pits of this country. They clearly show that an
interval must have elapsed between the deposition of the Purbeck strata and
that of the Lower green-sand, during which the surface of the former was
disturbed, by the operation no doubt of water.
(152.) The tough clays, near the junction of the incumbent strata with
the Portland beds, are well seen in many of the pits of the lower country,
as at Bishopstone and Southwarp, and in the heights about Whitchurch and
Quainton. It is difficult or impossible, in some cases, to determine whether
they are to be referred to the Fuller’s earth of the Lower green-sand,—to
some of the beds subordinate to the Weald-clay and Hastings-sand, or to the
Purbeck series. But it may be remarked that, although these clays alternate
with thin. slaty limestone, which contain Cypris and other freshwater fossils,
—
Dr. Firron on the Strata below the Chalk. 287
no bed strictly resembling the “ Black Dirt” of Portland has yet been found
here,—none including, like that bed, fragments of stone, and exhibiting so
obviously the characters of a coarse gravelly soil: nor have I seen or heard
of any instance north of Garsington, in which silicified wood has been found
in this part of the series. It can only be said, therefore, that the beds above
the Portland here resemble those of the coast, in their sudden contrast with
the Portland strata, from the abundance of the freshwater fossils which they
contain, and the frequent alternations of beds of clay, or mud, with the fissile
limestone near the contact.
Pit at Brswopstone :—in “ Church Furlong” belonging to Dr. Lee.
1. Soil bearing corn. Ft. In.
2. Fuller’s earth; greenish and brown. Thickness very irregular........-.000. Dig to Tin
In this bed are iridescent Mytili, like those of the bed 7. below, and of the sections at
Whitchurch; p. 288—289.
3. Rubble; white, freshwater limestone, decomposed: containing Cypris and casts of
PEA UCINGS, 1 CALCATEOUS Spar Ase. clk Moo ee cece ode ceccevceeseecnece sad
4. Clay and stone.
meant olive greenish Puller’s earth 2.2.0.0. cc ees ese rescccsctmens 0 4
BeOLO MIMESLOMC sp eee cic. sche anes Sieh be clear Dots hala shatete. Ws aiemeenrerags « 0 6
Sear eses TOA Hs UK Er asic, tile. csi) eo eis, 0: ti oie) o:6:,o10)'evejp aseres stayeie © seuaemeietetetess 56" “Ce 2
RERBEETCMMITIC CHO St stetetevave: stotori co tisichate eci'ere'e, «ois. ole'o:0seseviet eres’ aye okateRepeveievel eis, cle Ons
BRMMITISES GALEN poop pc ce csnocacaasccvnccss ainjeiea/e 0 oye SiMtehetatane We Inietet s 0 1%
5. “ Sandstone”, so called; firm, grey, and whitish, granular calciferous grit. It has distinct
traces of the lines of deposition, and on the surface some approach to ripple-marks.
_ — Que. does it represent the grit of the Hastings sands?.......+seeeeseeee 6in.to 0 9
6. Sand, alternating with ochre and clay.
a. Sandy ochreous clay ........ On ews oho 5 Mor iii Bee ae pias 0. 2
Weeeietrcenisht Fuller's earth 0.5... ee cece ssc cess scossseroncncs o°2
c. Greenish grey sand, mixed with calcareous matter, and including piers 0 7
of fishes
. Fissile, calciferous clay, or marl, passing into stone. In the upper part are iridescent
Mytili (Mytilus Lyellu? Pl. XXI. fig. 18.) like those of 2. above, and of the pits near
Whitchurch.
a. Dark, bluish grey, very fissile clay, containing Cypris in great numbers,
an oblong Unio, and small scales of fishes (Lepidotus). tars
b. Clay; somewhat harder, less plastic.
ce. Clay; lighter-coloured and still harder; approaching to stone.
All these divisions contain Cypris Valdensis and another species; a small
smooth Modiola, a striated species ; and Cyclas parva, Pl. XX1. fig. 7.
[ Purbeck. |
8. “ Pendle”: fissile, argillaceous limestone; here of a dark grey colour; in another
... adjacent pit almost white: containing Cypris; casts of Cyclas parva, some of which 6
include casts of Cypris; striated Modiole ; small Paludinz ; and other small uni-
ees a the Malm, of, Garsington. «.-..0r6iaaneie «nto «fsa os%eisieie sieml seam 4 in. to
In some of the pits hereabouts, the “* Pendle” contains also a depressed Planorbis, as
VOL. IV.—SECOND SERIES. 2p
eeereeoer eee ee ee eee eee ee see eeeeeeeeoreeeeseeseeeesesese
~I
288 Dr. Fitton on the Strata below the Chalk.
at Wockley in the Vale of Wardour, 5. b., p. 252., and at Garsington, 3.c., p. 277.;
with Potamides carinatus ?.
[ Portland. |
9. * Bottom Rock”. This, in one of these pits, is an agglomerate of fragments of shells;
of a dark bluish hue, specked with white. In an adjacent pit it abounds in Trigonize
and other Portland fossils.—Thickness not ascertained.
The beds below are not visible, and are unknown to the workmen.
The upper part of several other pits near Bishopstone (as at Southwarp and the vicinal of
Dinton, ) agrees with the foregoing list, in exhibiting an alternation of clay, more or less like Fu le
earth, with ochre and ferruginous sand: and the very dark elay which includes iridescent M ti
occurs in so many places that there can be little doubt of its former continuity throughout
part of the country. It is particularly distinct on the side of the road from Whitchurch t
Winslow, near the turn towards Dunton, about eight miles from Bishopstone; where, bes
are Paludinz, a Planorbis, and perhaps some other species. The whole group, therefore, cle rly
represents the strata above the Portland stone at Garsington, and in the Vale of Wardour; and
is, no doubt, the equivalent of the “Slate”, the ‘‘Cap”, the ‘ Dirt”, and the other lower b
of the Purbeck formation, on the Dorsetshire coast.
Pit near Warrcnurcn :—A. (Denchfield’s.)
(Compare with the Section at Quainton, p. 289—290.) q
' Ft. In:
Grass, over vegetable. soil .. 60... sc cess vc cecccc cece scence ctuces ve wees 6 ann
—
.
[Lower green-sand and Wealden.]
2. Greenish white, coarse, sandy clay ; including rounded pieces of sandy stone........ 7 0
a. Tough, grey, and greenish clay ; including b. ............2.--about 0 9 2
b. A dark band of very tough clay 2. 2202.5. 20 50 oo» ssi) epois oie AOU
c. Clay, like a.; the lower surface waved and irregular. This, at its junc-
tion with the darker clay above, and for a short distance below, is full of
a thin iridescent Mytilus, so fragile that I could obtain gy very imperfect ri
specimens=<.5522. SoD DO Nobo Ob BD NtE see ele » voles 6. #0 ofeibie «leleisat a an
4, A group, which my guide called ‘* Cornstone?”.
a. Grey and greenish sand, irregular in thickness............... -4in. to 0° 79m
b. Whitish clay, sand, and soft stone ............ otbi eyeveola eas ete Oven ooh as
c. Tough, grey, and brownish clay, passing into d............-000- 33h GOR
d. Similar clay, including concretions of gritty stone ..............about 1 0
5. “ Green-stone”, (so called), comprising,—
a. A thin bed of hard, brownish clay, like part of 3. above........lin.to 0 2
b. Fissile sandy clay, greenish grey .........2.ceeees cvcecce es 41D, (On ti
c. Hard calciferous gritty stone, in irregular concretions...........+.s.. O 4
d. A band of anon’ grey soft sandy clay or marl ..............about 1 0
The calciferous grit, 5. ¢., which is like that of Bishopstone (5. p. 287.), and of Qu
(9. p. 290.), deserves notice, from its resemblance to the grit of the Hastings sands: an :
contains at Quainton casts of a spiral univalve,—Paludina (or Natica?).
Dr, Firron on the Strata below the Chalk. 289
[Purbeck. ]
6. “ Heath”. Green and grey sand, of firm consistence ; at the bottom mixed with whitish
HEMIIGRINAGLED tgisie leo om isyessseve sic & pia citisi ie eietalaeere ts a caoha cilshaiets clays ins bite sie ehsie tetahers
7. An indistinct bed of soft fissile limestone (‘“ Pendle”, my guide calls it), which seems
to pass below into very hard stone, including Cypris and worn ovoid particles of
whitish stone. It contains also small bones and scales of fishes ...........e000e
8. The beds below 7. are here uncertain; but are visible in some other pits.
The Portland strata here, in general, differ from those of Portland Island and of Dorsetshire ;
no thick beds of good stone occurring, and no flints.
_ Isaw here no traces of silicified wood, nor of Cycadez, though I examined everywhere the
beds of clay, with the hope of meeting them.
In another pit near Whitchurch the lower beds were visible, the whole being thus:
Pit near WuircHurcH :—B.
Rubble.
[Weald Clay, and Hastings Sand?]. Ft. In.
Sey matter, MUCh decomposed .. 2.2.0.0. nec scene seccwrscerscerces aie} oiaetie ae 0
2. Dark brown and grey tough clay, with some layers of sand, including Mytili ........ 1 0
8. “ Cornstone”; (see 4. of the preceding list) .......... eer nioleer ee a OL oe 0 2
4. “ Cheesecakes”; clay in very thin flakes, alternating with sand. (Compare with me 0 4
alternation described in (83.) p. 168.) ....... Beer geeede oo fe ee ee :
SMeietatil Sandy STONE 2.0 fw. Me ve eee cc wand ewes cue slelldsiceles Oe Nelelors 0 10
6. “ Greenstone”; concreted sand, and grit, like that of Hastings ?—(See 5.c, List A. ot aire
EE cle.o+ s+ raion steretaie ie « So os yGocagorer eae tise cia eo Wate Stine oe.» O in. to
fee-abiesione +; soft limestone ............ Sits apeishisfode siehevoiaketele eteieiclersisictsis sere sora OA
8. a. Sand; uniform, greenish-grey, coherent....... ccc encccccscncces ch ind a
RMT Sats. aed has cic) oa ata) <\+,0.4.0\o-s sins 01s » bpojeie s.ciee.s sis ole .« sys vores snl Cink + 8
[Purbeck Strata. |
9. “ Pendle”; soft fissile limestone, including worn rounded particles of stone, which
give to the whole the aspect of oolite ; and containing Cypris ; Modiola, two species ; hi 6
a Mytilus; Cyclas parva; and portions of an Astacus ......s.-eeececseeceeecs
[ Portland. |
10. Limestone; often bluish, abounding in Trigoniz, Venericardia, and other Portland 5185
EPI ESMEMSEE TNE Fy cys 01 o> oj at or op av ov ever sy even, ove; 0 Shsiatlohetedaye’ ala “of otanetelfateyc) steteso.b “ale ters inte Oe ate
MipmGroodestone, called “ Buzlders”’ often bIWISh), ...<,0.0,5.0,0.0,9,0.0,010.0,000,0 0,9.0,0,0.0,0,9,0,0,0,0 66 24.6
Bottom of the Pit. Total about 10 ft. to 12 0
Pits at the top of Quarntow Hix1,
About a furlong east of the Ordnance Station, which is 754 feet above the sea _ Beds inclined
towards the south at about 3° 30'.—See the Transverse Section, Pl. X. b. fig. 10.
[Lower greensand, and Wealden? ).
1. Red sand, with concretions of hard ferruginous conglomerate ; ochre at the bottors :—
visible about 2 0
2: a. Clay and sand; brownish and grey, in thin alternating flakes ....about 1 6
b, Fuller’s earth ; wax-like, as at Brill, (4. p.280.) .......- Vile serose) YO Or. 298
2p2
290 Dr. Firron on the Strata below the Chalk.
Ft. In,
3. White, and brown, sand and clay .............- 6BTb Sige lae.lg > ‘oie 'ote bib pleflone halls 1a en
4, Alternate beds of white, reddish, and yellowish sand, and thin courses of grey clay A to 6 0
5, a, Dark brown clay, called here “ Black Dirt”. .......00++00++.--about : 1 0
b, Alternate beds of tough grey clay and sand........ ata cca apeverstenets atecats
6. Greenish sand, said to be 6 feet thick ,..........- ai sinteeveteeofetentneiens socccajeketctateteetene
Totalicicc.cavetac .+...-about a 0
The beds next below are obscure, from subsidence: the order was stated to be as follows :—
i. selaemairt «tough dark (clay \.</:2/<iletcierrl' sts oe) eee sleasses vc cc ccesenceee Om
8. “ Grey dirt”; grey sandy clay, with fragments of shells ............++. --.--about 6? 0
and Cyclas?. Has been found-in masses 5 feet thick 153 feet long: used for paving
9. “ Hard stone”, consisting of siliciferous grit or sandstone ; containing Paludina elongata? |
0
roads (Que. the grit of the Hastings sand?)...........0006. Boooo 901 PIE 2)
26a
The following, still lower than the beds above detailed, are seen in another part of
the hill, under red sand and hard ferruginous conglomerate, (carstone.)
[ Purbeck. |
10. “ Heath”; white sand and clay; full of decomposed shells in layers me ou
striated Modiola; and Cypris ........ So GON OOR SM toeeeeeciee ect slelsle mieten
11. “ Pendle”. Fissile oolitic stone, containing Cypris, Cyclas parva, Mytilus, and Mo- 0 em
diola ;—as at Dallard’s, in the Vale of Wardour, pp. 249,250 ....-..s.e0e -9veiele
I did not see any remains of trees, or of Cycadez, in these quarries, nor hear of
any from the quarrymen. But among the specimens which I obtained in the village
of Quainton, said to have come from the hill, was that represented in Pl. XXII.
fig. 11, which possibly may have been part of a Cycadeous plant?. The specimen
however, differs both from the trees and Cycadee of the Dorsetshire coast, in being
calcareous, effervescing copiously with acids.
The following beds were seen best in the eastern pits, near the Ordnance Station,— i
[ Portland. |
12. “ Builders” limestone, fit for building, containing Pecten lamellosus and noe 0 j
Modiolas tae cicnwetetetecteievens shevetavsbee oustsverovens Sarehe boo We c0.0 0 0 eke elleroleliele revert Um ORLTT MRE
Among the Portland fossils from the quarries of Quainton Hill which I saw in the
village was an Ammonite 18 inches in diameter, with a Belemnite imbedded in it.
13. “ Limestone”, full of petrifactions ; Trigonia extensa, T’. gibbosa, T’. incurva; Pecten 6 “One
lamellosus, with Gastrochenz ; Pleurotomaria ........-..-ee+e+ees 5 ft. 6 in. to
TA. JS and: cn tote ee weersteteleles bkeie ks Bie veieveiavenetaloeetatls Bn One OG solo te: eaten eee iin about 6 0
15. “ Middle Rock”, and Rubble; stone abounding in fossils alStele euacetetste tens erro
UG: (Sand sccayerebsyvocterenctoretorete Mhorstate tenet atoe tails ovesssér'e Sfeysifovsite satlausdeeteeiots cca aie oxetotoene coseee
17. Greenish concretional stone, rugged and sandy. .........0seeeeeeees 1ft.6in. to 2eao
18. ‘ Bottom rock”, greenish gritty limestone, with stems of Siphoniz. The pits are never
dug lower.
The Portland stone as it approaches the outcrop in this part of the country, becomes mueh
more sandy at the lower part, and seems to pass into the sand beneath. The quarries on the
north-west of Whitchurch, towards North Marston, include, between two beds of stone, a stratum
of uniform grey sand, eight feet thick; which preserves its thickness, and is well known to
the quarrymen in other parts of the adjacent country. The stone is worked (and perhaps exists)
only in a few places on the north and east of Whitchurch; but from its extensive occurrence at
Dr. Firron on the Strata below the Chalk. 291
Church Farm on the west of Wing,—and again at North Tinkershole south of Stewkley, on the
north of Dunton, and west of Hogstone,—it would seem that the upper part of most of the flat-
topped heights thereabouts may have once been occupied by this formation*.
The Portland strata also occur at Weedon on the south of Whitchurch, about midway to
Bierton, the western part of which village stands upon them. But I was assured that no stone had
been obtained, though often sought for, at Cublington, Aston Abbots, and Wingrove; the two
places last mentioned affording only sand and gravel +.
The Portland sand is little disclosed near Aylesbury ; though it comes to the surface around
the town beneath a thin capping of Portland stone. The road from Tring to Aylesbury, a little
west of the 37th milestone, is crossed by sand, which includes green particles and worn fragments
of black flint ; and the subjacent clay makes its appearance close to Aylesbury on the north. One
of the most distinct sections of the sand was visible at the entrance of Whitchurch, where the
road to Aston Abbots strikes off from the main. A good section also was obtained from com-
pining that of one of the pits at the Warren near Tinkershole on the south of Stewkley, with
another north of Dunton.
Waitcuurcn, at the cross-road to Aston Abbots.
[Lower green-sand ? ]
1. Yellowish sandy soil.
2. Greenish and reddish sandy clay.
[Portland Sand. | He) ae
8. Concretional soft stone, in irregular lumps, full of green particles ; with numerous shells; ue, 4
Venericardia, Pernee. Compare with that of the Section near Thame; 2. p. 282. :
4, Harder stone, in irregular concretions, abounding in green particles, and containing worn
fragments of blackish flint or chert. Very large specimens of Ammonites bipiex, as on
the shore near La Creche, Boulonnois; Pecten concentricus; large Venericardia
[Kimmeridge Clay.]
5. Dark bluish clay, continuous with that of the descent towards Hardwick, and thence to
Aylesbury ; here dug to the depth of about 20 feet, aud used for making tiles. It
contains Septaria, and nodular masses of phosphate of lime,—which, when acted upon
by marine acid, afford the peculiar smell of Coprolite, though they have not its form.
Among the fossils here are channelled Belemnites.
Pit at ToE Warren, south of Srew Key.
Soil and whitish rubble.........esssessceeecvaes at > ssipalatetepn'e/oiohs mieievatera tates about 2 0
[| Purbeck. |
1. a. Light yellowish grey clay, passing into stone ...... mielsiatelatalefelshetecsierets 1 Ol,
b. Rubbly limestone... 2... .cesccceccepesecesccvences Manca bee a5 O29
[Portland Stone. |
2. Soft, uniform, marly limestone, abounding in fossils ;—Ostrea expansa ; Pecten lamello- |
6
sus, Buccinum naticoide, Pl, XXIII. fig. 4, Perna alia Pleurotomaria, ee
Venericardia, and large Ammonites ........ john ospabonrounosnc0060- 4 ft. to
* Moor Hill, a height about a mile and a half north-west of the village of Quainton, has a
nearly horizontal top; and, not improbably, is capped with Portland stone or sand.
+ Smith’s map of Buckinghamshire represents the Gault as extending to the north-west from
between Hulcot and Wing, as far as Cublington and thence to Cottesloe. If this be correct, the
Portland beds may exist ‘within that space, at a depth below the surface at least equal to the
thickness of the Lower green-sand in this part of the country: but the map near Aylesbury re-
quires much correction.
292 Dr. Firron on the Strata below the Chalk.
Ft Im
3. Uniform, yellowish-grey sand; precisely resembling that which includes the la o-
called “ Les Grises” in the quarries near Boulogne....... Sasso cies . -visible about
{Portland Sand. |
4. Hard, dark brownish-grey stone, of irregular thickness, containing Perne. Appr
2 e
ing to the nodules of Shotover........+-sseeeeeees sie io ajo ieue byateteks piekelatey eel .
Bottom of the Quarry. a
5. Below is green matter, used to form the floors of barns ; not visible here at present, but —__
well seen near Dunton.
In a pit at Dunton, the equivalent of the bed 3. is only three feet thick ; and that of 4. consists”
of rubbly calcareous stone, alternating with sand, the whole full of green particles, with small
pebbles of black flint,—at the bottom of which is a continuous bed of greenish stone, about 2 feet
thick, with dark particles, containing large Ammonites, Perna quadrata, and many other fossils.
The equivalent of 5. is tough green matter, apparently the same with that which gives the greenish
hue to the stone. This has been dug to the depth of about 3 feet. ‘oo
Kimmeridge Clay.—This clay is sufficiently characterized, at several points near Aylesbulga
by its occurring immediately beneath the Portland sand, and by its fossils. On the north-
west of the town, towards Bierton, it appears beneath about five feet of brownish sandy clay, E
(Portland sand?,) which includes numerous fragments of flint; and it contains Septaria, with
Ammonites. The tiles made of it are of a full red colour. Thence to the entrance of W! hitchurch
on the south, the road appears to be cut wholly in the clay: but there are variations in the hue c of
the beds exposed along the road, and perhaps some alternating layers of sand. In descending to
the streamlet south of Hardwick, were iridescent fragments of shells, with Gryphea (Exogyra)
virgula, (Pl. XXIII. fig. 10), and Aptychus, (Pl. XXIII. fig. 11), in the ditches at the road-side.
At Quainton, clay forms the slope of the hill beneath the stone-pits ; and a well had been dug, at
Pi cet
the village, in clay, to the depth of 60 yards; among the fossils brought up from which, were
Pinan
beautiful specimens of Ammonites Gulielmi, like those obtained, along with 4. biplex, from East
Claydon, about three miles north of Quainton, where they were found about 20 feet deep in
clay. ,
The clay-pits beneath the hill at Stewkley, about midway between that village and the Warren
above mentioned, also afford Aptychus, and Exogyra virgula; with compressed Ammonites of the
Kimmeridge clay, and a species supposed to be new.
(153.) Section No. 21,—from Dunstable through Hockliffe to Woburn;—
and No. 2\', Hockhffe to Fenny Stratford—The tract occupied by the strata
below the chalk, from Aylesbury to the coast of Norfolk, is even less know mn
geologically, than that between Buckinghamshire and the south-eastern coast;
the maps of Mr. Smith and Mr. Greenough, and the general descripti yn
of Messrs. Conybeare and Phillips being the only publications relating to it.
The want of correct maps would alone have prevented the complete examina-
tion of this district ; but this impediment will soon be removed by the com-
pletion of the Gpdbance Survey from Bedfordshire to Cambridge. The fol-
lowing observations indicate only some of the more prominent facts connected
with the beds below the chalk.
Dr. Firron on the Strata below the Chaik. 993
The series of strata in Sections 21 and 21’, differs from that of the preceding
sections, principally in the absence of all the beds between the lower green-
sand and the Kimmeridge clay, which are found in immediate contact, at the
_ village of Little Brickhill, on the brow of the descent to Fenny Stratford :
—this junction, which was to have been expected hereabouts, from the evident
thinning out of the Purbeck and Portland formations in the north-east of
Buckinghamshire, is continued thence, through Bedfordshire, into Cambridge-
shire, and even to the coast of Norfolk.
The great accumulation of gravel and transported matter, rising in several
places into hills and extensively concealing the strata, is another circumstance
which distinguishes the vicinity of Leighton Buzzard from the country towards
the south-west, and renders the examination of the strata difficult or impracti-
cable. A similar coating of gravel is found not only throughout Bedfordshire,
and a great part of the counties on the north-east of it, but far to the east of
the chalk escarpment itself*. The fossils, and stony substances, which com-
pose this deposit, have been derived from many different formations, some of
them very remote, and are deserving of attentive examination. My collec-
tion includes only a few specimens from one of the ravines which descend from
Little Brickhill, and from the Platform between Stewkley and Soulbury,
about 510 feet above the sea, where the multifarious gravel includes frag-
ments of granite, and a large proportion of chalk. This deposit does not
there form an escarpment, like the sands at Brickhill, but declines gradually
towards the north, in a series of lower inequalities: on the ’south and east, it
occupies a great part of the surface towards Leighton, Wing, and Cub-
lington.
On the line of the Section, No. 21, the ridge of the chalk attains nearly
the greatest height which it anywhere exhibits,—Kensworth Hill, south of the
road near Dunstable being 904 feet above the sea; but the general elevation
and that of the principal summits both rapidly diminish towards the north-
east. Near Tring, the difference in height of the upper and lower chalk
escarpments is strongly marked ; and the retreat of the former is still more
conspicuous near Dunstable; but the boundary of the lower chalk is less
distinct.
The Upper chalk forms the elevated range from the Five Knolls, and Kensworth Hill, 904 feet,
by the heights above Zouche’s Farm, 850 feet, towards Luton, and thence to Whitehill Farm, on
* At Muswell Hill, on the north of Highgate in Middlesex, an accumulation above the Lon-
don clay, includes worn fragments of granite, porphyry, micaceous sandstone, mountain-lime-
stone, coal, lias, and chalk, with many of the characteristic fossils of those formations: the chalk
especially being so abundant, as to give the whole a chalky character.—Mr. Spencer, in Proceed-
ings of the Geol, Society, 1835—6; vol. ii. p. 181.
294 Dr. Firron on the Strata below the Chalk.
the north of that village, and Lillihoe in Hertfordshire, an Ordnance Station 604 feet above
the sea.
The Lower chalk, on which the village of Dunstable is placed, runs from Totternhoe on the
south-west of the main-road, through Houghton Regis, Upper Sundon, and Streatley, on the
north-east of it.
On the north-east of Totternhoe mines are driven into the hill at the bottom of the chalk, for
the purpose of extracting a bed of uniform light greenish-grey, marly and sandy, firestone, from
seven to ten feet thick. The strata are traversed by numerous cracks, which seem to pervade
the hill, and indicate disturbance,—or perhaps the effect of subsidence.
The Gault, in Smith’s map of Buckinghamshire, occupies a large part even of the higher ground
between Whitchurch and Wing. The Lower green-sand runs out without interruption from Whit-
church to Winslow, and is continued thence by Drayton, Parslow, and Soulbury, to the south of
Leighton. On the north of that line, a denudation on the course of the Little Ouzel river having
cut down to the subjacent clay, breaks in upon the outcrop of the sands, which would otherwise
have been continuous from Winslow to Brickhill, and the mass of the Woburn sand-hills. Be-
yond the two tracts at present continuous, several] outlying patches of sand, some miles distant
from each other and from the general escarpment*, are ascribed to this formation in the map;
all of which, as well as the wider tract between Winslow and Leighton, deserve examination, for
the purpose of ascertaining whether any of the Wealden beds are to be found there.
The greatest expanse of the Lower green-sand in the midland counties, occurs between Leighton
and Ampthill in Bedfordshire ; rising, at the Ordnance station on Bow-Brickhill, to the height of
685 feet above the sea,—or about 430 feet above the lowest point in the valley on the west of the
escarpment near Fenny Stratford. One of the most remarkable subordinate beds of the forma-
tion in this neighbourhood, is Fuller’s earth, which, when I was there (in 1824) was brought out
by mining from the north-west escarpment of the sand-hills, near Hogstye-end, between the main
road from Woburn to Northampton, and that from Hockliff to Stony Stratford.
Fuller’s earth Pit, near Woxsurn.
Ft. In.
1. Sand; nearly uniform, greenish-grey, and yellowish, including consolidated masses 130 0
of sand-rock, and dipping to the east and south. ........++eeeee0+++++ about
2. Fuller's earth.
a. “ Top” of inferior quality ; not diffusing itself in water till after it has ]
been dried: unfit for the purposes of the clothier .............-05 3.0 |
10
b. Ferruginous? clay ......... Beto cesib is eet (ors, soecseceeseveevabout 0
c. Fuller’s earth, of the best quality, very light olive green; (sold at the |
pit-mouth to cloth-manufacturers, for one shilling per cwt.) ..7ft.to 9 04
4. “ Bottom”; hard quartz or sand-rock ; the equivalent, probably, of the chert of the 5 0
Kentiand ‘Surrey sand-hillles ce pisitatia’ «le vlesfoitles bletn we btets bieyatave exe 2 ft. to
. Sand, like 1; thickness not ascertained.
or
The Geological place of the Fuller’s earth is here, therefore, nearly the same with that of
* ‘These outliers are represented on the Buckinghamshire map by patches of colour, each
about half a mile in diameter, at Roundhill, Whaddon, Totternhoe, Wroughton, Milton-Keynes,
Broughton, Moulsoe, and Astwood. In Mr. Greenough’s map, (1st edition,) both Winslow and
the heights of Whadden Chase on the north of that town form a portion of the tract coloured as
Oxford clay; but this, no doubt, requires correction.
Dr. Firron on the Strata below the Chalk. 295
Nutfield described above (141.); which, however, is thicker than this of Bedfordshire, and is
continued through a much larger space. I did not find here any of those nodules of sulphate
of barytes, which are frequent in the earth of Nutfield; and in neither of these two situa-
tions, does this bed contain the great number and variety of fossils by which the Fuller’s earth
at the bottom of the Lower green-sand is distinguished, at Atherfield in the Isle of Wight. In
the sands of this part of Bedfordshire silicified coniferous wood is frequently found in large
detached pieces.
These pits have continued to supply Fuller’s earth for more than a hundred years. They were
described, in 1723, by Dr. Holloway, in a letter to the celebrated Woodward, which is remarkable
in the earlier history of stratigraphical geology in England*: the author pointing out the paral-
lelism of the range of sands, to that of the chalk in the Chiltern hills, and suggesting distinctly,
upon geological grounds, the probability that other portions of the sand range would afford the
same valuable material; which, we have seen, coincides with the result of modern investigation.
The junction of the Lower green-sand and the Kimmeridge clay at Little Brickhill, (Section 21’ )
occurs at the north-west end of the village, in the garden of a small public-house called the
King and Queen, on the south of the road. Copious springs break out on the road about 50
paces above this house. The clay, which is here of a dark blue colour, includes very fine spe-
cimens of an Ostrea deltoidea, with Belemnites; and I was told that sand alternates with the
clay for a short distance below this point.
(154.) North-east of Bedfordshire.—The Lower green-sand, according to
Smith’s map, passes through the whole of this county, in a band which is in
general parallel to the chalk escarpment, and about five miles in width;
but its apparent dimensions vary much, in consequence of the irregular en-
croachments of the gault over the surface ; that stratum, immediately on
the north of Section 21, extending northward from the little village of Heath,
through Potsgrove and Froxfield, to Steppingley and Flitwick. Again, on
the east of Ampthill, an insulated portion of clay, (the colour of which, in
Smith’s map, is intended either for Gault or Kimmeridge clay,) stretches
in a north-eastern direction from around Maulden to South Hill, crossing the
great London road to Bedford, about the 43rd milestone. Since, however,
the full development of the Lower green-sand in Bedfordshire renders it
probable that the subdivisions of the Kentish coast may be found also in
this country, it may deserve inquiry whether some of these detached por-
tions, which have been considered as clay,—(especially between Maulden
and South Hill) may not belong to the middle, dark-coloured, and retentive
member of the sands; and the same question may be applied to a part, at
least, of the remoter tract assigned by Smith to the Gault, on the north of
Hockliff.
® This document has been inserted in Conybeare and Phillips’s “ Outlines”, p.138-9. Dr.
Woodward himself speaks almost poetically of the value of the English Fuller’s earth ; which, he
says, is beyond that of the Diamond mines of Golconda, &c. :—Edinb. Rev. 1819, vol. xxix. ;
and London and Edinb. Phil, Mag. 18382, vol. i. p. 155.
VOL. IV.—SECOND SERIES. 2e
296 Dr. Firron on the Sirata below the Chalk.
The course of the upper chalk is prominent on the north of east, from
Dunstable through Hitchin and Baldock, to Royston Down in Cambridge-
shire, which is 464 feet above the sea: but the boundary between the lower
chalk and the strata next below is not distinctly indicated by the external
features of the country. The change occurs on the main road from London
to Bedford, between Hitchin and Shefford, about the 37th milestone: and
there the difference in the elevation and general appearance of the ground
is very slight; in part from the very gradual rise of the strata, but chiefly
from the general diffusion of a coating of transported materials, which con-
ceals them.
(155.) List of Fossils from the Beds between the Chalk and the Oxford
Oolite, in part of Oxrorpsuire, Buckinenamsuire, and Beprorp-—
SHIRE-
[ Superficial Gravel. |
Ammonites (fragments). Chelsey, near Leighton, Bedf. (From the Gault ?.)
Belemnites minimus? (fragments). Stone Lane, north of Heath, Bedf.
B——. Gravel-pit north-east of Stewkley, Bucks: with fragments of chalk;
top of the high grounds, Brigginton, &c., near Leighton, Bedf.
Gryphea dilatata (much worn.) Gravel-pit north-east of Stewkley, Bucks.
G (fragments). Stone Lane, north of Heath, near Leighton, Bedfordshire.
G obliqua (much worn.) Gravel-pit north-east of Stewkley.
Ostrea deltoidea (fragments). Stone Lane, north of Heath, Bedf.
Serpula. Gravel-pit, north-east of Stewkley.
Terebratula. In rolled piece of sandy limestone. Gravel-pit north-east of Stewkley.
Spongia? Flint, enveloping Sponges?: worn. (No doubt from the upper chalk.)
Gravel-pit north-east of Stewkley.
[Lower Chalk and Chalk Marl.]
Ammonites lautus. In pale marly clay (chalk marl). Tetsworth, Oxf.
Terebratula semiglobosa. 'Tetsworth, Oxfordshire : in flint.
[Upper Green-sand. |
Inoceramus. Between Tetsworth and Thame, Oxf.; with Vermetus, in bluish grey
firestone.
Mytilus (new species?). Between 'Tetsworth and Thame: in soft gritty firestone.
Siphonia. Impressions of stems. Totternhoe, Bedf.
Vermetus. Between Tetsworth and Thame: with Inoceramus; in bluish grey stone.
[ Gault. |
Ammonites decipiens. Compton, Bedf. Mr. Goodhall.
Avicula. Compton, Bedf. Mr. Goodhall.
Crenatula. Compton, Bedf. Mr. Goodhall.
Dr. Firron on the Strata below the Chalk. 297
Exogyra conica. Compton, Bedf. Mr. Goodhall.
Inoceramus sulcatus. Compton, Bedf. Mr. Goodhall.
Nucula. Compton, Bedf. Mr. Goodhall.
[Lower Green-sand. ]
Siphonia, Casts of stem. Quainton pit, east of Ordnance Station: in the “ Bottom
rock.”
Wood, Coniferous, silicified. Woburn Sands, Bedf.
[Hastings Sand?. |
Cyclas, impressions of. Quainton, Bucks: pit at the highest part of the hill in grey
calciferous grit, “‘ Hardstone.”
Paludina elongata? Impressions. Same place and situation.
Serpula?. Coney Hill, Bucks. In grey uniform grit,—“ Sandstone”’.
[Purbeck Strata. |
Astacus?. Whitchurch, Bucks. In freshwater limestone, “‘ Pendle”, with worn par-
ticles like oolite.
Astarte. Same place and situation.
Cyclas media, Hartwell, Bucks; with Modiola. Whitchurch; with Cypris Val-
densis. Weedon; in stone like the “ tilestone ’’ of Ladydown, and the “ slate”
of the Isle of Purbeck.
C. elongata. Whitchurch, Bucks.
C—— parva. Horton’s Pit, near Bishopstone, Bucks; in slaty soft limestone.
Bishopstone (Dr. Lee’s pits) in soft bluish stone. In great numbers at Weedon,
in the “ Pendle”. Whitchurch ; impressions in freshwater limestone, with worn
rounded particles. Quainton; Western Pit, in the “ Pendle”’.
C— (a large species). Quainton, West Pit. Whitchurch, Bucks, Haddenham,
Bucks: in slaty limestone. Garsington, Oxf.: in the “ Malm”.
Cypris Valdensis?. Whitchurch, Bucks. Bishopstone, in soft bluish shale, Quainton.
C—— (species uncertain). Combe Wood, and Garsington, Oxf.: in the “‘ Malm”’;
with Paludina elongata. Denton, Bucks: in slaty soft clay. Weedon; in stone
like the ‘‘ Tilestone ”’ of Ladydown, and the “ slate”’ of Purbeck. Ford, numer-
ous. Horton’s Pits, Bishopstone in sub-oolitic ; stone: and in soft bluish slaty
stone, at Dr. Lee’s pit. Southwarpe. Quainton. Whitchurch.
Limnea?. Garsington: in the “Malm”’,—the representative of the “Cap” of Port-
land.
Melanopsis?. In dark-brown clay above the Portland strata. Road from Whitchurch
to Winslow.
Modiola. Remains of two or more species, one deeply striated. Garsington and
Combe Wood, Oxfordshire: in the “Malm.” Hartwell and Bishopstone,
Bucks. Southwarpe: in soft fissile limestone. Whitchurch. Quainton: a small
species in tough sandy clay: in the bottom of the “‘ Heath’’, over the “‘ Pendle ”’.
292
298 Dr. Firron on the Strata below the Chalk.
Mytilus Lyellii? Pl. XXI.f.18. Bishopstone: Dr. Lee’s pit. Near Whitchurch,
on the road to Winslow: numerous; in light greenish grey, alternating with
dark, tough clay, over the top of the Portland strata.
Another species, smaller and narrower than M. Lyellii. Combe Wood,
“Malm”. Dinton, Bucks. Bishopstone. Horton’s Pit; in slaty soft limestone.
Dr. Lee’s pits. Weedon. Whitchurch. Quainton.
Ostrea expansa. Horton’s Pit, Bucks. (Qua. in Portland-stone ?)
O—— (thin-shelled). Combe Wood: ‘ Malm”’.
O— (fragments of another species). Whitchurch, Bucks; in the “ Pendle.”
Garsington, Oxfordshire: “ Malm”’.
Paludina elongata. Combe Wood, and Garsington: in the ‘‘ Malm”; casts, with
Cypris. Southwarpe, Bucks. Bishopstone, pit near Morton’s.
Impressions of another species? Southwarpe, Bucks. Horton’s Pit: in
freshwater limestone. Quainton: in the grey uniform grit; Que. Hastings
M-
Je
sand.
(a ribbed species). Garsington and Combe Wood, Oxfordshire: in the
‘“¢Malm’”’.
Planorbis. Garsington and Combe Wood, Oxfordshire: casts in the “Malm”;
Horton’s Pit, near Bishopstone, Bucks.
Potamides carinatum. (Melanopsis, Min.Con.) Horton’s Pit, Bishopstone, Bucks.
Psammobia?. Garsington: “ Malm”’.
Unio. Bishopstone, Dr. Lee’s Pits: in soft bluish slaty stone. Quainton.*
P.
Fisues. Bones; impressions only. Southwarpe, Bucks: in soft earthy fissile lime- —
stone.
Vertebre. Whitchurch, in freshwater limestone, “‘ Pendle ’’. Coney Hill:
in calciferous grit.
Scales. Bucks: Bishopstone, Ford, Horton’s Pit, in oolitic stone: Dr. Lee’s
pits; in soft bluish slaty stone. Whitchurch in the “Pendle”, with worn
roundish particles. Quainton: pit top of the hill; in the “ Hardstone”.
Reptives. Portions of a spongy bone, probably Saurian. Garsington, Oxf.: in the
‘¢ Malm’.
Priants. A specimen, represented in P]. XXII. f.11., the nature of which is still
doubtful. It was bought at Quainton, Bucks, and said to be from the stone-pits
at the hill-top; but the precise place was unknown. Nort siliceous: effervescing
with acids ; and in this respect different from the Cycadee of Portland.
* Besides the shells above enumerated, the following were found in the strata representing the
fo)
Purbeck series, within the tract now under consideration; viz. Bivalves—of two or three species
probably new, but too indistinct to be determined,—at Combe Wood, Oxfordshire; Bishopstone,
Weedon, Whitchurch and Quainton, Bucks. Spiral univalves—at Garsington and Combe Wood,
Oxfordshire, (specimens exhibiting beautifully the internal column of the shell); at Great
Hazeley, Oxfordshire, with oolitic particles; and on the road from Whitchurch to Winslow,
Bucks,—(a new Paludina ?)
Dr. Firron on the Strata below the Chalk. 299
Impressions of very narrow leaves. Great Hazeley, Oxf. ; in fissile clay, re-
presenting, probably, the Fuller’s earth of the Lower green-sand.
Trees. At Brill, the trunk of a large tree converted into lignite, was found
in bluish grey clay. A most remarkable specimen, 40 feet long ; at first entire,
with numerous branches; but when I saw it, split into small fragments from de-
composition of the pyrites.
Wood. Coniferous, silicified wood, precisely like that of Portland, is found
in fragments, in the “ Malm’’, at Garsington, above the Portland stone, and
along with portions of freshwater limestone.
[Portland Stone. ]
Ammonites biplex. Road near Walton turnpike, Bucks.
A—— giganteus. Oving and Dinton, Bucks: with Exogyra nana, in sandy
stone.
A
Langcombe, Oxfordsh. Great Hazeley, Oxf.: in grey concreted sand.
The Warren, near Stewkley, Bucks: in limestone.
Arca (new). Stone-pits west of Great Milton: a cast in oolitic stone.
Astarte cuneata. Beneath Garsington, Oxf.: in concretional stone. Brill, Bucks: in
hard compact limestone.
Buccinum naticoide. PI. XXIII. f. 4. Whitchurch, Bucks. The Warren near
Stewkley ?.
B——. Quainton.
Cardium dissimile. Quainton, Bucks. Brill. Long Crendon: a cast, in grey, very
sandy stone. Bishopstone, Moreton’s pit: a cast. Tring, road near Walton
Turnpike. The Warren near Stewkley.
Cytherea? rugosa. Pl. XXII. fig.13. Southwarpe, Bucks.
Exogyranana. Dinton; Bucks: with Ammonites giganteus: in sandy stone.
E——. Whitchurch: adhering to Pecten lamellosus.
Gastrochena?. Denton, Oxf. : perforating Perna quadrata. Garsington: with Pecten
lamellosus ?.
Gervillia aviculoides. Langcombe, near Oxford: in calcareous spar.
Gryphea dilatata. Langcombe. A young shell; in Portland stone ?.
Lucina Portlandica. PI. XXII. fig.12. Southwarpe, Bucks.
Modiola (large). Denton, Oxf. Whitchurch, Bucks: in white stone.
Mytilus. Whitchurch.
Natica elegans. Pl. XXIII. f.3. Great Hazeley; a cast.
Ostrea expansa. Bucks: Village of Stone; Whitchurch, with Pecten lamellosus ;
Quainton; Brill; Horton’s pit, near Ford; the Warren near Stewkley, Bedf.
O—.. Remains ofa thick-shelled species are found at Great Hazeley, Oxf.: in con-
cretions of gritty stone, in yellowish sand. Haddenham, Bucks. Dinton, with
Plicatula.
Panopea depressa. Brill.
i gibbosa. Brill: a cast.
300 Dr. Frrron on the Strata below the Chalk.
Pecten lamellosus. Oxfordshire: Denton, with Trigonia gibbosa; Garsington, with
Gastrochena. Bucks: near Towersey Windmill; Brill, with Exogyra, adher-
ing; Quainton, pit east of Ordnance Station,—in soft limestone ; Whitchurch,
with Serpula, &c., in white stone; The Warren near Stewkley.
orbicularis. Oxf.: Beneath Garsington; in concretional Portland stone, with
Astarte cuneata; Langcombe, with Trigonia clavellata, in sandy stone. Brill,
Bucks.
Perna quadrata. Oxf.: Garsington?; Denton, with Modiola, &c.; Great Hazeley,
in gritty stone. Bucks: Towersey, in bluish limestone, with pyrites; Long
Crendon, in very sandy stone; Brill; Quainton, ‘‘ West pit.”
Plagiostoma rusticum. Great Hazeley, Oxf.; in calciferous gritty stone.
Pleurotomaria: with large whorls, roundish and flattened. Casts occur at Brill,
and at Garsington.
P
P———. A more acute and larger species, Great Hazeley, Oxf., in calciferous
sandstone. Brill; and at the Warren, near Stewkley, Bucks.
Plicatula. Dinton, Bucks: a cast, same as in the “ Roche”’ of Portland.
Pullastra. Remains of shells, perhaps referable to this genus, have been found at
Cuddesden, Oxf., in sandy Portland stone; and at the Warren, near Stewkley,
Bucks.
Serpula. Remains of. Oxf.: Langcombe; Great Hazeley, in very sandy stone.
Bucks: Whitchurch; in white stone ; Haddenham, in calciferous sand; 'Tower-
sey, some specimens of great beauty; Coney Hill.
Siphonia?, casts of Stems: Quainton; Bucks: in soft calcareous sandstone, “‘ Bottom
Rock’’.
Terebra Portlandica. Pl. XXIII. fig. 6. Abundant everywhere in the Portland
stone of Oxfordshire and Bucks: at Combe Wood, Oxf.; Southwarpe, Whit-
church, Towersey, &c., Bucks.
Trigonia clavellata. angcombe, Oxf.: in sandy stone; with a Pecten.
T: gibbosa. Universal and abundant in the Portland stone. Oxfordshire:
Denton, Great Milton, and Combe Wood, immediately in apposition with the
“Malm.” Bucks: Brill; Long Crendon ; Whitchurch ; Quainton; Bishopstone.
imcurva. Quainton, Bucks.
Venus?. Beneath Garsington: in concretional Portland stone; with Pecten orbi-
cularis, and Astarle cuneata?. Quainton, pit east of Ordnance Station : in soft
limestone *.
ry.
Fisnes, Vertebre of. Coney Hill: in “‘ sandstone”’ calciferous grit.
Chimera Townsendii : (Buckland, Proceedings of Geol. Soc. vol. ii. p. 286.; and
Lond. and Edinb. Phil. Mag. 1836. (vol. viii.) p.4—7.) The beak has been found
in the Portland stone at Great Milton, Oxfordshire, bythe Rev. C. Townsend.
* Besides the foregoing, fragments of bivalves, too indistinct to be determined, were found in
the Portland stone, at Great Hazeley in Oxfordshire; and at Haddenham, Southwarpe, Stone,
and Quainton, Bucks.
Dr. Firron on the Strata below the Chalk. 30)
Rertites. Bone of a Saurian. Great Hazeley: in ferruginous stone.
[Portland Sand. |
Ammonites bipler. Oxf.: Dropshot, near Thame, in grey sandy limestone, with
numerous green particles, and small pebbles of quartz. Bucks: Dunton, in
greenish stone, with dark particles ; Quainton, with a Trigonia.
A-———_ giganteus. Oxf.: Dropshot, (very large specimens): in dark grey lime-
stone, with green particles and pebbles of black chert*; Shotover; in grit.
Bucks: Brill; Whitchurch; Dunton; in greenish grey stone, with dark par-
ticles. Quainton.
i ? Dunton, Bucks: in greenish grey stone, with dark particles.
Avicula. Oxf.: Shotover, with Serpula and a Pullastra? in sparry grit. Bucks:
Whitchurch ; large, a cast.
Buccinum naticoide. Pl). XXIII. f.4. Brill: a cast.
Cardium dissimile. Oxf.: Langcombe ; Dropshot, casts, in matter almost wholly green.
Bucks: Hartwell Lodge, with Trigonia gibbosa, in bluish grey stone ; Dunton ;
Brill, with Serpula ; Whitchurch; Muswell Hill; Quainton.
Cytherea? rugosa. Pl. XXII. f.13. Hartwell, Bucks.
Gastrochena. The Warren, near Stewkley, Bucks: and Shotover Hill, Oxf.: in
Perna quadrata.
Lucina. Village of Stone, Bucks.
Mytilus (probably a new species). Denton Village, Oxf.: with Trigonia clavellata.
Brill, Bucks.
Ostrea solitaria. Dunton, Bucks.
O——. Species indistinct. Shotover, Oxf.,with Serpula, &c. adhering to Ammonites
giganteus, and bent into its inequalities. Brill, Bucks.
Panopea?. Whitchurch, Bucks.
Pecten lamellosus. Dunton, Bucks: in greenish grey stone, with dark particles: and
in a mass almost entirely composed of green matter (silicate of iron), with Perna
quadrata. Muswell Hill; Brill ?.
i, Another species ?. Shotover: with Serpula, &c.
Perna quadrata. Oxf.: Dropshot, near Thame, in dark grey limestone, with nu-
merous green particles and pebbles of black chert; Shotover, in sparry grit,
perforated by Gastrochena; witha Venus. Bucks: Muswell Hill, in stone ;
containing green particles; the Warren; with Gastrochena, in grey stone;
Dunton; in a green friable mass, and in greenish stone, including fragments
of black flint, with Pecten lamellosus.
Plagiostoma obliquatum. Near Thame, Oxfordshire.
P—— rusticum. The Warren near Stewkley: in bluish grey stone, with minute
dark particles.
* At the quarries in the Portland-sand at Barley Hill near Thame, imperfect worn casts of
several bivalves, in black flint or chert, are found in the sandy stone, along with pebbles of the
same substance.
302 Dr. Firron on the Strata below the Chalk.
Serpula. Shotover, with Ostrea ; Brill; Coney Hill; Dunton, in green matter.
Trigonia clavellata. Wong Crendon; Casts in conglomerate, with siliceous pebbles ;
and in sandy limestone, with numerous green particles. Dunton, Bucks; with
Mytilus.
ih gibbosa. Denton, Oxf. Hartwell, Bucks; with Cardium, in bluish grey
stone. Dunton, and Whitchurch, Bucks.
T. gibbosa: a variety, less oblique. Brill.
T. incurva. Brill, Bucks.
Venus. Shotover Hill, Oxf.; with Perna quadrata. Hartwell, Bucks; with Tri-
gonia, in soft stone.
[Kimmeridge Clay. |
Ammonites bipler. Clay-pits near Aylesbury. Road from Aylesbury to Whitchurch.
A= biplex (small). East Claydon, Bucks; 20 feet from surface, in clay:
A——— giganteus?. Clay pits south-west of Stewkley, Bucks: in blue clay.
A—— Gulielmi. East Claydon, Bucks: in clay ; beautifully iridescent.
A———— like Gulielmi. Quainton, Bucks.
A———— Selliguinus. Clophill, Bedf. Mr. Goodhall.
A——— (probably new). Clay-pits, south-west of Stewkley, Bucks, in blue clay.
Aptychus (Von Meyer). Pl. XXIII. fig.11. Roadside between Aylesbury and
Whitchurch, about a furlong from Hardwick. Clay pits south-west of Stewk-
ley ; fragments of very large specimen.
A—— (a smaller species ?). Roadside between Aylesbury and Whitchurch.
Exogyra nana. Between Aylesbury and Whitchurch: with Ostrea levigata.
E virgula. Pl. XXIIL f.10. (Gryphea virgula of Deshayes.) Roadside be-
tween Aylesbury and Whitchurch. Clay-pits south-west of Stewkley: good
specimens in bluish grey clay.
Gryphaa bullata. Clophill, Bedf., Mr. Goodhall.
G dilatata. Wolvercot, Bucks?. Clophill, Bedf.
G— virgula. See Exogyra.
Mytilus. Quainton.
Ostrea deltoidea. Aylesbury Clay-pits: a distorted form of the shell. Little Brick-
hill, clay immediately below surface: fine specimens.
O—— levigata. Between Aylesbury and Whitchurch.
O———\—— (young). Thornborough, Oxf.
O—— leviuscula (young). Road from Aylesbury to Whitchurch: in blueclay. Little
Brick Hill, Bedf.
O—— near to deltoidea, but wider at the hinge; still very thick. “Ina bed of stiff
“ clay, about two miles north-north-west of Leighton, under the red sand of the
“heath, and about 20 feet above the river.” Mr. W. Mathews of Leighton:
Roadside between Aylesbury and Whitchurch ; Bucks.
Panopea depressa, Headington Quarry, Oxf.
Pecten arcuatus. Vicinity of Aylesbury.
P Lens. Little Brickhill. Brow of the hill, in clay immediately below sand,
Dr. Firron on the Strata below the Chalk. 303
Pleurotomaria reticulata (Trochus, M.C.) Headington; Oxf.
Serpula tetragona. Clophill, Bedf., Mr. Goodhall.
S tricarinata?. Roadside between Aylesbury and Whitchurch. “In stiff clay,
“about two miles N.N. west of Leighton.” Mr. W. Mathews.
Fisues. Chimera Egertoni: (Buckland, Proc. of Geol. Soc. vol. ii. p.206.; and
Lond. and Edinb. Phil. Mag. (1836), vol. vill. p.4—7.) Shotover-hill, Oxf.
Psammodus reticulatus: (Agassiz; in Egerton’s Catalogue of Fossils); Shot-
over-hill, Oxfordshire.
Reptives. Bone of a Saurian. Clay-pits south-west of Stewkley : part of a flat bone.
Plesiosaurus; Vertebre. Headington Quarry, Oxf.
Coprolite ; or coproid masses of phosphate of lime. Beneath Whitchurch. Clay-
pits south-west of Stewkley: one specimen occupying the cavity of an Am-
monite.
[Oxford Oolite. |
Melania Heddingtonensis. Wheatley, Oxf.: cast of part of interior.
Ostrea? Thornborough, Oxf. Wheatley; in compact, blue, sparry oolite.
Pholadomya deltoidea. Headington (Coral rag).
Spongia?. Wheatley, Oxf.: in sandy stone.
Terebratula tetrahedra? Thornborough, Oxf.; and Wheatley.
C4M BRIDGESHIRE™*,
(156.) In this county, as in Bedfordshire, the Wealden and Portland groups
are wanting; and the strata, rising with a very slight inclination from the
south of east, and thinning off near their outcrop, are frequently cut through
by denudation, so that distant outliers, especially of the lower green-sand, are
frequent. Mr. M’Lauchlan, who was engaged in the Ordnance Survey of this
part of England, remarks, that the summits of the chalk decline rapidly in
* T am indebted to my friend Professor Sedgwick for the greater part of the following infor-
mation respecting Cambridgeshire. The only publications connected with the geology of the
county, are a paper by Professor Hailstone, Geolcgical Transactions, 1st Series, vol. iii. p. 243, &c. ;
a short paper on the Northern division of Cambridgeshire, by Mr. Lunn, (1818),—Geol. Trans.,
Ist Series, vol. v. p. 114, &c. ; an account of some verbal communications made to the Cambridge
Philosophical Society, London Philosophical Magazine, (1835,) vol. vi. p. 74; and the report of
a field Lecture by Professor Sedgwick, which appeared in the Cambridge Chronicle of the 10th
of April 1835.
Hunrinapowsuike I have passed over, not having myself examined that county ; and I am not
acquainted with any publication specifically relating to it, except Mr. Smith’s county map. A
small space at the south-eastern verge of the county, on the confines of Bedfordshire, is occupied
by the Lower green-sand ; but all the tract adjoining Cambridgeshire is assigned by Smith to the
Oak-tree clay, a term which I believe denotes, in this case, the Kimmeridge clay.
thereabouts are much obscured by transported matter.
VOL. 1V.—SECOND SERIES. 2R
The strata
304 Dr. Firron on the Strata below the Chalk.
height on the north-east of Bedfordshire: Kensworth Hill, south of Dunstable,
being 904 feet above the sea at low water ; the hills east of that town 850 feet;
Lilleyhoe, 664; Barkway, Windmill-hill, 513; the station near Royston,
A84 feet; Balsham, on the east of Cambridge, 380; Newmarket station,
267; Brandon in Suffolk, 190 feet. The summits of the lower chalk suc-
cessively decline in the same direction ; Orwell station being 250 feet, Chapel-
Bush, near Haslingfield, 220 ; Swaffham-Prior (near Reach), 140. And the
lower green-sand also falls rapidly : the hills near the outcrop at Bow Brick-
hill being 683 feet high; that of Haddenham on the north of Cambridge,
133 feet; and the general surface of the lower green-sand, which tops the
hills near that place, ranging from about 60 to 120 feet; at Ely 75 feet.
The level of the Cam, upon the gault, at Cambridge, is only 243 feet above
the sea at low water on Lynn Deeps; that of the Kimmeridge clay at Ely
Bridge, 14 feet; and of the Cam, at Upware, probably not more than 12 feet.
So that if the sea were not dammed out by artificial means, a great part of
the marshy tract on the confines of this county, Huntingdonshire, and Nor-
folk, would be inundated at high water, as appears to have been the case at
no very distant period. ‘The hydrography and drainage of this low tract,
which are intimately connected with geological principles, have been the
subject of some valuable publications, but do not fall within the immediate
scope of these pages.
(157.) Another general circumstance which characterizes the north-west of
Cambridgeshire, is the great extent and varied composition of the transported
masses with which the strata are in many instances thickly invested. This
superficial deposit includes worn masses of greenstone, with fragments of
many of the lower members of the English series,—and rounded pebbles of
chalk, in such abundance as to form a very large proportion of the entire
mass. With these stony substances are fragments of the fossils of most of
the strata, Belemnites, large Gryphites, the Ostrea (or Gryphite) of the Ox-
ford clay, and portions of the skeletons of Elephants, Rhinoceros, Hippo-
potamus, Deer of several species, gigantic Oxen, and of the Horse.
The mass thus composed forms many of the hills on the borders of Cam-
bridgeshire and Essex, and occupies a great part of the platform which runs
along the confines of the former county and Huntingdonshire; a brown
variety of it obscures the junction of the gault and lower green-sand on the
west of Cambridge, forming an upland which extends trom Bourne by Toft
and Hardwick to Dry Drayton, where it declines into the plain*.
* Mr. Hailstone mentions particularly, that the deposits just described are perfectly distinet
from that which occurs above the Gault in Cambridgeshire. ‘The former are very well known
Dr. Firron on the Strata below the Chalk. 305
These accumulations, it will be perceived, closely resemble those already
mentioned in the account of Buckinghamshire and Bedfordshire, especially
near Leighton, and at Stewkley. They occupy, in fact, a great extent of the
surface, and form one of the most interesting geological deposits throughout
the East of England ; but there are circumstances respecting their relations
to each other, and to the crag of Norfolk and Suffolk, which still remain to
be investigated and explained.
(158.) The strata therefore which are found below the chalk in Cambridge-
shire, consist of Chalk, Upper green-sand, Gault, Lower green-sand, Kim-
meridge clay, Oxford oolite, and Oxford clay ; the last occurring only in a few
places, and in the remote part of the county, in which it is the lowest member
of the series. The sections, Plate X. a, Nos. 22, 23, and 24, explain the
general relations of these strata, but have no pretensions to accuracy of local
detail. ‘The following notes describe some of the principal appearances con-
nected with the object of this paper; and the publication of the Ordnance
maps of the county will no doubt soon lead to the complete examination of
it by the geologists of Cambridge.
Chalk.—The upper chalk range passes from the heights near Dunstable, through the north-west
of Hertfordshire, by Hitchin and Baldock, to Barkway and Royston Downs, and thence by Balsham
and Newmarket into Suffolk. Mr. M’Lauchlan informs me that the chalk ridge at Thorfield (about
570 feet high) is an anticlinal line, and that the overflow of water in Wardington Bottom, near
Newsell’s-bury Park, while the rest of the country is dry, renders it probable that some of the
lower beds are there brought up to the surface. On the Ordnance maps two ridges are distinctly
marked, which meet thereabouts at an angle; one passing from Berry Barn through Norfield to
Barkway Mill (313 feet high), the other, striking off from Thorfield for about a mile towards
the north, turns suddenly to the east, to the group of hills above Royston and Burley, and is
continued thence to the north-east through Chishill, 470, and Heydon, 480 feet. ‘The lower tract,
in the angle between these ridges, from Newsell’s to Known’s Folly, may possibly be a valley of
elevation like those of Kingclere described by Dr. Buckland.
The outcrop of the lower chalk and chalk marl, is nearly parallel to the range of the upper
strata, and to that of the heights above mentioned ; its general course being from the neighbour-
hood of Orwell, through Haslingfield, Cherry Hinton, and Bottisham, to Reach on the margin
of the Fens. Thence, from about Milden-hall in Suffolk, near the confines of Cambridgeshire, to
Hunstanton, on the north-west coast of Norfolk, a distance of about forty miles, the direction of
the chalk escarpment is nearly from south to north.
The chalk which forms the principal part of the lower hills in Cambridgeshire, bears the local
name of “Clunch.” It is described by Mr. Hailstone as being harder than common chalk, and
usually of a grey colour. It affords, as the lower and marly chalk is found to do in many other
places, remarkably good lime: and it would seem that some of the lowest beds, which bear the
name of Clunch, agree in their properties, as in geological position, with the firestone of Surrey,
throughout the Isle of Ely under the name of White Gravel, (the latter is Red); and, Mr. Sedgwick
states, are older than the beds of flint gravel in Cambridgeshire.
ZR
306 Dr. Firron on the Strata below the Chalk.
being applied to the same purposes in the construction of fire-places, &c. Very large pits of clunch
have been opened at Reach, on the immediate confines of the Fens, and on the line of Section
No. 23.
Upper greensand. This formation here differs from that of some of the more southern counties,
in its much smaller thickness, in the absence of chert, and the comparative rarity of green
particles, which are here confined to a stratum not more than eighteen inches thick, by which the
lowest beds of the chalk are separated from the gault, as is well seen in the section exposed at the
Castle Hill, Cambridge. The presence of this green bed, however, is remarkably constant;
and it contains many fossils, some of which are common to this formation, and to the chalk,—
but others, at least in this country, are confined to the sand; among which, Mr. Sedgwick
informs me, Hippurites are found near Bottisham.
Gault.—The term Gault, or “Galt,” adopted by Mr. Smith as the denomination of this re-
markable stratum, is in Cambridgeshire the popular name for the blue clay, which comes in
between the green bed last mentioned, and the ferruginous (Lower green) sand. Its thickness
and relations have been well ascertained in this county, from the numerous borings to obtain
water, which pierce through the clay to the sand below, especially on the line from Basingbourne
north-west of Royston, through Meldrith, and thence towards Cambridge. Its average thickness
is about 150 feet*, which is nearly the same as on the south-eastern coast: but the surface of
this stratum is much obscured by superficial gravel and a thin coating of the lowest chalk; and
good specimens of its fossils are rare, as the upper beds contain but few. Among those, how-
ever, which I found between Cambridge and Ely, are the characteristic Anmonites of different
species, 4. inflatus, A. lautus, A. varicosus ; Exogyra conica; and spines of an Echinus. In
the museum of the Geological Society is a specimen from the Gault near Cambridge, which
M. Agassiz has found to belong to a new species of Chimera +.
Lower green-sand.—This stratum occurs throughout this county between the Gault and Kim-
meridge clay, in the form of sand of different shades of grey and brown, but chiefly as a coarse
ferruginous compound of quartzose sand, cemented by hydrate and oxide of iron, and more or
less indurated. At the top, however, is some green-sand, as appears from the first discharge from
the borings through the Gault, after the rod has passed the clay ; the water subsequently obtained
depositing an ochreous matter, of the colour of the Woburn sands. I have no fossils from this
stratum in Cambridgeshire. Its thickness is obviously much less than in Bedfordshire ; and its
internal composition was not discernible in any of the sections which I saw; but at Ely I found
numerous concretional blocks, precisely resembling Kentish rag ; which had been obtained, I was
informed, from a place near the gallows on the south-west of the town, in a deposit which there
forms an extensive outlier over the Kimmeridge clay, and consists of coarse, ferruginous, and sili-
ceous sand and conglomerate, containing a large proportion of brown iron-ore (hydrous oxide of
iron), like that of Shanklin in the Isle of Wight. At Ingoldsthorpe in Norfolk, where the thick-
ness of the stratum is probably not greater than at Ely, it is said to contain Fuller’s earth t.
Quitting Potton, in Bedfordshire, Mr. Lunn states §, ferruginous sand is observed within the
* Mr. Lunn supposes the thickness to be 200 to 220 feet.—Geol. Trans. vol. v. p. 115.
aE Proceedings of Geological Society, 1835, vol. ii. p- 205, note.
{ In Mr. Greenough’s geological map, sulphate of barytes is mentioned as occurring on the
main road from Royston to Huntingdon, at Longstow near Caxton. This mineral, it will be recol-
lected, occurs in the Fuller’s earth at Nutfield in Surrey, ((51.) p. 141.); a situation which answers
to that of the Lower green-sand on the line of section No. 22.
§ Geol. Trans. Ist Series, vol. v. p. 114, &c. 7
Dr. Fitton on the Strata below the Chalk. 307
borders of Cambridgeshire, at Gamlingay, with Gault resting upon it; ‘ and in some of the pits,
“the line of junction is as well defined as that of two immiscible fluids”; but the sand contiguous
to the clay is more highly impregnated with iron than the lower part, and is cemented by the oxide,
so as to form a hard rock. Leaving to the south-west the two villages of Hatley, both on
the Gault, the boundary passes between Little and Great Gransdon, and west of Caxton, (which
is on the clay), through the north-west sides of the parish of Eltsley, by Passworth St. Everard’s,
and Passworth St. Agnes, to Hilton and Fenny Drayton. In the parish of Fenny Stanton and
that of Croxton, a bed of clay (Gault?) rests on the sand. The sand can be traced across the
lower country, in a direction nearly parallel to the chalk, from Caxton (Section No. 22.) by Co-
nington, and Long Stanton, through Cottenham and Denny Abbey, where the surface is occupied
by low hillocks of gravel; and on the north of those places it forms the summit of many of the
heights of small elevation on the south-eastern verge of the Fens. Thus at Haddenham, the hill,
133 feet high, is capped with sand; and the prolonged height, or ridge thence to Aldreth, called
“the Sandy-way,” about 122 feet, is likewise composed of it. The junction of the sand and
subjacent clay is well seen, Mr. Sedgwick states, at the clay-pit on the east of Ely; and sand
is visible in the drains from about the fifth to the ninth milestone, along the road from Littleport
towards Downham, cutting across the Fens on the north-east of Ely, in a direction corresponding
to the previous course of this formation near Cambridge.
Kimmeridge clay.—This occupies all the lower tract on the north and west of the line of sands
above mentioned, as on the course of the Ouse, or Old West river, from Fenny Stanton and Ho-
lywell on the west, to its junction with the Cam at Thetford, and thence towards Ely. Sec-
tions are of necessity rare; but a very good one, exhibiting the junction of the clay and Lower
green-sand, is exposed in the pits east of Ely. On the west and south-west of Ely the clay is
capped in many places by sand, in the form of outliers, on the summits of the heights, which here
range from about 120 feet to 50 (see the list in the Appendix C.): and the clay is continued
uniformly through their bases, to a point north-west of Haddenham, on the road to Chatteris,
where it is succeeded by the Oxford oolite.
Oxford oolite.—A remarkable exception to this uniformity of structure occurs at Upware, on
the Cam, about three miles north-west of Reach (see the Section, Plate X.a. No. 24.); where the
upper strata of the Oxford oolite make their appearance, in a low ridge extending for about three
miles north of Upware, in a direction nearly parallel to that of the Cam, which is here not much
more than 12 feet above the sea at low water. The stone beds have been opened here in two or
three quarries; a very large one being near the river, and on the line of the section 24. The
strata are slightly inclined to the west of north, in a direction opposite to that of the beds below
the chalk. The stone here laid bare to a depth of about 10 or 12 feet, consists of a loose rubbly
limestone, of a cream colour, in some places coarsely oolitic, and containing many of the charac-
teristic fossils, for a collection of which I am obliged to Professor Sedgwick and Mr.M’Lauchlan :—
Spines of Cidaris; Corals; an Arca; Fusus, a new species; Gervillia aviculoides; Isocardia,
an acute species; Modiola; Ostrea gregarea; Pecten viminalis; Plagiostoma; Plicatula; Turbo
muricatus, &c.
The coralline beds (the proper “ Coral rag” of Smith) do not come up to the surface at this
place; but they break out, Mr. Sedgwick informs me, beyond Haddenham, going towards Chat-
teris; and he suspects that the shelly beds of this formation occur in some other places in the
county, between the Kimmeridge and the Oxford clays, from the occurrence of numerous bits of
the coral rag and of its fossils in the brown clay, which masks so much of the surface of Hunting-
donshire and Cambridgeshire, and in a condition which makes it probable that they had not been
drifted far.
308 Dr. Firtron on the Strata below the Chalk.
Oxford clay—The Oxford clay succeeds to the coral rag on the north-west of Haddenham, as
has been mentioned, and of Ely. It is the lowest stratum in Cambridgeshire, and forms the base
of the Great Bedford Level.
(159.) Chalk in Rutlandshire —The rise of the strata last mentioned, com-
bined with the general features and structure of Cambridgeshire, would seem
to indicate the final outcrop and disappearance of the upper members of the
Series ; but from a passage in a paper by Mr. Barker, published in the Philo-
sophical Transactions for 1791*, and quoted by Dr. Buckland {, it appears that
chalk has been discovered at Ridlington in Rutlandshire, about forty miles
from the general range of the chalk hills in Cambridgeshire and Norfolkf.
So that if this statement be correct, we might expect to find some of the beds
below the chalk, in the wide tract of intervening country. The only cir-
cumstance mentioned by Mr. Barker which throws doubt upon the suppo-
sition that this chalk is in its original position, is, that the flints, which he
states to occur “in rows, lying in it as is usual in the South of England,”
are “ broken, and not whole ones.” So that it is possible that the entire mass
may consist of transported fragments of chalk, and be analogous, but ona
much larger scale, to the loose pieces of that substance found by Mr. Cony-
beare in my presence during an excursion in Northamptonshire, near Sywell;
a place about thirty miles distant from the nearest point of the chalk
escarpment. Ridlington, where this patch of chalk is stated to have been
observed, is placed in Smith’s map of the county, on the verge of a platform
of the Lower oolite, resting immediately on the blue marl at the upper part
of the lias; and the map bears no indication whatsoever of any other
stratum.
* Vol. lxxxi.p. 281. + Geological Transactions, 1st Series, vol. v. p. 539.
t I shall here insert the whole passage, as the best mode of presenting the facts to the reader.
My. Barker, writing at Lynden, near Uppingham in Rutlandshire, says: “I did not know till lately
“* that we had any chalk nearer us than Moddingley”—(see Pl. X.a. No. 22.); “but several years
“‘ ago the people of Riddlington in Rutland, digging for stone to mend the roads, met with a bed of
“ chalk, at which they were much surprised, and did not know what it was, never having seen a
“ chalk-pit before. After I had heard of it, I went to examine the place, and found a regular chalk
** pit, with rows of flints lying in it as they are wont to do in England. The chalk is not soft, like
“* that they write with, but very much like that they dig about Baldock: nor are the flints so black
‘‘ as those in the South of England, but veined, of a light-coloured flint, and white; some parts
“much mixed with chalk, and are broken, not whole ones. ‘They may have dug the pit six yards
“long and two deep, but how far the chalk reaches I do not know.” Mr. Barker adds, that he had
seen a little patch of chalk a few yards long, in a bank by the road side, along the turnpike road near
Stukely, about three miles north-west of Huntingdon, which place is about twenty miles from the
nearest chalk-hills.
Dr. Frrron on the Strata below the Chalk. 309
Traces of the Wealden in Northamptonshire.—The preceding statement is rendered more in-
teresting by the discovery at Wansford in Northamptonshire, a place about ten miles east of
Ridlington, and thirty from the chalk-hills in Cambridgeshire, of a mass of calcareous grit,
containing an impression of Lonchopteris Mantellii*, a fossil species found by Mr. Mantell in the
grit of Tilgate Forest, Sussex, and hitherto peculiar to the Wealden strata; indicating therefore
the presence of that group at the distance of more than forty miles from the nearest point on the
south, at which its existence has yet been ascertained in England. For an opportunity of
examining the specimen in question, I am indebted to the kindness of Mr. Woodward of Norwich,
to whom it belongs ; and I find it to consist of crystalline calciferous grit, of a yellowish grey or
drab colour, containing a very large proportion of carbonate of lime,—which may very well have
formed a part of one of the concretions of grit subordinate to the Hastings sands. The form of
leaf of the plant is beautifully impressed upon the stone, and very well represented in the
plate of the Fossil Flora: and the only question is, whether the locality has been correctly
stated, which Mr. Woodward has no reason to doubt. It may be added, that the existence of
the Wealden in this new situation is rendered more probable by the occurrence of chalk in Rut-
landshire, at a point not less remote from the great body of that formation in the South-east of
England. :
Norrotx t.
(160.) The strata below the chalk appear only on the west of this county,
and the series is generally the same with that of Cambridge ; but the Upper
green-sand soon ceases to be conspicuous, or disappears altogether ; and the
Gault is so much reduced in thickness, and changes its character so remark-
ably, that it is only by means of its fossils and by tracing its continuity with
the more usual form of the stratum, that its identity can be ascertained. The
ferruginous beds of the Lower green-sand are sufficiently distinct, but the
formation is much thinner than in the south-eastern counties. No traces of
the Wealden or Portland groups have yet been found, nor are there any
* Lindley and Hutton’s Fossil Flora, (1835) vol. iii. p. 372. Plate 171.
+ The publications on the geology of Norfolk, besides the general maps of Smith and Green-
ough, and the County map of the former, relate principally to the eastern portion of the county.
But since these pages have been at the press, an excellent account of West Norfolk, by Mr.
R. C, Rose, of Swaffham, has appeared in the London and Edinburgh Philosophical Magazine’,
to which I beg to refer the reader who wishes for detail. The preceding papers relating to this
part of the county, are Mr. R. C. Taylor’s plate and description of Hunstanton Cliff, 1823°; a
paper by the same author, on the alluvial strata and the chalk of Norfolk and Suffolk’ ; and a list
of the fossils of Hunstanton, in Mr. Woodward’s Geology of Norfolk*. Some occasional notes
connected with the west side of the county, may also be found in the tracts more immediately
relating to the beds above the chalk.
1 Vol. vi. and vii. 1835—1836.
® Phil. Magazine, 1822, vol. lxi. p. 81—83,; republished in a tract on the Geology of East
Norfolk, 8vo, 1827.
5 Geol. Trans. 2nd Series, vol. i. p. 374—378.
* “ An Outline of the Geology of Norfolk,” 8vo, 1833.
310 Dr. Fitton on the Strata below the Chalk.
distinct indications of the Oxford oolite, between the Kimmeridge and Ox-
ford clays.
The line of hills, nowhere probably exceeding 600 feet in height, which
stretches for about forty miles from the chalk range of Cambridgeshire to the
north-west coast of Norfolk, bounds the fen-country like the low shore of a
sea ; and a very slight change of level would again convert the fens into a
shallow estuary, by the waters of which these hills would be washed at their
base. At present, the face of the heights is covered with vegetation, so that
it is only in detached spots casually exposed, that the strata can be seen.
Not having, myself, any good section of this part of the district, Mr. Rose
has been so good, at my request, as to prepare an enlarged copy of the
sketch annexed to his paper on West Norfolk, on the line from Swaffham to
Lynn, (see Pl. X.a, No. 25.); and I have inserted also a section and a
sketch of Hunstanton Cliff, (Plate X. a, No. 26; and X. b, fig. 12, a, b, andc,)
the only natural section that is visible upon the coast.
Deposits above the Chaik.—The portion of the fens immediately adjacent to the chalk-hills in
West Norfolk, bears the name of Marshland. It is composed of alternating beds of lacustrine
silt and peat, covering, in the vicinity of Lynn, a deposit of marine silt; the whole resting upon
a stiff clay, which incloses small nodules of chalk, and is obviously the same with the superficial
deposit, already described as including chalk fragments and being generally of similar com-
position, in Cambridgeshire and near Leighton; beneath which are the strata of Kimmeridge in
Oxford clay.
In a well, sunk and bored at Lynn, to the great depth of 630 feet, the detail of which will be
mentioned hereafter, a bed of the clay containing portions of chalk, was found beneath about 23
feet of sand, loam, and peat, and marine silt ; and the clay was, at the bottom, in immediate con-
tact with what Mr. Rose considers as the Oxford-clay, but with some doubt whether it may not
be that of Kimmeridge. For an account of the newer subaqueous deposits, and of the more
recent changes which the surface here is proved, by historical documents, to have undergone, I
refer to the publications of Mr. R. Taylor, Mr. Woodward, and Mr. Rose, in which references
will be found to preceding authors, some of whom are of very ancient date.
Chalk.—An account is given in the publications of this Society, of two borings in the south of
Norfolk, which illustrate the relations of the chalk to the beds immediately beneath it. One of
these, described by Sir H. Bunbury, was made at Mildenhall in Suffolk*, a spot about twenty miles
north-east of Cambridge, and thirteen from Ely, near the point where the chalk range changes
its direction from about south-west and north-east, and runs northward, to join the sea at Hun-
stantont. Another sectional list has been published by Mr. John Taylor, derived from a boring at
* Geol. Trans. 2nd Series, vol. i. p. 379.
+ The general course of the chalk escarpment in the Wolds of Lincolnshire (see a paper by
Mr. Bogg, Geol. Trans. Ist Series, vol. iii. p. 392.) and of Yorkshire, is from south-east to north-
west ; so that the line of its course in Norfolk may be considered as forming the bottom or most
eastern shore of a deep bay, (and the lowest part also of the range, with reference to the level of
the sea); from the extremities of which the escarpment diverges in both directions ;—north-
westward, for about ninety miles, to its final termination on the parallel of Flamborough Head ;
and towards the south-west, for more than two hundred miles, to the coast of Devonshire.
Dr. Firron on the Strata below the Chalk. 311
Diss, on the confines of Norfolk and Suffolk*, about five-and-twenty miles east of Mildenhall ;
through which place if a line were drawn on the line of dip, it would pass nearly through Down-
ham on the margin of the Fens. In this section, the entire thickness of the chalk was cut through,
and combining it with that at Mildenhall, the result stands thus ;—subject, however, to some un-
certainty, from the imperfect condition of the specimens brought up in boring.
Diss. Feet. MiILDENHALL. Reet.
mma, Clay ...... ain RAS 50 TY Sandy 10am». wesc eee Lines 1
MEDIC se ccc csc ssc eces 50 100
2. Chalk. II, Chalk.
a. Without flints, soft, marly. 100 a, White, without flints .. 35
b. With flints, in layers ope ee b. Yellowish, gritty...... 5
a yard from each other . e c. Grey, hard .......... 136 476
c. Grey,with occasional layers 60
of white: no flints......
d. Light bright blue chalk, TIL. a. Blue clay... + sei cee os 54
eng oy, with i 20 510 6. Ditto, darker and harder 10
white cha erator
[On penetrating the light blue clay,
the boring-rods sank rapidly, and wa-
ter rose to within 47 feet of the sur-
face. |
3. Sand;—characters not stated ...... 4
615
ce. Ditto, mixed with oy
10
sand 7h
250
IV. Green sand, with many fossils .... 11
V. Blue clay,abounding in fragments of
large shells, having a high polish. .
[Water coming in here, the work
was discontinued. |
9
270
The section at Diss is valuable, as it cuts through the entire thickness of the chalk, which is
here 510 feet; of which, it will be remarked, the uppermost 100 feet are marly and without
flints. The light blue stratum, 2. d, referred by Mr. Rose to the Gault, may, perhaps, rather
eorrespond to the lower portion of the chalk-marl, and to part of III. in the Mildenhall section ;
in which case 3. at Diss would represent the Upper green-sand. V.at Mildenhall is distinctly
referred by Sir H. Bunbury to the Gault, which he supposes to occupy the flat surface of the ad-
jacent fen.
Mr. Rose states that the chalk range in West Norfolk dips to the south-east, about five yards
in a mile; or about 1 in 350. He has requested me to mention that he considers the estimate of
the heights given in his paper as probably exceeding the truth; and at my suggestion, derived
from the levels in Cambridgeshire, he has reduced the altitudes in the section, Pl. X.a. No. 25.
The upper chalk of Norfolk includes the usual flint nodules; and among the larger flinty
masses are some like those described by Dr. Buckland, under the name of Paramoudra. Many
of the fossils of the uppermost strata, according to Mr. Woodward, are different from those of
what he has called the medial chalk, which also contains flints. Near Swaffham, the chalk
without flints, which seems to belong to some intermediate beds between the upper and lower
* Proceedings of the Geol. Soc. (1833-4), vol. ii. p. 93.
VOL. IV.—SECOND SERIES. 2s
312 Dr. Frrron on the Strata below the Chalk.
groups, forms a range of somewhat lower hills, on the west of that constituted by the superior
strata. It is hard enough to be used as a building stone, divides naturally into rhomboids, and
contains horizontal seams of argillaceous matter ; but Mr. Rose remarks, that although the hard-
ness increases progressively downwards, the increase is not regular nor uniform, some portions
as hard as any of the lower occurring in the upper part of it. His list of fossils from the chalk
with flints contains about 78 species; of which, according to Mr. Mantell, only 40 occur in the
corresponding part of the formation in Sussex.
The relations of the lower strata of the chalk are best exhibited in the section at Hunstanton
Cliff, which will be presently described. Mr. Rose’s list of fossils from the chalk without flints,
includes altogether 54 species; of which 30 are found in the upper part of Hunstanton Cliff:—
of the whole number only 15 species are wanting in Mr. Mantell’s catalogue of the Sussex chalk
fossils*.
Upper green-sand.—It is probable that attentive examination would discover the usual green
matter on the confines of the chalk and the representative of the gault in this county: but gene-
rally the Upper green-sand is scarcely perceptible. In the section at Mildenhall, inserted above,
10 feet of clay mixed with green particles, precede 11 feet of (upper) green-sand with many
fossils, which rests on blue clay, no doubt the Gault: and the five feet of sand which occur at
the bottom of the boring at Diss may also (possibly) belong to the former. Mr. Murchison
considers one of the beds at Hunstanton, as the representative of the malm rock of Western
Sussex; and Mr. Rose also mentions a rock like firestone, on the confines of the chalk, a re-
semblance which I find is indicated in my own notes.
Gault.—This stratum is very distinct at Mildenhall, below green-sand ; and is represented in
Smith’s map, as occurring all along the line of escarpment, between the lower chalk and the
lower ferruginous sand. I have myself seen it with the characteristic fossils at East Winch and
several other places. Thus at Mosshill Farm (“ Muzzle” of the Ordnance Map), west of the
house, towards Denver, are several pits, in a patch, or cap of bluish clay, over the Lower green-
sand: the former including Belemnites in great numbers, phosphate of lime in kidney-shaped
(coproid) concretions, a few specimens of Ammonites, and fragments of Inocerami in great num-
bers. On the heights between Middleton Tower and Devil’s Bottom, north of the section, Pl. X. a.
No. 25, are patches of white and yellowish grey clay, containing many of the Gault fossils;
—Belemnites, Inocerami in fragments, Echinus-spines, and portions of Encrinites. In fact, most
of the heights in this part of the country, are thinly covered with gault; while the sand beneath
it rises slowly towards the west.
The average thickness of the Gault in West Norfolk is not more than 15 feet, according to
»,
Mr. Rose, who has traced the connexion between the detached portions, indicated in Smith’s
map, as far as West Newton, about three miles south of Ingoldsthorpe. The valley between the
chalk and Lower green-sand is there interrupted by an advance of the chalk, and beyond that
point the blue Gault is no longer observable ; its place being occupied by the red marly stratum
of Hunstanton Cliff. The position of this red matter falls in with the strike of the blue Gault in
the southern part of the range, at Newton; and it has been detected, between that place and Hun-
stanton, at Dersingham Mill, and at Ingoldsthorpe, where I myself have seen that the red stratum
is immediately succeeded by sand, the blue beds being wanting.
* Geol. Trans. 2nd Series, vol. iii. p. 201, &c.; and Geology of the South-east of England,
(1833.) p. 370, &c.
Dr. Firron on the Strata below the Chalk. 313
Lower green-sand.— This formation here consists, at the upper part, of highly ferruginous coarse
sand, one of the most remarkable components of which is Titaniferous oxidulated iron*. The
sand abounds in hard concretions of siliceous grains cemented by ferruginous matter, in the form
of thin flakes or bands, irregularly ramified, which, in Norfolk, are called “ Carstone ”;—beneath
which is finer sand of different shades of grey, yellowish, and white. The course of the out-
crop is generally parallel to that of the chalk: the chief localities and the local varieties are indi-
eated in Mr. Rose’s memoir.
In descending a hill on the road from Lynn to Snettisham, about a mile from the village of
Dersingham, is white sand, under yellow slightly consolidated sand; and near the line of the section
No. 25, between 38 miles and 39 from Norwich, about half a mile from Middleton, are pits of
yellowish and white sand, with ferruginous concretional bands, apparently belonging to the upper
member of the Lower green-sand; and very like the Woburn sands.
Organic remains must be very rare in this formation, as Mr. Rose states that he had not obtained
any specimens. At Ingoldsthorpe, however, in a brick-field near Mount Amelia, 1 found casts of
the following shells, in masses of agglutinated ferruginous sand, like those of Parham-park in
Western Sussex, and of the cliff on the west of Shanklin Chine in the Isle of Wight; Auricula
incrassata; Avicula, a new species; Corbula striatula; Mya plicata; Rostellaria calcarata ;
Turritella granulata; Venus Faba; and some other indistinct bivalves and univalves.
No indications occur in the sections of this formation which I saw, nor in those mentioned by
Mr. Rose, of the threefold subdivision of the Kentish coast; but in the lower part are thin
courses of Fuller’s earth, not more than an inch in thickness. The lower beds are stated by
Mr. Rose generally to contain thin strata of Fuller’s earth; as in Surrey and at Woburn.
(161.) Hunstanton.—The cliff at this place exhibits an epitome of all
the lower strata above described: the section is very distinct, and the dif-
ference in the characters and proportion of the beds from those of the south-
ern counties is so remarkable, that I think it necessary to give an account of
them, although the place has been already described by Mr. R.C.'Taylort
and Mr. Rose.
Pl. X.a. No. 26, represents the cliff, on the same scale with the other
sections in that plate, and with Plate X. b. fig. 12. a, which is copied
from a portion of the Ordnance Map of Norfolk. Fig. 12. b. is a sec-
tional elevation, for which I am indebted to Mr. Murchison; and fig. 12. c,
a sketch of part of the cliff, by Mr. Whewell, with whom and Professor
Sedgwick, I had the pleasure of examining the place in 1827.
The following is Mr. Murchison’s description of his section, (Pl. X. b. fig. 12. b.), with some
additions from my own notes. The dip is, generally, to the north-east ; but it will be observed
that there is an angle in the coast; so that the section is strictly divisible into two portions, in
different planes, neither of them coincident in direction with the line of dip.
* London and Edinburgh Phil. Mag., 3rd Ser., vol. vii. p. 179-; Phillips’s Mineralogy, 3rd edit.
p. 223.
Tt Geology of East Norfolk; and Phil. Mag. 1823, vol. Ixi. p. 81.
2s2
314 Dr. Fitton on the Strata below the Chalk.
Section at HunsTantTon CiirFr.
Ft. In.
1. Dunes * of loose blown sand.
2, Reddish clay, passing downwards into fine laminated sand; with bands of small
) 10 0
pebbles ...-.. see eeereececeeeeecs sie tiehe SHINO DO Oe soeceseess 9 Oto
. Chalk, increasing as it rises, and attaining its greatest thickness in the cliff under the
lighthouse. It is there about 30 feet Nee ‘and divisible into three :—
a. Grey chalk, in thin beds..... Bre DOO OOS THOS OF Oe <paieibifegeie ayia COMED
b. Grey chalk, in beds, from 1 to 3 feet in thickness .... Ba =.) oe
c. The lower part, for about 8 or 10 feet, includes myriads of = 8a
rami, chiefly in fragments, with large Ammonites . pel LOmMONCO
about 30 0O
In my own notes I find it stated, that some of the gritty portions of the beds in
this part of the cliff are very like the Surrey jirestone.
| Upper green- -sand??|
4, A “hard grey bed” like the malm-rock of Western Sussex (the upper member | 2
2 C=
the Upper green-sand), including great numbers of ramified stems.—Que. of Si-
phonia?.......0....eeee oouddyOs Udo DeooUDDDOdgaS¢ Homoododom ih ti
Pees! ney
. Red calcareous and argillaceous matter ; with multitudes of Belemnites Listeri, Ino- iJ
ceramus, Pecten orbiculari 2s, and some Terebratule ; ; generally divisible into two beds.
This is essentially a conglomerate, or breccia; being composed of angular fragments 4a
of black flint or flinty “slate, imbedded in a very large proportion of hard, “marly,
chalk-like matter, and varying in hue from a full to a pale brick-red. The colour |
is not improbably caused by oxide of iron derived from the ferruginous sands below J ,
[Lower green-sand. | ‘
6, a. Yellow sandstone, rather incoherent, with hollow concretions, and
curved bands of bluish oxide of iron (the ‘‘ Carstone” of Norfolk, 12 0
“ Clinkers” of Hampshire), with quartz pebbles the size of beans. { ~
Some stems of Siphonia in the upper portion......... 10 Oto i
b. is composed of siliceous pebbles and broken fragments of flint, united "i
by a very large proportion of dark brown ferruginous matter; | |
which, under the salt water becomes nearly black. The mass is igke |
traversed by fissures, which divide it into oblong blocks, and are r
sometimes occupied by carbonate of lime. Continued downwards: a
about 14 feet are visible ....... evo Netetaletattete prio tel oye Booancec oe 26 0
On the shore at the west end of the cliff, I observed numerous concretional
masses of a green conglomerate; obviously part of a bed, like that of the shore a
below the cliff at Shanklin, and at Sandown Bay, in the Isle of Wight. S
Total thickness of the Sectiont ............ 60 @ b
Hi
:
The Chalk without flints, which forms the upper part of the cliff at Hunstanton, rises, according —
to Mr. Rose, about 15 yards in a mile; the general inclination of the strata around Swaffham
(Section No. 25.) being about 5 yards ina mile. This part of the chalk at Hunstanton comes
down into contact with the Red Chalk (the Upper green-sand being wanting), and, according to
Mr. Rose, admits of subdivision into three portions. 1. Chalk, of a pure white colour. 2, Grey
chalk, of a sandy texture,—(No. 3. of Mr. Muggridge’s Section given in the note below). This
* This word is in some parts of Norfolk written “‘ Denes.” In the village of Hunstanton are
loose blocks of green-stone and basaltic porphyry, of considerable size and worn at the edges; and
in the transported matter, at the signal end of the cliff, were some pieces of mountain limestone.
+ The measurements of Mr. Taylor and of Mr. Muggridge (published by Mr. Rose) coineide
Sn SN ee
Dr. Firron on the Strata below the Chali. 315
contains very hard masses distributed through softer matter, and is stated by Mr. Woodward,
to include a mixture of the fossils of the Upper green-sand with those of the chalk marl. 3. A
bed of hard chalk, composed entirely of a ramose zoophyte ;—(No. 4. of Mr. Murchison’s Section
and part of 4. of Mr. Muggridge’s mentioned below).
The beds between the white chalk and the Lower green-sand here, differ much from those of
the southern counties. The Upper green-sand, if it be present at all, is very indistinct: the
green particles which, in other places, abound in this part of the series, are wanting; and the
thickness, which in the Isle of Wight is 60 or 70 feet, is here reduced to 2 feet. The Gault
has but a doubtful representative ; and instead of resembling the blue clay of the South, appears
under the form of reddish marl, not more than 4 feet thick*.
Mr. Woodward gives a list of 16 species of shells, from this red matter at Hunstanton; of
which number only five occur in the Gault of the southern counties: seven are found in the
Chalk ; four in the Upper green-sand, at some other places; three in the Lower green-sand; and
the five following occur only in the red chalk,— Ammonites alternatus, Spatangus planus, Spongia
paradoxa, Terebratula pentangulata, T. triplicata.—Geology of Norfolk, p. 54.
Kimmeridge clay.—This stratum, in West Norfolk, succeeds immediately to the Lower green-
sand, all along the line of escarpment. It can be seen in several detached points, between
Southrey, about the tenth mile on the road from Ely to Lynn, and the shore beneath Hunstanton
very nearly, with those of Mr. Murchison and myself, though their divisions of the strata are not
quite the same.
Taylor, 1823. Ft. In. Muggridge, 1835. Ft. In. Murchison, 1831 -—
Mesoiland diluyium...Gin.to. 4 0/1. Soil and diluvium.......:..c- nie bigs ial
2. Chalk, with few or- 2. Lowest chalk......... 28 0
36 0 Se
ganic remains ... . In
oy Veryhard .. 3 9 39 g|8. Chalk marl... 2 6to3 0 9, 9 No.3. . 20 0
4, White, with a ramified 1 6| 4: Whitezoophyticbed...1 4to 1 6] No.4. 1 6to2 0
zoophyte, like roots of trees
5. Deep red matter; lin. to...... 0 6 Seam of red ar- 7}
gillaceous matter} 0 3
Gupkved chalk..........0+. 2 0 0 2to |
5. Red zoophytic lime- NO. 5. ese oe 4 0
7. Red chalk; darker stone, (represent-
: ; 3 10
and more compact 2 0 ing the gault,) in J
RADU Gre ccasccscosess 4 0 4W.O BEDS da. ccwe ven. 4 1
8. Sand, light brown ferruginous, 6. Lower green-sand ............ No. 6.
containing taneous ion | TO" VO.) 72 Carstone ’....scccccssecsecseecess } eee a. 10 ft. to 12 0
RIE clo pa Selca's ose sdcieec's
9. Puddingstone and _ sandy 40 0 |8: Sandy breccia ...... 14 0 BS. cabettasn 14 0
breccia, very dark brown...
10. Very dark puddingstone, in
some places almost black :
discernible only at low
RAUCH! csuccscee visible about
20 0
* Similar beds of Red marl occur in the corresponding place beneath the chalk-wolds of Lin-
colnshire, (see a paper by Mr. Bogg, Geol. Trans. Ist Series, vol. iii. p. 392, &c.); and appear
again at Speeton, near Flamborough Head, on the Yorkshire coast ;—where, however, they are
distinctly superior to the blue gault, and are regarded by Mr. Phillips, as forming part of the
chalk.—Geology of Yorkshire, (1st ed.) p. 75; and Section No. 3.
316 Dr. Firron on the Strata below the Chalk.
Cliff, where its occurrence is mentioned by Mr. R. C. Taylor; and Mr. Woodward states, that
beneath 13 feet of brick-earth, near the former place, a few inches of bituminous shale were
found, which burned readily and contained between its lamine impressions of an Ammonite, and
a small bivalve, (Tellina?), *
At Southrey, I found in the clay many of the characteristic Kimmeridge fossils, among which
are Ostrea deltoidea, Ammonites Lamberti, Aptychus, like that of Buckinghamshire (Pl. XXIII.
fig. 11.), and a Vermetus ; with fragments of the teeth and bones of Saurians.
In a brick-field beneath Downham Market, where 5 or 6 feet of clay were exposed, I found
Ostrea deltoidea, another large bivalve, and a great number of Ammonites (4. biplex?) much com-
pressed. In a section at Denver Sluice, near Downhan, the order was as follows t :—
Ft. In
1. Sandy loam, peat and clay ; containing roots of plants ...6...+e+seeeee wie eietetels 23 :
2. Wark ferrUGINOUS SANG so ese allele | teleleeeleielaietaeie tole /ouals\ofe «cle laieleleein icicle ile
3. Clay; which, from its position and contact with sand, seems to be that of Kim- 7 0
MRICTIG LE vain faveie estore «ele oho lores Vel-letel serene terehel ee efeleiets ote ietekae cece cece ereesees
The Oxford oolite has not been found in this part of the country; nor the subjacent calca-
reous grit, :
The only mode, therefore, in which the presence of the Oxford clay can be ascertained, is by
its fossils; for, although the great depth of clay passed through at Lynn, in the well sunk and
bored at Mr, Allen’s brewery, exceeds the average thickness of the Kimmeridge clay, even when
combined with the Weymouth strata, identity cannot be safely denied, on the evidence of thick-
ness alone. More than 630 feet of clay were cut through in this well, after passing through
between 40 and 50 feet of loam, peat, clay, and marine silt. Of this great thickness a part
no doubt belongs to the Kimmeridge clay; and the fossils obtained from the lower beds, now
in Mr. Rose’s possession, offer no very decisive proof that the Oxford clay is there. But on
the other hand, none of the more characteristic fossils of Kimmeridge occur in it, except,
Ostrea deltoidea ;—no Gryphea Virgula, nor Aptychus. The list given by Mr. Rose, includes
Ammonites decipiens; A. excavatus, and another very small species; Belemnites abbreviatus ;
Gryphea bullata, with Serpula tricarmata attached to it; Mya depressa (a Kimmeridge clay
fossil?) ; a Pecten impressed upon a Venus; and a muricated spine of an Echinus. Among the
specimens from the deep well which I find mentioned in my notes of 1827, are a large Ammonite ;
two others of small size (one very like 4. Kelloviensis); Gryphea dilatata, with another bivalve
adhering ; Ostrea deltoidea; two indistinct bivalves ; and part of a flat bone.
( 162.) List of Fossils of the Beds below the Chalk, in Beprorpsarrez,
CAMBRIDGESHIRE, and NorFroLk.
Gault :—including the red stratum at Hunstanton.
Ammonites dentatus. Ingoldsthorpe, Norfolk : in grey sandy clay.
A — inflatus, young. Between Cambridge and Ely.
A———— lautus. Between Cambridge and Ely: in green sand, at the bottom of the
Gault.
A—— varicosus. Between Cambridge and Ely ?
* Rose, p. 176. t Ibid., p. 173.
eee, hee
Dr. Frrron on the Strata below the Chalk. 317
Belemnites attenuatus. Ingoldsthorpe, Norfolk.
B minimus. Ingoldsthorpe: in very light gray marl, with an Inoceramus.
Hunstanton: a very large specimen, in the red marl.
Dentalium, with Exogyra conica. Between Cambridge and Ely.
Echinus ; spine and fragments. Between Cambridge and Ely: in gray marly clay;
Ingoldsthorpe. Hunstanton.
Exogyra conica. Between Cambridge and Ely: with part of a Dentalium.
Gryphea globosa. Hunstanton: with fragments of Inoceramus, and numerous
quartzy particles, in red marl.
Inoceramus concentricus ? Hunstanton: in red marl.
[— Cripsit: (Mantell). Hunstanton: red marl.
J——_—— intermedius? Hunstanton.
I— sulcatus. Woburn, Bedfordshire.
J ———— (indistinct.) Ingoldsthorpe: in light gray marl ; with Belemnites minimus.
Hunstanton: shell very thick, in red marl; with Belemnites minimus?
Pecten Beaveri. Hunstanton: with stems of Siphonia ?
Siphonia. Wunstanton: in gray marl; (Lower chalk ?)
Terebratula biplicata. Hunstanton; in the red marl.
T——_ subundata. Wunstanton; in the red marl.
Lower Green-sand.
Auricula incrassata. Brick-field, near Ingoldsthorpe, Norfolk; in ferruginous masses,
like those of Parham Park, Sussex,—with the following :—
Avicula (new); Natica; Panopea plicata; Rostellaria calcarata; Turritella gra-
nulata; Venus Faba.
Kimmeridge Clay.
Ammonites biplex. Asplay, near Woburn: in gravel.
A————. Lamberti. Between Cambridge and Ely: in clay, probably that of Kim-
meridge.
Aptychus; Von Meyer:—(Trigonellites of Parkinson.) Pl. XXIII. fig.11. Roadside
between Cambridge and Ely. The same as near Whitchurch and Stewkley,
Bucks; supra, pp. 292 and 302.
Ostrea; fragments. Between Cambridge and Ely.
Oxford Oolite.
At Upware, on the banks of the Cam, about eight miles below Cambridge, the fol-
lowing fossils are found, in coarse limestone :—
Arca. Astrea. Cidaris; spine. Cucullea; with Pecten and other fossils. Fusus.
Gastrochena. Gervillia aviculoides; with Turbo muricatus. Isocardia (new) ;
very acute. Litiorina muricata. Modiola (indistinct.) Ostrea gregaria. Pecten
vimineus. Plagiostoma cardiiforme. -Plicatula. Trigonia Pullus. Turbo (in-
distinct). Twrritella muricata? Venus (cast, imperfect).
318 Dr. Firron on the Strata below the Chalk.
SUMMARY AND GENERAL REMARKS.
(163.) The order of the strata mentioned in the preceding pages is repre-
sented generally in the abstract Section, Pl. X.b. fig. 13,
Tuickness or StratA.—I have not inserted in the engraved section the thickness of the
groups; both because it varies much in different places, and that in general my estimates are so
loose as not to be relied upon. Accurate measurements of the thickness of the English strata
have very seldom been made. The following are approximate numbers, derived however, princi-
pally, from estimates by the eye.
Chalk.—The entire thickness of the chalk is exposed in many of the sections on the south-
eastern coast; but westward of the Isle of Wight the beds are convergent and much reduced in
bulk. Between Deal and Folkstone, Mr. W. Phillips has estimated the total thickness at 820 feet!.
The two sections at the extremities of the Isle of Wight, between Whitecliff and Sandown Bays
on the east,—and between Alum Bay and Broadbench, at the western extremity of the central
ridge, furnish good evidence ; the strata being so nearly vertical, that the horizontal line across
their direction, does not very much exceed the perpendicular to their surfaces. Mr. Greenough
has accordingly estimated the thickness at Culver at 1300 feet?; and the interval on the Ord-
nance map, which is very nearly the same at the two extremities of the island, (being in both
places about 2 furlongs, or 1320 feet,) may probably be considered as somewhat exceeding the
maximum thickness of the chalk in England.
Mr. Conybeare estimates the chalk as ranging between 600 and 1000 feet?; and Mr. De la
Beche at 700+. The height of the cliff at Beachy Head, which includes at top part of the flinty
chalk, and goes down very nearly to the Upper green-sand, is only 535 feet®; but if 250 feet be
added, for the remainder of the flinty chalk, (350 being the thickness of that division near Dover®,)
the aggregate thickness on the Sussex coast will be about 800 feet.
At Wendover Hill, the summit employed as the Ordnance Station is 905 feet above the sea7 ;
and the canal at Wendover being 4044 feet, and still within the chalk, the difference, 500 feet, is
certainly less than the total thickness at that place.
But the whole of the chalk passed through in the boring above mentioned, at Diss in Norfolk’,
(which includes at the top 100 feet without flints,) was only 510 feet.
The wide range of variation in thickness above stated (supposing the measures to be correct),
arises in a great measure from the unequal abrasion and removal of the upper strata; but must
in part also be ascribed to original inequality in the thickness of the chalk itself.
Upper green-sand.—The thickness of this group near Folkstone does not exceed 30 feet, and
is probably much less®; but it swells out considerably near Godstone, and Merstham, and at the
latter place is upwards of 30 feet thick'*. The depth of the wells sunk through it, in the
Malm rock strata of Hampshire, varies from 60 to 100 feet!'. In Western Sussex the thickness
1 Geol. Trans., 1st Ser. vol. v. p. 18. * Conybeare, Outlines, &c. p. 85.
> Ibid. 4 Tabular View, 2nd edit. 5 Section, No. 6. Plate X. a.
6 Phillips, Geol. Trans., 1st Ser. vol. v. p. 18. 7 Supra (149.), p. 284; and Sect. 20, Pl. X. a.
5 (160.), p. 311. 9 (9.), p. 107. 10 (49.), p- 140. ‘Murchison,
Geol. Trans., 2nd Series, vol. ii. p. 99.
Dr. Firron on the Strata below the Chalk. 319
is between 70 and 80 feet!; in the Isle of Wight, about 70 feet®. At Blackdown the thickness
of the sand is about 100 feet? ; in the Vale of Wardour, probably from 60 to 80+; near Swindon,
30 to 50 feet®: but at the Castle Hill, Cambridge, it is not more than ,18 inches®. Thence
through West Norfolk, the stratum is not anywhere distinctly seen; and at Hunstanton, the
only beds which can be supposed to represent it, are not more than 2 feet thick7.
Gault.—The thickness of this stratum near Copt Point, derived from barometric measurement,
is about 130 feet®. In the interior it is difficult to obtain good estimates, and accurate measures
can be expected only in wells. At Merstham it is about 150 feet thick®; in the Isle of Wight
probably about 70 feet'®: at Ridge, in the Vale of Wardour, it is about 75 feet!!; at Cotmore
Wells near Thame, 90 feet'*.. In Cambridgeshire, the entire stratum has been cut through re-
peatedly in wells and borings, which give an average thickness of 150 feet !°; but at Mildenhall in
Suffolk, the blue clay, which seems to represent it, is only 9 feet'*. In West Norfolk Mr. Rose
considers that the utmost thickness cannot be more than 15 feet'!®; and at Hunstanton the red
marly beds which are supposed to contain Gault fossils, are only 4 feet thick!®.
Lower green-sand.—The measured thickness of this formation can be most easily obtained on
the shore between Copt Point and Hythe, where the uppermost subdivision is about 70 feet
thick '7; the middle group, 70 to 100 feet '*; and the lowest, 60 to 80 feet'!’; the total thickness
consequently about 250 feet. In Western Sussex, Mr. Murchison states that nearly 400 feet of
sand were passed through in a boring, at Petworth Summerhouse2°; and Mr. Martin conceives
that the two lower members may be together about 150 feet thick®!. In the Isle of Wight the
thickness, between Bonchurch Cove and Sandown, Rocken End and Atherfield Rocks, cannot be
less than that of the formation near Folkstone, and seems to be much greater. At Brill, in Buck-
inghamshire, about 26 feet remain”; in West Norfolk, Mr. Rose considers the thickness of the
whole formation to be about 80 feet *.
Wealden.—No measures, on good estimates, of the thickness of the strata in this group have yet
been obtained. Mr. Martin assigns 281 feet to the Weald-clay cut through in boring, at Petworth
in Western Sussex2*; but in the section at Tiepit and Cowleaze Chine in the Isle of Wight, the
clay seems to be no more than 140 feet thick®.
The section of that part of the Hastings-sands which is visible between St. Leonard’s Church
and the top of the great sand rock bed, may be about 200 to 250 feet; the-sand rock bed
itself, under the castle, about 80 to 120 feet; and thence to the lowest point upon the coast,
east of Hastings, about 200 or 250.—Total thickness, between 400 and 500 feet 26,
It is difficult, from their contortions, to estimate the thickness of the Purbeck strata on the
coast. Mr. Webster has given in detail the stratification of a portion of them, which amounts to
124 feet, 8 inches?” ; to which may be added about 150 feet,—making a total of about 275°. In
the Vale of Wardour, the total remaining thickness of the group appears to be from 40 to 60
i EEE ann ina
! Martin, p. 20,—who states, however that 100 feet would probably be no exaggeration of the
thickness, where the stratum first emerges from beneath the chalk. 2 Webster, Letters, &c.,
p- 140.: and supra (93.), p. 183. 3 Supra (120.), p. 236.; and (93.) p. 183. = (t28.),
p 216.; (129.), p. 247. * (1441.), p. 265. © (158.), p- 305. 7 (161.), p. 314.
8 (11.), p. 109. 9 (49.), p. 140. 10 (93.), p. 184. 11 (129.), p. 247. 12 (148.),
p.279. 13 (158.), p. 306. 14 (160.), p. 311. 15 Rose, p. 181. 16 Supra (161.), p. 314.
a (17.), p. 116. 18 (25.) p. 122. 19 (32.) p. 126. 20 Geol. Trans., 2nd Ser. vol. ii.
p- 102. 21 Martin, p. 36—40. 22 (148.), A. p. 280. °3 Rose, p. 176. 2 Martin,
p- 36.and40. °% Supra(100.), p. 198. 26 (80.) to (84.), p. 163—172. °7 Geol. Trans.,
2nd Ser. vol. ii. p. 39. 28 Supra (104.), p. 209.
VOL. IV.—SECOND SERIES. a
320 Dr. Firron on the Strata below the Chalk.
feet', and in Buckinghamshire still less. Mr. De la Beche estimates the whole formation at
250 feet’. The aggregate thickness, therefore, of the three groups which compose the Wealden,
cannot, probably, be less than 800 feet.
Portland stone.—This formation being well defined and fully exposed, its thickness is well as-
certained ; and in Portland Island it seems to range between 60 feet* and about 70,°; at Swindon
it is about 60 to 65°: at Great Hazeley in Oxfordshire 27 feet7; at Brill, about 23 feet®;
near Quainton and Whitchurch in Buckinghamshire, from 4 to 20 feet’.
Portland sand.—Near St. Alban’s Head, Isle of Purbeck, 120 to 140? feet!°; in the Isle of
Portland, 80 feet!!; near Thame in Oxfordshire, about 50 feet '*.
Kimmeridge clay.—The thickness of this group is uncertain, and seems to vary much in dif-
ferent places. On the coast Messrs. Buckland and De la Beche assign to it 600 feet, at Kim-
meridge Bay'’; but they state the thickness at Ringstead Bay to be only 300 feet'*. At the
Headington quarries in Oxfordshire, I found, in one of the pits, only 20 feet of clay'*. The
general thickness is stated by Mr. De la Beche to be 500 feet'®.
Oxford oolite.x—On the coast near Weymouth, 150 feet!’.. The whole, in Wiltshire, according
to Mr. Lonsdale, about 200 feet !*; Mr. De la Beche, 150 feet 9.
Oxford clay.—On the Dorsetshire coast, near Weymouth, 300 feet®: at Lynn in West Nor-
folk Mr. Rose assigns to this formation the whole depth of a well, which would make the thickness
about 630 feet®'; but part of this depth may possibly be Kimmeridge clay. Mr. De la Beche’s
estimate for the whole formation is 600 feet 2%.
(164.) Order of Geological Events.—The succession of events which the
preceding pages demonstrate, has been already detailed in some other pub-
lications* ; but they are too important not to be recited here. The evidence
bearing on the following propositions, derived from the South Eastern Coast,
the Vale of Wardour, and Buckinghamshire, is all in perfect harmony; and
the inferences are so directly connected with the facts, as to be rather corol-
laries than deductions from them.
1. Deposition, beneath the sea, of the following groups of strata, beginning with the lowest :—
a. Oxford oolite. b, Weymouth and Kimmeridge strata. c. The Portland sand and stone.
. Elevation of the Portland strata above the sea.
. Submersion, by fresh water, of the newly disclosed land.
tm CoO to
. Deposition beneath fresh water, above the Portland strata,—first, of a thin bed of clay ; and
then of a crust of freshwater limestone, the “ skull-cap.” (111.) p. 224, and (118.) p. 226.
| Supra (132.), p. 251. 2 (150.), p. 285-6. 3 Tabular View. * Webster, Geol. Trans.
vol. il. p. 42,43; and Pi. VI. fig. 3. | ° Buckland and De la Beche, PI. III. fig. 1. of this volume.
® Supra(141.),p.267. 7 (144.),p. 276-277. ° (148.), C.p. 280-1. 9 (152.), p, 288, 290.
10 (106.), p. 212.—Section, fig. 5. Plate X.b. ‘' Buckland and De la Beche, p.19. of this
volume. 12 Supra (148.) p. 282-3. 1S Page 19. of this volume.—This estimate, however,
appears to be too great : see above, (107.) p. 212-13. __'* Pl, ILL. of this volume, fig. 1.; and p.22,
1.6. 15 Supra (146.), p. 278-9. 16 ‘Tabular View. '7 Buckland and De la Beche,
p- 23. of this volume, |. 2. from bottom. 's Geol. Trans. 2nd Series, vol iii. p. 261.
'9 Tabular View. °° Buckland and De la Beche, p. 28. of this volume. "1 Rose, p. 174.5
supra (161.) p. 316. 2 Tabular View.
* See the works of Mr. Mantell; Dr. Buckland’s and Mr. De la Beche’s paper in the present
volume ; and the ‘‘ Geology of Hastings”, p. 79, &c.
Dr. Firron on the Strata below the Chalk 321
5. Deposition upon the “ skull-cap” of a bed of “dirt”, (110.) p.223.; and exposure of it as
dry land.
6, Growth upon this land, of the Cycadezx now found in the Dirt-bed, i situ, and in the upright
position. 10: p. 223-4.
7. Second submersion (at least), of the Jand, in fresh water; proved by the deposition and exist-
ence of the “cap”. (111.) 9, p.222, 3; and (113.) p. 226.
8. Exposure of the surface of this “‘cap” as land; and growth upon it of coniferous trees, and of
Cycadez. (111.) 8, p. 220-22.
9. Ravages (from the effects of currents of wind, or water,—or from earthquakes), by which the
trees were overthrown, or broken off at short distances above the roots.
10. Third submersion, in fresh water ; and deposition of slaty limestone, containing freshwater
fossils only, but near the bottom alternating with clay*. (111.) p. 219, 220.; and (113.)
p- 226.
11. Alternation of Oysters with freshwater fossils in the slaty Purbeck limestone; proving
access of the seat, apparently in an estuary (104.) p. 208; and (113.) p. 226.
12. Continuance of the estuarine condition during the whole remaining epoch of the Wealden ;
proved by the occasional presence of oyster-shells, throughout the Hastings-sands and
Weald-clay. (98.) p.190.; and List of Fossils, p. 178.
13. Sudden, or rapid, depression of the entire Wealden, to such a depth as to be covered with
salt water; proved by the sudden and exclusive appearance of marine productions and
fossils, above and in immediate apposition with strata containing only freshwater fossils,
though mineralogically of the same composition, (100.) p. 196-7.
(165.) Local Distribution of the Strata.—If a line drawn from the coast at
Folkstone, touching London on the north, and thence towards Newport
Pagnell; and another line from about Atherfield in the Isle of Wight
towards Faringdon in Berkshire, the tract intervening wiil comprise the
space throughout which the beds immediately below the chaik are most
fully developed : and if the standard be taken from the condition of the strata
when possessed of their greatest bulk, that of the Green-sands and Wealden
may be said to occur in Kent, Sussex, and the Isle of Wight; from which
central tract these groups appear to thin out in every direction.
The whole series immediately below the chalk is finely developed between
* The alternations, in this case, are distinguished from those of the coal formation, (in which
also the remains of terrestrial and freshwater productions alternate—in some instances repeatedly—
with those of marine origin), by the growth of plants upon the surface of some of the alternating
strata ; a proof of their exposure, as dry land, between successive immersions. Mr. Prestwich,
in a valuable paper on the coal-field of Coalbrook Dale, has justly remarked, that the repeated
alternations in that district are no proof that the tract itself was raised above the sea and again
depressed, as many times as the freshwater remains alternate with the marine ;—since the facts
may be accounted for by supposing that the strata were accumulated in an estuary liable to
freshes from a river of considerable size.—Proceedings of Geol. Society, 1836, vol. ii.
+ Lamarck (Animaux sans Vertébres, vol. vi.) mentions altogether 81 species of the genus
Ostrea; 48 of which are of existing species, 33 known only in the fossil state. Of the 48 recent
species, 40 are marine, and 8 uncertain, but also probably marine. In the present state of our
knowledge therefore, the occurrence of Oysters may fairly be considered as proof of the former
access of the sea.
Pin ©
Be) Dr. Firron on the Strata below the Chalk.
Farnham and Petersfield and around the west end of the Wealden denu-
dation; the Lower green-sand, especially, is nowhere better disclosed, except
in the Isle of Wight. It is not improbable, that the part of these groups
which once intervened between the Isle of Wight and the Sussex coast, and
is now concealed by the sea, was likewise fully expanded; but at Folkstone
the Upper green-sand has already become much thinner.
It remains yet to be ascertained whether in their prolongation northward
in England, and towards the east on the continent of Europe, these groups
again assume their more bulky and varied form, as our Upper green-sand
is observed to do after reduction, even within very short distances; and
whether, if they do so expand, the relative proportions of the component
members be the same in remote countries ; an inquiry which is the more in-
teresting in the case of the green-sand formation, from its very wide diffu-
sion, and the great space which it occupies in different parts of Kurope.
Deraits.—The following are some of the local variations in the strata composing the groups
above referred to :—
Chalk.—It may be remarked that the chalk rises much more rapidly towards its outcrop,
between Wiltshire and Hertfordshire, than in the more northern counties of the South East of
England. In departing from that central tract, both towards Devonshire on the south, and
northwards, the rise is comparatively small; the beds shooting out very gradually, and occupying
very wide spaces of uniform, flat country. The disturbance, by which the ridge of the Wealds
and the parallel range of elevations through the Isle of Wight and Dorsetshire were produced,
wasprobably the principal cause of this variation: and the mean course of the Thames itself,
from the point where it cuts through the chalk, may possibly be connected with that derange-
ment. But in the chalk itself, on the south-west of London, much local variation is found
in the angle and direction of the dip; and from the facts mentioned by Mr. De la Beche, respect-
ing the faults in Devonshire, and what I have seen of the minor irregularities on the shore
near Hastings, it is probable that if the whole surface in this part of England were examined
with equal attention, it would prove to be pervaded by cracks and slight dislocations.
The Upper green-sand is especially remarkable for great variation in its thickness and compo-
sition; and it is everywhere so intimately connected with the lowest beds of the chalk, that
if we had more accurate measurements of our strata, the total thickness of that formation, in-
cluding the Upper green-sand—might, perhaps, be found to be nearly uniform. The latter passes
most commonly by insensible gradation into the soft dark-coloured marly chalk. In many cases, it
forms a very thin and scarcely distinguishable group,—as near Folkstone, where it is not more
than 20 feet thick ; in others, the chert which it contains becomes conspicuous, and it affords also
beds of firestone, which together giving it firmness and durability, cause it to project as a step
or prominence beyond the foot of the chalk range.
On the west of Portland, the green-sands thin out so rapidly, that at Blackdown a series about
200 feet thick is their only representative ; and it is difficult to decide whether this be a con-
densed equivalent, of the whole group between the chalk and the lowest green-sand,—or, (which
seems to be more probable,) only a continuation of the lower part of the Upper green-sand,
from the Vale of Wardour. In following the range of these formations towards the north-east,
Dr. Firron on the Strata below the Chalk. 323
a similar reduction of the green-sands is observable, as the section at Hunstanton remarkably
proves; but the diminution is by no means uniform throughout the intermediate space. Along
the coast of Devonshire, the beds at the bottom of the upper sand seem to adopt the characters
which the Lower green-sand exhibits in other places ; and the latter, as well as the usually inter-
vening gault seems to be wanting. In the Vale of Wardour also, where the Lower sand is
scarcely apparent, the Upper green-sand exhibits many of its characters; but the Gault is very
distinct between them.
The Gault is seen in the greatest perfection on the coast at Folkstone, where its fossils are
especially beautiful and numerous. It seems to be thinner and to contain few fossils in the
Isle of Wight, and is almost wholly wanting on the west of Purbeck. But in the interior—in
the Vale of Wardour, and thence northward to the sea at Hunstanton,—this stratum everywhere
appears, and contains throughout many of the same fossils, though it changes its character and
is much reduced in bulk in Norfolk.
The almost constant presence of this distinct band of clay between the chalk and Lower green-
sand, considering its small relative thickness, is a remarkable fact: and its retention, both in En-
gland and on the Continent, of the same mineralogical characters and fossils, renders the Gault
a very important member of the series. I have seen it in its proper place, and in the form of
bluish clay, all around the Lower Boulonnois; in the vicinity of Aix-la-Chapelle ; and in the
country between that place and Liege.
The Lower green-sand thins out remarkably towards the west, from the central tract just men-
tioned, (p. 321-2.). The traces of it in the Vale of Wardour are obscure, but they become gra-
dually more distinct towards the north. The subdivisions of the Kentish coast, detailed in (16.)
to (35.) and in Sussex (72.), deserve comparison with the more expanded equivalents of this
formation in other countries. Their existence in the Isle of Wight is almost certain; and they
will probably be found in Bedfordshire: but thence, north-eastward, the sands again become
thinner, though they still preserve their relative place.
The Wealden.—This group, also, is best developed near the central tract already pointed out.
The Weald-clay is seen in the greatest perfection in the Isle of Wight; and the Hastings-sand in
the Forest ridge of Kent and Sussex, &c. But the Purbeck strata are fully expanded only in the
Isle of Purbeck, and on the adjacent coast of Dorsetshire. No traces of any member of this
group have been found west of the Isle of Portland; nor eastward of that island, near the coast,
except in the vicinity of Battle in Sussex. In the Vale of Wardour, the Weald-clay and
Hastings-sands are reduced almost to nothing ; and they have not yet been found along the line of
the green-sands between that place and the neighbourhood of Oxford*. Thence, to Quainton
and Whitchurch in Buckinghamshire, the representatives of the Purbeck strata, though perfectly
distinct, are but a few feet in thickness, and belong to the lowest beds of the formation. Other
indications of the Wealden may be looked for, north of Whitchurch, in the detached portions of
sand represented in Mr. Smith’s maps of Buckinghamshire and Bedfordshire: and the speci-
mens of Lonchopteris said to occur at Wansford on the north-east of Northamptonshire, (if they
be really found in situ), would prove that the Hastings-sands exist at that place.
* The subdivisions of the Wealden, especially at the upper part, being in some measure
arbitrary, it is often difficult to determine which of the three groups any given portion of
unconnected strata ought to be referred to. The same fossils pervade the whole; and beds
of sand, clay, and stone, almost identical may be produced from all parts of the series; so that
collective evidence alone can be resorted to for the purpose of distinction.
324 Dr. Firron on the Strata below the Chalk.
The places beyond the limits of the tract described in the preceding pages, in which the
existence of the Wealden has been ascertained, or rendered probable, are mentioned hereafter,
(168.) p. 526.
The sudden change from the marine fossils of the Lower green-sand to the freshwater pro-
ductions of the Wealden is remarkably exhibited at Atherfield in the Isle of Wight (100.) p.196;
where the former stratum contains nearly thirty species, of about twenty genera; while the Weald-
clay, not more than ten feet vertically beneath, contains scarcely any other shells than Cypris,
Cyclas, and Paludina*. The contrast, in descending from the Wealden group, is equally striking
and abrupt ;—the Purbeck strata near their junction with the Portland affording scarcely any
fossil but Cypris, while the “‘ Roche” at the top of the Portland group, within a few inches of the
freshwater limestone, is full of marine remains. (111.) p. 224.
The Wealden strata, though differing so widely as to their fossils, appear to be conformable to
those of the adjoining formations, both below them and above. On the Dorsetshire coast, in
the Vale of Wardour, and in Buckinghamshire, the Purbeck beds correspond exactly in dip and
direction to the Portland stone beneath; and at Hythe in Kent, and in the Isle of Wight, the
lowest beds of the green-sand are perfectly continuous with the upper beds of the Weald-clay,
(98-) p. 189. The only place with which I am yet acquainted, where a want of conformity is in-
dicated between these formations, is at Stopham in West Sussex, adverted to in (74.) p. 156.
But the eroded cavities, filled with what seem to be green-sand and Fuller’s earth, in the upper
part of many of the quarries in Oxfordshire and Buckinghamshire, (of which those at Great
Hazeley and Dinton are good examples,) indicate an interval and some intervening disturbance,
between the periods of their production. (114.) p. 276; and (151.) p. 286.
(166.) Theory of the Wealden.—The mode in which the Wealden is
disposed, in the South-east of England, accords with the hypothesis of its
having originated in a lake of fresh water, or in the estuary of a large river.
it remains to be determined whether similar deposits are found to occupy
a corresponding situation in other parts of the great European basin, of
which England is but a small portion.
The chalk and green-sands in England are so frequently prolonged be-
yond the limits of the beds below, concealing their outcrop, that no certain
* Wocdward, so long ago as in 1702, pointed out the resemblance of the Wealden Paludine,
to some recent freshwater species': and Mr. Sowerby, about 1812, after mentioning their oc-
currence at Bethersden in Kent, remarks that ‘from these different localities of shells, appa-
“rently of the same genus, we must conclude, either that analogy is not sufficient to prove that
** these fossils are of freshwater origin; or else that there are more freshwater formations than
‘are generally supposed?”. Mr. Webster, about the same period, distinctly mentioned the
existence of freshwater shells in the Purbeck strata, and the probability that a part of that
formation had been deposited from fresh water’. In 1822, Mr. Mantell reasoned with great
sagacity upon the inferences derivable from the fossils, discovered by himself at Tilgate Forest*:
but the geology of the strata connected with that group was then undetermined ; and the diffi-
culties, I believe, were not removed till 1824.
' “History of Fossils”; quoted by Webster,—Letters, &c., pp. 142, 192. | % Min. Con. vol. i.
p- 76. tab. 31. > Letters, &c. to Sir Harry Englefield, pp. 192. and 237. + Illustrations
of the Geology of Sussex, 4to, 1832.
Dr. Firron on the Strata below the Chalk. 325
inference can be drawn with respect to the continuity beneath them of the
Wealden and Portland strata. It is not improbable that what now appear to
be detached portions, may in many cases be united ; but it seems to be con-
sistent with the mode in which freshwater deposits have been formed, whe-
ther in lakes or estuaries, that they should, in more extensive regions, occur in
detached, rather than continuous portions; and that the outlines of the spaces
which they occupy should be irregular. The former existence of the upper
Wealden strata in the interior of England, is rendered probable by the ero-
sion of the Purbeck beds in many places where the Lower green-sand comes
into contact with them, (151.) p. 286,—which has clearly been effected by
the action of water, and proves that something was carried away, before the
sand was deposited: the argument from these appearances being the same
as that derived from the erosions on the surface of the Oxford oolite and of
the chalk, (143.) p. 274.
The great extent of the surface occupied by water in North America is a
striking feature in every ordinary map. Dr. Richardson, in his observations on
the geology of that region, has remarked that a large tract near the confines
of the primitive and secondary regions is occupied by lakes of the most varied
outlines and dimensions ;—in which the deposition of shells and other exuvie
of organized beings has been going on ever since the surface of the globe
assumed its present aspect. If that part of the northern hemisphere were
now to be sunk beneath the sea, we should probably have, after a short
time, one universal sheet of marine strata, lodged upon the surface of the
present land, so as to conceal not only the deposits of the several lakes, but
the intervals between them: and if we could, then, examine the interna!
structure of the tract, we should find it to be occupied by a numerous series
of Wealdens, detached from each other, and bordered, it is more than pro-
bable, by deposits analogous to those of the dirt-beds of Portland, wherever
the fluctuations of the lacustrine waters left time and space for the growth of
plants upon their margin. The external boundaries of these deposits would
be as various and irregular as that of the lakes which now diversify the map
of North America: and we should expect, in such cases, that the mineral!
components in the deposits of the lakes, would vary according to the nature
of the surrounding land. Their fossil contents would, probably, have a
great general resemblance throughout large districts ; but, in the remoter
tracts would differ as much as the productions of modern lakes are found
to vary ;—as those of the lakes in the North of England differ from those
of Switzerland, and both from those of the South of France, &c.; or, as
in America, those of Slave-Lake differ from the productions of Lake-Superior
326 Dr. Fitton on the Strata below the Chalk.
or Lake-Erie. 'The lacustrine deposits, again, would be occasionally diver-
sified by the presence of the products of estuaries, such as those of the St.
Lawrence and of other rivers around Hudson’s Bay and the north-east coast
of America; and in these we should probably find, along with the species of
shells which usually inhabit the mouths of large rivers and the borders of the
sea, some scattered remains of the products of the adjacent shores,—the
plants and animals of the land, with some admixture of freshwater shells.
(167.) Wealden in other Districts.—The following are the places beyond
the limits of the tract described in the preceding pages, in which the presence
of the Wealden strata has hitherto been ascertained, or rendered probable.
Scottanp.—In the Isle of Skye Professor Sedgwick and Mr. Murchison discovered, in cliffs
of blue shale associated with trap, on the eastern shore of Loch Staffen, flattened masses of
limestone, containing several species of shells; some of which are identical with fossils which
I had found in the upper beds of the Weald-clay at Swanage Bay on the Dorsetshire coast;
and all the rest are freshwater species belonging to genera found in the Wealden of the south*.
The coincident species are the following; some of which are figured in the plates subjoined to
these pages :—Cyclas media (Plate XXI. fig. 10.); Cyclas, a larger species (C. major, Pl. XXI.
fig. 13., Isle of Wight); Cyclas cbovata?; Neritina Fittoni, Mantell (Pl. XXI. fig. 7.); Ostrea
distorta, found with Cyclades in the Isle of Wight, (Pl. XXII. fig. 2.); Paludina elongata; Isle
of Wight and Swanage Bay; a transversely elongated Bivalve, (Isle of Wight); an Unio, or
Anodon.
There can be little doubt, therefore, as Mr. Murchison has inferred, that this deposit was con-
temporaneous with the English Wealden.
Continent oF Evrore.—The places out of England, where the equivalents of the Wealden beds
have hitherto been found, are the two following.
1. In the Lower Boulonnois the presence of the lower member of the group, at least, is certain;
the strata bemg almost identical with some of those upon the confines of the Purbeck and Port-
land formations in Dorsetshire and the Vale of Wardour. Having given an account of that part of
the French coast on another occasion f, it will be sufficient to mention here, that the line of the cliffs
from Equihen on the south of Boulogne to Cape Gris-nez on the north of that place, is capped at
intervals with a thin crust of the Purbeck strata, resting upon those of Portland, and consisting
of slaty beds of limestone, which contain freshwater shells, and include a bed of tough dark-co-
Joured clay, in which are numerous fragments of silicified coniferous trunks not distinguishable
from those of the Isle of Portland. It is highly probable that a more exact examination of this
part of the series, in the cliffs near Boulogne, may lead to the detection of these trunks in the
upright position; and of the Cycadez by which they are accompanied on the Dorsetshire coast.
2. The Pays de Bray, near Beauvais, is a narrow tract on the line from Dieppe to Beauvais,
extending in length, from the north-west of Neufchatel to the south of the latter city, a distance
of about thirtyEnglish miles, and in breadth, at the widest part near the middle, about eight English
miles. (See the annexed Map, Plate IX.) It is an opening, or valley of elevation, in the chalk,
* « Supplementary Remarks”, &c., (1827,) Geol. Trans., 2nd Series, vol. ii. pp. 352 and 366.
t In a paper including some account of the Lower Boulonnis: See the abstract; Geol. Soc.
Proceedings, Dec. 1826, vol. i. p. 9.
Dr. Firton on the Strata below the Chalk. 327
within whick a very slight elevation of the central tract has brought into view the subjacent
strata, as far down as those which immediately precede the representative of our Oxford oolite,
with perhaps the mountain limestone beneath. I have not myself examined this interesting district ;
and the only publications relating to it that I have seen, are the report of the proceedings of the
Geological Society of Paris during their excursion to Beauvais in 1831 *, and the splendid work
of M. Passy on the Geology of the Department of the Lower Seine} :—but from the notes and
sectional sketch of M. Cordier in the former of these works, and the full descriptions of M. Passy,
there can be no doubt that the strata in the Pays de Bray are the same with the upper part of the
series in the Lower Boulonnois.
The following is the order of the strata in the Pays de Bray, with what appear to me to be
their equivalents in England; my list of equivalents, 1 am glad to find, coinciding very nearly
with that of M. Passy himself.
1. La Craie.—(CHaAxx).
2. Glauconie sableuse de la craie.—( Upper GREEN-SAND),
Fossils said to be the same as of the Lower Chalk.
3. Marne micacée et Marne blewe.—(Gavtt).
Divisible, (at Ferte en Bray) into two portions :—1. Brown and micaceous. 2. Blue. At Meulin
the blue marl is about 50 feet thick; it abounds in iridescent fossils, among which are, Ammonites
splendens; Hamites intermedius; Inoceramus sulcatus; Nucula pectinata.
4, Gres, et sable, Glauco-ferrugineux.—(LowER GREEN-SAND).
At Cap la Héve are two beds of sand and ferruginous conglomerate, separated by a micaceous
and glauconious marl. Que. the three subdivisions of Folkstone??. At Forges and Neufchatel
the ferruginous sand is 70 feet thick: it occurs above the Argile bigarée, mentioned hereafter,
and contains, among other fossils, Gryphea sinuata. At Les Friches de St. Germain is iron ore
in grains, including small portions of ochreous hydrate of iron, with marine shells.
5. Argile bigarée (Glaise Marbré.)—Variegated marl clay, and, sand,—(of tHE WEALDEN ;
—or Beds subordinate to the Lower GREEN-SAND.)
This deposit, which, according to M. Passy, is found everywhere in the Valley of the Pays de
Bray, seems from the description to be very like the variegated sandy clay of the Wealden; but
at St. Paul, near Beauvais, it is said to contain marine shells, the species of which, however, are
not mentioned. Its place is commonly below the first stage of ferruginous sand and grit, and above
the Argile a fougéres ; a situation corresponding to the place of some of the Wealden marls.
6. Argile a creusets; Argile de Forges; Argile a fougéres—(WEALD-CLAY).
This clay in one place, at Neufchatel, is extracted by means of a shaft 70 French feet in depth,
and occurs beneath sand of different shades, belonging to the Glauco-ferruginous beds,No. 4. above.
At St. Germaine la Poterie, a bed of slaty clay (lignite) is found, containing impressions of
Lonchopteris Mantellii, and from one to two metres thick§: and among the beds found by M.
Graves near Songeons, is one, described as ‘‘ Marbre d’eau douce a Paludines,” and referred by him
to the Purbeck strata||.
There can be little doubt, therefore, that some equivalent of the Wealden heds exists in this
tract; but M. Passy appears to me to be in error when he is led, (no doubt by the indistinctness
with which the strata are developed and exposed in the Pays de Bray), to regard the Wealden
* Bulletin de la Société Géologique de France, 1831, p. 1.to 23.
t Description Géologique du Departement de la Seine Inférieure, 4to, Rouen, 1832.
t Passy, p. 237 to 272 ;—and Plates I. II. II. IX. and XVII. fig. 1.
§ Passy, p. 255. || Ibid., p. 257.
VOL. IV.—SECOND SERIES. Oh
328 Dr. Frrron on the Strata below the Chalk.
generally, in England, as no more than in a particular and subordinate bed of the Glauco-ferru-
ginous sands*.
7. Grés glauconnieux; Grés vert.—(PoRTLAND-sTONE AND SAND.)
These terms are applied to green-sand passing into grit, which again passes into a calcaire
glauconnieux. Both the grit and limestone are full of green particles: they alternate with beds of
sand, and are generally quarried throughout the Pays de Bray: and the grés calcaire is stated to he
identical with that observed by M. Rozet, at Mont Lambert in the Boulonnois. Among the fossils
are Ammonites ; Crassatella ; Cuculleea; Ostrea; Serpula ; Trigonia; and teeth of the Diodon.
M. Passy justly expresses doubt whether this grit has hitherto been recognised in England, —
I believe it to belong to what I have proposed to call the Portland-sand; the characters and
relations of which, though long since generally intimated by Mr. Conybeare, have not hitherto been
fully understood in England: and, from my own observation, I have no doubt that some of the
concretional masses of the Boulonnois belong to this part of our series. It will be observed, on
comparing M. Passy’s sections with those in the interior of England, that the lower greenish
grit (Portland-sand) of M. Passy ‘+, is not conformable to the beds above ;—a fact analogous to
the existence of chasms and “ gullies”, in the Lower Purbeck, and upper part of the Portland
strata, in Oxfordshire and Bucks:—supra(111.), p. 218; (141.), p. 265; (144.), p. 276, (151.).
8. Calcaire glauconnieux ;—a limestone composed of fragments of shells, united by sparry
carbonate of lime, containing green particles, rolled grains of quartz, and flints of different hues.
The fossils include Ostrea gregarea, and other indistinct species; T’rigonia; and Crassatella. The
limestone in this group alternates with grit, and includes a bed of green or bluish marl. The
whole belongs to the group between the Portiand-sand and the Oxford-oolite in the Lower Bou-
lonnois and is represented in England by part of the series on the coast near Weymouth.
9. Marne et calcaire marneux ;—a Gryphea Virgula; Calcaire lumachelle.
The strata of this group are described as occurring unconformably—(‘ étendues en couches dis-
cordantes”), beneath the ferruginous sands: a statement which accords with the relations of the
group to the Upper green-sand,—but not to the sands of Portland. The formation is characterized
by Gryphea Virgula, and some of the beds contain Ostrea deltordea. On the coast, from Havre
towards Henqueville, it occupies a thickness of 30 metres (about 100 English feet), between the
chalk and the oolite{; and it seems to be the equivalent of the series of shale, limestone, and cal-
ciferous grit abounding in petrifactions, which connects the Kimmeridge-clay with the Oxford
oolite, on the coast of the Boulonnois, and of Dorsetshire.
10. The lowest strata of the Pays de Bray “consist of blackish compact limestone, like that of
‘“« Marquise in the Lower Boulonnois ;—the carboniferous limestone of England:” and these suc-
ceed immediately to the group last mentioned. If this be so, the oolitic series, from the Oxford
oolite to the bottom of the lias, is wanting; together with new red sandstone and the coal forma-
tion :—another point of resemblance to the Lower Boulonnois.
(168.) Marine deposits coeval with the Wealden.—It is obvious that, during
a period of time sufficient for the accumulation of the Wealden, the deposition
of matter in the adjacent seas could not have been inconsiderable ; so that we
might expect to find, interposed between the strata which then formed the
* « .,..que l’argile Veldienne qui contient les coquilles d’eau douce, n’est qu’une couche
“ particuliére de terrains glauco-ferrugineux d’Angleterre.”—p. 256.
+ Passy, p. 272; and Plates I. and II. t Ibid., p. 262, 265.
Dr. Fitton on the Strata below the Chalk. 329
‘bottom of the sea, and the Lower green-sand, a series of beds coeval with
the Wealden in point of date, but differing from it in possessing the charac-
ters of a marine deposit, and including marine shells and other productions of
salt water ;—with which, near the shore, the productions of the land, or even
the freshwater shells of the rivers, might be occasionaly intermixed. And if
the Portland strata constituted at that epoch, both the dry land, and the
bottom of the sea, and were afterwards submerged, we ought now to find the
Lower greensand, in some places immediately in contact with the Portland,—
in others with the Wealden,—and in others again with the marine equivalent
of this latter group.
Two results would probably attend the state of things here supposed, which
are deserving of notice: Ist, That the Wealden and its marine equivalent
could not both be found in the same place ; and consequently, (since we have
the former in England), that the marine beds of that date are not to be
expected generally in this country: 2ndly, That the marine fossils of the
beds cotemporaneous with the Wealden would probably be distinct, both
from those of the Portland group beneath, and of the Green-sands above
them ; a consideration which gives peculiar interest to the fossils of this in-
termediate group.
The strata between the chalk and the oolitic system on the continent of
Europe have not yet been sufficiently examined, to furnish all the evidence
that may be expected upon this subject ; but indications of such an equivalent
to our Wealden as has been mentioned, have been already found in so many
detached points, that its occurrence in other places, or even the existence
of a continuous marine deposit of that age, is by no means improbable.
Mr. De la Beche* has brought together evidence which shows that such a
group exists in the department of the Haute Sadne, in France ; at Candern, in
the Brisgau ; near Aarau ; in Poland ; and on the confines of Silesia. To these
may be added the Isle of Bornholm in the Baltic, and the vicinity of Helsing-
burg, in Scania, which have afforded specimens of fossil plants resembling those
of our Wealden, along with marine shells ; but at Bornholm, although the
shells are also marine, they are generally such as may be supposed to have
inhabited, either the estuary of a large river, or the seas immediately ad-
jacent to the coast.
In most of the cases mentioned by Mr. De la Beche, a group of strata between the chalk and the
dolitic system is found to contain pisiform iron ore; but the fossils which accompany that mineral
are marine. A very extensive deposit of this kind in Poland and Silesia is described by Professor
Pusch, which includes also argillaceous iron ore; and among its-fossils are the genera Ammonites,
* Geological Manual, (1833.), p. 309.
2u 2
330 Dr. Firron on the Strata below the Chalk.
Cardium, Venus, Trigonia, Sanguinolaria. The pisiform ore of the Haute Saéne appears from the
statements of M. Thirria to be above the Portland strata; butits relations to the superior forma-
tions are less distinct. It contains Ammonites, Hamites, Nerinea, Cirrus, Terebratula, and
Pentacrinites, with teeth of fishes and of Saurians : and it is observable that the uppermost stratum
in the group supposed by M. Thirria to represent the Portland stone, is “‘a compact conchoidal
** limestone, a little tubercular, which contains a species of Paludina? near to Vivipara fluviorum
“of Sowerby ;”—a description which might very well be applied to some of our Purbeck
strata.
M. Walchner has ascertained that the pisiform and reniform iron ores of Candern, belong te
two distinct formations, of very different date. The lower rests upon beds of “ Jura limestone ”,
which he refers to the Coral-rag or Portland-stone, and which are decidedly below the molasse of
Switzerland. The second and more recent pisolitic deposit occupies eroded cavities on the sur-
face of several different formations; it consists of transported matter containing fossil bones, and
is not covered by any solid strata. M. Merian is cited by M. Walchner in support of this view of
the relations of these deposits; but in the description given by the former, of the strata which im-
mediately cover the pisiform ore of Aarau, there are features very like those of our Wealden
itself: for they are mentioned as consisting of ‘“ grit and bituminous schist passing into lignite, and
“containing a great number of petrifactions, among which, though commonly indistinct, are a
‘Planorbis, and other freshwater shells.”
The doubt which obviously presents itself with respect to the evidence above mentioned, is,
whether a formation thus contiguous to the green-sands, and so very nearly coeval with them, may
not really be a part of that formation itself; the presence of some fossils distinct from ours, not
being sufficient to prohibit this identification. But the peculiar character and abundance of the
iron ore, are important circumstances of difference.
The evidence respecting Bornholm occurs in a paper read before the Geological Society by
Dr. Beck of Copenhagen*, who states that the beds below the cretaceous group in that island,
exhibit many of the characters of a coal formation, containing coal and numerous impressions of
ferns, among which are several of the genus Pecopteris; and with these was found the seed
vessel of a Restiacea, considered by Dr. Beck as identical with one from the Hastings-sand at
Heathfield in Sussex, which he himself had seen in Mr. Mantell’s collection. The existence
in the vicinity of Hoer, of fossil plants analogous to those of the Wealden, but probably be-
longing to the oolitic series, had been previously pointed out by Mr. Adolphe Brongniart+: but
from what has been very recently mentioned to me by Professor Nilsson of Lund, after he
had examined some of our best collections of the Wealden fossils, it is probable that a deposit
contemporaneous with that formation may be found at Helsingburg in Scania, between the chalk
and green-sands which occur near the coast of the Baltic, and the Lias, known to exist on the
north-west of that place
The observations of M. Boblaye in the northt, of M. Desnoyers § in the north-west, and of
M.Dufresnoy|}; in the south-west of France ; with those of M. Elie de Beaumont, on the boundary
of the Paris and London Basins] ; of Mr. De la Beche **, M. de Caumont++, M. Desnoyers{f,
* « Proceedings ” (1835-6) vol. ii. p. 217. + Annales des Sciences Naturelles, 1825.
+ Ibid., 1820, t. xvii. p. 35. § Ibid., 1825, t. iv. p. 353. || Ibid., 1829, t. xvil. p. 192
@ Ibid., 1829, t. xvii. p. 354. ** Geol. Trans. 2nd Series, vol. i. p. 13.
++ Mém. de la Soc. Linn. du Calvados, t. i. 1824, p. 49 et 67; t. ii, 1825. p. 447, &e.
cs Mém. de la Soc. d’Hist. Nat, de Paris, t. ii. 1825.
at
Dr. Firron on the Strata below the Chalk. 331
M. Constant Prevost*, and M. Passy t, on the coast of Normandy and the adjacent district ;
and more recently of M. Thirria, in the department of the Haute Sadnef, have shown that many
of the beds between the chalk and the oolitic system in the different provinces of France, agree
with each other, and with those of England, perhaps as nearly as the more distant portions of the
same formations are found to do in our country: the Portland strata, which form the lower
boundary of the Wealden, occurring at several detached points along their course ; while above
them, the chalk affords a limit which cannot be mistaken. It may deserve the inquiry, there-
fore, of resident geologists, whether traces at least, of all the intermediate groups between the
Portland and the chalk may not be detected generally along the line of connexion; and I am not
without hope that the task of comparative examination may be assisted by the preceding pages.
Among the points deserving of notice by those who examine the beds below the chalk in dis-
tricts imperfectly known, I would mention especially the characters of the Portland Sand ;—from
the facility with which that formation may be confounded with other sands, likewise charged with
green particles. I have reason to believe that a neglect of the distinctions between these dif-
ferent sands, and a consequent ignorance of the distance by which they are separated in the series
of strata, has produced difficulty, and led to much confusion in the arrangement of the groups be-
tween the chalk and the oolitic system.
(169.) Beds below the Wealden.—The groups next below the Wealden,
in the tracts described in the preceding pages, are connected by several cha-
racters; the Portland sand forms a transition to the Kimmeridge clay;
and the latter, at its lower part becomes charged with sand and calcareous
matter, and passes insensibly into the Oxford oolite. The fossils, also, of
these associated groups are very much allied, and there is no reason to suppose
that the deposition of this part of the series was interrupted by any important
change of circumstances.
Portland strata.—The space occupied by the Portland strata, so far as they have yet been dis-
covered in England, is bounded on the west by a line passing from Portland to the outcrop of the
Portland stone in the Vale of Wardour, and thence towards Swindon. On the east of that line
the Purbeck and Portland formations are visible only in the remaining portions of the once-
continuous sheet, which seems originally to have invested a great part of Oxfordshire and Buck-
inghamshire. Whether the Portland beds exist, or ever have existed, under the sands of the
Isle of Wight, Sussex, and Kent, it is now impossible to say; though it is probable that they
did so, from their occurrence on the opposite coast of France, and their thickness in that
quarter.
The peculiar circumstance relating to the junction of this formation with the Purbeck beds, is
the distinct character of superficial soil, which the bed in which the trees and Cycadee are found,
exhibits in the Isle of Portland. Trees and plants have occurred in the upright position in
many other places, and in other parts of the series of strata; but the soil in those cases had lost
its recent character, and been in a great measure assimilated to the surrounding matter. Some
other thin beds alternating with the lowest strata of the Purbeck limestone, have likewise more
* Mém. de la Soc. d’Hist. Nat. de Paris, t. ii. 1825. p. 389.
+ Sur le Département, §c. 4to, Paris, 1833.
t Mém. de la Soc. d’Hist. Nat. de Strasbourg, 1830, t.i.
332 Dr. Firron on the Strata below the Chalk.
or less of the character of a mechanical agglomerate ; but none of them approach to the grayel-
like texture and composition of the “ Black-dirt” of Portland and the adjacent coast.
The small extent which the Portland strata occupy with reference to the Kimmeridge clay, is
a remarkable fact ; showing either that the former, like the Coral-rag, was originally deposited in
detached portions ;—or that the portions of the Portland group that we now see, are only the re-
maining and eroded borders of one continuous coating originally lodged upon the clay.
It is remarkable, also, that the Wealden has not yet been found beyond the limits of the Port-
iand group; never reposing, as the green-sands are frequently seen to do, on any of the
formations beneath the Portland stone: but before this exclusion be adopted, it will be necessary
to examine more completely the counties on the north of Buckinghamshire. Reciprocally, in all
the places where the Portland beds have hitherto been found, one or more members of the
Wealden group are connected with it. It is possible, therefore, that the Portland strata formed the
only land, at the period when the freshwater beds of the Wealden group began to be deposited.
The Kimmeridge clay thus more widely diffused than the Portland and the Wealden, forms
the continuation upwards, of a long series of alternate strata of oolitic limestones, sand, and
clay. The extent, thickness, and development, of this formation, vary much in different places,
the upper beds alone being visible at the point from whence the name has been derived. The
relations of the groups are fully seen on the coast near Weymouth, and still more completely on
the shore of the Boulonnois, and near Scarborough: but, although the clay extends, without
interruption, from Dorsetshire to Norfolk, it is seldom seen to advantage in the interior of En-
gland. Near Oxford, the lower members, which form the transition from the bituminous clays
of Kimmeridge to the Oxford oolite, are evidently wanting; and the surface of the calcareous
reestone beneath the clay, is deeply worn and eroded.
(170.) Composition of Strata.—Among the circumstances relating to the
composition of the strata above mentioned, below the chalk in the South-East
of England, the following are deserving of attention.
1. Proofs of the formation of stone, in the midst of strata of gravel, sand, and clay, distinctly of
mechanical origin. This fact, which is of universal occurrence throughout the series of secondary
strata, is especially remarkable in the Lower green and the Hastings sands of Kent and Sussex :
sex: the former containing masses of siliceous grit, chert, and chalcedony, and concretions of
chert, evidently formed subsequently to the division of the beds which inclose them, yet traversed
by the same lines of false stratification which pervade the looser matter :—(22.) and (23.)
2. The change, in the fossil trees of Portland, of the original woody substance into silex ; and
the contrast of their composition with that of the surrounding matter in the “ Dirt-bed”, in which
fragments of soft limestone are abundant; the strata, both above and below, likewise, consisting
principally of carbonate of lime. In the Lower green-sand also, at Woburn, the petrifying
petrifying matter of the coniferous wood is silex*.
3. The shells preserved in the green-sands of Kent, consist of carbonate of lime; but in the
sands of Blackdown, though shells occur in still greater numbers, the calcareous matter has almost
entirely disappeared, and with very few exceptions has been replaced by chalcedony; and the
surrounding sand, instead of effervescing with acids, imbibes them tranquilly.
* The fact remarked by Mr. Brown, that all the fossil wood hitherto discovered in the strata
mentioned in these pages, is either monocotyledonous, coniferous, or cycadeous, has been
already adverted to: (112.) p. 225.
Dr. Firron on the Strata below the Chalk. 333
4, The occurrence of oolite containing freshwater shells, near the bottom of the Purbeck strata
at Combe Wood (144.), p. 275-6, is another fact deserving of notice, and may perhaps explain
some doubtful appearances in the uppermost bed of the Portland Series (the Roche); which,
although full of marine petrifactions, and commonly oolitic, has very much the aspect of fresh-
water limestone. It can easily be imagined that the bank, or land, consisting of the Portland
strata, when first raised above the sea, was covered with marine remains, which might subse-
quently have been cemented together, at the bottom of a freshwater lake.
5. The existence of pisolitic (or granular) oxide of iron, in the Wealden, is probably not con-
fined to the coast near Hastings, where I found it to be generally diffused; p.166. The fact of its
occurrence in this formation is the more deserving of notice, from the great abundance of that ore
in the marme deposits supposed to be contemporaneous with our Wealden, in other parts of Eu-
rope: supra, (168.) p. 330.
(171.) Stmilarity of Deposits of different Epochs.—The mineralogical
resemblance between some of the strata above and beneath the Wealden,
is very remarkable.—T he upper part of the Portland formation in the Vale
of Wardour is so like chalk, that it bears that name in some of the quarries;
and both there and upon the coast of Dorsetshire it contains flint nodules,
not distinguishable from those of the chalk.—The Portland sand abounding
in green particles, cannot, in itself, be distinguished from the green-sands
above the chalk, nor from those below; the green matter in all is of the
same nature; the calcareous concretions are like those of the ‘ Kentish-
rag”: yet the deposition of these groups was separated by intervals
of time sufficient, in the first two cases, for the accumulation of all the
Wealden strata, and in the two latter, for that of the chalk.—The strong re-
semblance of the variegated sands and marl of the Wealden to those of the
new red sandstone, and of both to the tea-coloured and variegated marls of
the beds above the chalk in the Isle of Wight, has been already mentioned.
—The Wealden, again, has many striking points of resemblance to the coal
measures. ‘The shale, sandstones, and clay iron-stone of the latter are not
distinguishable from those of the Hastings-sands, which are, in fact, a coal
formation : and in addition to the Unios and other freshwater shells long
known in the coal formations, the recent discovery of Cypris, in freshwater
limestone, among the coal measures in Scotland*, is another point of agree-
ment.
These resemblances, of which other examples might easily be given, in de-
posits separated by great intervals of time, demonstrate the identity of the
processes which are still going on with those of the more ancient epochs,
* See, however, upon this subject, the remark of Mr. Sowerby, as to the possible resemblance
of the fossil crusts of the marine genus Cytherina, to those of Cypris: Appendix, p. 345, under
the head Cypris Valdensis.
334 Dr. Firron on the Strata below the Chalk.
and prepare the mind for the reception of other proofs of that continuity of
action, which has of late been so ably discussed.
(173.) Fossils.—A systematic list of all the fossils mentioned in the pre-
ceding pages* is given in the Appendix B: andI have connected with ita series
of columns, exhibiting at one view the stratigraphic distribution of the several
species. My collection is so incomplete, that many of the columns are un-
occupied ; and most of them afford very inadequate representations of the
facts: but it will be advantageous to keep in view the completion of such a
list, whenever sufficient materials shall be obtained to fill it up. The number
of specimens collected from any given district or series of strata, depends on
so many circumstances purely accidental,—the texture of the matrix, the num-
ber of open quarries, the relative skill and activity of collectors,—that the
richest collections can very seldom be regarded as fairly representing the
fossil contents of the groups from which they are obtained ; and there still
are large tracts, in every part of the English series, the fossils of which are un-
known. The proportion, therefore, which the species we are acquainted with,
bear to the whole number contained in the strata, is so far from being de-
termined, that any general reasoning upon this subject at present would be
of little value.
From the imperfect lists of fossils given above, it would seem that even
short distances are attended with greater variation in the contents of the
strata, than might have been expected ; and that although some species pervade
the whole range of the formations in which they are found, others occur in
several of the tracts described which have not yet been obtained elsewhere.
I cannot conclude these pages without expressing my great obligation to
Mr. Lonsdale, for his kind and unremitting assistance during their passage
through the press ; which has been doubly acceptable, from its having been
conferred on me by one of my most valued personal friends.
W. H. EF
London, August 16, 1836.
* It may be proper to mention here, that the whole of the author’s collection re-
ferred to in the preceding lists, has been presented to the Geological Society, and will
be found in their Museum.
App. A. | Dr. Fitton on the Strata below the Chalk. 335
APPENDIX.
APP. A.
Descriptive Notes respecting the Shells figured in Plates XI. to XXIII.
By James pe Carte Sowersy, F.L.S. &c.
PLATE XI.
Fig. 1. Tornatella elongata. Elliptical, elongated; surface furrowed; furrows crossed by
short lines ; whorls about four ; lip slightly thickened. This resembles Acteon ( Tornatella) simu-
latus (Min. Con. t. 163. f.2.) of the London clay, even in the dotted furrows upon the surface of
the shell, but it is much longer in proportion, and is only half the size.
Fig.2. Lucina? globosa. A nearly globose smooth shell, with the lines of growth peculiarly
waved near the posterior margin. TI have not seen the interior.
Fig. 3. Avicula Grypheoides. ‘The convex valve nearly orbicular, with a projecting incurved
beak, and two small unequal ears: when alone, it may easily be mistaken for Znoceramus con-
centricus, but the parts about the beak, especially the ears, show the difference. The other valve is
nearly flat, orbicular, and has one small and one large ear. The convex valve a. is represented
from specimens found at Nursted in Hampshire ; the other valve, b. is from Cambridgeshire.
Fig. 4. Pentacrinus. The stem only has yet been found; it is various in size, the sides are
concave, the angles rounded. Joints equal, the margins of their surfaces ornamented with short
strie. Some specimens show the bases of lateral arms. It strongly resembles a species found in
the chalk ;—(Mantell ; Fossils of the South Downs, p.183; Geol. of the S.E. of England, p.112.);
which is, however, much larger.
Fig. 5. Pollicipes levis. The lateral valves are rhomboidal, smooth, thin, and nearly flat: in
the partially decomposed state in which they are found, they appear to be composed of layers, of
different degrees of transparency and depths of colour. This species also occurs in the green-
sand at Blackdown: see Plate XVI. fig. 1.
Fig. 5*. Pollictpes unguis. Smooth, the valves are all remarkably curved, and broad in pro-
portion to their length.
Fig. 6. Pollicipes radiatus. Valves wedge-shaped, flat, marked with sharp, elevated rays, di-
verging from their apices.
Fig. 6*. Pollicipes rigidus is distinguished by thin transverse elevations, which are very promi-
nent upon the posterior valves: the lateral valves are elongated.
Fig. 7. Venus? tenera. Shell lenticular, rather transverse, neatly marked with concentric
strie ; lunette lanceolate.
Fig. 7*. Venericardia tenuicosta. Transversely oblong, approaching to square. It varies
much in convexity: and when old or interrupted in its growth, is nearly globose, rather heart~
shaped. Specimens have been found twice the length of that represented in the figure, both
of the oblong and globose form. The surface of the rays is rough, with slightly elevated obtuse
scales. The interior of the margin is crenated. Lunette rather deep, heart-shaped.
Fig. 8. Nucula bivirgata. Very convex; the surface ornamented with two sets of linear
furrows, which meet towards the posterior slope, at acute angles directed towards the beak of each
valve; the junction producing a regular line, without forming a ridge. Lunette broad.
VOL. 1V.— SECOND SERIES. 2x
336 Dr. Firron on the Strata below the Chalk. App. A.J}
Fig. 9. Modiola bella. Neatly striated, convex, with parallel edges, nearly equal sides, and
obtuse beaks.
Fig. 10. Lima semisulcata. (Plagiostoma semisulcatum, Nilsson, Petrif. Suec. 25, t. ix. f. 3.)
Ovate elongated, very convex, the beaks incurved, short ; ears nearly equal, sinall. Where the
lines of growth cross the ridges, which vary in number from 11 to 16, they form obtuse, short
scales or grains.
Fig.11. Auricula inflata. (Benett’s Catalogue of Wiltshire Fossils, 4to, p. 2.) Shell ovate;
spire small, pointed ; the last whorl large; aperture at the lower part approaching to square,
but with one of the upper angles elongated and acute; the lips united, thick, obtuse; the colu-
mella has two plaits, the lower sometimes divided by a groove along its middle. The surface of
the shell is marked with numerous spiral lines of elongated punctures. The thick lip separates
this from several species of Tornatella, to which in other respects it bears a strong resemblance.
Auricula incrassata of Min. Conch. t. 163. is shorter and smaller, and has the lip more enlarged.
A. incrassata of Mantell (Geol. Sussex, t. xix. figs. 2, 3, and 34.) also resembles it, but has a
much shorter spire.
Fig.12. Natica canaliculata. (Ampullaria canaliculata, Mantell, Geol. Suss. tab. xix. fig. 18.)
Globose, depressed, smooth. Umbilicus large, circular, gradually expanded into the base. Around
the upper edges of the whorls is a concave, transversely striated groove, best defined in the
young shell,—as in c. The inferior specimen, a. b. is filled with brownish phosphate of lime.
See the figure of a much larger specimen, Plate XVIII. fig. 6.
Fig. 13. Solarium ornatum. Discoid, with a small portion of the spire elevated and acute ;
aperture rhomboidal. Surface, above ornamented with obtuse, radiating ribs,—and near the
margin, both above and below, with granules in quincunx order.
Fig. 14. Solarium conoideum. (Min. Conch. t. 11.) A conical shell as high as it is wide; the
umbilicus large and smooth. The outer coat of the shell is represented in this figure; and shows
the upper part of each whorl to be concave, and elegantly marked with decussating strize forming
rows of granules; aperture rhomboidal, nearly square.
Fig. 15. Pyrula Smith. Ovato-fusiform; two obscure keels and numerous strie wind
round its surface; spire rather elongated, acute. ‘These two figures, perhaps, represent different
species: fig. a. is more distinctly keeled than fig. b., which, however, being considerably worn, —
has lost much of its external sculpture; but shows also longitudinal undulations, which can
hardly be traced upon fig. a. Both the specimens are from Copt Point, near Folkstone. Murex —
Smithii (Min. Con. 578), lately removed to the genus Pyrula, is a different shell. ie
Fig. 16. Rostellaria elongata. Presumed to be a Rostellaria, from its resemblance to R. mar-
ginata, fig. 18. ; from which it differs principally in its great length and the smaller number of”
ribs. Turrited, much elongated, ribbed, transversely striated; upper edge of the whorls smooth.
Fig. 17. Rostellaria buceinoides. A neat, subulate, costated shell, approaching to A. rimosa ;
it has but one varix upon each whorl: the lip is not lobed.
Fig. 18. Rostellaria marginata, ‘Turrited, conical, transversely striated ; ribs eight or ten upon
each whorl, short and obtuse ; last whorl keeled, without ribs. Named from a ridge or narrow
band upon the upper edge of each whorl; which is more or less conspicuous in every specimen,
and assists in distinguishing the species from Rostellaria Parkinsoni. See Pl. XVIII. fig. 24.
Fig. 19. Rostellaria carinata. (Mantell; Fossils of the South Downs, p- 86, Pl. XIX. figs. 10,
11,12, and 14.) This figure, from a drawing by the Rev. G. E. Smith, exhibits the lip in an ad-
vanced stage of growth. The spire is nearly subulate, composed of eight or nine convex whorls;
a row of small tubercles, or short ribs, winds round the middle of each whorl except the last,
-
v3
a
App: A] Dr. Firron on the Strata below the Chalk: 337
which has two acute keels; the lip has a long forked projection arising from the upper keel ;
the beak is long and subulate; the whole surface striated.
Fig. 20. Ammonites? circularis. Aperture circular; whorls just touching each other: nearly
close, acute, cif¢ilar; sometimes forked ridges cover the surface. This specimen may, perhaps,
be a portion of an Hamites or Scaphites ?
Fig..21.. Ammonites symmetricus. Aperture nearly square; ribs blunt, slightly tumid as they
approach ‘the hollow in which the rounded keel is immersed, and though not equal in length,
elegantly uniform in their elevation; the sides of the whorls flattened. The specimen here fi-
gured, though a fragment only, differs from every Ammonite known to me.
Fig. 22. Ammonites crenatus. Sides flattened; the inner whorls much exposed, their margins
nearly smooth and rounded, those of the outer whorls crenated on each side of a narrow concave
space over the siphuncle. Distinguished from 4, splendens by the more exposed inner whorls.
Fig. 23. Ammonites cristatus. (De Luc, in Brongniart, Env. de Paris, pl. vii. 10.) Some of the
ribs being acute and much more elevated than others, form the distinguishing character of this
species. I believe 4. cristatus and A. subcristatus of De Luc to be varieties of the same species :
I have seen both from Folkstone : the specimen before us belongs rather to the latter variety.
PLATE XII.
Figs. 1, 2. Hamites rotundus. (Min. Conch. tab. Ixi. fig. 2, 3.) The peculiar structure of the
inner extremity in this species, is indicated, rather than distinctly seen, in these figures ; which
have been engraved from drawings by the Rev. G. E. Smith, taken from specimens collected by
Lord Greenock, near Copt Point in Kent. Mr. Smith observes, in a note sent with the drawings,
that the termination in a minute whorl, (imperfectly seen in the figures,) had been
traced distinctly in more than one specimen; which proved that the coils of the spiral
were nearly parallel to the straight part of the stem, and the axis at right angles to
it. The spiral appears to have been open, as in many recent Serpule; so that its
perfect preservation in the fossil could scarcely have been expected : and this would 4
account for the defective state in which the Hamite is commonly found. Mr. Smith adds that the
spiral portion appeared invariably to have been decayed, as if it had been filled up with soft
Matter, as in the case of Magilus. The figures show the remains of the spiral, in two different
specimens; but in both much broken and displaced. The spiral part is round, with contiguous
annular ribs, also round and regular.
Fig. 3. Hamites attenuatus. (Min. Conch. t. lxi. fig. 4. and 5.) Both ends of this species, when
complete, are similarly bent or folded in, not spirally, but so that the segments become parallel
toeach other. The larger parts are rather compressed, the smaller cylindrical; the ribs are
annular and rounded.
Fig.4. Hamites spiniger. The general form of this species is like that of Scaphites Yvanii,
(Bull. de la Soe. Géol. de France, vol. ii. p. 355, pl. ii.) ; one portion being a flat volute, like an
Ammonite, but with unconnected whorls; the other bent into the characteristic form of a Hamites:
the sides are flattened. The spines form one of the chief specific characters: there are three
rows of them on each side, placed upon the larger ribs on the involute part of the shell ; they are
gradually lost upon the other parts.
PLATE XIII.
Fig. 1. Echinus? arenosus. 'The underside is imperfect, and the genus therefore doubtful.
Fig. 2. Panopea rotundata. Only a cast, which is nearly smooth. The ridge separating the
posterior area, which is small, is strongly marked, and projects on the margin.
2x2
338 Dr. Firron on the Strata below the Chalk. [ App. A.
Fig. 3. Trigonia spinosa, var. Distinguished from Trigonia spinosa (Min. Conch, t. lxxxvi.),
of which it is a variety, by the presence of longitudinal ridges continued from the bases of the
spines, and by its more oblique form. It is often longer than the specimen here figured.
Fig. 4. Diceras Lonsdalii. The small portion hitherto examined of the external impression
of this curious fossil, shows the shell to have been squamose, like an Oyster, and of considerable
thickness. The two valves are less equal in size than is usual in the genus Diceras. The
larger valve is an elongated cone, rather flattened and curved twice round; and it appears to have
been attached to some foreign body, as in Diceras arietinum. The other valve has only an
oblique conical umbo.
PLATE XIV.
Fig. 1. Pholas giganteus. In general aspect much resembles a Pholadomya; but the appa-
rently squamose structure of the surface shows it to belong to the same section of the Pholades as
P.candidus. Its valves are so convex as to form nearly a cylinder when closed. The reflected
margin near the beak, so large in some Pholades, is probably broken away in this specimen.
Fig. 2. Modiola lineata. ‘The depth of each valve is equal to its width; the beaks are ob-
tuse ; the margins are arched and nearly parallel; the surface Jongitudinally and finely striated.
Fig. 3. Avicula pectinata. A slightly convex shell, with large, square, depressed ears, and
short acute linear ridges, alternately longer.
Fig. 4. Ostrea retusa. This, like most Oysters, is very variable in form, but generally much
curved and nearly orbicular; the shell is moderately thick, plain in the middle, but strongly
plicated at the margin with angular plaits. It occurs in massy groups. It is not so flat as
O. semiplana, a fossil of the chalk ; nor are its valves so equal, nor so thin, as in that species,
which it otherwise much resembles.
Fig.5. Anomia radiata. Irregularly orbicular, flat, finely radiated. The radii are coarser,
and more distant, than the fine striae which occur in the London clay species, Anomia lineata,
(Min. Conch. t. 425.)
Fig. 6. Anomia levigata. Much smoother, and more even, than any other known species :
very thin, orbicular, and flat. The figures a. and b. are taken from different specimens; a. in
Mr. Smith’s collections; b.in Mr. Sowerby’s.
fig. 7. Anomia convera. A remarkably convex species, with a large and prominent beak,
and smooth surface. The furrows are produced by a Terebratula to which this specimen was
attached, and to which it consequently bears a great resemblance.
[The name of this new species has been omitted, by mistake, in the list of Lower green-sand
fossils of the Isle of Wight, p.204. It was found there in the debris fallen from the cliff, on the
shore east of Shanklin Chine. |
Fig. 8. Yerebratula Tamarindus. Nearly orbicular, smooth; margin very obtuse. Disk
rather flattened ; beaks but little curved, with an angular, slightly prominent ridge on each side,
passing down the sides of the valves.
Fig. 9. Terebratula quadrata. Ovate, gibbose; beak large; front broad, straight, with a
few large plaits.
Fig. 10. Terebratula Faba. Elliptical, narrow, gibbose; front concave, but not elevated,
very narrow ; the perforated beak short, but prominent.
Fig.11. Terebratula elegans. Transversely obovate; beak prominent, pointed, nearly straight;
plaits numerous, sharp ; front slightly elevated, straight.
Fig.12. Terebratula convera. Angles rounded; valves very regularly convex; beak large;
plaits numerous, rounded ; front slightly elevated.
App. A. | Dr. Frrron on the Strata below the Chalk. 339
Fig. 13. Terebratula parvirostris. Imperfectly tetrahedral, rounded; beak small, sharp;
sides slightly produced and angular; plaits numerous, angular ; eight or nine of them much ele-
vated in the front.
Fig. 14. TYerebratula prelonga. Ovate, much elongated, gibbose; front slightly elevated,
with a depression in its middle ; beak prominent, large ; surface smooth. The figure a. is from
a drawing by the Rev. G. E. Smith; b. from another specimen, also found near Sandgate.
Fig. 15. Lingula? truncata. Ovate, depressed, flattened most along the middle; front
straight.
Fig. 16. Pleurotomaria gigantea. (Trochus; British Mineralogy, t. 403.) Conical, height and
breadth equal; whorls slightly overlapping each other; sides straight; surface concentrically
striated. The transversely striated band proceeding from the deep sinus in the lip, which marks
the genus, is well preserved on a specimen seven inches in diameter, in the collection of Charles
Manning, Esq., who obtained it from near Hythe, after this plate was engraved. Some speci-
mens of this shell are so much changed by pressure as not to be above one inch high, while they
are three or four inches in diameter, with a sharp margin.
Fig.17. Ammonites furcatus. Discoid, sides and front flat; inner whorls partly exposed ;
aperture with a square front, oblong, deeply impressed with the preceding whorl, lateral angles
truncated ; ribs not very numerous, thick, curved, many of them forked, passing at right angles
across the front.
PLATE XV.
Scaphites Hillsii*. General form obovate, compressed ; the inner whorls exposed, not touching
each other, but still curved into a regular volute, compressed, bearing numerous small, close»
rounded ribs: the outer whorl strikes off from the others, in nearly a straight line, to a con-
siderable distance, and then bends back so that the aperture nearly touches the preceding whorl,
furnished with ten or more distant, very prominent, sharp-edged ribs, which are most raised
upon the sides. Aperture nearly square, thin-edged, preceded by a short rib over the front;
Siphuncle small, close along the front, or outer margin of the whorls ; septa much sinuated, not
very close. ‘The system of inner whorls occupies rather more than half the longest diameter of
the entire shell, which is about fourteen inches.
Fig. 1. represents a specimen of the inner whorls, reduced to half the real diameter. A small
Exogyra was found attached to the inner margin of one of the whorls of this individual, showing
that there was always a space between it and the next whorl.
Fig. 2. is drawn from a portion of an outer whorl, also half the natural size. The specimen is
irregularly flattened.
The above description has been made from several nearly entire specimens, obtained from the
vicinity of Maidstone after this plate was engraved, and now in the possession of Sir Philip Grey
Egerton, Mr. Bowerbank, and Mr. Sowerby. An outline, taken principally from Sir P. G. Eger-
ton’s specimen, on a scale of one fifth of the original dimensions, is inserted in the plate at fig. 3.
Mr. Sowerby has also a specimen, from the same place, of a species nearly agreeing with this
one, but probably distinct: it is much larger; and its system of inner whorls is free from radii
and undulations.
* In the list at p. 128, this fossil is erroneously called Hamites; perfect specimens not having
been found, when that page was printed.
340 Dr. Fitton on the Strata below the Chalk. [ App. A.
PLATE XV. a.
Siphonia pyriformis. (Goldfuss, Petrefactenkunde, tab. vi. fig. 7.) This plate represents several
varieties in the form of this Siphonia, with some details of its structure ; from which it may be
inferred that the upper, enlarged part becomes broader in proportion, and more pear-shaped,
as it increases in size. But although this may be stated as a general rule, the exceptions are
numerous, and there seems to be as much variety in the form of the full-grown specimens of the
fossil, as in that of the fruit from which this species has been named.
Figure 4, a specimen nearly entire, shows the root-shaped, lower, part of the stem, by which it
was fixed to the rock on which it grew. The condition of the fossil does not enable us to speak
decidedly as to the original state of the external surface in the living animal: we can perceive,
however, that beneath the surface was a system of large tubular canals, placed in a circle, with
some degree of regularity as to their distance from each other, and succeeded at intervals by
other concentric circles of similar tubes. These are shown in the vertical and horizontal sections
fig. 6. and 7., which had been very carefully ground down by the late Mr. Miller, for the pur-
pose of showing the structure, and in the broken and abraded specimens, fig. 4. and 5. Fig. 8. is
a specimen of a lower portion of the stem which belonged to the late Mr. Goodhall, F.G.S:
Its external surface having been removed, the tubes which form the lower part of the stem are
well displayed: and a similar observation may be applied to the head, fig. 5.
In fig. 9. a head is represented, the greater part of which is embraced by a Serpula. From
this tube being at present nearly half immersed in the substance of the head, and from the
groove-like impression visible in some places, it would appear that after the Serpula had attached
itself, the head must have increased considerably in diameter; still, however, preserving its
general form and proportions, where not covered by that tube.
PLATE XVI.
Fig. 1. Pollicipes levis: from Blackdown, Devonshire. Supposed to be of the same species
as Plate XJ. fig. 5, found in the Gault near Folkstone.
Fig. 2. Serpula filiformis. The mode of grouping in this Serpula is remarkable. It consists
of smooth, round tubes, slightly curved, and aggregated into elongated, often branching masses.
The tubes are rather thick, nearly equal throughout their substance. This fossil may be the same
with that which Goldfuss calls S. soczalis, (Petrefactenkunde, tab. lxix. fig. 12.) ; but as he iden-
tifies the species from the oolite with that of the green-sand, I would retain his name for the
former only. The substance of this shell in our green-sand fossil is thinner, and the tube gene-
rally more curved, than in the S. soczalis of the oolite.
» Fig: 3. Serpula Tuba. Simple, almost solitary tubes, of nearly uniform diameter throughout;
shell ‘thin. ;
- Fig. 4. Serpula Vermes. The tube gradually increases in size, and has a carina along its
upper surface. It is a larger, coarser species than Serpula carinella, (Min. Conch. t. 598. fig. 2.).)
S. conformis of Goldfuss (Petrefact. tab. Ixvii. fig. 13.) is like it, but has subangular sides.
Fig. 5. Panopea ovalis. The regularly oval form shown by the lines of growth, distinguish
this from the species found either in the crag or recent: neither does the anterior side gape so
much as in any of them. It is moderately convex and smooth; the beaks are nearest the anterior
side, which is closed; the posterior extremity is rounded and gaping.
Fig. 6. Mya leviuscula. So perfect is this cast in calcedony, that even the asperities of
the epidermis, such as occur in recent species, are preserved. The shell, which is nearly twice as
|
App. A. | Dr. Firron on the Strata below the Chalk. SAl
wide as it is long, is moderately gibbose, and has a characteristic depression along its middle.
The sides gape slightly. ;
Fig. 7. Amphidesma? tenuistriatum. A transversely elongated, oblong, very flat shell, with
numerous impressed stria, the posterior extremity slightly truncated ; the beaks nearly central,
not produced. The genus is rather doubtful. ’
Fig. 8. Corbula truncata. Very similar to one, or two, species in the London clay. Its form
is oblong-ovate; the posterior side is produced, obliquely truncated, and pointed towards the
front. ‘The surface is transversely striated.
- Fig. 9. Mactra? angulata. Smooth, subtriangular; the posterior side defined by a ridge ;
beaks small, nearly close ; hinge unknown.
Fig. 10. Petricola nuciformis. Suborbicular ; striated longitudinally ; the edge serrated ; the
beaks small, sunk into the shell.
Fig.11. Petricola canaliculata. Orbicular, very convex, longitudinally furrowed; furrows
nearly covered over edge graiiulated. The concealed furrows are represented in the magnified
section; the edges of the costae between them are sometimes connected across the furrows.
Fig. 12. Psammobia? gracilis. Much elongated transversely, nearly cylindrical; surface
marked with many raised lines, which are most elevated at their extremities; posterior side de-
fined, produced, and pointed.
Fig. 13. Lucina? orbicularis. Orbicular; convex; longitudinally striated; striae numerous,
often forked; beaks small, distant; edge entire.
Fig. 14. Lucina Pisum. Nearly globose ; fifteen, or more, reflected ridges cross the surface.
Fig. 15. Astarte concinna. Oblong, convex, concentrically furrowed, thick; lunette elon-
gated, deeply sunk; beaks oblique. In everything, except the elongated form, this resembles
Astarte striata, (Min. Conch. t. 520. f. 1.), which is orbicular.
Fig. 16. Astarte formosa. Orbicular, approaching to triangular, rather flat, with thick edges ;
about ten prominent reflected ridges on the surface ; lunette elongated, concave. Found in great
numbers at Blackdown.
Fig. 17. Astarte multistriata. Very convex; rather wedge-shaped; with many concentric
ridges, and numerous fine longitudinal striae between them ; lunette large and broad. A small,
rare species.
Fig. 18. Astarte impolita. Obovate, convex, rather angular at the beaks: surface anti-
quated ; ligament imbedded in a lanceolate groove.
Fig.19. Cyprina cuneata. Cordato-cuneiform ; surface even; posterior side straight, a little
produced at its extremity ; beaks prominent; valves deep; shell rather thin. The specimens
found at Blackdown are seldom larger than the small figure: the large one was in the collection
of the late Mr. Goodhall.
PLATE XVII.
Fig. 1. Cyprina rostrata. Distinguished by its general form from Cyprina (Venus) angulata
(Min. Conch. t. 65.), which it nearly resembles. It is less convex, the posterior extremity is more
produced, and the line thence to the beak straighter.
Fig. 2. Cytherea subrotunda. Fiat, lenticular, nearly orbicular, smooth; lunette elongated ;
fulcrum arched. One specimen has an Exogyra adhering to an eroded part of the surface.
Fig.3. Venus? truncata. Rather less convex than V. lineolata (Min. Conch. t. 20.); strongly
marked with lines of growth; the posterior side expanded and truncated; lunette obscure,
lanceolate.
342 Dr. Firron on the Strata below the Chalk. [App. A.
Fig. 4. Venus? submersa. Nearly orbicular; valves tumid; the posterior extremity truncated ;
lunette obscure; hinge-slope rather straight.
Fig. 5. Venus? sublevis. Very fiat, elliptical, smooth ; lunette undefined, not sunk.
Fig. 6. Venus? immersa. Very flat, ovate, smooth ; lunette deeply sunk ; its edge not defined.
Fig. 7. Cucullea formosa.’ More deeply striated than C. fibrosa; and in form resembling
C. carmata (Min. Conch. t. 207.). Very convex, transversely elongated; posterior extremity
pointed.
Fig.8. Arca rotundata. Surface longitudinally striated; the sides unequal; both rounded.
There is no space between the beaks.
Fig. 9. Nucula lineata. Elliptical; posterior extremity slightly truncated, with a short point
af its upper angle; surface transversely striated, with lines straighter than the lines of growth,
which they consequently cross twice.
Fig. 10. Nucula apiculata. Convex, smooth, transversely obovate; posterior extremity pointed.
Fig.11. Nucula obtusa. Convex, smooth, elliptical ; lunette prominent, elongated.
Fig.12. Trigonia quadrata. Nearly square, flat; anterior extremity rounded ; concentrically
ribbed ; each rib bent at a right angle in the middle, where there is an obtuse knob.
Fig.13. Modiola reversa. Transversely elongated, rather flattened; the posterior portion
expanded ; surface ornamented with thin concentric ridges, which are bent back or reversed
upon the shell. In some individuals they are worn away.
Fig. 14. Mytilus tridens. The hinge is furnished with three unequal teeth; elongated, convex,
carinated ; beaks pointed; the surface very smooth. The teeth distinguish this species from
M. edentulus (Min. Conch. t. 439. fig. 1.).
Fig. 15. Mytilus prelongus. Hinge without teeth; shell very thick, much elongated, keel-
shaped. It approaches to M. lanceolatus (Min. Conch. t.439. fig. 2.); but, independently of its
remarkable thickness, the sides are nearly parallel, as far as the termination of the hinge-line,
which is marked by an angle.
Fig. 16. Mytilus inequivalvis. Shell broad; one valve much flatter than the other; both
smooth.
Fig. 17. Perna rostrata. Ovate, nearly flat; the surface very smooth; the lesser wing pro-
duced; the shell thin, contracted at its base. Fragments of this species are very common at
Blackdown, but perfect specimens rare.
Fig. 18. Avicula anomala. Obliquely elongated, imperfectly five-angled, flat along the middle;
many longitudinal, narrow, elevated ridges extend over the surface, and are crossed by fine lines
of growth. The valves are very deep, together measuring about 14 inch, with a square section;
length three inches. This shell I believe to be an Avicula, although the hinge is not visible.
Fig.19. Pecten Millerii. Oblong, rather convex ; radii smooth, sharp, numerous, especially
towards the edge; close together. The two smaller figures represent an unusually convex
specimen.
Fig. 20. Pecten compositus. Oblong; with about 20 smooth, sharp, radii, and two rows of
scales between each of them.
Fig. 21. Lima? subovalis. Rather quadrangular, elongated; radii very numerous, equal to
the furrows between them, and ornamented with one row of rather obtuse distant scales.
PLATE XVIII.
Fig. 1. Pecten Stutchburiensis. Suborbicular, compressed; radii more than 60, alternately
smaller, scaly ; those towards one side large and distant, with oblique striz between them.
+
App. A. ] Dr. Firron on the Strata below the Chalk. 343
Fig. 2. Terebratula dilatata. Wider than long, depressed, imperfectly three-lobed; plaited,
plaits about 50, sharp; central lobe elevated; beak of the larger valve short and large. This
resembles Terebratula Vespertilio of Brocchi, but is not so wide nor so distinctly three-lobed.
Fig. 3. T'erebratula megatrema?. Moderately convex, transversely obovate; with a few
distinct ribs. The beak is large and produced, with a very large perforation: whence the name.
Fig. 4. Dentaliwm medium. (An inferior figure is in Min. Conch. t. 79.) Subulate, very
slightly curved, striated ; stric sharp, elevated, alternately smaller, gradually disappearing towards
the aperture.
Fig. 5. Litorina pungens. Conical, acute, smooth; whorls five or six, the last inflated ;
aperture orbicular, with a projecting angle above; columella slightly compressed. This species,
probably, belongs to a group of shells which Lamarck has called Ampullaria; and which in the
Mineral Conchology is referred to Natica, but in the Index to that work is named Globulus.
The columella is, however, rather different.
Fig. 6. Natica canaliculata. Species the same as Pl. XI. fig. 12, but a much larger specimen.
Fig. 7. Natica granosa. Subglobose ; spire prominent, pointed, small; covered with spiral
ridges which are divided by the lines of growth into rounded granules; whorls very convex ;
aperture oblong, expanded ; umbilicus open.
Fig. 8. Natica? carinata. Oblong, with a small distinct spire ; surface marked with five pro-
minent rugged keels ; aperture large. This shell appears to be umbilicated, but is not perfect ;
hence the genus is doubtful.
Fig. 9. Tornatella affinis. Ovate, pointed; base truncated; surface grooved, grooves
crossed by lines; columella with one simple and one double fold. Very like Acteon ( Tornatella)
simulatus of the London clay, (Min. Conch. tab. 163. fig. 5. to 8.) but more elongated, more
acute, and smaller ; yet shorter than Tornatella elongata, (tab. 11. fig. 1.),
Fig. 10. Vermetus concavus. (Min. Conch. t. 57. fig. 1.to 5.) Tube rounded, curved into a
depressed spiral, which is concave beneath; the whorls united by an expansion of the shell from
the sides. These figures show the prolongation of the tube beyond the spiral part, which is not
shown in the Mineral Conchology.
Fig. 11. Scalaria pulchra. An acute shell, with blunt costz ; whorls ten, close: a band con-
necting the costz passes along the bases of the whorls.
Fig. 12. Littorina gracilis. A pretty, elongated, acute shell, with round whorls, bearing de-
cussated furrows on their upper parts; aperture round, with an angle at the base.
Fig. 13. Phasianella pusilla. Elliptical, elongated, pointed, perfectly smooth ; aperture ellip-
tical, more than half as long as the shell.
Fig. 14. Phasianella formosa. Elliptical, elongated, rather blunt; smooth, except a few striz
at the base; aperture more than half the length of the shell.
Fig.15. Phasianella striata. Elliptical, pointed, strongly striated ; aperture oval, above half
the length of the shell. This is like Phasianella princeps (Defrance), but more regularly oval.
Fig. 16. Fusus rigidus. Fusiform, costated, transversely striated ; costze rounded, roughened
by the lines of growth; transverse striae prominent, about 10 upon each whorl; whorls five or
six, swelled in the middle, compressed at the upper part; aperture more than half as long as
the shell, elliptical, pointed at both ends; beak variously elongated. The individuals of this
species differ much in length and asperity ; the edge of the aperture is frequently reflected.
Fig.17. Fusus quadratus. (Murex quadratus, Min. Conch. t. 410, young.) Fusiform, rhom-
boidal, with a short conical spire, transversely striated and obscurely bicarinated ; base produced,
conical ; whorls about five ; aperture sub-rhomboidal. The form of the shell is fully developed
in the specimen here represented.
VOL IV.—SECOND SERIES. 2Y
344 Dr. Firron on the Strata below the Chalk. [App. A.
Fig. 18. Fusus rusticus. A short, rugged, ovato-rhomboidal shell; with 10 or 12 ribs, each of
which is formed into two knobs, so arranged as to give a squareness to the whorls; transversely
striated ; aperture ovate.
Fig. 19. Fusus clathratus. Sub-pyriform, costated and transversely striated; four carine
crossing the costz divide the surface of each whorl into three rows of cells; spire very short.
The form is nearly that of a Pyrula.
Fig. 20. Pyrula depressa. Pyriform, with the spire sunk beneath the surface of the last whorl.
Ornamented with many transverse, thread-shaped ridges.
Fig. 21. Pyrula Brightu. Ovate, sub-rhomboidal, ventricose, transversely bicarinated, and
coarsely striated: aperture sub-rhomboidal; whorls four or five. Some specimens resemble Fusus
quadratus, (fig. 17.); but they are shorter, have fewer and more thread-like strize, and crenated
carine.—Named after Richard Bright, Esq. of Ham Green, near Bristol.
Fig. 22. Rostellaria retusa. A short, ovate, striated shell; whorls rounded, with one distinct
and one obscure carina on each. It has only one elongated, narrqw branch to the lip. The
surface between the strize is particularly smooth.
Fig.23. Rostellaria macrostoma. Turrited, with convex, carinated whorls; carine five, the
middle one most prominent ; aperture small, round, with a very much expanded and flattened lip,
furnished with at least two branches besides the curved beak.
Fig. 24. Rostellaria Parkinsoni. (Mantell; Geol. of Sussex, t. 18. figs. 1, 2,4, 5, 6, and 10.
Min. Con. t. 558, upper fig. 3.) Turrited, transversely striated, costated; costee numerous,
oblique, long; aperture narrow ; its broad lip furnished with one large subulate process directed
upwards, and a broad angular expansion below it; beak long and subulate. The specimen, of
which two views are here represented, is not perfect, but yet shows the form of the shell better
than any before published, and proves that Mr. Parkinson’s specimen from Faversham is a dif-
ferent species, although figured as the same in the Min. Conchology.
Fig. 25. Nassa lineata. Ovate, acute, wide at the base, transversely striated ; whorls flattish,
the upper edges sharp, distinct; aperture longer than the spire. Several species from the crag
of Suffolk somewhat resemble this; but in them the body whorl is much smaller.
Fig. 26. Nassa costellata. Subulate, costated, and transversely striated ; whorls about eight,
ventricose, each bearing one varix; aperture nearly orbicular ; lip thick.
Fig.27. Ammonites triserialis. Discoid, with a flat margin, umbilicate, radiated. Three
rows of protuberances, upon the marginal portions of the radii, and about ten tubercles around
the umbilicus, distinguish this species. The aperture is nearly square. All its parts are elegantly
rounded.
PLATE XXI.*
Fig. 1. Cypris Valdensis. (C. Faba?, Min. Conch. t. 485.—See the observations on the specific
names; supra, p.177.) Oblong-ovate, convex, punctated; front slightly concave; at one ex-
tremity of each valve is a small oval lobe; back hollow between the valves. It is very doubtful
whether this be the Cypris Faba of Desmarest+, which is the inhabitant of a much newer fresh-
water formation than the Wealden, and appears from the figure to be of a somewhat different form.
When the figure in the Min. Conch. above referred to, was published, the author was not aware
of there being more than one fossil species of Cypris, and supposed that the minute differences
* Plates XIX. and XX, containing representations of Endogenites erosa, are described above,
p. 172—176.: see also hereafter, p. 349.
+ Bull. de la Soc. Philom. 1818, p.259. P1.1V. No. 8.; Hist. Nat. des Crustacés Foss, p. 141.
Pl. XI. fig. 8.
App. A.] Dr. Fitton on the Strata below the Chalk. 345
which he himself had observed, might have escaped the notice of Desmarest’s draughtsman ; nor
has he yet seen specimens from either of the localities given by that author. Besides the fossil
species of Cypris engraved in this plate, we are now acquainted with five others; one in the
freshwater formation at Hordwell, (see Lyell in Geol. Trans. vol. iii. p. 288.); one in the coal of
Newcastle, (Cypris arcuata, Bean MSS.); and three found among tertiary marine shells of a
modern period, in the island of Java;—though the last possibly may belong to the Cytherina of
Miller, a genus so near to Cypris, that it may not be distinguishable in the fossil state, and
the living species of which inhabit the sea.
Fig. 2. Cypris tuberculata, Discovered by the Rev. G. E. Smith at Seabrook near Hythe.
Oblong-ovate, convex ; with a narrow border to the margin, and from three to twelve tubercles
upon the surface. The defined tubercles, and a distinct margin distinguish this species from
C. Faba; it is also rather broader and flatter; but the general form and the number of the tuber-
cles are variable, as well as the division across the middle of each valve, which in some speci-
mens, as at letter a., is so remarkable, as to indicate a distinct species, or even genus. More
perfect specimens, however, shown at 6. and c. are quite free from this division; and interme-
diate forms have been observed. The specimen represented in the upper figure at a.is from
Swanage Bay; all the others are from the vicinity of Hythe.
Fig. 3. Cypris spimigera. Discovered by Mr. Lonsdale in the Weald-clay of the Isle of
Wight. Oblong-ovate, broadest at one end, punctated ; furnished with a single, short, conical
spine on each valve; by which, and a shorter form, it is distinguished from the other species.
It has a narrow lobe at one end of each valve of the same kind asin C.Faba. The specimens
a, are from Sandown Bay; 0b. from Atherfield.
Fig. 4. Cypris granulosa. Oblong-ovate, punctated ; with prominent granules upon its sur-
face ; the lobe at one end observable in C. Faba is wanting in this species.
Fig. 5. Corbula alata. A rather gibbose, smooth shell, with the posterior side produced and
truncated.
Fig.6. Psammobia? Tellinoides. (Psammobia, Mantell, Geol. S.E. of England, 251.) Shell
’ transversely oblong-ovate ; nearly flat, with conspicuous lines of growth. There are a few longi-
tudinal furrows upon the posterior side.
Fig. 7. Cyclas parva. Rather thick, smooth, obovate, approaching lenticular ; longer than
Cyclas media. The larger figure, under letter a., is magnified. The shell is found in great pro-
fusion in the Vale of Wardour. In the specimen represented at b., from Dallard’s Farm, (supra,
p- 259, and also from pits at Dashlet,) the shells are filled with the crusts of a small smooth Cypris.
Fig. 8. Cyclas subquadrata. Transversely oblong, with straight sides; strongly marked with
lines of growth ; flat (perhaps from pressure). Found,at St. Leonard’s, Sussex.
Fig. 9. Cyclas elongata. Transversely elongated, convex, nearly smooth; posterior ex-
tremity more or less obliquely truncated : the casts of the outside show that the surface is finely
striated concentrically. There are two species of Cyclas in the specimen of slaty clay repre-
sented in the upper figure, a., which was found at Etchingham near Robertsbridge in Sussex. The
same forms occur also in the ferruginous sandstone of Langton Green, near Tunbridge Wells,
with Unio, (see below Pl. XXI. fig. 16.); and ina bed of clay at the top of the cliffs on the west
of St. Leonard’s. It is probable that the rounder species is Cyclas parva. Fig. 9. 6. is a variety
of C. elongata, from Hollington near Hastings.
Fig.10. Cyclas media. (Min. Conch. t. 527. fig. 2.) Alarge specimen; with another showing
the hinge and its single tooth under the beak. Transversely obovate, depressed, thick, smooth ;
anterior side small; posterior rather pointed.
2y 2
346 Dr. Fitton on the Strata below the Chalk. [ App. A.
Fig.11. Cyclas media: var. Gibbose; posterior side rather cuneiform and truncated. It
has the appearance of being a little distorted by age.
Fig.12. Cyclas angulata. 'Transversely ovate, convex ; posterior side truncated, and sepa-
rated by anangle and a point. A wider, thinner, more transverse, and larger shell than C. media.
Fig. 13. Cyclas major. (Cyrena, “larger species,” Ann. of Phil. N.S. vol. vili. p. 376, et passim.)
A convex, smooth shell :—the specimens are generally so imperfect, that their size is almost the
only character to be observed.
Fig. 14. Unio Mantellii. Dorsal and ventral margins nearly parallel, straight; valves flat-
tened, twice as wide as they are long; anterior side small, rounded.
Fig. 15. Unio subtruncatus. Ovate; valves flattish, thick, with obtuse edges: the posterior
extremity obliquely wedge-shaped.
Fig. 16. Unio Gualterii. Nearly square, with the anterior side rounded ; depressed; marked
with twice bent parallel rugz ; posterior side somewhat eared. The only fossil species known
that shows to any extent the waved ruge so frequent in the recent species of this genus. The
depression in the middle is not constant.
Fig. 17. Unio Martini. Ovate, rather convex, nearly smooth, posterior side pointed ; um-
bones not far from the middle, not prominent.
Fig. 18. Mytilus Lyellu. Oblong-ovate, somewhat flattened, especially towards the front;
convex towards the pointed beaks.
PLATE XXII.
Fig.1. Exogyra bulla. Oblong, convex, nearly smooth; beaks short, curved. The laterally
curved beak distinguishes this shell from the Ostreze of the same beds. Its shape, however, is _
very variable.
Fig. 2. Ostrea distorta. (‘‘Ostrea; an undescribed species”, Ann. of Phil. N.S. vol. viii. p. 376.)
Elongated, narrow towards the hinge; one valve flat, both nearly smooth. This and the Exogyra,
fig. 1. occur in masses, so closely grouped, that the form of the shells can seldom be traced.
Fig. 3. Bulla Mantelliana. (Bulla, Mantell, Geol. S.E. of England, 249.) A smooth cylin-
drical shell, nearly twice as long as wide, truncated at both ends: here accompanied by a small Pa-
ludina, supposed to be P. elongata, but which has a smaller spire than that shell generally has.
Fig. 4. Melanopsis? tricarinata. (Melania tricarinata, Amn. of Phil. N.S. vol. viii. p. 376.)
Subulate, conical; whorls seven, carinated. Three carinze occupy the exposed portions of the
whorls, and are crossed by distinct lines of growth; the central one is the most prominent. More
perfect specimens have induced me to remove this from the genus Melania to Melanopsis.
Fig. 5. Melanopsis? attenuata. Subulate, elongated ; whorls about nine; with several carine
crossed by undulations, strongest at the upper part of each whorl. The length is in proportion
greater, and the whorls more numerous than in the last species, fig. 4.
Fig.6. Paludina Sussexiensis. Spire an elongated cone, with nearly straight sides; whorls
five, smooth, more numerous than in either P. fluviorum, lenta, or carinifera of Min. Conch.
There are, probably, several other species of Paludina in the Wealden strata.
Fig.7. Neritina Fitton. (Mantell, Geol. S.E. of England, p. 248.) Convex ; tricarinated;
aperture large; spire very small. The specimens do not show the aperture, and are hardly suf-
ficient to prove this shell to be a Neritina rather than a Nerita. The lowest figure is magnified.
Fig. 8. Tornatella Popii. Elliptical, pointed, smooth; spire small, of about three whorls.
The cast shows two plaits upon the columella. Named from the Rev. W. L. Pope, of Tonbridge
Wells.
~-
App. A. | Dr. Frrron on the Strata below the Chalk. 347
Fig. 12. Lucina Portlandica. Orbicular, compressed ; surface finely striated concentrically.
Very like ZLucina concentrica, (Annales du Mus, tome vii. p. 238, and tome xii. Pl. XLII, fig. 4.
a. b.), but much more neatly striated ; as shown by the cast of the outer surface, represented in
the lower figure, which is from the Isle of Portland. The upper figure is from Swindon.
Fig. 13. Cytherea rugosa. Subtriangular; posterior extremity and beaks pointed ; valves very
convex near the beaks; outer surface concentrically furrowed, furrows most numerous on one side.
Fig. 14. T'rigonia incurva. (T. incurva, Benett, Wiltsh. Fossils, tab. xviii. fig. 2.) Convex, flat-
tened posteriorly, transversely much elongated; surface tuberculated ; width more than twice the
length. Since this Plate was finished, I have seen specimens from Brill, retaining the shell, which
is tuberculated, as in 7’. clavellata, but the tubercles are smaller.
PLATE XXIII.
Fig. 1. Ostrea falcata. Elongated, curved towards the posterior side; one valve flat, thick ;
the other unknown.
Fig. 2. Nerita angulata. (Nerita, 2nd species ; Benett’s Catalogue, p. 4.) Subglobose? ; with
a single carina; spire rather small, obtuse; aperture oblong. This cast shows the muscular im-
pression very distinctly.
Fig. 3. Natica elegans. Ovato-rhomboidal, smooth; spire small, pointed; whorls four or
five, rather angular, their uppermost edges rounded ; aperture more than two thirds of the length.
The shell in this specimen, whose form is well preserved in silex, is very thin and smooth.
Fig. 4. Buccinum naticoide. (Ampullaria elongata, Benett’s Catalogue, p. 2.) Ovate, smooth,
thick; spire produced ; whorls four or five, their upper edges rounded, the last whorl ventricose ;
aperture ovate, two thirds the length of the shell; spire longer than in the last species; shell very
thick.
Fig. 5. Buccinum? angulatum. Fusiform, short; sides of the spire straight; the last whorl
has one keel in the middle; aperture rhomboidal, with a short rounded beak. In the produced
beak, this specimen approaches to the genus Fusus, but the canal appears to be too broad. The
external form has not been seen. ;
Fig. 6. Terebra Portlandica. (Turritella, Smith, Strat. Ident. Portland-plate, fig. 2.) Tur-
rited, longitudinally striated ; whorls rather concave near the upper edge, where they have also
longitudinal furrows; aperture acutely elliptical; beak very short, curved. A very common
species in the Portland stone; where, however, the form of the aperture is rarely seen. Here, it
is preserved in chalcedony.
Fig. 7. Serpula variabilis. A cylindrical, rugose shell; with a considerable portion of the
tube unattached, and an irregular suture on one or more sides. When young, the attached por-
tion is triangular. .
‘Fig. 8. Serpula triserrata*. A thick, externally triangular, attached tube; with three thin,
serrated keels upon the upper angle. Attached to a portion of Ostrea deltoidea.
Fig. 9. Mya depressa, var. Oval, compressed, smooth, twice as wide as itis long. A much
wider specimen than that figured in Min. Conch. t.418. Intermediate forms are also met with.
Fig. 10. Exogyra Virgula; Goldfuss, tab. lxxxvi. fig. 3. (Gryphea Virgula, Defrance.) Much
elongated, arched; one valve convex, the other concave or flat; convex valve marked with ele-
vated lines; by which the species is well distinguished.
* This specific name is substituted for “ tricristata,” given to fig. 8, at p. 231; the latter
having been appropriated by Goldfuss to a different species, from the lias near Bantz.—(See
Goldfuss, p. 226. tab. Ixvii. fig. 6.)
348 Dr. Firron on the Strata below the Chalk. [App. A.
Fig. 11. Trigonellites latus Parkinson*. (—Ichthyosiagones problematicus, Dr. Riippell+;
A ptychus levis, Von Meyer}.) Oblong, triangular, compressed; one edge and one angle rounded ;
the longest edge flattened; one surface concave, striated; the other nearly flat, smooth, but
marked with numerous minute circular pits ; tissue cellular. I have just learnt from a specimen
lent by Mr. Bean, that fig. 18. in Pl. V. of Phillips’s Geology of Yorkshire, is a species like
this. It is referred by Mr. Phillips to the Oxford clay; but Mr. Bean observes that he has
had the same fossil from the Kimmeridge clay of Shotover Hill. A larger species is found at
Scarborough, perhaps the same as that before us. (supra, pp. 273, 292, and 316.)
Dr. Fitton, by whom the specimens here represented were found, in clay, near Whitchurch
in Buckinghamshire, and at Southrey between Cambridge and Ely, (supra, pp. 273, 292, and
316,) remarks: “ When I found this fossil in 1827, I was unacquainted with the publications then
“ relating to it, and those of Dr. Rippell and Mr. Von Meyer had not appeared ;—but so far as
“TI can recollect, there was nothing in the circumstances attending these remains that could illus-
“ trate their origin and connexions. Along with them I found in Buckinghamshire Gryphea Vir-
“* gula, but no Ammonites: in Cambridgeshire, Ammonites Lamberti is mentioned as occurring
“at the same place (p.316.). The valves of the fossil, like those of the Gryphza, at both places
“Jay in the clay which contained them, as detached shells might be expected to do, if they had
“ been lodged confusedly in soft mud. Smaller and thinner valves, perhaps of a different species,
“‘ accompanied the larger specimens at Whitchurch, Bucks.”
“Of the many names given to this fossil, I have, after some hesitation, retained that of T’ri-
“* gonellites, which indicates no more than form; the relations of these singular bodies being still
“obscure. As the valves are very often found detached, the term may be used provisionally, or
“‘ even ultimately remain, as a convenient denomination; in the same manner as Belemnites con-
** tinues to be employed, although the bodies to which that appellation is given, are no more than
‘* subordinate portions of some complex structure.”
“If the fossils represented in Plate XXIII. be truly of the same species with those of Solen-
‘‘hofen, their identity is deserving of notice, geologically.”
Fig. 12. Nerinea Goodhallu. Turrited, smooth; whorls numerous, half as long as they are
wide, concave. There are three plaits in the interior, one upon the columella, one opposite to it,
and one above it within the whorl; aperture rhomboidal. The section represented in the left
hand figure shows the generic character. The same species but much larger, is found in the Bou-
* “ Organic Remains &c.,” vol. iii. Plate XIII. fig. 9. and 12.
+ Abbildung und beschreibung einiger neuen oder menig gekannten Verstemnerung, aus den
Kalkschiefer Formation von Solenhofon: von Dr. Ed. Rippell,—4to, Frankfurt, 1829. Since this
sheet has been at the press, (July 1836,) a short paper by Dr. Riippell has appeared in the Lon-
don and Edinburgh Philosophical Magazine, (July 1836, vol. ix. p. 32, &c.), to which I wish to
refer the reader. Dr. Riippell regards the two species of Parkinson’s Trigonellites, as belonging
to distinct genera: in one of which (7. lamellosus, P.) he supposes the valves to have formed the
opercula of an animal somewhat resembling an Ammonite, but destitute of septa: this he proposes
to denominate Pseudammonites. For the second genus, (to which the specimens represented in
Plate XXIII. appear to belong,) Dr. Riippell retains the name of Jchthyosiagones, originally used
by Bourdet ; and in this case the valves appear to have been internal shells, in large elliptic mus-
cular masses, the structure of which has not yet been brought to light. Subsequently to the pub-
lication of Dr. Riippell’s first memoir, Mr. Von Meyer, in a paper referred to below', proposed a
different view of the relations of these bodies; and gave the name of Aptychus to a genus compre-
hending all the different forms.
' Acta Acad. Leop. Carol. Nat. Cur. vol. xv. Part Il. Read October, 1829; pp. 68—125.
tab. Iviii. fig. 1, 2, 4.
App. A*.] Dr. Firron on the Strata below the Chalk. 349
lonnois ; where also other smaller species of this genus occur. This species is named after the
late Mr. Goodhall, F.G.S., an indefatigable collector of fossils, and remarkably liberal in affording
the use of them to inquirers.
The Wood-cut at p. 129. represents a portion of Nautilus plicatus, one third of the original size.
The parallel linear furrows which pass over the whorls, are bent three times at acute angles, once
on each side and once in the middle, the central angle being directed backwards. There is often
some irregularity in the junction of the lines at the angles.
APP. A.
FIGURES OF VEGETABLE REMAINS.
Sphenopteris gracilis—The wood-cut at p.181 represents the impression of a species of fern,
discovered in the Hastings-sands, near Tonbridge Wells, by the Rev. W. L. Pope of that place.
It has been referred to the genus Sphenopteris of Adolphe Brongniart*, notwithstanding its acu-
minate pinnule, and a certain degree of resemblance to Odontopteris minor, (Brongn. Veg. Foss.
Pl. Ixxvii.), on the ground of its apparent affinity to Sphenopteris Mantelli (1bid., p. 170. Pl. xlv.
fig. 3—7); its pinnule having a midrib, but no lateral veins. This specimen was accompanied
by the impression of a species very nearly allied to, and perhaps no more than a variety of,
Sphenopteris Mantelli.
PLATES XIX. anp XX.
Endogenites erosa.—The description of the plates representing the external form and internal
structure of this singular fossil will be found above; (85.) to (89.), p- 172,176. After those
pages had been printed, two remarkable varieties of the form were discovered, in cutting down the
cliffs near the White Rock at Hastings; in which the stony nucleus was not only very irregular
in figure, but apparently divided into flat lobes, disjoined, or scarcely connected by very thin
flakes of stony matter; the whole being externally coated with lignite, which occupied the en-
tire thickness of the fossil in the intervals between the lobes. The form and mode of connexion,
or apposition, of these stony nuclei, when divested of their covering, were such as to suggest a com-
parison with some varieties of Cactus.
PLATE XXII.
All that is known of the Cones and cone-shaped body, Figures 9, 10, and 11, of this plate, is
mentioned in the list of fossils, at pages 181, 230, and 290. A section of that represented in
fig. 11. on its longer diameter, did not exhibit any indication of vegetable structure: but the ge-
neral resemblance in the outline and aspect of this specimen to part of the reduced figure of
Zamia horrida given in Dr. Buckland’s plate, (Geol. Trans. 2nd Series, vol. ii. Pl. xlviii. fig. 4.)
is, perhaps, deserving of notice.
A Cone has recently been found on the shore of the Isle of Portland, not improbably derived
from one of the beds of clay, or “ Dirt”, subordinate to the lower part of the Portland strata,
the structure of which, according to Mr. Brown, approaches in some respects to that of Arau-
caria. Iam indebted to the kindness of the Rey. David Williams, of Cross, near Bleadon in So-
mersetshire, to whom it belongs, for an opportunity of submitting this beautiful specimen to the
examination of Mr. Brown, who will, I hope, describe its structure in the Transactions of the
Linnzan Society.
* Prodrome, &c., p. 50.—Hist. des Vég. Fossiles, p. 169.
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VOL. IV.— SECOND SERIES.
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APPENDIX C.
LIST OF HEIGHTS.*
Tue following list may be useful to those who examine the country described in the preceding
paper, by furnishing some points of known elevation, from which it will be more easy to estimate
the surrounding altitudes, than if the entire heights above the sea were to be conjectured.
The height of the tides upon the English coast is influenced by so many variable circum-
stances, that in selecting a zero for a list of heights, some permanent natural or artificial mark,
of easy access, is very much to be preferred to the level of the sea, either at high or at low
water; the latter, especially, being objectionable, from the greater difficulty of ascertaining it,
and from its being frequently concealed. On this point, I am supported by the opinion of
Mr. Lubbock, whose publications on Tides give great weight to his authority. In the subjoined
lists, therefore, I should have adopted, as the common point of reference, one of the standard
marks hereafter mentioned, had not the heights obtained during the Ordnance Survey, and some
others mentioned below, been all referred to the level of the sea at low water; while, as the
mode in which that point was determined is unknown to me, I have thought it best not to make
any change in the original measures, by conjectural reduction.
The Tide-marks on the Thames, in London and its vicinity, which are referred to in legal pro-
ceedings, and which form the base line, or “ datum”, of many of the railroad sections, have been
derived from a long series of observations on the depth of water, first made, I believe, at the
East India Docks, by Capt. Huddart, and subsequently at the London Docks; from which
latter place, marks, corresponding to the average spring tide high-water mark, have been
transferred by levelling, to most of the bridges, and to the lock on the Thames, at Teddington
above Richmond, which is, at present, the farthest range of the tide. The time of high water
varies a little, at different points along this interval, but the ultimate heights are supposed to be
the same throughout.
In the year 1830, Mr. Lloyd having fixed a standard mark at the Sheerness dockyards, found
the mean rise and fall of the spring tides at that place to be 17°6150 feet; and of neap tides
* The exact determination of heights is, by geologists, regarded as of small importance ; but the
judgment upon this subject is, perhaps, unconsciously influenced by the difficulty which attends it;
since if we could measure heights as easily as horizontal distances, it cannot be doubted that the
former would be recorded and reasoned upon more frequently. As geology advances, it becomes
more and more necessary that none of the elements which enter into the physical history of the globe
should be neglected; and it is probable that many important inferences, not at present foreseen,
might result from a correct acquaintance with the levels throughout large portions of the earth’s
surface. Already it has been ascertained in Sweden, that the land has been gradually raised
within a few years, by a small but very perceptible quantity ; and in all countries, especially those
subject to earthquakes, it is a point of great interest to determine whether the relative levels
of the sea and land, are truly as permanent as they are supposed to be. In the Survey now in
progress in Ireland, and in the operations for a new map of France, the heights are carefully
ascertained and inserted on the maps: perhaps it may still be hoped, that some general system
will be adopted for connecting the measurement of heights in England with the Ordnance
Survey. In the mean time it is satisfactory to find that at the late meeting of the British
Association for the Advancement of Science, (August, 1836), a committee was appointed, and a
portion of the funds placed at their disposal, (small, it is true, with reference to the object), for
the purpose of devising and conducting observations on the relative level of the land and sea
upon our coasts»
3 Ba
370 Dr. Firron on the Strata below the Chalk. (App. C.
11:320 feet ; his mark (called the “ North Standard”), being 4°0661 feet above the mean level
of high water, and 21-6811 feet above that of low water at spring tides, He then ascertained
by very careful levelling, the heights above the standard, of several points in the vicinity of
the Thames, between Sheerness and London*: whence it appears that what is called the “ Trinity
TRINITY
H.W.
1800.
A
‘* high-water mark,” at the London Docks, ( answering to XXIII. of the indices
‘“‘ marked on the south-west side of the entrance”,) is 2°0112 feet below his “ North standard,”
and consequently 19°6699 feet above low-water mark at Sheerness. The last-mentioned quan-
tity, therefore, must be added to the height of any station above the Trinity mark, at the London
Docks, in order to obtain the height of the same station above the sea at low-water at Sheerness.
The places in the South-East of England mentioned in the subjoined lists, are grouped in the
order of the counties referred to in the preceding pages, beginning on the north. The names
are disposed alphabetically. The heights are expressed in feet and decimals of a foot. The au-
thorities and references to them are the following :
1. “ O.”—An alphabetical list of all the heights ascertained during the progress of the Ord-
nance Survey, given in the official account of that operation, published in 18111, calculated
from the level of the sea at low water. The places of the stations are mentioned in the Phil.
Trans. for 1800, pp. 576 to 583; and in the “ Account,” above mentioned, pp. 70 to 81.
2. “C.”—Bradshaw’s maps of the canals and navigable rivers in the midland counties of En-
gland, in three parts. The heights are taken from low water at Liverpool, (at a point 6 feet
10 inches below the sill of the Old Dock); which point is stated to be 21 feet below the Trinity
House high-water mark at the London Docks, and consequently 1°331 feet beneath low-water
mark, mean spring tides, at Sheerness, according to Mr. Lloyd.
8. “ M.”—A manuscript list of heights, principally in Cambridgeshire, ascertained by
Mr. M‘Lauchlan, of the Ordnance Survey, and Mr. Glaisher of Cambridge, and for which I am
indebted to the former gentleman. In this list (which is not an official document,) the heights
are counted from the level of the sea at low water, in Lynn Deeps.
4. “ B.”—A MS. list of heights above the sea at low water, ascertained by the late Mr. Bevan
of Leighton, for which I am indebted to his son, Mr. Bevan of Wellingborough, and to Mr. Mat-
thews of Leighton.
5. “ W.”—A short list of heights in the Isle of Wight, subjoined to Mr. Webster’s letter to Sir H.
Englefield. These are chiefly barometrical, and from their being connected with some of the mea-
surements of the Ordnance survey, it is probable that the zero was low-water mark.
* Phil. Trans. 1831; p. 167 et seg. Mr. Lloyd (p. 190,) “ concluded his levellings at a
“standard mark at the landing-place on the north-east side of the New London Bridge;”
which “ mark was 2°3967 feet below the North Standard mark at Sheerness;” and conse-
quently 0°3855 foot, (= 4°626 inches), below the Trinity mark at the London Docks. The
mark here referred to is a flat piece of brass, let into a cavity in one of the two large flags or
slabs of granite, which form the landing-place at the bottom of the second flight of steps, de-
scending from the footway on the north-east side of the bridge. The upper flight consists of 29
steps ; the second, at the foot of which is the mark, of 26 ; the lowest flight is commonly more or
less concealed by the water. The cavity in which the mark is lodged, is about 3 inches square,
with rounded angles; and is two feet from the eastern wall or side of the bridge, and 2 feet
8 inches from the southern edge of the stone. The surface of the brass is about half an inch
beneath that of the stone, which is itself a few inches below the level of the water at high spring
tides.
+ “An account of the Trigonometrical Survey, &c. 1800, to 1809; by Lieut.-Col. Mudge, and
‘Capt. (now Lieut.-Col.) Thomas Colby, R.E.”; 4to, 1811, vol. i. p. 299—311. This work refers
to the previous publications in the Phil. Trans. for 1795, 1797, 1800, and 1803, and carries on
the account of the operations to the end of 1811.
App. C. |
Dr. Firron on the Strata below the Chalk.
371
6. “ F,”—A small number of heights upon the coast of Kent and Sussex ascertained by myself,
from observations with excellent barometers and thermometers by the late Mr. Carey. The
lower station in these observations was‘either the shore itself, (the height of the barometer, below
or above the spring-tide high or low water marks, being estimated),—or the drawing-room floors
of the houses at Sandgate and Hastings, in which I resided, the height of which above the sea
was ascertained by a mean of several observations, sometimes checked by comparison with more
elevated stations measured directly from the shore, and again from the houses. The variation of
the tides at Sandgate was assumed to be the same as at Dover, = 18°30 feet, and at Hastings,
= 21°50 feet; which Capt. Beaufort, by whom I have been favoured with these numbers, states to
be respectively the mean derived from a series of observations at those places, in 1834 and
1835.
Above
the sea
Stations. at Low
Water.
Norrouk. Yee
Denver Sluice, near Downham Market,
above the Deeps at Lymn ,...scssseceeseee
CAMBRIDGESHIRE.
Aldreth station, between Haddenham Mills
and Aldreth..........0000. Revccscesccarssers O.| 122
Ps GIShAMOVA.| StAUOM <cscsensccocseneayareces O.| 380
—ISCEEPLEs (COP) sesisacecesascesceeces M.| 410
Barton Hill, between Madingley and Bar-
(AYO. eerocone panies seenanecaas SpROneReD Coo. M.| 175
Brandon Station (Suffolk) .............0.00- M.} 190
Burwell Steeple, bottom ..........ssessesseee M.| 96
CamsripcgE, level of the Cam...... eeaeemeiss M.| 24:50
South Chimney of S¢. John’s
College ......+++ Sonpenonasoreccacece Sonaenncee M.| 71-25
- Observatory, top of the Dome. M.} 123°50
Chapel Bush, Hazlingfield ...............0++ M.} 220
Cherry Hinton, Chalk-pits ...........020000+ M.| 150
Cottenham Steeple, top ......... eegaseeaay M.| 116
Duxford-Pen, Duxford :—(Duxworth,Ord.
BEBILAD) caectaptiensanoscecaccscesco=teasecseneteas M.} 372
Ely, Water at the Bridge ..............260+ M| 14
——,, ground at Cathedral........... seccbee M.| 75
peloplof the! VOWercccsscsesscesceateres M.| 290
Fulbourn Windmill ..........s.eceescssesseeee M.| 140
Gog Magog clump ......+++.+000 eeaesoriae M.} 250
, Telegraph Station ............ O.| 260
Haddenham Steeple, (bottom) ............ M.} 133
Hardwick Spire (bottom) ..............000 M.| 225
King’s Hedges, cross roads in the Roman
Way pecnenccscieee se eciarcases sav aleeseseiesscpe M.| 55
Linton, Rivey Wood, (top) .......seeseeeeeee O.| 387
Madingley Station ......sccecscscssssseaee -..O.| 188
Maggots Mount, obelisk ..........sseeceseees M.| 152
Newmarket, Four-mile Stable ............ M.| 180
——_—_——-, Ordnance Station............ es)| 267
Orwell Station <...<0...cecersscsessserassere ...O.| 255
Stations.
Quy-cum-Stow Steeple, (bottom) ......... M.
Swaffham Bulbeck, Mills .......s0eeee00ee M.
Prion Wills cocovewesttcceeesnsc M.
Soham Steeple, (bottom)..........cseeceeeees M.
SCUNi ney MEANPUILY Uasadcscersceccceseameneeee M.
Sutton Steeple (top). The tower is said to
belOSteethighccncsssserencersccsess epapdlil ls
Thorney Hall, near Ely ......0.+00seec-cess M.
Wicken Steeple, (bottom) ..........0.se008 M.
Wilburton Steeple, (bottom) .........0.600. M.
Witcham Steeple, (bottom).........sseeeeees M.
BEDFORDSHIRE.
Brogborough House (chimney), near Led-
IWS. Gaghooadossoseeca0o0d pecoedacococadcacc B.
Dunstable; hill above Zouche’s farm,
east of the town.......... PRECOLEOoCOIOICAC O.
Grange Mill, Leighton Heath ...... opcon! ot
Hockliffe Church, battlements............+0.B.
Tvinghoe Church, top of spire .........++ coal h
Leighton Buzzard churchyard ............ B.
, Grand Junction Canal +
mile south of the towM.......ssceccscsseees B.
- , Turnpike between the
town andwWVangieaccattarsseccreneseeserene se B.
— ~ Mile Bush, betweer.
Leighton and Soulbury ...cccocsesseseeee B.
——— , Canal level from Stoke-
Hammond Lock, to the three Locks at
IS OULU UNI eNTeiereaeh ea eisiecieiees ancleabiotetesrt serects C.
Lidlington Mill Hill...........seesssecosees +B.
Mentmore, ground near the church......... B.
Overend Green, east of Reach............ «. B.
Ridgmont Castle; hill) ..2-..s..cevsese--sso00s B;
Shire Ash, on the road between Hockliffe
and Woburn ......c00eee Sod coogNODNaTIOOUON B.
Toddington, ground near the Church...... B.
Totternhoe=Castlemnilly.....vssscseseas<esseers B.
Woburn Church, (battlements) ............ B.
Above
the sea
* It will be found that some of the heights mentioned in the text of the preceding paper, differ from those
of the lists here subjoined, having been-calculated froman estimated mean level of the sea, instead of the level
at low water, The difference is one half the mean variation of the spring-tides at the respective places men-
tioned.
3712 Dr. Firron on the Strata below the Chalk. [ App. C.
Above Above
the sea the sea
Stations. at Low Stations. at Low
Water. Water.
Feet. Feet.
Clifton Hampden, Canal, W. of Oxford ...C.| 159-08
NOR THARE TONS Hine Culham, canal south of .......sseeseeseeeee C.| 161:25
2 Junction of the Thame and Isis, below
Arbury Hill, near Daventry «..++++++..s+6 O.| 804 Wittenham Wood ........000. eke silciss am C.| 154°25
| River at Bensington Ferry ....+.0.seeseee0 . 158-25
River Jsts, south-west of Ensham ‘village... 205°25
Henrtrorpsuire. Evenlode river, west of Oxford .......... ea 19483
Barkway Windmill: top..............seseee O.| 513 Heyford, upper, canal north of the village..C.| 254-83
Berkhampstead, general level of the Vale...B.| 350 —-— south of the village. .C.) 250
aa , adjacent hills, general Iffiey, canal below the village .........2..++ CJ 185-69
lev.c eee et a Mac a eee B.| 600 Lechlade, (Gloucestershire?) .......+eseee0+ C.| 243-08
Bridgewater Monument, (gallery) ibaa B.} 811 Nettlebed, \ivaintravill Gaoscsoonsoccodocuon0000 O.| 820
Burley Hill, neav Royston ....++s.seeeceeees O.| 342 Old Nan’s Wear, on the Isis, south of
Great Chishall, (steeple) ....s+seesesereers M.| 470? BaMpton .....ccccccscosssoocscoecasaseeseess C.| 224°34
Heydon Hill, Chishall ID Yo EE aotannoonanaane M.| 480? Oxrorp, Canal Lock on the south-west of
Kensworth, hill near Dunstable ............ O.) 904 the city nie cleveis(ajx\sislale oleveiele’a's\ele/eluiefeluiajeluipielsiateiele’einys C.| 190
Lilley hoe, Ord. Station ......++ idekcnaseoee O.| 664 | Purley, on the Thames, below Maple Dur-
Rickmansworth, CULVent ..scscsssceseseeeeees B.| 159°75 ham Lock ....0.....0secersssereesssves Secosess| 20-34
Royston, Ord. Station ......-.+scseseeeecrenes O.| 481 Sandford, by Nuneham .......sseeseeeeeeeee C.) 177-59
Tharfield Windmill, (Downs).........+0++4 O.| 570 Shotover. ELA, tOPesecececeeee soca s=eeeecens O.| 599
Two-waters, Grand Junction Canal...... ...B.| 275:08 || River Isis, east of Stanton-Harcourt ...... C.| 206°25
Streatley, (within the course of the
Thames across the Chalk), at the Ferry...C.) 138-50
BucKINGHAMSHIRE | Wallingford, canal level, by North Stoke,
LOM MGS ONO sansteseedersrcsescsissietses +020.) 149°34
Aylesbury, Grand Junction Canal ...... ..C.| 359°17 Wantage, Canalvateneosesenece pdadosnoonooasend C.| 288°75
, church, top of spire ........0..- B.| 425
Great Billington, hill near church ......... B.| 428
Bow Brickhill, Ordnance Station ......... O.) 683
, Church battlements ...... B.| 600 Mipp.LeEsex. |
Brill; Redshill, north-east of the town, |
(lower than the church) ............+.000 O.| 555 Cranford, junction of the Paddington and |
Buckingham; level of Canal ........00.00+- C.| 265 Grand Junction Canals ........ssssse00e. C.) 251 |
Cheddington, church, top of tower ......... B.| 429 Hanger Hill.......cccocerecssecssssovesesersces O.| 251 |
Crawley, North, church battlements...... B.| 437 KANg’s Gr DOUr ..ccocrcrecersosssoscscscscersens O.| 182
Fenny Stratford, level of canal ............ B.| 240 Thames river, north of Wargrave ......... C.) 108-75 © |
, (to Stoke Hammond lock).C.| 249-25 —, above Great Marlow ..........0.... C| 94:17
Muswell Hill, Ordnance Station............ O.| 744 ———, near Maidenhead ............0.000+ C.| 79:08
Newport Pagnell, (canal) .......00..006008. C.| 196-25 4» AL ELON ..cecacscecsccececerserererers C.| 65:59
, canal near, from Wol- » MEAL HGhaM ....0.ecevcersenone see! 52:08
verton to Woolston, by Great Linford...C.| 247-75 AULA CLEN Ch sa sertsietiastctestereistar pooond Gi) aisieilizy |
Quainton, Ordnance Station ,...,.......06 O.| 754 ———,, at Shepperton......ercccsesescraneeee C.| 40°59 |
Stewkley, ground near the church ......... B.| 508 , at Teddington, above the Lock .. .C.| 28°75 |
Stony Stratford, canal level, from Thorn- _ , at Limehouse entrance of Re- |
KOLO ETA = 51105906612000005000000 10035 DORR LOSE C.) 252-25 gent’ 's Canal (high-water) .........s00+0 Ca 2 |
Tring, (canal to Wendover, summit level) . C.| 404:50 || Hunton Bridge ..cssccscaresseeveneseeercrees C.| 225:59 |
Vendover Hill, Ordnance Station ....,.... O.| 905 Lonpon; reservoir of the Royal Society’s
Wingrave, Church, top of tower .......... .B.| 530 Standard Barometer at Somerset House,
| above “a fixed mark” on Waterloo
Bridge*.....secscscocscevsccssreseccsesececers 83:21
OxrorRDSHIRE. Rickmansworth, canal near to mill...... Roa Gal) Ui7AORiley
j F F eer River, 0 posite Hampton Court...... C.) 28°25
ington ena sore the ek at Hore] 55 | Weairdye, Basngsake Canal vecesC] 5
Banbury, Canal, North of the town ...... C.) 312°17 BE, Paner as, Regent's Canal a saseeee aaa 79°59
S: (Southiof ae town mine tO)NS05-50 peice Grand Junction Canal, south o F ,
Barnwell, canal to East Chatton Cae re Qh 288-75 TIS EOWAIG creicic’esicicteielesie/sieinie.eie\eloleia’a(alelalbis eccceee -| 113:08
—, at Uffington Wharf ...... C.| 283°75
Caversham Mill, canal .......ssccccssccesseses C,| 12525
* Itisvery desirable that the “ mark” here referred to eon the Register of the Barometer, &c. published
periodically in the Phil. Trans.), should be connected with the standard marks on the Thames: its height
above the mean level of the sea, is “presumed about 95 feet.” Observations of the barometer and ther-
mometer, are taken by one of the officers of the Royal Society twice every day; at 9 a.m. and 3 p.m.
App. C.]
Above
the sea
Stations. at Low
Water.
Feet.
BERKSHIRE.
Kennet and Avon canal, above ae
Or darn caeedncasatecedateescetes aeeasadesicees 326.50
—— at Kintbury .. el 300-17
—_— west of New-
DUT ceo se eodteiaint cated lalate evade bones enenesey C.| 257°58
SSSR south of Read-
WO eomccacecewdseuesewor cress. atu cessnaeercrecet Ot muece(o
Netilebed Windmill.........s.s0+- pogasogeci20c ":0 | 820
Nuffield Common ...scossccssccasscevecees sees.) 75%
Scutchhamfly Beacon (chalk) .........++. +0.) 850
The River Thames, at Sonning, north-west
Of the village. .ticcsecssaceestees'sccotteovees cs C.} 115-75
Wytham Hill (north-west of Oxford)...... O.| 576
Whitehorse Hill ......... deseeascssessecessees Ont Cow
WILTSHIRE.
IS GACOMVIE Mcendudcaccnonsecctenetecte ean terens: O.| 690
Great Bedwin, canal below the village .C.| 385°69
Calne, level, of canall.....c.0c..cecscesscsoseces C.| 227-92
ChiPenhatNascsadseceersedetecessnevedccceddss: C.| 190-08
Clack, canal west of the village mete sale voeeC,| 233°08
River Zsis, north of Cricklade ....0ccceeseess C.| 276°58
—-, canal near, at Kempsford...... C.} 261-25
—_—-- , hear Inglesham above Lechlade C.| 245°42
, near Buscot, below Lechlade...C.| 233°34
Melksham, junction of the Wilts and Berks
with the Kennet and Avon canal.........C.] 185°42
Vale of Pewsey, canal from Devizes
to Wooton Rivers...... Masleas eae dacscaciian aC 429°5
(The canal falls tena Melksham
from this level, by 29 locks, 239 feet.)
- canal level at Burbage
WHOIS Nacecsovanweoseeeescss cst seasancesataes 462°5
Seend, canal north of, (Kimmeridge clay).. C.| 190-50
206°25
Stanley Abbey, levels of canal............ C.+ | 191-08
Thames and Severn Canal, north-east of
CrICllaG er adaadexsessdeseas-vaecencenseeteees C.| 268°5
Wilts and Berks Canal, at Swindon Wharf,
SuUMIMIUt levelssc..ssescesnececancecsaceeanees C.| 333°75
ee , level near Shriven-
NGM wecsoccdescecstsecsseteacacrersasessccstes 302°34
Westbury Down, Ord. Station, (chalk) Os eiine
Wootton Basset, canal, south of ...... qon008 C. 301°5
HampsuHire.
Butser Hill, near Petersfield ............+-: O.| 917
DeGnETHAl, | snccesewcwo sions ss oonctagssc6sedon05 O.| 539
Eighelere BeEgeon, <niescsucsesnssoueescees ses O.| 900
Tnkepen Began, w.deuvescvecsseeseoe toon oe O.)1011
Portsdown Hill (top of Nelson’s Monu-
MENG), senses adcaedencasseweconsceneieectees O.| 447
Itching Navigation, at S. Stoneham ........+ C.} 16°17
at Bishopstoke .......+. C.) 56:42
———— west of Twyford ...... C.| 101:50
Dr. Firron on the Strata below the Chalk.
Stations,
Itching Navigation, south-west of Win-
GLUGUGR CecceececelecCone POMCEEReCCLECPE CCH Ee Cc.
‘Stockbridge Hill ...... Masisvececeres nese strats O.
Andover canal, at Red-Bridge.........0..04 C.
—— at Romsey ..ccccsceves veeeee.
— at SLockbridge...ercveverreveess
—— At ANAOVEN ..cocesoacascesssnees
SuRREY.
St.) A 00078) FLOLL eaenseciae CeOcroeBOLCIECOICAOTC 0,
Bagshot heatic secccecscrceee conver castoceoscon O.
Banstead Down, near Banstead . Sere cneces Aa
- , hundred acres (chalk) .. O.
Botley HI osavactaunnscmadensetecc eter oataes ‘0.
Croydon Canal, et SYMenham .e.eseserereees C.
——- , junction with Surrey
Canal, Deptford! c.sccccceccrcnedcaceseceres C.
Hiidiiondl MiG cnn a Ln sooncorot Oh
Leith Hill, Tower, (base 2) ee coc en.
INOPUOOD Tenant euavadesarersedcee ses wesaceseae i
Surrey and Sussex Canal passing Wonersh C.
summit level,from
Rushwood to Sidney Wood ......00.0+0+0 C.
River Wey, at Godalming ....ss.ssereees se Ge
_—————- below Catherine Lock .........C.
Kent.
St. Alban’s Court, near Wingham ......... F.
Allington Knoll... “coongepoodoEcos7esague05 O.
Copt Point, Gault Cliff ........ socccouobente F.
Dover, Castle wevensldecdetecceteocescetitectens O.
mean range of spring tides 1834. secsne
—_—— & aponod “|
——-- by report
of Harbour-Master 1828........0000s..008 F.
mean of neap tides do. .......0.... F.
, extreme variation of spring tides...F.
Folkstone, hill, Ordnance Station ...... oo"
» Turnpike - ......000 Seiesses Oi
Folkstone, mean difference of spring tides
by report of experienced boatmen ...... Ee
eee of neap tides...F
, top of the Chalk elift, nearest
to the town mo qogoconossncoteobougocoLcabepar |i
» Martello T en, No. 1. Base...F.
Ears Ditto No. 2. Base...F.
a Ditto No. 3. Base...F.
— , cliff near the town, on the east F.
—— , cliff at the Church................ F.
Goudhurst, Kent .......+. aedaesaaeeass easeceen 0.
Greenwich, Observatory .....0scseeeerseeeens O.
High nook, near Dymchurch .........+.048. QO.
Hollindburn RAW , veces me seisteseatelse sie an sont
Nail Down, west of Sandgate ......e.sscee0 F.
Paddlesworth, Bill .+.5.0..ccccesereseoeereees O.
Ramsgate, mean range of spring tides; tape .
— 5*
373
Above
the sea
at Low
Water.
Feet.
129°58
620
5°83
61:42
120
184:83
* Capt. Beaufort, R.N. MSS. from the Reports of the Coast Guard Preventive Service Officers.
314
Stations.
Kent, (continued.)
River Medway, at Tunbridge. ....++++. Brann
at Brand Bridge......++. Aad Ge
west of Yalding
south of Teston, above the
weecesescceeeeerssaes
- south of M aidstone, ( Low-
CY QTEEN-SANA) ....ceeceersceseerecsereceeees C.
north-west of Allington
Castle ..cc.ccsececscscscscecscccccece coecress
Ruckinge church, west of Aldington
Saltwood Castle, near Hythe, in the court...F.
Sandgate, drawing-room floor of a house
in Prospect Place .....-+scesseeeseseeeeeeees F.
-, hill top over Prospect Place, ... F.
Shakspeare’ S Cliff, top...ccccecocerecreeensacs F.
Shooter’s Hill .reccocreocsssesnccveves Sgasooan O.
South Foreland, Upper Light-House, base..F.
———, Lower Light-House, base..F.
Swingfield, steeple- (1) Daqouoo0ce Socospccacne nd)
Tenterden, (steeple)......+++ bopoostdcaos arene O}:
Tolsford Hill...
Sussex.
Arun river, at Thorndell, before it enters
the Chalk range .......sssssseeseeee AGOOCOD C.
Bec Head, highest i IE F.
OldUsioNallesccwwereseeceoncnss O.
, base of the house. F.
, Holywell chalk pit, cliff top. a
—
Bell-Tout ; cliff CU PO Mepacrecantceteanscesstoes ;
or ‘First of ioe
, First Sister,
Sevens,”
Brig ightling-Down near Battle
Brighton, site of a former signal-house ¢ on
the! TACECOULSC-.essssc50ce¥asseserecwescsces F.
Lanal, west of Loxwood, 11 Locks below
thie ‘summit, Leviellcppcwsecesictetemeiemeencrbecte Cc:
near Spurland farm, below Mallam
Wi OCkiss cecsancssacesaseelscenewees Seanwter eos:
sscewaesesincctees one
— near Rowner, farm
——- near Snape, below Middle eck saCe
- near Neville Wood, and thence 5
J AOUOTRORTHIO: . coca nop000x.d—ds50000003d0000 4000 C.
Chanctonbury ring, South Downs, (Chalk),
OrdnancelStatlon=-cs-sewec severe snspeceeess O
Clayton, range of the chalk on the south,
about 200 feet lower than the general
height of the ridge ...........006 spdeG5000 O.
Crowd oro1gn-Beacon) jessccsdeceretsiacuieuiscaele O.
Ditchling-Beacon ..........0.ese+0«se cevoeeesO:
Fairlight Down, top, Ordnance Station ...O.
a » SAME PlaCOsvecscvecewecovsee F.
—-, floor of the octagon room
in Dr. Batty’s house.........+-.s0e--ee Godo0! 6
espocoaosdticonn O.
Firle Beacon, South Downs
ecceeercenee .
poonosdaosocaonoacHoonOc +0,
(Cliffstop) Wetwewemescccnemernmcene F.
Dr. Fitton on the Strata below the Chalk.
Above
the sea
at Low
Water.
Feet.
79:69
47:08
41.69
33°69
[App. C,
Above
the sea
at Low
Water.
Stations.
Frant, near Tunbridge Wells, (top or
steeple)
Hastings; Castle hill, highest point ...... r
, East cliff, average level...... Saalde
—_—., * the Lovers’ Sedte..sso-ss+es ccoveel’.
, average range of | pene nso)
SRY sgnod0snqn0da000009 AOA SOIO HO IOGNTII00
» Ditto.........--.at a point at
3 miles west of the town; 1835.......... *
————— mean nf
TWO YEAS. oecccccccsceccccvcsarerecersecesees
Newhaven, highest point of the Castle hill. r
Ouse River, at Ryeland Bridge ......+++06 C.
, north-west of Lindfield ...... C.
, west of Sheffield Park ......... C.
——-——,, north of Goldbridge Lock......C.
, Sharp’s lock, 2 miles west of
Wick Aeldi.c. sd. ssn cen eee C.
,"Barcombe Mill, above the locks.C.
- ; Hamsey Place, north of Lewes C,
Portobello, top of cliff; about the average ay
level of the cliff from Rottingdean to
WNCwWh AVE Krcticccbacsecicceocseaceniececsssste
Rooks Hill Beech, near Gesdwnode Ord-
NANCE Station ....e.eeeeeee Soocncncde enen ;
Rother River, west of Midhurst . eee ce
- , near Pulborough ......000+. C.
Rottingdean, cliff top beneath the Wind-
TI tere eetleltelle se see cetlcieetleeaie= seaceenscne sel
Seaford Cliff, top, N.E. of the Signal .
Isye or Wicut.
Bembridge WOW maaeloeicsceseviesestscesisscinen W.
Black-gang Chine, guardhouse on the
Iheadland)ecccocveccccsesceseseavencuasseneaae W.| 400
St. Boniface Down veeccseveee seesveceneconees Wiel “O00
St. Catherine’s Lighthouse .........++.ese0es 0.) 830
— Down, cliff top under the
hill fenteeseececscmescewsronceeene SPE OUDCI00S0 W.| 591 |
Culver-cliff top reer iacseecteaneesnenececeene «W.| 259 |
Mottestone Downecaees BOKER OIOIRSORONOS 190006 O.| 698 |
Shanklin Down, (Dunnose of the Ord-
Nance SUrVeY) ...ecscceceseee Sone A0nedaG0000 O.| 792 |
DorseETsuire. |
Blackdown hill,(north-east of Abbotsbury). O.| 817
Bull-barrow (south of Sturminster) ...... O-| 927
Charlton, Common (north of Wincanton).O.| 582
ConferCastleyhill mracsdeesecescesereeeter sees 20K
Downs over Handfast Cliff ....scecsceeees O.| 584
Heightiof the Clif itself .s---:essseeesescenee O52
Nine Barrow Down (Isle of Purbeck) ...0.| 642
Pillesdon hill (west of Beaminster)......... +) 934
Wingreen hill (south-west of Berwick St.
VOM) “podooa0s son00a0 qupdcoddosadodoucso0 --O.| 941
* Capt. Beaufort, R.N.; MSS. from the Reports of the Coast-Guard Preventive Officers.
App. C. | Dr. Firron on the Strata below the Chalk.
375
7. Railroad Sections.—From the uncertainty of the tide levels, and the inherent defects of the
methods, both trigonometric and barometrical, by which most of the heights above mentioned
were obtained, they cannot be absolutely depended on within a few feet. Those given in the
sections of the numerous railroads through England, having been ascertained by levelling, are
much more to be relied upon: they are, probably, as accurate as any that ever have been
obtained in undertakings not expressly directed to scientific purposes ; and are the more valuable,
as the two other modes of measurement are most erroneous when the elevations are small.
In the course of a few years the entire surface of this country, wherever the introduction of
railroads is practicable, will thus be covered with a network of intersecting lines, along every
A
well-arranged collection of the levels will then form a very useful compilation to inquirers in
one of which the heights will have been determined to within a few inches of the truth.
various departments of physical science; and it is to be hoped that some person properly quali-
fied, who has leisure for such a purpose, may be induced to enter upon the undertaking *.
The following Lists contain only the approximate height of a small number of points, along
the principal lines of railroad in that part of the South-East of England which is represented in
the map, P].IX. The first two cut through the chalk range of the midland counties, in passing
from London ;—1. North-westward, as far as Stony Stratford;—2. By Reading, through the de-
file of the Thames, towards Abington; and thence, westward, to the vicinity of Chippenham.
3. The South-eastern line, after passing the chalk near Godstone, descends the Valley of Kent,
by Tonbridge and Ashford, to Folkstone and Dover. 4. and 5. The Brighton lines traverse the
chalk downs and the Wealden denudation, southwards, between London and the Sussex coast.
6. The Southampton railroad crosses the continuation of the anticlinal line of the Wealden to-
wards the Vale of Wardour, and connects the basins of London and the Isle of Wight.
I.—HEIGHTS ON PART OF THE LONDON AND BIRMINGHAM RAILWAY}.
oe Height
: above the : above the
Stations. Tate Stations. ie
Feet. Feet.
The Datum in the Section of this Railroad, Highest point of the ground over the Tunnel
is the same with that of Bradshaw’s map near Primrose Hill, about 0:1 mile north-
of canals; viz. Low-water mark at the Old west oflettermPl§ socsctt.Neccccsteua ates cotaees 189-50
Docks, Liverpool, (6 Ft. 10 In. under the Road from London to Edgware, at Kilburn .| 130
Dock sill.) South-east bank of the Brent, about a mile
Datum below the Trinity high water mark, at CASE OL APPCHLOM vosesceccioes saeeaineneee veoee.| 87°6
the London Docks: (Bradshaw)...21 feet. Road from Harrow to Harrow Weald, about
[The datum at Liverpool, therefore, is be- 3 mile beyond Greemhill....scccseceeeceeeees 190
neath low-water mark at Sheerness, Stanmore to Pinner, near Dove-
(21 — 166699 =) 1:330 feet. ] MOUSE MAUI Wewacshe seaseeedsects sasiencenmeteascss 218°08
Height of railway above the datum at the Highest point of ground over the Tunnel at
Regent's Canal near Camden Town ...... 118°75 Oxhey-lane: north of the e in lane......... 287
* In the present unfinished state of the works, the attempt would be premature; but when the railroads
have been completed, the several lines will furnish admirable facilities for accurate levelling along them, and for
connecting the heights in the interior of England, with fixed and durable standards at well-chosen places on
the coast, the height of which above the sea, may be afterwards ascertained by long-continued observation.
From the first of these operations, we should obtain the relative height of a number of points, any one of which
might be taken as a standard, and all of which are, probably, themselves in motion, and may be expected to
differ in elevation after the lapse of years. On this account, the multiplication of standard marks, both inland
and on the shore, is very desirable; while the latter should be compared, from time to time, with the supposed
invariable mean level of the sea. The height of the tides themselves, however, is in some degree affected by the
features of the coast, which it is well known to geologists, are in a state of constant and even rapid alteration.
+ Where roads, canals, and streams are mentioned in these lists, the points referred to are those of their
intersection by the railway. The names of the places are in the Ordnance Maps ; and the precise points are
indicated by reference to adjacent words, letters, or objects on the map.
VOL IV.—SECOND SERIES. 3¢
376 Dr. Firron on the Strata below the Chalk.
Height
; above the
Stations. Datum.
. Feet.
Bremincuam Raitroap (continued).
Railroad at south-east end of Tunnel ......| 236
Bend of the Brook, east of Oxhey-lodge......| 214°83
Turnpike road from London, near the en-
ELAM COOL MAU OLM merntesevedeiieaicosies seas eels 200°50
Valley, or flat, of the Gane north-east of
Wai for deeduasenenterseasasccesecesscecceesn sa 189-25
Road from Watford to St. Alban’s, midway
between Callow-land and Nascot-farms...| 251:83
Highest point over the Tunnel at Russel-
jarm, near the top of R in Russel ......04- 342
Railroad at entrance of the Tunnel ...... cog) ZO)
Grand Junction Canal, about 4 mile south-
CAStIONON GS il Vallcsenacence ss cise cemasan slays 249
Canal, about 3 miles from the Jast place, be-
tween Boxmoor and Bourn-end .....ceeeeee 297°83
Road to Berkhampstead Place, between the
Canalland'the Castleicascccccsccssene daseeisen| MOU L
Highest point over the Tunnel, near the road
from NV. Church to Ashridge; bottom of
letter NV in Northchurch .......cscceceecsees 442°42
Highest ground over the railway at Three-
score-acres lane; east of ain Grand......| 461:83
Road from Tring to Dunstable (boundary
between Herts and Bucks); about midway
between Polly and Bulborne .....0006 sse0e 446:17
Grand Junction Canal, south-east of Sea-
brook....- sieeesea Kewawsaes sevele serchisbs sacieaeeeesss 847-75
Stations.
Road from Jvinghoe to Leighton-Buzzard ;
on the south-west of Horton; (a continua-
tion of the Vale of Aylesbury) ............
Road from Leighton to Wing, at an elbow
Gast) OfpS OUCH COL Mesdesecmmaresitactecciee steric
Railroad at entrance of the Tunnel Lins-
lade Wood, north-west of Leighton.........
Highest point of ground over the Tunnel,
about letter 7 in Linslade...........0+.+ss0a0.
Road from Great Brickhill to Soulbury, near
Rislip farm; north of # in Rislip... .....
—_——_—_—_—__-—— to Newton Long-
GOUT. pocochoodaqabogonsasconsnubosqobadsoobegeNces
Stream under the railroad between Water
Eaton and Bletchley, about 4+ mile west of|
the word Water, and south-west of Stony
ISTE CUOT. Duvelateaelsele'selontece deieeeiieteeeceeeccecndes
Brook under the main road to Stony Strat-
ford, near Denbigh Hall; about 464 miles
HOW PZONE ONY deer eteiseeeicnassttascnictes eens
Average height of railroad, from the Tunnel
at Linslade Wood, to the road last men-
IONE Cpe iinte'sons csis'scieices scicldeessialeasescens about
Grand Junction Canal, about 4 mile east of
Wolverton, north of letter Jin Canal......
Bottom of the Va alley of the Ouse and Tove
Rivers ; about 24 miles north-east of Stony
Stratford; near rin the words River Ouse
[App. C.
Height
above the
Datum.
Feet.
332°58
318
306
302°75
317-69
247
264'42
300
247°75
213
IIl—PART OF THE SOUTH-WESTERN RAILROAD; LONDON TO BRISTOL.
The former terminus, or starting point, of this
road, was on the Birmingham railway,
about a mile west of Kensal Green. The
present terminus is at Westbourn Green,
about 4 mile north of Bayswater, on the
Uxbridge road from London.
The Datum, or base, of the Section is sup-
posed to be about 7 feet above the Trinity
high- water mark, at the London Docks.
{ Therefore, (approximate) height of the da-
tum, above low-water mark at Sheerness
is (19°6699 + 7) = 25-6699 feet.]
Paddington Canal, at the north-west angle o
River Thames, about + mile south of Mai-
GLACOTE IBGE easncocoobosnosnoges00s000004
Highest point of ground over the railroad ;
north-east of the road fiom Shottesbrook to
Knowle Hill; about 4 mile north of the let-
EOELSHOD ‘alc ccleicsiciesiclclele scissile sleeisialsielelsiaisienlosinieare
| River Lodden, about a mile south-west off
Ruscombe church.........e00+++ Sandososagesa0:
Road from London to Reading, about 363
miles; near letter k in Holme Park (over
the [umn el) fermcecciwtenaascttselesetleteeiecenenct
Railroad at the entrance of the Tunnel on the
east; south-east of the 36th milestone ..
Highest ground over the Tunnel near its
Western extremity, -ccesscscascvccnceeeresmnse
River Kennet, near Broken- Broa north-west
of letter B; about 4 mile east of Reading
General level of the Valley of the Thames,
from Broken-brow to near Kentwood,
Highest point of ground over the Tunnel
near Purley; south of east of the words
TERED 12 ll fseaos000d0d80003000710906000000000
Road about 43 miles from Reading to Pang-
bourn, morn of y in Purley Hall .........
Thames River, about 4 mile north by east
from Moulsford Church, Berks ......seee0
Highest ground over the line of railroad, be-
tween the Thames and West End, on the
Old-0ak: Common s.ccccscccecverssssse ee Raopod| ela
Brent River at Hanwell, south of letter H...) 14
Road from London to Uxbridge, near the
cross road from Greenford to Norwood and
OS EHENLACTAR cneccoudspnecaenbasedeosc006dobo0 65
Paddington Canal, east ot letter Y in Yed-
CIngUBrOOk) vcdeneasasecsceaseassencresssestie 84
Grand Junction Canal, near Botwell.... 84
River Colne, near W. Drayton; west of! the
WOLdSs ColnamuMall vesscccscceeceserenenencees 68
General level of thesurface, on the line from
near Southall, to the heights over the Vai-
ley of the Thames, east of Maidenhead
Bridge......... sosleiteeaiieiiecsavles seeviocios about} 86
Road nae Slough to Stoke Poges; about +
mile from the cross roads ..... SoucHOdOURI0H 90
Cross road from Amerton Bank to Taplow,
about 244 miles from London, on the road
to Mastentend paoooded Scobcoosaconddo6 ecosceat 69
south-west of Cholsey Field...cscccccessseoee
Paper mill stream, north-east of South More-
ton; and north-west of P in Paper ......
56
App. C. |
Dr. Firron on the Strata below the Chalk.
377
Height Height
Stations. epee piabone: ‘Daas
Feet Feet.
General level of surface, from the Thames River Cole, about 4 furlong west of canal at
near Moulsford to East Hagborne ........| 152 Hackron Bridges ; (county boundary en-
Road from Dudcot to Appleford ; west of the tering Wilts from Berks) afeipetatslsliside te ete edicts 2638
WORD auc all rca araveiw delet arsreaterarscrotceeccieeee 173 Roman Ermine Way; about 4 mile south-
Road to Abingdon and Oxford, at the en- east of Stratton-St. Margaret's ......0..0. 324
trance of Steventon on the south-east...... 195 North Wilts Canal, west of Lower Eastcott,
Berks and Wilts Canal, about 0:4 mile north- Mearsthe) bottom Of Li) casccocscccccscccess cece 308
east of Pinmarsh fart... seciseviscdecececesse 191 Brook at Westcot, about 4 mile from
Brook north of Grove-Wick ...... pp Ae Re ah 206 Okus:..%» Maleerevelsece/cielecce sire sila aicwieeiaceemelacese 284
Brook near Circourt; east of the word farm, Brook under the turnpike and railroad at
between Denchworth and Challow Marsh Hunts-Mill, about 3 mile south-west of
LALTIN CG Se taveders isc sarcdddteec sao eee 205 Wotton Basset eaeiebinte cetseanntsenisiacisaeeiiace ss 238
Road from Wantage to ee south-west River Avon, about 4 mile north-west of Avon;
Of Wi in) Westenead® 285.0 sess 240 near the final e in Newhouse farm, 34
Highest ground on the north- meee of Collier's miles north by east from Chippenham
farm, towards Baulking ...... secocesesseees 280 Church .ccscitencee seabaceeesecs dee tmeeeectetan | 180
Canal about a mile south-east of Longcott... 258 Level of the railroad at that place ia/sfalelatnrnetstels 170
Highest point over the railroad, on the slope
north of Bourton, 0:9 mile east of Hack-
WORMB TAGES 2 ah cnceeseceancaatasdeyeehs coseeiss 319
iII.—_ON THE SOUTH-EASTERN RAILWAY, FROM LONDON, BY TONBRIDGE AND
ASHFORD, TO DOVER.
This line was originally intended to join
the Southampton railroad. The starting
point has since been altered, and is not
yet determined.
The datum, or base of the section, is the Tri-
nity high-water mark at Vauxhall Bridge.
Height of datum above low-water at Sheer-
HESS cans oatingecang ACOA TAC MQdODOI60NC 19°67 feet.
Level of Mitcham Common near the Work-
house’ <.:2-: Soededancesartascscondiadenseaeiters
Entrance of a proposed Tunnel through the
chalk, at Woldingham oo... cossececscsseveees
Road to Woldingham Church, about 4 ‘mile
south) ofithe Church)....yss,¢6-caleseeress
Highest point of ground over the Tunnel, ‘at
the meeting of two roads, south of letter)
Wein Woldinghaim x. coso-seacennesdovsdeatete
Oxtead Bridge, at the east end of the village:
—(Stream, about 270 feet)'..,....-scsesseees
Brook south-east of the farm-house, about
= mile south of Win Willwood Farm ......
Road to Edenbridge, about a furlong north
of the cross roads at Holdfast....... Secsotoe
Brook east of Bowbeach farm, where crossed
by roadito Mionbridcen.ccec.qaecerscnsceeeee
River Medway, south-west of Powder Mills,
and 14 mile from Tonbridge; west of the y
it Med ayl ta. caccdsaesassasasecavecne seenenens
General level of qurfaged from the road east
of Tudely church (70 feet), to a road west
Of Hoghill Green (58) ..ccceccsssscecececesees
Main road from Tonbridge to Tonbridge
Wells ; about 4 mile from the separation...
——— ———_——- to Hastings..
Road at Rat’s Castle, on the eastern verge
of Paddock Wood
eee eeeresevarssses ereeecees
River Teise, south-west of the final e, near
IBGCKENTOTO! sccceeesnessasseccsster eensece
Road to Maidstone, immediately on the north
of Marden; west of letter WZ ............0+5
Riyer Beult, about 0:4 mile south by east of
Hockenbury WED TLAG Camadasee saadecsenedeneeae
Road from Cranbrook to Charing, at Hog-
HillGreenwavecsese-caccreesceteagerecccsesuers
Stream about + mile east of Ninhouse, about
two miles south-west of Ashford............
Road about 4 mile south-west from Mersham
C@hurelive.cecccsncnses-cassereiesepmatwenecsteats
Road from Sellinge to Hythe, about 4 mile
from Grove Bridge over the Stour
River Stour, south of Stanford Church, about
14 mile from its source near Postling......
Summit of the sand heights cut by railroad
near Stone Farm
Stream at Beachborough, nearly south of the
summer-house, 0°38 mile west of the word
Mill .
Ground at Cheriton Tile-pits
Streamlet (valley of the gault), about + mile
from Inbrook, south of St. Thames’s Well.
Ground at base of Martello Tower, No. 1....
[The same place above low-water, barome-
trically ....seccccccecsersveserecceroeces F. a
Deduct diff. of tides, (at F olkstone)...
Height of the chalk cliff, at the ee =
the undercliff east of Copt Point........+...
Height of proposed termination of the rail-
road, near the Arch-cliff fort, Dover; 58
miles 7 furlongs from London
eee cceeesesecneees
ecererescere
32
30
83
30
97
378
Height
F above the
Stations. ines
Feet
SourH-EASTERN Rariroap (continued).
A change in the beginning of this line has
been since proposed, which will carry it
through Godstone and Tandridge. ‘The
following are some points on the new sec-
tion :—
Road from Croydon to Addiscombe, north o
NIN OROWD ON Merctcteiciselcicisinalcis(esio'e ioeciicieeeesicies 209
Park hill; top of ridge, south of letter a ...| 263
Combe lane, bottom of C ...........0ececceecers 210
Road from Croydon, near Purley House, bot-
HOEN CLENCUIO? Je dnegonogooradooodbondadoo005590000 254
Hill on which is the o/d London road, south
of Zin Riddles’ Down ....... Protececacetonset 407
Opposite to the road to Cattersham ....+4... 413°69
Beginning of the proposed Tunnel, west of
Milling dow Wkav Min c seen eeseisaeelieesseeesesee se 473
Highest ground above the Tunnel ............ 573
Road at the Dog-kennel (Marden Park ?)...' 46005
IV.—SIR JOHN RENNIE’S LINE
The beginning of this line, in the section
laid before Parliament, is at Kennington.
The datum, or base of the section, is the Tri-
nity high-water mark in London.
North-eastern angle of Mitcham Common { se
Smithham Bottom, near the road from Croy-
don to Merstham; letter P. of T.P..........
Same road, south-west of buildings called O/d
brewhousein the Ord. ma
Road to Coulsdon, at the place where it
strikes off from the main, about 4 mile
south of the Red Lion
Above Hooley House, on a line through the
second o in the former word.............e.00+
Turnpike-road, where crossed by a line drawn
through the words Cottage—(Stoney Cot-
tage), and Downs—(Farthing Downs) ...| 303
Ground above the railroad, opposite to the
Star Inn near Chipstead; between the let-
ters ¢ and in a Star
Road (above the proposed Tunnel) from the
Turnpike to Dean's Farm; about three
fourths of the distance from the Turnpike
TREE Xt soadcocdsodod so scand0o00sc0bedeMoNnSaHoscoUd
Highest point of ground over the proposed
Tunnel at Merstham Hill; about 44 fur-
longs south of the point last mentioned..
Turnpike-road north of Merstham, at the Jos
liffe Arms, north of the letters ¢ in Parsee. .
Ground near the Windmill, Merstham, on
the ridge of the a green-sand (fire-
stone)
Millstream, et of ithe bottom i letter M
in Mill
Stream, where cut by a line from the top of
the letters in the word Linkfield. Rreceecnrets
Road from Nutfield to Reigate ; immediately
on the south of the second a in Zanyard.
200
225
Oe ee eee ceeeesetens
297
Peewee reese eserenssnee
323
358
BO ee reer eee ereresecsseeeees
397
498
363
362
Oe eee ee ee re i
285
232
238
Dr. Firron on the Strata below the Chalk.
Road to Edenbridge, immediately on the
Stations.
Road, or lane, from the Oxtead road to God-
one Church ° avcessoacenaecstseecesanouannce
Road to Yandridge Church; near & in Old
Park Wood
Road from Oatead to Crawuest south o
the turn to Whitehall; about 0°05 mile
FLOM! SeIN COC /LUES Lae eaaeee ee esenaeeeenenen
Brook, between Jincoch’s and Sveuihouse
Pere eee eee eee eee ee rr
Road from Crowhurst to Limpsfield, at “Mil
ston Wood, about 9:1 mile south of letter
éin Milston sees SSloleieleieiejele(elstabicialecioteciielesieeere
Road at Wi illwood LAE a oauecicemenenaarereetens
Yo BERR EEE CECE DR EROS COCH ON SEOCBO CO NDEOUCO IEE
[The new line hereabouts joins that first pro-
jected. ]
south of road from Hole Farm
OF RAILROAD, FROM LONDON TO BRIGHTON.
Earl’s Wood Common; on a line with the
lower part of the word Common, on the
east
Height east of Pertridge Common; at the
AKSt OlMMt he word sIV/OOW weccevenseseeseerceee
Stream, a tributary of the Mole; immediately
above, and north-east of the letter P. in
TP:
Stream tributary to the Mole, between the
two letters B in Bonehurst Bridge docono0as
Peete meee eee eee eee eee eee eeeseeesesestessees
eee eer eee eee reer e ee eee ey
224
190
233
167
1567?
152
[From the brook at Bonehurst Bridge, to
that north of Hazlick Mill (more than 4
miles), the surface is nearly flat; on the
Weald-clay. |
Brook, about 2 miles south of the place last
mentioned ; above the second letter e in
iorley-lane Karma weevecsasuaise-teccsorereete
Lane dividing Surrey and Sussex ; south-west
of the second a in Oakland ............00.008
Stream at Hazlick Mill; where crossed by the
road from Jordan’s Farm to Wakeham’s
Green
River Mole, near the road from Crawley to
the Workhouse, south of the letter g in
PRT Cee BTLUGeS mecasedeessaceneteeeee nen eee:
[Near this place, the ground begins to rise
into the Forest ridge, (Hastings-sand). ]
The Mole river, in Tilgate Forest; on a line
with the word Tilgate, and north-west of
letter Cin Cinder Banks .....
Ground in Tilgate Forest, about half a. fur-
long north of re in Green Di CES sncancecceus
Ground over a proposed Tunnel through the
summit of Balcombe Down; (about a fur-
long east of the letter B in Baleombe) .
Road from Cooper’s Corner to Balcombe
Church; at the letter ein Cooper’s.........
[A rapid ‘descent of very irregular ground
Seg gn htt ri rrr iit
succeeds. |
254
304
293
App. C.] Dr. Frrron on the Strata below the Chalk.
S1o*
Height He
; Eee eight
Stations. ead Stations. ge
Feet Tae ele
Stream of the Ouse River; immediately on Road, from the London road to Brighton Hest:
the south of the letters / and s in Pil- towards the Windmill on Clayton Hill
Oe Ae WG te CO Rie eae S 54 south of D, and north-west of G, in the
Highest point of ground over a proposed words Dunetan’s Gate ..c..¢..00.0sess sos. ten 382
Tunnel through the heights north o Highest point of ground, over a proposed
Cuckfield; about half a mile south o Tunnel through the chalk; about half a
letter a in Taylor’s Barn....s.cscoscessevveee 371 furlong south of the point last mentioned, 458
{Irregular ground, rapidly declining, suc- [Ditchling Beacon, 2+ miles eastward,—(the
ceeds for about 2 miles. ] highest point of the chalk range in this
Stream of a large branch of the Adur; about neighbourhood,) is, according to the Ord-
2-1 miles directly south of the bottom of nance Survey, 858: feet above low water. ]
letter & in the word CuckrieLp, and about Exit of the proposed Tunnel, about 4 mile
2 miles west of Wivelsfield ......c.ccsceeoees 49 morthy of Rangdea paraneataieess saree 204
[The surface here for about 4 miles is very [The ground thence descends rapidly and
irregular; the greatest height, about 250 uniformly towards Brighton, along a val-
feet; the average, 80 to 100.] ley of the chalk. ]
Stream, south of the letters Oa in Friar’s Lane to the church at Patcham, about 0:1
OGY tse ecssecocatcoscenstrseasssteces Spcopco6e 98 mile from the turnpike road ...........066 164
Road from Hurster Point to Keymer; where Termination of the proposed railroad, on the
cut by a line drawn from r in Friar’s, Lewes road to Brighton, near the Royal
through a in Wickham, north of Clayton .| 165 Garden...... Rods pobaCPoDanSOOnOUOCHSeSHaCoeOGeBe 82
!
V.—MR. STEPHENSON’S LINE OF RAILROAD, FROM LONDON TO BRIGHTON.
This line is intended to strike off from the
Southampton railroad. The datum or base
of the section is consequently the same as
of that line; viz. the Trinity high-water
mark at Vauxhall Bridge.
Road from Wimbledon to Merton, +
south of ed in Wimbledon......s.sesesseereees
Road on Merton Common, to Cannon Hill;
west of the top of letter Cin Common ...
Stream from Pylford Bridge, crossed by
railroad about 0-2 mile north-east of letter
P in Park Farm ........ S608 ‘agnbonds00* onenes
Height at Sparrow FArm...cccccsecseececnees ose
Road from Kingston to Ewell, over a at
ridge; between the end of the word Ewel
ANGE COUT Gacace cos ace sssccspesaaeanaaeentmeeas a
Stream of the Hog’s mill river ; at a'point due
south of letter Cin the word Court ......
Road on the northern verge of Epsom Com-
mon; at a point due north of letter o in
Epsom Wells
Highest point of ground over a Tunnel
through the ridge on Epsom Common; 0°1
mile due south of the second m in the word
Common
Height of the railroad at the exit of the Tun-
VS Gbepoc Reelelonineticlnsleeintsaiaselsaissnaaaiiccesiceeas
General level of the ground, on the south-
west of the ridge, by Duke’s Hill, to the
north-west of Ashstead
Road from London to Leatherhead, north o
the first letter e in Leather...... acovonGnoose
Road from Leatherhead to Dorking, east o
letter MZ in the words R. Mole
River Mole, due south of the letter e in Mole ;
nearly on a line joining the words Fetcham
ANd LUGChIChAIM Sn scsscessncacsescrsosascncescos
Bete Cees Coes este eEeeeeseseees
fetes eeweee Poor eee rrosseresesneeeseses
ee eeercceeeaseeonsces
54
39
54:4
141
104
72
172
244
153
156
169
125
93
Highest point of ground over an intended)
Archway in Norbury Park; north of the
HIST TIMOR) gadcoocondénoonopeaco5osde. 225°5
Level of railroad at bottom of Archway ...| 134
River Mole ; immediately south of the Arch-
way, and of letter y in Norbury ............ 98
River Mole; about 0°8 mile south of the last
place, north of letter e in the word West-
HUN OleWancscnseesecsessesscencecacen scot aeeeete 108
Millstream, 4 mile north of letter Pin Punch-
BOW ecenescdsmtensconcecsvccsodnenecnssreete -.| 128
Road from Dorking to Reigate, at the cross-
roads south-east of the words Punch Bowl) 184
Highest ground over a proposed Tunnel,
about 0°35 mile from the cross roads last
mentioned; south-east of c in Dorxine...| 345
Height of the bottom of Tunnel at its exit...) 82
Lane or road, west of letter P in Park Farm} 218
Stream between two lanes north of letter S
in Scammet’s Farm ..ccccceeseoeee ACaCOnGOaBEC 165
Stream (another tributary of the Mole,
springing on Holmwood Common); at a
point south of the second m in (Brockham)
(COTTIER dacotbobboobonacocooeHpsdobooHaACoosocd 207
Stream which runs to Ewood Pond; on the
north-west margin of a wood, about 4 mile
from the edge of the pond .............. »--.| 205
Height, in the wood, between the words Hen-
fold and Park Gate ..cecscceseceveseressoneees 285
Streamlet on the south of the wood, due east
of the word Knole Farm ........ssssesseseees 221
[The highest point of the railroad hereabouts,
is between the streamlet last mentioned
and the village of Newdigate, and is 247
feet above the datum. The road then de-
clines rapidly to Warnham, and thence to
the seaside. ]
380*
above the
Stations.
Mr. Sterpnenson’s Bricuton (continued).
Brook between Green’s Farm and Rushet,
where crossed by a line joining letters x
and ¢ inl thoseswordssenesseer sss ceceaceceesees
Highest point of ground cut by the railroad,
on the east of Plaistow Farm, 1 mile from
the point last mentioned
Boundary of the counties of Surrey and Sus-
sex; immediately above letter MW in Mug-
geridge Farm
Brook on the east of the London Road, abeu
1:7 mile south of Kingsfold; and 1:15
mile from Warnham so. ..cosesccsssece Gages
Brook south-east of Slaughter’s Bridge, under
the letter B
Height, east of the main road, on the west of
a small wood above the words Lake Barn.
Stream, a tributary of the drun, on the south-
west of Horsham; north of the letters ar
in Farthings, and a little south of west
from the words Tower Hill
Railroad at the same point
Road from Horsham to Worthing; about 23
miles from the former, between the word
Prior’s, and a short lane leading to that
farm-house
Cece eee e sees eseeereseseeeeeeee ee
Coe weer eee een sees reese eeeeeeoes
Peewee se eseeseee
COCO eee ero ener eeesoresesaneseeaneeee
Dr. Firron on the Strata below the Chalk.
Height
Datum.
136
| Stations.
|
| Heights cut through by the railroad, on the
| south-east of Cobb’s Hill; about 0-1 mile
south of letter s in Tuckman’s.......+..000++
Two streamlets, south-east of the point last
mentioned, where cut by the line passing
from a in Tuckman’s to ha in Smallham :
| the level in both is, about
Heights on the north of Joulsfield Common,
east of West Grinstead; about 0:1 mile
north-west of a Windmill ..................
/Road north of letter a in Partridge Green,
| about 4 mile east of the main road to Stey-
ning
| Principal branch of the Adur, on the north-
| west of Henfield,—(called in the section
Henfield Cut) ;—where crossed by a line
| connecting letter e in Bine Farm, with L
| in Lashmer’s: nearly on a level with the
| Datum
|
| [Thence to the seaside, the railroad follows
|
Cees e re eeaeewoenee
Pee eee e ewer eer er eee oe eeseseesceeesreeeeeeee
CORR eee e ewer seesresasscesaesoresssesceee
the valley of the ddur; passing through
the chalk range, by the defile of that
| river, to Shoreham. |
Part of a hill cut through by a projected
Tunnel north of Brighton, on the road to
Preston, about 071 mile north of a wind-
millvoniits suMMIt, 1S AbOUtsscesseseeeesereee
[ App. C.
Height
above the
Datu.
Feet.
123
25°5
0-6
VI.—LONDON AND SOUTHAMPTON RAILROAD, BY BASINGSTOKE AND WINCHESTER.
This road begins on the bank of the Thames,
near Nine-Elms, about + mile south-west
of Vauxhall Bridge.
The datum or base of the section -is the
Trinity high-water mark at that bridge.
The levels were ascertained under the di-
direction of Mr. Giles, engineer to the Com-
any.
The height of the datum above low-water
mark at Sheerness, is ........+0.- 19°67 feet
[The natural surface for about 2 miles from
the point of commencement, across Batter-
sea Fields, is 1 to 5feet below high-water}
mark. }
Road from Battersea Rise to Wandsworth,
immediately on the west of the cross-road
to Battersea
Highest point of ground on Wandsworth
Common, about the letter 2 in the words
Half Farthing
River Wandle, where crossed by the railroad,
near letter ¢ in Garret Mill......0..s.ssece+e
[From the foot of the height near Kingston,
south-east of Surbiton, to Walton Com-
mon, is a continuous flat. ]
London and Portsmouth Road, on Ditton
Marsh, south of letter a in Marsh
Railroad at the same point
Road from Walton-on-Thames to Hersham
Green, at the turn to Burwoed Park
Cetera ewww sees eeeeseeeeseesces
FOC ee eee ease neers ereeeseeenes
oe ecceces
Perce weeeeeereerenne
40
80
10
29
45
37
Ground above the railroad, outside of Oat-
land’s Park; directly south of the second
ain Oatlands
Old River Wey, north-east of the letter / in
LOC SNE ALI. caennece tees sseneteaenaeteee
Wey navigation, at the commencement of]
the Basingstoke canal]; south-east of let-
ee CB Ny a Nid BIG. sacocn connooneonodesecaacbe
ftoad on Woking Heath, from Horsell to
Heathside; under letter W, and immedi-
ately west of letter 7 in Heath ............
Summit of a ridge of sand (called Goulds-
worth in the section) ; south of letters Gr
in Royal Oak Green, and west of the word
Crossland
Stream on the north-east of Pirbright Com-
mon, south of letter m in Hermitage ......
Height on Pirbright Common, north of let-
ters i in Pirbright
Ground at the eastern angle of Furzehill
1 BOO fe Soest pooaacoconocosaaconccocabasouodesscoan
South east extremity of Lodge Pond, on Pir-
bright Common; south of the canal at
Weatherhead L1G ersswesseenecscaceene tease
Highest ground between Lodge Pond and
the canal at Frimley Wharf; about 4 mile
north-west of the word Lodge ............0+
Basingstoke Canal, west of the word Wharf.
Ground at Blackwater Brook, or River, di-
viding tle counties of Surrey and Hants;
Peewee eee esses cesses oesssssenes
POOP e emo eseesreereseeseesseesssesesee
ree eee eee ee
about 4 mile south of F in Frimley Green.
1038
29
42
90
185
103
173
168
227
272
235
192
App. C. ]
Height
above the
Stations.
Datum.
Feet.
Road from: London to Farnham; + mile
south of the word hill in Windmill-hill ...
Stream where crossed by a line joining the
words West-heath and Workhouse
FTighest ground on the line east of Fleet Pond;
1 mile from the point last mentioned......
Margin of Fleet Pond, north of letter / in
JAG AG Ate ae oS Cee SRE EDO OCDE PDOUDOL HACODSCHC
Height west of Fleet Pond; 4 mile south of|
letter @ in Broomhall, and 0:4 mile west
of the pond’s edge
Ridge about 14 mile west of Fleet Pond, and
3 mile east of letter Fin Greenham’s Fm.) 237
Stream, between the letters m and sin Green-
TCIOIS. 7 ae cboncconee acon ac cnoaspabapaoosonand.
Highest point over the railroad at Shapley
Heath; between the letters e and a@ in
the word Heath
Railroad at the same point
Whitewater River, at the separation of two
branches, south of the word Holt.........
Road from London to Basingstoke, on Hook
Common; about + mile from the cross
roads in Hook village
Height cut through by the railroad, 3 of a
mile from Newnham Church
Stream on the south-west of Newnham, and
0:08 mile north of the zo in the words Red
Lion
Highest point of ground cut through by the
railroad between Newnham and Old Ba-
sing ; 0°35 mile south of letter WZ in Basing
Mill
Road at Old Basing, west of top of letter O.
Mill Head, River Loddon; + mile west o
bottom of the word Old
Main road from Basingstoke to Reading ; on
a line with the bottom of the word Pen-
ton’s, in Penton’s Mill
Road from Basingstoke to Whitchurch, at
Worting, about midway from the cross
POAAS £0) tHeyCOUNCH -rescrsescrcescsnmscennee
Railroad at the same point
Height south of the word Worting
Road from Church Oakley to Fairdown
Copse; about 0°63 mile from the church,
onithe south-east ic. -cc-cseseasalerosssmmensees
High ground about 4 mile south of the place
last mentioned
[This point is a little higher than the gene-
ral range of the heights between Worting
and Steventon. |
Railroad, 38 feet lower ....+ss+s00.
217
sonaoecod 188
224
214
245
Deere see ee essere eee eeneee
187°5
307
247
Comer eee eesessseeeeesssseeeees
eee eeeeeeeeeesessees
200
293
301
Beem emcee weer esa see ese esses esses es seesseesess
Pema meee errors sees eee sess eee eeeesees
Core caeeeeeeeeeserers
Reece eee ee eeeeeeseseeee
Ce eee ee eeeeesessseee
Peewee eee r cree eeoessesessecesees
382
Dr. Firron on the Strata below the Chalk.
381*
Height
Stations. above the
Datum.
7 Feet.
Highest ground, south-west of Steventon
Church; in a wood east of road at South
WOOU Rate ce cwens sae Secrslosee tees ee 456
Depression on the south-west of the height
last mentioned; northern extremity of
Cobley OO derac-uctscnsseacdewssrecoe cence. 874
Height at the angle of an inclosure, west of
the words Popham Beacon ......... Semececets 454
Railroad (83 feet below) ....-....s..cssess0sse0e 872°5
West side of the inclosures at Warren’s
BOM a ncswrateesscnse vacates teeasek cae atoe ees sees 815°3
Depression 0°7 mile south-west by south of
Warren's Farm; north of S in Sheep Ho.| 268
Height north of Sheephouse Farm, about +
mile north of top of letters Sh.........2.s0+. 313
Stream and road near Weston, about 0°86 east
of the church at Stoke Charity.....sssc0.ee0s 208°5
Railroad at same place, 84 feet above ...... 292'5
Height about 0°15 mile south-west of the
cross roads between Waller’s Ash and Lun-
COORG DEED. “aocson0a -cosnqanoanenatoaqucoedbdS 347
Ground in a road south of letter F, in Hook
PitMhar (ices weceheeedacciscnsccassaceteocaets 164
Summit of height on the east of New Farm .| 228
Road immediately on the south of h in
PLE GAL ORRCMIY OFENY voces scenes sesaceeessasespe 152
Turnpike road from Winchester to Andover ;
east of the words Turnpike gate, on the
MOR (ha) 1/42el SecncoseopaeorindoondorBococedocseonad 177
Railroad at the same place ................0s00+ 177
Height on the north-east of the point last
MACMEONE Op enecteatese-coseseacesones ssrcesacadee 217
Road from Winchester to Southampton, about
0°1 mile from the first s in the words St.
(CFDS s5005c000 qnococdoQsbbCdHODnCOD IIe ONOCHOOONGS 146
Railroad at the same point ..........sseeseeeees 130
[From this place to the shore, east of South-
ampton, the railroad follows the line of
the River Itching, with a nearly uniform
descent. |
Road at Allbrook, crossing the Itching navi-
GQULOW, Maccneseasecernacesersisce sas Sadeocadc0ne%00 41:5
Railroad at the same place...... adoonodaoca0nd: 52°5
Road from Southampton to Twyford and
Winchester, about 4 mile north of Swath-
LEGAG) ecebsbdotcooondobuodancidooobosnagaccooNdease: 23
Y
[The railroad reaches the level of the Lon-
don high water-mark, within the grounds
of Portswood House. |
382* Dr. Firron on the Strata below the Chalk. [ Arp. D.
D.—ADDITIONS AND CORRECTIONS.
Coast west of Hastings.—The alterations and improvements on the coast west of Hastings
were so rapid, soon after the preceding pages 163. to 171. were written, that, within a few weeks,
an entirely new face of the cliffs was brought to light; a great part of the original surface having
been cut away, so as to throw back the vertical section to a much greater distance from the sea,
while the debris were employed in raising a quay, by which the shore is now concealed. The
Rev. Granville Vernon Harcourt, who had examined the new features thus disclosed, was
so good as to point out to me several appearances, which proved that the structure of the shore
was not quite so simple as I had supposed it to be, though the sections above described, and that
represented in Plate X. b. fig. 3., are in the main correct. Several intermediate though slight
derangements occur between the principal fault at the White Rock and the site of the church west
of St. Leonard’s; and the whole of the phenomena show that the original stratification hereabouts
has been fractured and dislocated throughout, although the disjointed portions are seldom
widely separated.
It would be impossible, without the aid of a map on a very large scale, to represent these
derangements, nor have they more than a local interest. The place of one of the principal inter-
ruptions between the White Rock and Warriors’ Gate is represented in Pl. X. b. fig. 3.; and the
beds composing the group thus divided, which, on the east of that point, dip slightly towards
the sea (or to the west of south), could be detected in several places within (or north of ) the
Marina at St. Leonard’s, in the sides of the new roads and streets then in progress, inclining, ge-
nerally, to the north. Their identity could be traced by the aid of two thin beds of greenish Fuller’s
earth, frequently concurrent, but sometimes about 4 or 5 feet apart, and separated by about 8 feet
of grey sand and sandrock, from a bed of dark grey clay, much charged with portions of lignite,
in which indications of vegetable structure were perceptible, but none so distinct as to indicate
the species. ‘These beds are all superior to the Endogenite group of the White Rock ; and their
distance above that group, on the north-east of St. Leonard’s church, was clearly seen to be
nearly the same as at the White Rock. At the roadside, on the east of St. Leonard’s church, I
myself found a specimen of Endogenites, at the place mentioned by Mr. Parish from report.
The greater part of the ground formerly above the White Rock had been removed by the
operations above mentioned, and the fault there was distinctly uncovered to the extent of several
yards. The strata which form the cliff at the brewery descend gradually to the sea, without
apparent disturbance, but the ruins of the superior strata, including numerous fragments of the
lignite bed, were mixed in great confusion on the western and upper side of the fault; which
rising gradually towards the north-east, seemed to cross the valley there separating the cliffs
from those of Hastings Castle Hill, in a direction from about south 35° west to the east of north.
On that line a wide but not deep fissure, or ravine, could be discerned passing towards the place
called Bohemia ; and on the opposite side of the valley, a detached portion of confused matter,
including, as at the White Rock, masses of clay iron ore, was visible in a highly inclined position,
at the corner of one of the lanes descending from the Castle Rock to the marsh. It is not im-
probable that the fault may be continued further up the valley on the north-west of Hastings.
Bones of Birds in the Wealden.—Mr. Mantell, in a short paper read before the Geological So-
ciety, June, 1835*, has shown by anatomical evidence that the bones found at Tilgate Forest, and
* “ Proceedings,” vol. ii. p. 203.
Apr. D.] Dr. Firron on the Strata below the Chalk. 383*
suspected to belong to Pterodactyles, were correctly referred to birds, On placing some of the
questionable fragments before Mr. Owen, of the College of Surgeons, that gentleman found,
in a tarso-metatarsal bone, the articular surface and place of attachment of the posterior, or oppo-
site toe, distinctly indicated ; and on a comparison of these fragments with the foot of a recent
Ardea, no doubt remained as to the similarity of their structure. This short paper beautifully
illustrates the bearing of exact comparative anatomy upon Geology.
Supposed Wealden in Northamptonshire.—Mr. Lonsdale having, during the last summer, resumed
his examination of the oolitic system, and followed out the series from the north of Oxfordshire
to the Humber, informs me, that he did not observe any traces of the Wealden in the vicinity of
Wansford ; which is mentioned at p. 309. as the place where a beautiful specimen of Lonchopteris
Mantellii was supposed to have been found. ‘The tract belongs to the great oolite, which is the
highest formation, and is extensively quarried in every direction around Wansford: on the west
of Peterborough, the highest formation is the cornbrash. Mr. Lonsdale, therefore, thinks that the
occurrence of any portion of the Wealden group in such a situation, is extremely improbable, and
that the specimen above referred to may have been ascribed to that place by mistake.
Supposed Chalk in Rutlandshire.—The existence of Chalk, i situ, at Ridlington, in Rutland-
shire, Mr. Lonsdale considers also as being very improbable. The village stands on the ferru-
ginous sand of the inferior oolite; about half a mile west of it, is a small pit of the bottom
beds of the great oolite, now a subsided mass: and great oolite is quarried near Brooke Hall, two
miles north of Ridlington; but with the exception first mentioned, there is no trace of any stratum
superior to the inferior oolite, in the immediate neighbourhood of that village.
Inoceramus intermedius.—T his fossil, which is mentioned at p. 317, as from Hunstanton cliff in
West Norfolk, is a new species, ascertained by Mr. Sowerby; by whom a drawing of it was
made, for a Wood-cut, published in Loudon’s “ Magazine of Natural History,” for 1829, vol. ii.
p- 296. Mr. Sowerby informs me that its occurrence is not unfrequent in the flinty chalk of Nor-
folk and Kent; and that it is found occasionally, in flint, in the gravel around London.
VOL. IV.—SECOND SERIES. So*
384* Dr. Firron on the Strata below the Chalk.
CONTENTS.
INTRODUCTION, (1.)—(5.), pp. 103—108.
OssecTs of this paper, (1.), p. 103.; General characters and arrangement of the strata to be
described, (3.), (4.), p. 104, 105.; Fossils named, drawn, and engraved by Mr. Sowerby,
Plates XI. to XXIII., (3.), p. 105.
DESCRIPTION OF SECTIONS, (6.)—(162.), pp. 105—817.
KENT, (6.)—(44.), pp. 105—136.
Vicinity or Forxstone; (6.)—(8.), p. 106.; Sketches of the coast by the Rev. I. D. Glennie,
Plate VIII. and X. b. fig. 1.; p.106.; Authorities; Packe, (7.), p.106.; strata described,
(8.), pp. 106, &c.
Upper green-sand, (9.), p. 107; green matter, (10.), p. 103.; analysis by Dr. Turner,
108. note.
Gault, its rise and extent, (11.), p.109.; pyrites, (12.), p-116.; phosphate of lime,(13.), p.111.
Fossils, (14.), p. 112.
Loner green-sand, (15.), p. 155.5 subdivision into three groups, (16.)—(36.), p. 115. :
Ist or upper subdivision, (7.), p. 116.; its composition, (18.), p. 116.; conglomerates,
(19.), p. 116.; “ Kentish-rag”; chert, (20.), p.117.; Sectional Lists, (21.), p. 118.;
false stratification, (22.), p.120.; adopted by concretions, (23.), p. 123.
2nd, or middle subdivision (24.), pp. 121, 122.; Sectional Lists, (27.), p. 123.; diver-
sity of hue and consistence, (28.), p. 124.
3rd, or lowest subdivision, (29.), 124.; its rise and extent, (30.), p. 126.; relations to the
upper groups, (31.), p. 125.; composition, (33.), p. 129.; disturbances, (29.), p. 124.
Fossils of the Lower green-sand, (36.).
Interior oF Kent; (37.)—(44.), p. 131.; general description; (37.), p. 132.; unequal extent
of strata, (40.), p-140.; quarries at Boughton, (38.), p. 132. ; Iguanodon, p- 132, note;
transverse course of rivers, (39.}, p. 132.3; anticlinal ridges between Sevenoaks and God-
stone, (41.)—(44.), p. 133—136; probable mode of their formation, (44.), p. 136, and note.
SURREY, (45.)—(68.), p. 137.
Gopstong, (45.), p. 137.; Upper Green-sand; firestone pits, (46.), p.137.; Gault, (47.), p.138.;
Lower Green-sand ; Tilburstow Hill; remarkable stem-like arrangement of the sand, (48.),
p. 139.
Merstuam; Sectional List, (49.), p. 140. ; Lower Green-sand, (50.), p. 141.; Fuller’s earth at
Nutfield, &c., p. 141.
Reicate; structure, (51.), p. 141.; local disturbances of strata, (52.)—(54.), p. 140. ; ranges,
breaks and interruptions of escarpments ; anticlinal lines, (54.), p. 142.
Dorkine to Lerru Hitz; river gorges, height of outcrop, disturbance, (55.), p. 143.; struc-
ture west of Dorking, p. 142.; flint-gravel upon Lower green-sand, (56.), p. 144.
Guitprorp ; the “ Hogsback,” (58.), p.145.; high inclination of the chalk beds, (59.); Sec-
tional List, (60.), p. 146.
Dr. Firron on the Strata below the Chalk. 385*
GopaLmine ; strata at Holloway Hill; Bargate-stone, (60.), p- 146.
Farnuam to Hinpueap; (61.), p. 147.; barren tract of sands, (62.), p.147.; structure and suc-
cession of strata, (63.), p.148.; Weald-clay between Guildford and Godalming, (64.),
p. 148.; Tucksbury Hill, beds above the chalk, fog level, Bagshot-sands, (65.), p. 148. ;
Drainage of this tract remarkable, (66.), p. 150.; assisting and maintaining causes of trans-
verse drainage, (67.), p. 151.
Fossits of the Gault and Green-sands, in the interior of Kent, and part of Surrey, (68.), p. 152.
HAMPSHIRE and WESTERN SUSSEX, (69.)—(75.), p. 153.
Authorities, (69.), p.153.; gravel in Hampshire remote from chalk, (69.), p.153.;
springs, (70.), 154,; prominence of Upper green-sand, (71.), p. 154.
Vicinity or PurzoroucH; Section from South to North Downs, by Mr. Martin, Pl. X. a.
No. 5., (72.), p. 155.; disturbances, (73.), p.155.; earthquakes around Chichester,
p- 155, note ; junction of green-sands and Wealden at Stopham, (74.), p. 156.
Fossits of the Green-sand and Gault of part of Hampshire and Western Sussex, (75.), p. 156.
Tue WEALDEN IN GENERAL, of Kent, Surrey, and Sussex, (76.)—(90.), p. 159.; acceptation of
the term Wealden extended, (76.), p. 159.; Valley of the Wealds, (77.), p. 160.; beds
of sand, sandrock, and limestone subordinate to the Weald-clay, (77.), p. 160.
Wealden on the coast of Kent, from Hythe to Rye; Rev. G. E. Smith, (78.), p. 161.; the
word “ Hurst ;’ Rev. Joseph Hunter, p. 161, note.
Hastings-sand, (Pl. X. a. No. 6.; X.b. fig. 3.); Mr. Webster, (79.), p. 167.3 strata of the
coast west of Hastings, (80.), (81.), p. 164. ; Sectional List and details, (82.) p. 165. ;
White-rock ; fault, p. 166.; granular, or pisolitic oxide of iron, p. 166, and note; Sec-
tional Lists, p. 167. ; remarkable alternation of sand and clay, (83.), p. 168.; Beds at
St. Leonard’s, (84.), p. 168.; similar group near Tonbridge Wells, p. 170, note.
Fosstts of the Wealden, in Kent, Surrey, Hants, and Western Sussex, (85.)—(90.), pp.
172—181.
Endogenites erosa, (85.)—(89.). pp. 172—175.; its place in the cliffs; external forms,
(85.), p.172.; size of specimens, coating of coal, (85.)—(88.), p.172.; internal structure,
(89.), p. 175.
Other Fossils of the Wealden, in Kent, &c. (90.), p.176; Wood-cut of Sphenopteris gracilis,
p- 181.
ISLE OF WIGHT, (91.)—(102.), pp. 182—206.
Authorities; Mr. Webster, (91.), p. 182.; General structure, (92.), p. 182.; and order
of strata, Pl. X. a. No. 7.—X. b. fig. 4., (93.), p. 182.; Wealden, its resemblance
to beds above the chalk, and to new red sandstone, (94.), p. 184., M. Constant
Prevost, 185, note.
Local distribution of strata, (96.) p. 18€.; Sectional Sketches by Sir John Herschel, p. 186, note.
List or Strata, from Bembridge Down to Sandown Bay; (97.), p. 187.; junction of Green-
sands and Wealden, (98.), p. 189.
Bonchurch-Cove to Sandown Bay; (99.), p.191.; Dunnose, its true place, 191, note.
Blackgang Chine to Brook Chine, (100.), p. 194.; junction of green-sands and Wealden; Weald-
clay near Cowleaze Chine, p.198.; Conleaze, Barnes’ and Grange Chines, p. 199.
Afton Down to Brook Chine, (101.), p. 200.
Fossits of the strata below the Chalk, in the Isle of Wight, (102.), pp. 202—206.
3 c*2
386* Dr. Fitton on the Strata below the Chalk.
DORSETSHIRE, (103.)—(120.), p. 206—233,
Iste or Purseckx; Pl. X.a. Nos, 8. and 9., and X. b, fig. 6. and 7, General arrangement and
distribution of strata; list at Worbarrow Bay, (103.), p. 206.
Purbeck strata; thickness, (104.), p. 208. ; remarkable appearance near Swanage, p. 209, note.
Portland-stone, (105.), p. 210. Portland-sand, (106.), p. 210.
Section at Emmet’s Hill, p. 211. Pl. X. b. fig. 5. and 6.
Kimmeridge-clay, (107.), p. 212.
Coast west or Purseck; General structure and stratification from Purbeck to Portland Island ;
great disturbances, (108.), p. 214. Sections to Whitenore, (109.), p. 215, and note. Lulworth
Cove, p. 216; Man-of-War Cove, Plates X.a. Nos. 8.and 10.; X. b. fig. 7. and 8.; p. 217.
Iste or Portitanp. Authorities, (110.), 217.; Section and Detail of stratification, (@bhis
p- 218.; large silicified trunks, Wood-cut, pp. 221, 222.5 slices for microscope, p. 222, note.
Two beds containing Cycadex; above the “Cap”, p. 222.; and beneath it, p.223; large spe-
cimen, 223, note. General remarks; plants either Coniferze, or Cycadez; and silicified
amidst calcareous matter, (212.), p. 225.
Order of deposits, (113.), p. 225.; supposed analogy to phenomena at the mouth of the
Indus, (114.), p. 226. The quarries in Portland ought to be frequently examined, (115.),
p- 227. Portland strata on the opposite coast of France, (116.), p.227.
Fosstts of the beds below the chalk, on part of the Coast of Dorsetshire, (117.), p. 228.
DEVONSHIRE, (118.)—(123.), pp. 233—242.
General structure, (118.); subdivisions of coast to the east not discernible, p. 233.
Berehead, Whitechiff, p. 234., Blackdown Hills, (119.), p. 285.; Sithestone pits, (120.), p. 236,
Beds beneath green-sands, (121.), p. 238.
Fossits of the Blackdown pits; their abundance and general characters, (122.), p. 122.; Mr.
Miller’s collection ; Plates XV.a., XVI., XVII., and XVIII., p. 239.
List or Fossits of Blackdown, and some other places in Devonshire, (123.), pp. 239—242.
WILTSHIRE, (125.)—(142.), pp. 243—-269.
Sourn Wittsuire :—Blackdonn hills to Shaftesbury, (124.), p. 243.
Vaxe or Warpour; Anticlinal line, (125.), p.244.; descriptions of sections, (Map, Pl. VII.
fig. 3.; and P]. X.a. No. 13.); General structure, (126.), p. 244.
Details of strata; Chalk, (127.), p. 243.; Upper green-sand, (128.), p. 246. Gault, section
at Ridge, (129.), p.247.; Lower green-sand, (130.), p, 248. Wealden, (131.), p. 248.
Purbeck strata ; sectional lists, Dallard’s, Dashlet, Chicksgrove, Wockley, (132.), pp. 249
—253.; junction of Purbeck and Portland formations, (133.), p. 253.; petrified trees,
upright, (134.), p.254.; Portland strata, (135.), p. 254,
StourHEAD; supposed section, (Wood-cut), (136.), p. 256.
Vate or WarminsTER; (137.), p. 257.
List or Fossits of the Vales of Wardour and Warminster, (138.), p. 257.
Nortu Witrtsnire :—Devizes, Calne, Sections by Mr. Lonsdale, (139.), p.261.
Va.e or Pewsry; Dr. Buckland’s valleys of elevation, (140.), p. 263.
Swinpon ; general structure, (141.), 264.; contact of Lower green-sand and Portland formation,
(Wood-cut), 265. ; sectionat the great quarry, 266.; great nodules in the Portland-sund, 267.
Fosstxs of the strata below the chalk, in part of North Wiltshire, (142.), p. 267.
Dr. Firron on the Strata below the Chalk. 387*
BERKSHIRE, OXFORDSHIRE, BUCKINGHAMSHIRE, parr or BEDFORDSHIRE,
(143,)—(155.), pp. 269—303.
General structure and distribution of strata, (143.), pp. 269—279,
Sections, from the chalk, through Great Hazeley, Garsington, and Shotover, to Oxford, Pl. X.a.
No. 18.; and through Tetsworth to Wheatley, Pl. X.a, No, 18'., and X. b. fig. 11., (144.)
—(147.), pp. 274—279.
Shotover Hill; supposed Wealden beds, p. 274.; Purbeck strata, Combe Wood, freshwater
fossils in oolite, 275.; Great Hazeley Quarry; erosion of the Portland-strata; “Gullies”,
(Wood-cut), p. 276.; pits at Garsington, p. 277. ; Portland and Kimmeridge beds at Shot-
over, p. 278.; Kimmeridge and Weymouth beds, (145.); at Lancomhe, 278.; Oxford-oolite,
(147.), pp. 279—283.
Sxcrion, Pl. X.a., No. 19., from the chalk, through Thame and Long Crendon, to Brill and
Muswell Hill, (148.), p. 279.
Brill, p. 280., lignitized tree, (section B.), p.280.; Long Crendon, Thame, p. 281.; Portland-
sand of Thame, at Barley Hill, p. 282.; large concretions in sand, (Wood-cut,) p. 283.
Sections, Pl. X. a. No. 20. and Pl. X. b. fig. 11., from the chalk at Wendover Hill, through
Aylesbury and Whitchurch, Bucks, (149.)—(152.), pp. 283—293.
Stratification of the contiguous Counties, (150.), p. 284. ; sectional list at Stone, p. 285.; at
Dinton, p. 285.; disturbances above the Portland, (151.), p. 286.; clay like that of Port-
land, but not the “ black-dirt bed”, (152.), p. 286.3; sectional list at Bishopstone, p.287.;
near Whitchurch, p. 288.; at Quainton, supposed Hastings-beds?, 289.; Portland-sand at
Whitchurch, p. 291.; Stewkley, p. 291.; Kimmeridge-clay at Hardmicke; Trigonellites,
Exogyra Virgula, p. 292.
Sections, from Dunstable through Hockliffe, to Stony Stratford, P}. X.a. No. 21.; andto Woburn,
No. 21'., (153.), pp. 292—295. Fuller’s-earth near Woburn, Dr. Holloway, (1723.), p. 294.
Norrtu-East oF BEDFORDSHIRE, (154.), p. 295.
List oF Fossirs in part of Oxfordshire, Bucks, and Bedfordshire, (155.), pp. 296—303.
CAMBRIDGESHIRE, (156.)—(160.), pp. 303—309,
Authorities, (156.), p. 303, note; abundance of transported matter on the surface, (157.), p. 304,
Description oF sections, Pl. X.a, Nos. 22, 25, and 24, (158.), pp. 305—309.; decline of
height of chalk range, p. 305.; Upper green-sand, p. 306.; Gault, p. 306. ; Lower green-
sand, p. 306.; Kimmeridge-clay, p. 307. ; Oxford-oolite ; forms a wave, or low anticlinal
ridge at Upware on the Cam; seen also on the north-west of Haddenhan, p. 307.
Chalk, in Rutlandshire, (159.), p. 308, and note ; its existence, in situ, doubtful, p. 383*,
Supposed traces of the Wealden in Northamptonshire, 309. ; doubtful, p. 383*.
NORFOLK, (160.), (161.), p. 309—316.
West Norrox :—General structure, (160.), p. 309. ; Authorities, p. 309, note.
Section, Pl. X.a., No. 25., by Mr. C. B. Rose. Chalk, at Diss and Mildenhall, pp. 310, 311.
Upper green-sand, p. 312. Gault, p. 212.3 Lower green-sand, p. 313,
Hunstanton Curr; (161.), p. 313. Pl. X. a. No. 26; Pl. X.b. fig. 12. a, b, and c. Section,
fig. 12. b. View, fig. 12. c. Sectional list of strata, p. 314. ; comparative lists, p. 314, note ;
red chalk also in Lincolnshire, and Yorkshire, p. 315, note ; Kimmeridge-clay, p. 315.; deep
Well at Lynn, p.316.
Fossits of the beds below the chalk, in part of Bedfordshire, Cambridgeshire, and Norfolk,
(162.), pp. 316, 317.
388* Dr. Firron on the Strata below the Chalk.
SUMMARY AND GENERAL REMARKS, (163.)—(173.), pp. 318—334.
General or abstract Section, Pl. X. b. fig. 18.; Thickness of strata, (163.), pp. 318—320.
Order of Geological events, (164.), p. 320.
Local distribution of strata in the South-east of England, (165.), p. 321.
Chalk; Upper green-sand, p. 822.; Gault; Lower green-sand; Wealden; pp. 328, 324. ;
Authorities on freshwater beds below the chalk, p. 324, note.
Theory of the Wealden, (166.), p. 324. ; Lakes of North America, p. 325.
Weaiden in other districts, (167.), pp. 826—328 ; Scotland, p. 326.; Lower Boulonnois;
p- 326.; Pays de Bray, p. 326—328.
Marine deposits coeval nith the Wealden; probable a priori, (168.), p. 328.; results connected
with their deposition, p. 329.; places of the occurrence of such deposits, p. 329, 330. ;
Isle of Bornholm, Helsingburg, pp. 329, 330.; may be expected, probably, in central
France, p. 330. ; Portland-sand to be distinguished, p. 331.
Beds below the Wealden ; intimately connected, (169.), p. 331. ; remarks upon them, p. 331.
Composition of strata, (170.), p. 332.: formation of stone amidst loose materials ;—of sili-
ceous petrifactions amidst calcareous matter, p. 332.; petrified shells, sometimes sili-
ceous, p. 332.; Oolite in Oxfordshire, with freshwater shells, p. 333.; pisolitic iron
ore in the Hastings-sands of England, p. 333.
Similarity of deposits of different epochs (171.), p.333.;—of Portland beds to Chalk; of
Portland-sand to Green-sands ; of Wealden to the red and variegated marl of the New
red-sandstone, and of beds above the chalk, and to the coal formations, p. 333.
Fossils, (173.), p. 8334. 5 systematic list referred to; too defective to justify general infer-
ences, p. 334. Acknowledgement of Mr. Lonsdale’s assistance ; Conclusion: p. 334.
APPENDIX.
A.—Descriptive notes respecting the shells figured in Plates XI. to XXIII., by James pe Carre
Sowersy, F.L.S., &c.: pp. 335—848.
A*,.—Figures of Vegetable Remains; Sphenopteris gracilis; (Wood-cut, p. 181.). Endogenites
erosa; Plates XIX. and XX., p. 349. Fossil Cones from the Wealden, Plate XXI. figg. 9,
10, and 11; Cone approaching to an Araucaria, p. 349.
B.— Systematic and Stratigraphical List of Fossils, pp. 350—368.
Explanation of references, p. 350. Tables of Fossils, pp. 351—368.
C.—List of Heights, pp. 869—381*.
Explanation, and authorities, p. 369—371. List, pp. 371—381*. Railroad Sections,
375—881*.
D.—Additions and corrections ; p. 382*, 383*.
Coast west of Hastings, 382* : Bones of Birds in the Wealden, 382*: Supposed Wealden
in Northamptonshire, 383*: Supposed chalk in Rutlandshire, 383*: Inoceramus in-
termedius, 383*,
V.—Zoological Observations on a New Fossil Species of Chelydra,
from CEningen.
By THOMAS BELL, Esq., F.G.S. F.R.S.
{Read January 18, 1832. ]
THE Testudo serpentina of Linnzus appears long since to have been con-
sidered as constituting a distinct generic form by the accurate Schweigger,
who applied to it the name Chelydra; but from the paper in which this di-
stinction was first given to the world being little known, this tortoise has
since received the generic appellations of Saurochelys, applied to it by La-
treille, of Chelonura by Fleming, and of Rapara by Gray. The last-men-
tioned author has, however, very properly restored the name first given to it,
in his Synopsis Reptilium, the first part of which has recently appeared.
The extraordinary length of the neck and tail, the great comparative breadth
of the head, and especially the shape of the sternum, sufficiently distinguish it
from every other form of the Testudinata. The sternum is very narrow and
lozenge-shaped ; and the ramus of the sternum (constituting on each side the
symphysis between its body and the sterno-costal suture) is exceedingly long
and narrow, so as to give the whole somewhat the form of a cross.
One recent species only has hitherto been discovered, the Chelydra serpen-
tina; and I cannot find any mention of fossil remains of the genus in any
work that I have been able to consult. The fine specimen which I will now
proceed to describe is, however, fortunately, sufficiently perfect to leave not a
moment’s doubt of its relation to this genus, whilst it also retains sufficient
osteological characters to establish it as a distinct species.
Of the specimen itself *, although but little of the dorsum remains, it is evi-
dently the upper side of the sternum which is exposed, as is shown by some
portions of the dorsal margin, which are still seen lying over the limbs as they
emerge from the carapax. This is most obvious at the part where the left
humerus may be observed, partly lying under the marginal extremity of the
anterior ribs. With this exception, therefore, the whole of the dorsal portion
is wanting, having most probably been removed with the superincumbent
* Plate XXIV.
VOL, V.—SECOND SERIES. 3 D
380 Mr. Bett on a fossil Species of Chelydra.
layer of the stone when the mass was split. It is necessary to state these
particulars, as a superficial view of the specimen would convey the impression
that the under surface is the one exposed.
The following tabular view of various parts in the recent and fossil species
will show at once the distinctions which exist in their relative proportions.
It is necessary to bear in mind that the skeleton of Chelydra serpentina, from
which the measurements in the second column were taken, is considerably
smaller than the fossil. ‘The dimensions are given in inches and tenths of an
inch.
Fossil. Recent.
In. Tenths. In. Tenths.
Length of the dorsal shell ............ cies ace swseess 18 0 11 0
Breadth of the dorsal shell at the union with the sternum... 14 5 oo
Breadth of the dorsal shell rather further backwards..... 15 5 e's
Breadth of the sternum at the symphysis, including the ex-
pansion of the waa. tetetetetetteteteyele rs -terel ole) «1s /ele!n'e w! ole! eier> 12 0 8 5
Breadth of each ramus of the sternum at the narrowest part 1 7 ty)
Length from the central union of the bones of the sternum
to the posterior margin of the dorsal shell............ 10 5 6
Length of the tail beyond the margin of the shell ........ 12 0 6 5
From a comparison of these details, we find that, taking the dimensions of
the dorsal shell as the standard, the following proportional differences exist
between the fossil and recent species. The expansion of the upper shell in
the fossil is greatest at some distance posterior to its union with the branches
of the sternum ; that of the recent is widest at the union. The breadth of the
lateral branches or rami of the sternum, in the former, is not less than one
eighth of the whole breadth of the sternum ; in the latter it is not more than
one seventeenth. These differences, with the much greater comparative
length of the tail in the fossil species, warrant me in considering it as a distinct
species, to which I propose to give the name Chelydra Murchisonit, after
the distinguished president of this Society, to whose kind interference I owe
my possession of it. To his pen I leave the detail of every particular relative
to the geological situation of the specimen *, but I think it may not be uninter-
esting to state a few facts illustrative of the habitat and manners of the recent
species, especially as the organization of the two species is so similar as to
preclude the possibility of any considerable difference in their habits.
The Chelydra serpentina is strictly and exclusively an American form.
There is no approach to it in any species inhabiting the Old World. It is
found in the southern states of North America, where it is known by the
name of the snapping turtle. It has also been termed the alligator tortoise,
* Geological Transactions, Second Series, vol. iil. p. 281.
“Mr. Bett on a fossil Species of Chelydra. 381
an appellation which it has derived from its general form, especially the
deeply carinated tail, as well as from its predatory habits. It is strictly a
freshwater form, and is highly carnivorous, seizing its living prey with great
avidity, and with a sudden snapping movement; to which circumstance it
owes its common name. Its food consists of young water-fowl, fish, and
aquatic reptiles ; and the length of the neck, the strength of the jaws, and
the robust and sharp claws with which the feet are armed, are admirably
adapted for seizing and tearing its prey. I have observed in several speci-
mens which I have kept living, that when teazed they will remain for a time
motionless, the head withdrawn underneath the shell, until, at a convenient
moment, the head is thrown forwards by an instantaneous extension of the
neck, and the object of its attack seized by a sharp sudden snap of the jaws.
I have seen a stick nearly as large as the little finger snapped in two by this
sudden movement.
It frequently wanders to a considerable distance from the lakes in which it
habitually resides, and is said to hybernate either in mud or in the ground
near the water. A specimen which I possessed last year repeatedly endea-
voured to dig a retreat for itself in soft earth, which it removed by its fore
feet with great rapidity, entirely concealing itself in the space of a few minutes.
The whole of the freshwater forms are strikingly contrasted with those of the
terrestrial group, in the ease and rapidity of their movements, and in their
carnivorous habits, for the enjoyment of which these qualities are essentially
required; and the group to which the present genus belongs may be con-
sidered as possessing those powers and habits in the greatest degree, with
the exception, perhaps, of the family of the Trionychide, which, however, if
they exceed the former in the quickness of their motions, must yield to them
in strength.
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VI.—On the new Red Sandstone Series in the Basin of the Eden, and
north-western Coasts of Cumberland and Lancashire.
By tue Rev. ADAM SEDGWICK, F.R.S. V.P.G:S. &c.
(WOODWARDIAN PROFESSOR IN THE UNIVERSITY OF CAMBRIDGE. )
[Read February 1, 1832.]
Introduction.
IN two papers read before the Geological Society during the Sessions of the
past year*, 1 endeavoured to describe the phenomena exhibited along the
line where the carboniferous chain of Yorkshire and Westmoreland strikes
against the old slate rocks of the Cumbrian mountains. ‘Taking up the sub-
ject where it had been left by Mr. Phillips}, a series of enormous faults and
dislocations were traced, nearly along this line of junction, to the foot of
Stainmoor; and it was shown that mountain masses of rock, torn off from the
carboniferous series, were thrown down with a reversed dip into the higher
part of the valley of the Eden, near Kirkby Stephen; and that after many
breaks and contortions, they gradually gained a more regular strike and dip,
and were prolonged into a chain, forming the northern outskirt of the primary
Cumbrian system, and terminating at Egremont. It was at the same time
shown that another fault, ranging under the escarpment of the Cross Fell
chain, produced a corresponding effect on that part of the carboniferous series ;
and that both these great disruptions took place at a period anterior to a
portion of the conglomerates of the new red sandstone}.
In this paper I purpose to give a sketch of the new red sandstone series,
which spreads from both banks of the Eden to the base of the neighbouring
mountains, and afterwards skirts the coasts of Cumberland and Low Furness.
In performing this task I shall endeavour to describe in order,
Ist, The geographical distribution of the red sandstone series, and the
features of the country through which it ranges ;
2ndly, Two or three masses of older rock, which appear within the limits of
the red sandstone ;
* Geological Transactions, Second Series, vol. iv. pp. 47, 69.
+ Geological Transactions, Second Series, vol. iii. p. 1. + See Plate XXV. fig. 2.
384 Prof. Sepawick on the New Red Sandstone Series in the
3rdly, The successive deposits entering into the red sandstone series, with
a view to their comparison with the corresponding groups in Yorkshire and
Durham ; :
Athly, By way of conclusion, I shall endeavour to give a general compa-
rison of the red sandstone series of Scotland and England, in the hopes of
thereby establishing some general subdivisions, by help of which the several
groups may be brought into at least an approximate comparison with each
other.
The details of this, and of the two other papers, will nearly define the geo-
graphical limits of the primary Cumbrian mountains, a general description of
which I hope in a short time to lay before the Society.
§ 1. Geographical distribution of the Red Sandstone Series, &c.
Between the chain of Cross Fell and the primary Cumbrian mountains the
red sandstone series fills a triangular area, the vertex of which may be placed
in one of the tributaries of the river Iden, not far from Brough, and its base
on the frontier of Dumfriesshire and the Solway Firth. Respecting the range
of the north-eastern side of this triangular area, I have few details to offer which
are worth recording ; but I may state in general terms, that if the vertex be
placed on the banks of the Belah (above the bridge on the road from Brough
to Kirkby Stephen), the bowndary line may thence be drawn, by Brough
Castle and the north-eastern side of Brough Hill, to the foot of the carboni-
ferous chain a little above Helton ; and that in the remaining part of its course
to the frontier of Scotland, it continues to skirt the chain very nearly, as is
represented in Mr. Greenough’s map*.
* During the summer of 1834 I examined a part of the Cross Fell chain with Mr. Bowstead, of
Corpus Christi College, Cambridge ; and from our joint observations, as well as from information he
has had the kindness to communicate, I may add the following account of the north-eastern demar-
cation of the new red sandstone. After skirting the north-eastern side of Brough Hill, it ranges
nearly in the direction of Burton; and the rock is seen, in the form of a highly calcareous conglo-
merate, in Walk Mill Beck. Thence the line ranges above Burton; and skirting the hills at a con-
siderable elevation, passes under the base of Roman Fell (which is composed of disturbed beds of
old red sandstone), and is prolonged a little above Helton, and just above Murton. Beyond the last-
named village the line has, for a few miles, a more westerly range, so as to pass considerably below
Keisley ; after which it is, by amore northerly course, brought a little above the village of Dufton,
from which it may be traced across Swindale Beck, near the village of Knock. From this place the
line (still skirting the hills at a considerable elevation, though the beds of red sandstone are nearly
horizontal) may be traced above Milburne, Ouseby, and Melmerby; through Raven Beck, a little
above Renwick; and just above Croglin, from which place it is prolonged near the base of the
great carboniferous escarpment, as may be seen in numerous sections where the rocks are laid bare
Basin of the Eden ana north-western Coasts of Cumberland, &e. 885
The direction of the south-western boundary has been ascertained much
more correctly, by observations carried on from one end of it to the other.
Its minute description is, however, thrown into an appendix, being necessarily
made up of details, which, though tiresome and uninstructive if read before
the Society, may assist in the completion of our geological maps, and be of
some value as matters of reference. Such facts only will be mentioned here,
as throw light on the structure of the red sandstone, and help to establish its
subdivisions.
Where the red sandstone series first appears in the ramifications of the
Eden, near Brough and Kirkby Stephen, it is chiefly seen as a conglomerate,
abounding in fragments of mountain limestone, and cannot, when it has that
form, be mineralogically distinguished from the overlying conglomerates on
the skirts of the Mendip Hills. It is generally in a state of complete indu-
ration where the calcareous fragments abound ; and it sometimes passes into
mere brecciated beds of liméstone: but other parts, especially where the peb-
bles are rounded, and the sand and cement abundant, are soft and crumbling.
In the arrangement of the several varieties of the formations, though the
beds are nearly horizontal, there is very little approach to symmetry or order.
Hence the conglomerates offer a very unequal resistance to the action of the
elements ; and above Kirkby Stephen, where the Eden makes its way through
them, they have been worn into channels of extraordinary complexity. Chasms
and deep basins are naturally scooped out where the rock offers the least re-
sistance ; and by these inequalities great eddies are formed in the river during
every mountain flood, which by whirling round the hard pebbles at the bottom
of each basin, gradually grind away the solid rock, and carry on the work of
excavation far below the surface. Caverns are thus formed; and masses of
conglomerate become so far undermined, as sometimes to allow a new passage
to the river far below the level where it once flowed.
A fine example of this kind occurs at Stenkreth Bridge near Kirkby Stephen,
where the waters, after washing the inclined strata of mountain limestone be-
low Pendragon Castle, plunge among the horizontal masses of conglomerate ;
after which, for a short space, they are heard roaring in a subterranean chan-
nel, communicating by a narrow cleft (called the span of the Eden) with what
by mountain torrents. Further towards the north the calcareous chain declines in elevation, and
the demarcation of the new red sandstone is often ill defined. The best approximation to its course
that has yet heen published, may be seen in Mr. Greenough’s map. It passes (as there represented)
to the east of Brampton, after which it ranges, in a sinuous line, very much concealed by alluvial
detritus, but on the whole bearing nearly due north till it crosses the Liddel and enters Scotland ;
then it is deflected nearly to the west, and crosses the Esk just above Canobie Bridge.
386 Prof. Sepewick on the New Red Sandstone Series in the
appears to have been the ancient bed of the river. Within the memory of man
this cleft might be spanned by the human hand; but it is now, by an act of
wanton mutilation, despoiled of a portion of its honours, so that the projecting
ledges of rock, at their nearest point of approach, are about two feet asunder.
A little way below Kirkby Stephen the conglomerates are in a state of ex-
treme induration, and rise in large flat beds, sometimes used for coarse flag-
stones and coping-stones, a purpose to which the conglomerates of the new
red sandstone are also applied in the neighbourhood of the Mendip Hills.
The relations of the overlying series are extremely obscure for several
miles below Brough and Kirkby Stephen, being much concealed by enormous
masses of transported materials. ‘The new red sandstone is however seen, in
several places, in the channel of the Eden, and the line of demarcation passes,
on the whole, considerably to the south of its left bank*. In the rivulet which
descends to Little Ormside, and at Burrels, to the south of Appleby, the conglo-
merates are again exposed; and (though the sections are obscure) appear,
from their position, to be at the base of the red sandstone seriest. Near
Burrels they form a fine escarpment, parts of which contain large fragments
of mountain limestone (sometimes rounded but generally angular) and are
extensively burnt in the neighbouring kilns: other parts of the escarpment
are of a finer structure, rise in thick flaggy beds, and are used for building.
The imbedded pebbles and fragments of gritstone and limestone seem to be
derived exclusively from the neighbouring carboniferous formations ; and are
held together by a red, calcareo-ferruginous cement, more or less mixed with
siliceous sand, and in a very variable state of induration. Subordinate to the
cement (which does not, as in some parts of England, contain an excess of
magnesia) are a few concretionary nodules of red oxide of iron.
The range of the demarcation through the remaining part of Westmore-
land, till it crosses the Eamont below Eamont bridge, presents no phenomena
of much interest. It, however, deserves remark, that in this district, especially
near Cliburn, the red sandstone is sufficiently hard and thin-bedded to be used
* In this portion of the range, by far the greatest area of the red sandstone is expanded beyond
the right bank of the Eden. Partly in consequence of the great fault above noticed, all the older
formations, near the base of the Cross Fell chain, have a high angle of inclination, and must have
once formed a deep trough for the reception of the newer deposits. As a natural result of this
position, the red sandstone is often found abutting against the inclined strata close to the base of
the chain; which throughout presents a steep escarpment towards the neighbouring plain. The
south-western boundary of the red sandstone rests (on the contrary) on slightly inclined beds of
the carboniferous series; and is, consequently, thrown off to a great distance from the primary
central groups, and in one or two places approaches very near to the left bank of the Eden.
t+ See Plate XXV. fig. 3.
Basin of the Eden and north-western Coasts of Cumberland, &c. 387
for roofing-slate. In England sucha structure must be considered rare ; but in
Dumfriesshire the new red sandstone not unusually rises in flagey beds which
are, I believe, sometimes applied to a similar purpose.
The further range, to the coast of Cumberland, is detailed in the Appendix
(p. 405); and it is sufficient in this place to state, that the line of demarcation
incloses Penrith Beacon, Thiefside Fell, and the great quarries of Highhead
Castle ; and that, after skirting the Bolton coal field, it stretches in a direction
nearly east and west, and runs into the sea on the south side of Maryport. Along
this line there are no traces of conglomerates (like those above described) ;
nor, in general, is there anything in the position of the red sandstone beds to
prove that they are unconformable to the carboniferous beds on which they
rest*. They make no regular escarpment, and there is moreover a difficulty
in determining their exact limits, of which those who have only studied the
types of our south-western coal fields can hardly form a just estimate. The
gritstone beds of the carboniferous series are, here and there, of a deep red co-
Jour, and cannot always be distinguished from the new red sandstone. More-
over there seem to be, along some portions of this line, traces of a lower red
sandstone, forming a connecting link between the true carboniferous rocks
and the formation I am now describing f.
Between the south-western boundary of the new red sandstone and the
banks of the Eden, there’are many tracts of wild sterile land. For the rich
gypseous marls, which give so much fertility to the great plain of central
England, are there almost entirely wanting ; and the subsoil is composed of
a barren sandstone, on the parallel, if I mistake not, of the forest sand of Not-
tinghamshire. This sandstone has been exposed to great degradations since
the time of its first deposit ; but by taking the height of Penrith Beacon, and
adding to it the depth of the borings in search of coal, near its base, we have
a proof that the portions of red sandstone, still remaining, are in some places
of a very great aggregate thickness t.
The great degradation of the red sandstone is proved, not only by the
* The neighbourhood of Rosley seems an exception to this remark, for the coal strata are there
much shattered, and in some places highly inclined, while the overlying formation of red sand-
stone is nearly horizontal.
+ Among the dislocated and highly-inclined beds near Brough, the grits of the carboniferous
series are generally iron-shot, and not unusually of a deep red colour. Rocks of a similar colour,
but of more doubtful relations, occur near the line of the road between Penrith and Newton Raney;
also in the same neighbourhood near Catterlem and Hutton. Again, a few miles west of Mary-
_port, there are examples of a red grit (probably portions of the “lower red sandstone”) near the
demarcation above noticed.
t Ata place called Honey Pot, close to the banks of the Eamont, a little below Penrith, they
VOL. V.—SECOND SERIES. 3) 101
388 Prof. Sepewick on the New Red Sandstone Series in the
outline of the country, but also by the enormous masses of drifted materials
by which it is accompanied. It is no part of my object to describe these
materials in detail; but I may here remark, that mingled with them, and
overlying them, are great bowlders of Shap granite, which have been drifted
over the hills and plains skirting the Eden from Appleby to the foot of Stain-
moor* ; that enormous masses of Carrock Fell syenite and other crystalline
Cumbrian rocks have been drifted as far as the shores of the Solway Firth,
where they are found mixed with other great bowlders, brought by opposite
currents from the mountains of Dumfriesshire ; and lastly, that the red sand-
stone is often buried, for miles together, under great heaps of the old alluvial
detritus, which has modified all the external features of the region, and some-
times produced a fertility little known where the undisturbed rock is near the
surface.
From the red cliffs of Maryport to St. Bees Head (a distance of thirteen or
fourteen miles, estimated in a straight line), the whole coast is occupied by the
coal measures, excepting one place a little north of Workington, and two or
three places near Whitehaven, where we find an intermediate sandstone, form-
ing, apparently, a connecting link between the true carboniferous and new red
sandstone groups. The red sandstone of St. Bees Head appears to dip con-
formably to the coal measures, from which it is separated, not only by the in-
termediate sandstone before noticed, but also by thé magnesian limestone and
conglomerate which strike across the headland to Ben How quarry +, where
they are cut off by the valley of St. Bees, to the south of which the yellow
limestone is no more seen in Cumberland.
Notwithstanding the position of the beds at St. Bees Head, it is obvious
that, when considered on a great scale, the formation is unconformable to the
coal series; for the same beds, in their prolongation to Egremont, cross ob-
liquely over the range of the mountain limestone, and the new red sandstone
is expanded in irregular outliers far within the limits of the coal fieldf.
Between Egremont and Gossforth, the formation appears to have undergone
a movement of elevation ; for its beds dip at a considerable angle to the west,
bored seventy-four fathoms in search of coal. It is said that they passed through only fifteen
fathoms of red sandstone before they reached the coal measures.
* It is well known that the bowlders of Shap granite have drifted over Stainmoor to the plains of
Yorkshire, and even as far as the eastern coast. They have also been drifted to the western coast
below Milnthorp in Westmoreland ; and they abound in the masses of gravel which are found near
the tops of the high hills between Sedberg and Kendal. + See Plate XXV. fig. 4.
{ These outliers will be laid down on a map to accompany a subsequent memoir on the White-
haven coal field.
Basin of the Eden and north-western Coasts of Cumberland, &c. 389
and the demarcation ranges at a high elevation along the flanks of the neigh-
bouring mountains*. To the south of Gossforth, all the low region border-
ing on the coast is so much concealed by transported matter, that the red sand-
stone is visible only in a very few places: it, however, comes to the surface,
or has been reached by artificial excavations, in several places north of Bootle,
where it appears to rest immediately on the granite+. Indeed, all the cliffs
for eight or ten miles south of Ravenglass are composed of a coarse red gra-
vel, looking like materials formed by the breaking up of the red sandstone,
and probably resting on it,—a conclusion confirmed by the appearance, during
low spring tides, of two reefs of red sandstone (Brandreth Scar and Codlin
Rock) not far from the coast. Between Bootle and Duddon Mouth no red
sandstone has been found zm situ, though the coarse red gravel extends several
miles to the south of the former place. All the southern part of the promon-
tory (with the exception of Hodbarrow Point, where there isa patch of moun-
tain limestone), is, however, composed of marsh land or of drift sandt.
To the south of the Duddon estuary, the red sandstone again appears in
great force, overlying the carboniferous series ; and though buried in many
places under enormous mounds of diluvial gravel, there can be no doubt that
it forms the subsoil of the whole south-western extremity of Low Furness.
It deserves remark in this place, that at Hole Beck, near Stank, in a very
deep denudation, yellow, cellular beds of magnesian limestone are exposed at
the base of the red sandstone §.
The red sandstone is probably also expanded under the low region at the
south-western extremity of Cartmel Fells ; as it is said to have been reached
in two places by excavations, and it appears, as a very characteristic conglo-
merate, unconformable to the mountain limestone near Flookborough Spaw.
No traces of it have, I believe, been discovered on the neighbouring coasts of
Westmoreland and Lancashire; but it reappears (far beyond the limits of the
country Iam attempting to describe) in a small patch, at Westhouse, near
Ingleton ; as has been already noticed by Professor Phillips |].
These detached masses of the new red sandstone prove, at least, that the
formation was at one time expanded over a much larger surface than it is at
present : indeed, there can be little doubt that it once extended, in a conti-
nuous mass, from the shores of Cumberland to South Lancashire and Cheshire.
That much of it has been swept away, is shown by the whole aspect of the
* See Plate XXV. fig. 5. + See Plate XXV. fig. 6.
+ By comparing this description with Mr. Greenough’s geological map, it will be seen that he
has extended the red sandstone of the Cumberland coast considerably too far south.
§ See Plate XXV. fig. 7. || Geological Transactions, Second Series, vol. iii. pl. 2.
SE2
390 Prof. Sepewick on the New Red Sandstone Series in the
neighbouring country. I have already noticed the accumulations of old allu-
vial detritus south of Eden ; but they bear no comparison to the vast heaps of
similar materials which cover, to an unknown depth, nearly all the tracts of low
land bordering on the coast of Cumberland : and all the islands off the coast of
Low Furness are exclusively composed of rounded masses of rock (sometimes
many tons in weight,) brought down from the old Cumbrian and Lancashire
chains, and imbedded in a kind of red alluvial loam derived from the degra-
dation of the red sandstone *. In some parts of the coast the alluvial con-
glomerates are solidified, and only to be distinguished from the true conglo-
merates of the new red sandstone by the greater freshness of the imbedded
pebbles : for the pebbles of the old conglomerates (however distinguishable
in mineral structure,) have, in the regions | am describing, almost universally
undergone a progress towards decay, and are sometimes hollow and entirely
incoherent f.
Before I go on to the next section of this paper, it may be well briefly to
recapitulate.
(1.) The red sandstone series above described appears among the last ra-
mifications of the Eden, in a position decidedly unconformable to the carbo-
niferous limestone f.
(2.) In its prolongation it rests upon the upper portion of the carboniferous
* The erratic blocks of the Cumbrian mountains are not confined to the places above indicated,
but have been carried, in incredible abundance, over the plains of South Lancashire and Cheshire.
They are also found, at a great elevation (for example, near the top of the pass from Macclesfield
to Buxton), on the chain of hills which separates Cheshire and Derbyshire. I also found them
last summer, though generally much diminished in size, on the flanks of the Denbighshire hills,
above Oswestry. To what cause are we to attribute this drift of the Cumbrian rocks? Whatever
it may have been, it must have acted at a comparatively recent period ; for many of the travelled
bowlders, though lying bare on the surface, are very little decomposed, and still ring under the
hammer. The present condition of the Cumbrian valleys confirms the previous statement ; for an
examination of them leads us inevitably to two conclusions: Ist, that they were not formed by the
erosion of the waters now flowing through them; 2ndly, that the causes by which they were brought
into their present form must have ceased their action at a comparatively recent period. Every Cum-
brian valley which contains a lake gives an independent proof of what is here asserted.
+ Considered as mere mineral specimens, the conglomerates of the old red sandstone, in the
North of England, have often a much newer appearance than those of the new red sandstone. This
fact may be partly due to the cementing principle, and partly to the more indestructible nature of
the imbedded pebbles of the old red conglomerates. Both in the South-west and North of England,
the fragments of mountain limestone, which enter so largely into the new red conglomerates, are
generally well preserved where the cementing principle is highly calcareous; but where the cement
is siliceous, the limestone pebbles are, I believe, universally decomposing, and in some instances
have almost disappeared.
t Plate XXV, fig. 2.
Basin of the Eden and north-western Coasts of Cumberland, &c. 391
series ; and, in the long range from Appleby to Maryport, there are few places
where the two formations can be shown, by their dip or inclination, to be in
an unconformable position.
(3.) At St. Bees Head it has apparently the same dip as the coal measures *.
But in the same neighbourhood it is proved to pass obliquely over their out-
crop; and, after overlapping the mountain limestone, to range along the
flanks of the primary mountains f.
(4.) It overlies the carboniferous system of Low Furness, and reappears in
the next promontory, as a conglomerate unconformable to the mountain lime-
stone.
It offers, therefore, most obvious analogies to the new red sandstone series
of many other parts of England. In one respect, however, it greatly differs
from the overlying red sandstone of the great Bristol and Welsh coal fields ;
as its beds are, in a part of its range, not only parallel to the beds of the car-
boniferous series, but appear, through an intermediate sandstone, so nearly to
pass into them, that it becomes extremely difficult to define the precise limits
of the two formations.
§ 2. On some detached Masses of the Carboniferous Series within the area
of the New Red Sandstone.
There may be three causes to account for the appearance of such masses :
Ist, When the chain of Cross Fell was severed (by the great dislocation
above noticed), from the carboniferous chain now forming the outskirts of the
primary Cumbrian system, it seems probable (independently of direct evidence),
that some large dislocated masses of rock would be left in the intervening area
which is now generally covered with the new red sandstone. 2ndly, The red
sandstone may, when first deposited, have been of a very irregular thickness,
and in some places may have left the inferior rocks partially uncovered.
3rdly, The protruding masses of the older rocks may have been laid bare by the
great denudations already mentioned. ‘To one or more of these causes we
may attribute the appearance of the detached portions of the carboniferous
series I am about to notice.
The first example occurs near the middle of Broadfield (once a wild heathy
tract of land, but now inclosed), about six miles due south of Carlisle, and
about a mile and a half east-south-east of the village of Gatesgill. Close to
the meeting of four roads, fine contorted masses of mountain limestone are
exposed in three quarries, two on the east side of the Penrith road, and one
* Plate XXV. fig. 1. + Plate XXV. fig. 5 & 6.
392 Prof. Sepewick on the New Red Sandstone Series in the
on the west*. In the two eastern quarries we have fine thick beds of moun-
tain limestone, some dipping south-south-east, and others nearly perpendicu-
lar, surmounted by several impure beds, which will not burn to lime, and
by about fifteen feet of gravel, tinged red with fragments of the new red sand-
stone. In the western quarry the dip is about north-north-east. At one end
of it the limestone is more than twenty feet thick ; but it thins off, at the other
end, to about half that thickness. This mass is associated with a white free-
stone, and with an impure, ferruginous, encrinite limestone unfit for use. Some
purple-coloured shale and siliceous gritstone, laid bare in a small excavation
about half a mile south-west of these quarries, appear also to belong to the car-
boniferous series ; but how far they are expanded over the plateau of Broad-
field, it would be no easy matter to determine, in the present concealed state of
the country. In the valleys of Ivegill and Raw Beck, to the south and east of
Broadfield, there are, however, very fine escarpments of new red sandstone.
The next example is seen in Chalk Beck, about a mile north-east of Rosley,
and three quarters of a mile above Chalk Foot. On the right bank of the
rivulet there is an escarpment of limestone between 20 and 30 feet thick, sur-
mounted by 30 or 40 feet of red diluvial gravel. Close to this escarpment are
beds of new red sandstone, partly resting upon the limestone, and partly sepa-
rated from it by thin beds of conglomerate containing angular fragments of
limestone. In such a position it might easily be mistaken for a portion of the
formation of magnesian limestone, especially as some of the beds are earthy
and cellular; and all of them are yellow, and contain magnesia. It, however,
on the whole, more resembles the dolomitic varieties of mountain limestone ;
and it dips slightly to east by south, while the nearest beds of red sandstone
dip north-north-west. Moreover, it contains Orthoceratites, beautiful corals
of the genus Caryophyllia, resembling species well known in the mountain
limestone, and large Producte, among which, if I mistake not, is the Pro-
ducta Scotica ; but it does not contain any characteristic fossil of the magne-
sian limestone formation. On these accounts I do not hesitate to class it with
the outlying rocks of Broadfield, which are undoubtedly of the carboniferous
order +.
The last instance which fell under my notice, of any outlying portion of
* The locality is defined on the county maps by the meeting of four roads,—from Gatesgill, from
High Burnthwaite, from Burghthwaite, and from Itonfield.
+ There may be some doubt whether the Chalk limestone be mithin the area of the new red
sandstone, of which it is impossible to lay down the demarcation in a continuous line. There is,
however, an outbreak of the red sandstone at Green quarry, about half a mile further up Chalk
Beck.
Basin of the Eden and north-western Coasts of Cumberland, &c. 393
the carboniferous rocks within the area of the new red sandstone, occurs near
the village of Aketon, about four miles north of Wigton. Some of the neigh-
bouring country is much covered by ancient turf bog and a peculiar sandy al-
luvion ; but to the north of the village some beds of limestone and shale are
laid bare on both sides of the road; and if I have not been misinformed, a
bed of coal 16 inches thick was proved, by boring, to be associated with them,
at a place called Moor Dyke, on the west side of the road. I mention these
facts in the hopes of calling to them the attention of future observers; for I
know of no place within the limits of the red sandstone, where a search for coal
could be commenced with the same prospect of success. My knowledge of
the central portions of that great area, within the basin of the Eden, which
is chiefly covered by the new red sandstone, is, however, extremely limited.
My examination of Cumberland was chiefly confined to the carboniferous
rocks and the central cluster of mountains ; and whenever, in making a tra-
verse, I was led to the edge of the new red sandstone, I generally considered
my immediate labours at an end.
§ 3. On the successwe Deposits which compose the New Red Sandstone
Series, &c.
The preceding details give a general notion of the distribution of the new
red sandstone series within the basin of the Eden, and on a part of the coasts
of Cumberland and Lancashire ; but they give only a very inadequate indica-
tion of the structure and order of those great mineral masses of which it is
composed. This information is, however, conveyed in a much more perfect
manner by the coast section, from Parton to St. Bees Head, which I now pro-
ceed to describe*.
The rich coal field of Whitehaven, constituting that part of the carboniferous
series which is superior to the millstone grit and mountain limestone, may be
separated into two divisions, the upper containing the great maz and bannock
bands, the lower containing four or five workable beds, but of inferior quality.
The united thickness of these two divisions is, perhaps, not less than two
thousand feet; and from this estimate the carboniferous limestone and its asso-
ciated beds are of course excluded. The upper beds are worked in a small
field on the coast, immediately south of Workington ; but in consequence of
an enormous upcast fault they are thrown out, and the lower division is
brought into the cliff, and occupies an extensive plateau stretching from Har-
rington to the hills north of Morresby, about two miles and a half from the har-
bour of Whitehaven. Near the crown of these hills (and about a mile from
* See Plate XXV. fig. 1.
394 Prof. Sepewick on the New Red Sandstone Series in the
the point where the accompanying section commences) another great fault,
producing a downcast to the south-west, probably of not less than a thousand
feet, once more brings in the upper rich division of the coal field. Unfortu-
nately, however, between this fault and the village of Parton, the beds dip to
the east; so that all those which are below the high-water mark necessarily
crop out under the sea. The result is, that no one has been able to extract the
coal, in consequence of the great quantity of sea water which finds its way
through the beds along their planes of dip.
At Parton there are other considerable dislocations, not merely altering the
relative level of the beds, but again producing a reversed dip, by which the
whole series of coal measures, as well as all the overlying groups extending
to St. Bees Head, are made to plunge to the south-west at a small angle of
inclination. The successive strata, therefore, after this last inversion of dip,
have their outcrop in the interior of the country; and the coal seams are
perfectly protected from the sea water by the impervious overlying beds of
shale.
Such is the position of the submarine portion of the coal field of White-
haven ; and it does not seem possible to assign any limit to the works that
may there be conducted under the sea in the direction of the dip. But it
is foreign to my purpose to give any description of these works, as the pre-
ceding remarks are introduced for the sole purpose of explaining the nature of
the base line on which the accompanying section is constructed™.
The north-eastern extremity of this section commences at Parton, among
some broken and contorted beds. The confused ground extends about 150
yards, after which the beds acquire their regular south-western dip above de-
scribed. Following the coast towards Whitehaven, we find the cliff composed of
shale and sandstone, which, after being continued several hundred yards, is sud-
denly cut off by a downcast fault, of 24 fathoms, to the south-westt. From
this point to the north end of Whitehaven, we find an uninterrupted rock of
coarse sandstone (resembling many well-known varieties of millstone grit),
generally of a gray or brownish gray colour, but here and there with stains and
streaks of red. Parts of the rock are of a very strong texture, and have been
extensively quarried for the new piers at Whitehaven. It has also been cut
through by the old tunnel between Whitehaven and Parton, as well as by a
* I owe the knowledge of most of these facts to my friends Messrs. Peile, of the Colliery Office,
Whitehaven; and in a subsequent memoir on the carboniferous series of Cumberland (in which a
description of the Whitehaven coal field will of course form an important part), Mr. W. Peile has
promised to be my fellow-labourer.
+ This is the second fault marked on the section.
Basin of the Eden and north-western Coasts of Cumberland, &c. 395
new tunnel, now excavating for the purpose of a ready communication with
the hills west of Dissington, where the main coal seam is about to be worked.
Its structure is therefore very well exposed.
Close to the north end of Whitehaven comes in another fault, producing a
downcast to the north-east, of eleven fathoms ; but if we follow this fault into
the interior, the quantity of dislocation produced by it is enormously increased.
By this and two other faults, elevating the strata in the same direction, we
may explain the high position of the quarry sandstone in the hills immediately
south of the town. At Saltom, as is seen in the section, are two faults, pro-
ducing downcasts in opposite directions: their joint effect is to bring the
great sandstone once more to the level of the sea, after which it is continued
nearly a mile in a lofty cliff; and its component beds are carried by their dip
(with the interruption of one fault) in regular succession towards the base of
St. Bees Head.
The general character of this sandstone is the same as in the tunnel cliff,
north of Whitehaven ; but it is of a much redder colour, contains many small
ferruginous nodules, andin mineral character is perfectly identical with many
portions of that peculiar red sandstone which separates the Yorkshire coal
measures from the magnesian limestone. It is generally without any trace of
fossils: the very extensive excavations carried on in it on both sides of White-
haven, have; however, brought to light a few obscure impressions of Equiseta
and Calamites. It makes, therefore, a very near approach to a true coal grit ;
and in the surveys hitherto published, as well as in the estimation of the coal
viewers of the neighbourhood, it has, I believe, always been regarded as a
true member of the coal measures.
Under Barrowmouth this sandstone is surmounted by a conglomerate,
exactly like the magnesian conglomerates of our south-western coal fields, but
only two or three feet in thickness. Its lower part is of a reddish colour, and
contains, among other fragments, rolled masses of mountain limestone mixed
with hydrate of iron. The upper parts of it have a calcareo-magnesian ce-
ment; and it is surmounted by, or rather graduates into, a yellow, foliated,
cellular, magnesian limestone. This limestone is not well exposed at the
sea-side, being almost buried under the overlying red marls; but some of its
upper beds are mixed and striated with red ferruginous matter, and seem to
pass into a singular, red, siliceous sandstone containing jasper and chalcedony.
It is, however, extensively worked at Barrow and Preston How quarries, and
shows in great perfection most of those peculiarities of structure which so well
mark the formation. I do not know of any section where all its beds are exposed ;
but it probably never exceeds 60 feet in thickness. Of its relations to the coal
VOL. IV.—SECOND SERIES. 3 F
396 Prof. Sepewick on the New Red Sandstone Series in the
measures, there could not be a shadow of doubt, though there were no other
section besides that on the coast ; and in Croft Pit it has been sunk through
into the lower sandstone and down to the mazn and bannock seams. Along
with the other upper strata, it strikes across the peninsula of St. Bees Head,
and is seen in Ben How quarry (near Green Bank farm), on the low road
from St. Bees to Whitehaven, where it is made, by a remarkable fault, to
abut against the lower red sandstone*. Beyond this point the yellow, cellular
limestone beds do not appear ; but the magnesian conglomerates are found to
the south of the valley of St. Bees (at Parkhouse, and in the rivulet which runs
down thence towards Linethwaite), forming the base of the new red sandstone
group.
Over the preceding deposit of the coast section, come several feet of gray,
thin-bedded, sandy marls, to which the red jaspideous bed, above noticed, ap-
pears to be subordinate. This sandy deposit is surmounted by alternating
beds of unctuous, red marl and gypsum, amounting in thickness to eight or ten
fathoms. ‘The two substances are so mixed together, in some places, as not to
be separable ; but in other parts of the section (and especially in the higher
and lower portions of it) the gypsum is found in strong beds, which have been
much worked; and in one of the excavations was found a bed, about half
an inch thick, composed of a nearly pure, earthy, semi-indurated carbonate
of zinc. This fact deserves remarking, as carbonate of zinc occurs in con-
siderable abundance in deposits on the Mendip Hills, nearly of the same age
with those here described.
Lastly, the gypseous marls are surmounted by sandy marls and micaceous,
slaty sandstone, rising to a considerable height in the red precipice of St. Bees
Head ; and these are overlaid by a great, thick-bedded freestone, which in some
places loses the lines of stratification, and decomposes into rude, grotesque,
castellated forms. These upper rocks are identical with the finest specimens
of the new red sandstone of Cheshire and Lancashire, of Low Furness, Ap-
pleby and Carlisle, and may be regarded as one of the most characteristic
exhibitions of the formation to be seen in our island.
The several beds entering into the structure of St. Bees Head, are carried
by their south-western dip, and by a downcast fault, one after the other under
the sea; and no superior formation is visible on any part of the neighbouring
coast. The “upper red marl and gypsum,” completing our red sandstone
series up to the lower lias marls, are therefore wanting, either having been
washed away by those causes which have produced the present deep indentations
of the coast, or being, perhaps, buried under the waters of the western sea.
* See Plate XXYV. fig. 4.
Basin of the Eden and north-western Coasts of Cumberland, &c. 397
So far the account of the accompanying section, and of the successive groups
of rocks overlying the Whitehaven cecal field, has been purely descriptive, and
unmixed with any hypothesis. The facts themselves contain, however, their
own interpretation. I have already stated that the lower sandstone, overlying
the Whitehaven coal field, resembled in structure the lower sandstone imme-
diately overlying the great Yorkshire and Durham coal fields. The former
contains, though very sparingly, impressions of Equiseta and Calamites; and
so does the latter, as I have now ascertained, though I was unacquainted with
the fact at the time the detailed account of the structure of the magnesian
limestone series was published in a former part of our Transactions *.
Again, though the “lower red sandstone” of Yorkshire and Durham ap-
pears, in some cases, to graduate into the coal measures (on which account it
was classified with them by Mr. Smith in his geological map of Yorkshire) ;
yet, when considered on a great scale, it is unconformable to them, and on that
account was separated from them and arranged, in the paper just quoted, as
the lowest member of the new red sandstone group. In the same manner,
in the coast section above described, the lower overlying sandstone appears
to be conformable to, and to graduate into, the coal measures of Whitehaven.
But, during many excursions in that neighbourhood, I have traced it from the
sea-side to the interior of the country, to the top of the hills above Dissington,
over the summit of Whillimoor, and to the crest of the hills overhanging Ar-
lecdon ; and thus ascertained that it spreads over the edges of the coal mea-
sures, and that, when considered in its whole extent, it is, as far as regards
the position of its lower surface, perfectly analogous to the “lower red sand-
stone” of Yorkshire and Durham.
But the analogies do not end here. It is proved by several of the sections
published in a former part of our Transactions}, that the “lower red sand-
stone” in certain parts of Yorkshire had undergone considerable movements,
and been exposed to considerable degradations, before the deposition of the
magnesian conglomerate and magnesian limestone: for they are here and
there seen resting on its inclined edges, while in other places (for ex-
ample at Pontefract, in many parts of the County of Durham, and on the coast
of Northumberland), the “lower red sandstone’ and magnesian limestone
graduate insensibly into each other, without any break of continuity what-
soevert. Now we meet with precisely the same accidents of position in the
* Vol. iii. p. 37. et seg. Very fine impressions of Equiseta or Calamites have been found in the
“lower red sandstone” of Hooton-Lovett in Yorkshire.
+ Geological Transactions, Second Series, vol. iii. Plate VI. figg. 3. 4. 5. 6.
$ Ibid., vol. iii. p. 67.
3F2
398 - Prof. Sepewick on the New Red Sandstone Series in the
neighbourhood of Whitehaven: for in following the overlying deposits into
the interior of the coal field, we find many traces of magnesian conglomerates,
with rolled masses of mountain limestone, in every respect identical with those
of the coast section (for example, at Gilgaron, near Arlecdon, at Sand
Closes, &c.) ; and we have the clearest proof that the lower red sandstone
had been exposed to considerable degradations, and scooped out into great
hollows before the conglomerates, which form the base of the magnesian lime-
stone, were first accumulated. It follows, therefore, that the “lower red sand-
stone’? overlying the Yorkshire and Durham coal fields, and the lower red
sandstone of Cumberland, are identical in their structure, their relations, their
fossils, and in all the accidents to which they were exposed during their de-
position. We may therefore conclude that they are true geological equiva-
lents ; that they are probably on the parallel of, at least, the lower portion of
the eres des Vosges ; and that they are unquestionably the equivalents of the
rothe todte liegende overlying the coal series at the southern extremity of the
Hartz mountain.
The magnesian conglomerates, described in the previous details of this
paper, cannot be classed with the lower red sandstone, to which they are
sometimes unconformable ; but they graduate into, and form an integral part
of, the magnesian limestone, sometimes appearing entirely to replace it.
The magnesian limestone of the coast section is evidently on the exact
parallel of the magnesian limestone of Nottinghamshire, Yorkshire, and Dur-
ham, though not developed on so large a scale, or separable into the same
number of minute subdivisions. It is not coextensive with the upper division
of the overlying sandstone series ; but it may exist in many places, under the
great heaps of transported matter; and it breaks out, as above stated, ma
very characteristic form, from beneath the new red sandstone of Low Furness,
in a deep valley near the village of Stank*. With this exception, I have never
seen it beyond the promontory of St. Bees Head, in any place within the
limits of the range of country above described.
The red marl and gypsum under St. Bees Head are very nearly on the
parallel of the “dower red marl and gypsum” of the Yorkshire series} ; and
the red sandstone of St. Bees Head is unquestionably the exact equivalent of
the upper red sandstone of that series. ‘The ‘upper red marl and gypsum”
* See Plate XXV. fig. 7.
+ There are in Yorkshire two deposits of red gypseous marls under the great mass of the upper
new red sandstone ; one under, the other over the thin-bedded limestone of Ferrybridge. With
either of these the gypseous marls of St. Bees Head may be brought into comparison, as the
Ferrybridge limestone is not seen in Cumberland.
Basin of the Eden and north-western Coasts of Cumberland, Se. 399
(probably on the parallel of the marnes irrisées and the keuper of France and
Germany) do not appear in the coast section, for reasons already stated.
From all these facts, I conclude that the series of deposits overlying the
Cumberland coal fields is, as far as it goes, perfectly analogous to the corre-
sponding series of Yorkshire and Durham, as described in a former paper.
Nor need we he surprised at this analogy, when we consider the almost
perfect agreement of the great groups of the new red sandstone series in En-
gland and central Germany. I need not repeat the evidence on which this
conclusion rests ; but I may add, that it is even more complete than I supposed
at the time the former memoir was published. Three obscure corals, found
in our magnesian limestone, had already been figured by Mr. Goldfuss under
the generic name of Gorgonia*; and on referring to his account of the lo-
calities from which his specimens were derived, it will be seen that they come
from the magnesian limestone formation of Mansfeld. Nor has this conclusion
been drawn from the mere resemblance of the figures; for both the British
and German specimens have been examined by that accomplished naturalist,
and the fossils found to be specifically identical, as he has himself informed me.
This fact alone, to which, however, a thousand others might be added, is a
sufficient reply to the assertions of some modern writers, who have ventured
to affirm that organic remains are of no value in determining the contempo-
raneity of distant formations.
In our south-western coal fields the deposits immediately overlying the car-
boniferous rocks are subdivided into three principal groups: the lowest com-
posed chiefly of conglomerate, with a calcareo-magnesian cement; the middle
group of red and variegated sandstone ; and the highest of red and variegated
gypseous marls. I think it at least probable that the conglomerates of the
Bristol coal fields are on the exact parallel of the magnesian conglomerates
described in this paper; from which it follows that the Bristol conglomerates,
as well as those in the valleys of Devonshire (if they be all of the same age),
are the true representatives of the magnesian limestone, and not of the rothe
todte lLegende.
I ventured to express this opinion in a former paper}; and it is greatly con-
firmed by the facts here stated, as well as by some other facts which fell under
my observation last summer (1831), while crossing over one of the coal for-
mations of Shropshire. About six or eight miles south-west of Shrewsbury
there is a small coal field, stretching at the base of a greywacké chain from
* See Goldfuss, tab. vii. fig. 1; tab. xxxvi. fig. 1; and tab. x. fig.1; Gorgonia dubia, G. anceps,
G. infundibuliformis; and compare them with Geological Transactions, Second Series, vol. ili.
p. 120; and Plate XI). figg. 5. 6.7. 8.
+ Geological Transactions, Second Series, vol. iii. p. 122.
400 Prof. Sepewick on the New Red Sandstone Series in the
Pontesford towards Westbury, and surmounted by a series of deposits con-
nected with the group of the new red sandstone. The order of succession,
as laid bare by a deep cut for the road near Aldbury, is as follows: 1st, Coal
measures. 2ndly, Coarse reddish sandstone, in character intermediate between
a coarse coal grit and a true red or variegated sandstone. 3rdly, A very fine
magnesian conglomerate, forming a distinct range of hills by Cardeston,
Rownton, and Adenbury, and in mineral structure like the Bristol and De-
vonshire conglomerates*. 4thly, Red and variegated sandstone descending
into the great plain of Shropshire, and of unknown thickness. Here, there-
fore, the section is more complete than at Bristol, and is perfectly analogous
to the Cumberland coast section, with this exception, that the conglomerate
is developed at the entire expense of the magnesian limestone. The con-
clusion naturally deduced from this section is the same as that at which I
before arrived —viz. that the magnesian conglomerates do not represent the
rothe todte liegende, but a part of the next superior division—the magnesian
limestone, or zechstein.
In comparing the Bristol and Exeter conglomerates with the rothe todte
hegende, our geologists made use of the best evidence with which they were
acquainted. But the new red sandstone group is now better understood ; and
in future comparisons with Continental deposits of the same age, we should
use, as our types, those sections which are most complete, instead of the Bristol
or Exeter overlying groups, in which more than one half the series is abso-
lutely wanting. Nor is any assistance to be derived from the accidental pre-
sence of porphyry pebbles ; in as much as they occur in the Shropshire con-
glomerates, as well as in those of Exeter, and are in truth of no value in de-
termining the relative age of any secondary rock.
it must, however, be allowed that a considerable part of our difficulties have
arisen from the ill-defined language of some of the German geologists. ‘The
term rothe todte liegende has probably been often applied to conglomerates of
the same age with our magnesian conglomerates. It originally designated
certain, coarse, red sandstones overlying the coal measures of the Hartz, which,
after a personal examination of them, I believe to be the exact equivalents of
the “lower red sandstone” above described. In the late works of Mr. Hoff-
mann the same term is applied to a red sandstone under the coal measures of
Wettin, and therefore on the parallel either of some of our lowest red coal
grits, or perhaps of our old red sandstone.
* The condition of the pebbles imbedded in this conglomerate is very remarkable. Some of
the mountain limestone pebbles retain their mineral structure and characteristic fossils; others are
so altered as hardly to be distinguishable ; some having become granular, and some perfectly pul-
verulent. See a previous note, p. 390.
Basin of the Eden and north-western Coasts of Cumberland, &c. 401
It only remains for me to notice the importance of the lower red sandstone
in another point of view, entirely distinct from the former. All who have
written on our south-western coal fields, have noticed the total break of con-
tinuity between their component strata and the overlying series: and in the
beautiful illustrations accompanying the paper of Dr. Buckland and Mr. Cony-
beare*, it is impossible to point out the highest members of the inclined coal
measures, in as much as an indefinite number of them may possibly be buried
under the superior horizontal deposits. In Shropshire there is, I think, no
such break of continuity, the gap being filled up by the lower red sandstone.
Again, though the lower red sandstone of Yorkshire is, on a great scale,
unconformable to the coal measures, and ought, on that account, to be consi-
dered as the base of the new red sandstone series ; yet there are places in that
county, where, for twenty miles together, there is no trace of any want of
conformity ; and the lower red sandstone (containing, as already stated, a few
coal plants) forms a true connecting link between the highest coal grits and
the group of the new red sandstone f.
Considering, then, that the red sandstone group sometimes forms a passage
into the coal series, —that the fossils of the magnesian limestone are very nearly
the same generically, and sometimes specifically, with the fossils of the carbo-
niferous limestone {,—that the grits of the coal measures in the North of En-
gland are not unusually of a red colour,—that on the confines of Scotland the
lowest division of these coal grits alternates with red gypseous marls, and
passes downwards into beds of red sandstone and red shale, nearly, if not
exactly, on the parallel of the old red sandstone §,—considering all this, I think
that the phenomena exhibited by our lower secondary deposits lend some
support to a classification now generally adopted in Germany, which regards
the whole carboniferous group but as an integral part of a great formation
of red sandstone, commencing with the old, and ending with the new red
sandstone series. The zoological argument certainly gives some consistency
to this arrangement.
I do not, however, mean to deny the full propriety of the classification of
the same great groups, now adopted by English geologists. It is good,
because founded in nature ; and each country ought to be described without
any accommodating hypothesis, according to the type after which it has been
* Geological Transactions, Second Series, vol. i. p. 2i1.
¢ Ibid. vol. iii. p. 57. No. 5. { Ibid. p. 119:
§ The description in the text was derived from phzenomena, observed in 1830, in the valley of
the Tweed. The gradual passage of the coal measures into the old red sandstone is still more
strikingly exhibited on the coast of Scotland, north-west of St. Abb’s Head.
402 Prof. Sepewick on the New Red Sandstone Series in the
moulded. But in comparing the unconnected deposits of remote countries,
we must act on an opposite principle ; learning to suppress all local pheno-
mena, and to seize on those only which are coextensive with the objects we at-
tempt to classify. In this general view the arrangement of the red sandstone
and carboniferous series in one great group, is perhaps the best fitted to the
present state of our knowledge.
§4. General Comparison of the Red Sandstone Series of Scotland and England.
It has been shown by Mr. Murchison and myself, that in the Isle of Arran
a carboniferous series is interpolated between two enormous masses of red
sandstone and conglomerate ; and that the whole group passes, in the ascend-
ing order, into a formation of red sandstone, which may represent either one
of the red, sterile parts of the Scotch carboniferous series, or the lowest di-
vision of the new red sandstone*. It is almost impossible to ascertain the
precise limit of this upper red sandstone of the Isle of Arran: but the best
way of approximating to it would be to trace the old red sandstone group
from the south flank of the Grampians to the west coast of Scotland; and from
thence to follow the red sandstone series to the coasts of Ayrshire. By the
help of such an examination (a desideratum in Scottish geology), we might
perhaps establish such analogies as would enable us to determine the exact
upper limit of the Arran section.
I consider it now established beyond doubt, that the great masses of red
sandstone and conglomerate which fringe the Highland coasts, and range, on
the south flank of the Grampians, from one side of Scotland to the other,
belong almost exclusively to the old red sandstone. The large development
of the bituminous schist of Caithness has thrown some unnecessary difficulties
in the way of this conclusion. Jt alternates, however, with the old red con-
glomerates to their base, and cannot be separated from themT ; it is overlaid
by a red sandstone decidedly of older character than any variety of the new
red and variegated group ever seen in other parts of Great Britain ; it con-
tains a suite of fossils peculiar to itself; not, as far as is known, interchanging
a single species with the magnesian limestone ; it is represented (and by no
means in an unusual form) on the south flank of the Grampians by a series of
thin-bedded strata, placed by Mr. Lyell even lower than the old red sand-
stone}: and, lastly, the remains of fish have been found by Dr. Fleming in
groups of slaty sandstone, which, though superior (like most of the Caithness
schists), to the lowest old red conglomerates, are inferior to the true carboni-
* Geological Transactions, Second Series, vol. ii. p. 21; and Plate III.
¢ Ibid. pp. 140. 157, 158. ¢ Ibid. vol. ii. Plate X.
Basin of the Eden and north-western Coasts of Cumberland, &c. 403
ferous formations of Fifeshire. I conclude, therefore, that the true position of the
ichthyolites of Caithness is out of ali doubt, and adhere, with very slight modi-
fications, to the classification published by Mr. Murchison and myself*.
By way of conclusion, I may add, that the anomalies at which I have
pointed, in different parts-of this paper, and the difficulties they throw in
the way of any universal classification, can be no matter of surprise. The
great cause for wonder is, that among such vast and rude, mechanical
operations of nature, we should be able to trace even the approximate ele-
ments of order. Whatever may be hereafter decided about the general group-
ing of the coal measures, the near coincidence of even the minute minera-
logical subdivisions of the new red sandstone series in the North of England
and central Germany, and the general correspondence of their fossils, must be
regarded as one of the most satisfactory conclusions of secondary geology.
POSTSCRIPT.
Cambridge, August 7, 1835.
In consequence of the long delay in printing our Transactions, memoirs
must sometimes appear which, at the time of their publication, do not express
correctly the opinions of the respective authors. The preceding paper is
published (with the exception of verbal corrections and the addition of the
short notes) as it was read to the Society. Had the concluding remarks been
written now, they would have been considerably modified.
I have taken for granted that the Exeter conglomerates, and those over-
lying our south-western coal fields, are of the same age. Mr. De la Beche
has, I believe, ascertained, since this paper was read, that the former are older
than the latter. Hence, the remarks intended to show that the magnesian
conglomerates (e. g. those of the Bristol coal fields, the flanks of the Mendip
Hills, &c.) were not the equivalents of the rothe todte liegende, cannot be
applied to the conglomerates of Exeter, at least without some modification.
The Exeter conglomerates may, then, be equivalents of the upper part of that
sandstone which, in the North of England, fills up the chasm between the coal
measures and the group of the new red sandstone. There is, however, in all the
sections of Somersetshire, Devonshire, and South Wales, a want of continuity in
these formations. Their position is perfectly discordant, so that it is physically
impossible the successive deposits should be complete: something is wanting,
which is supplied by the uninterrupted sections in the North of Englandf.
* Geological Transactions, Second Series, vol. iii. p. 157.
+ Precisely in the same way, the sections in the North of England, connecting the old red sand-
stone and the slate rocks, are not continuous; and there is just the same break in Denbighshire
VOL. IV.—SECOND SERIES. oO) (e!
A404 Prof. Sepawick on the New Red Sandstone Series in the
The discussion on the age of the Caithness schists might now be con-
sidered unnecessary ; but when the paper was read, there were many mem-
bers of the Society who were disposed to identify them with the ichthyolites
of Mansfeld. The question is now set at rest by the generic and specific
characters of the Caithness fossils, and by the discovery of fossil fish in the
old red sandstone of Herefordshire, identical with specimens found in the old
red sandstone of Scotland.
Were I to make any change in the Caithness section, published by Mr.
Murchison and myself *, I should alter the colour of the sandstone of Dunnet
Head, and make it of one tint with the lower conglomerates ; thus including
the highest beds of the series in the old red sandstone. The formation would
then have three divisions, which might be respectively compared with the
three divisions of the Herefordshire sandstone, first given by Dr. Buckland
and Mr. Conybeare; and the echthyolites of Caithness would then come on
the same parallel with the cornstones of Herefordshire.
If such a comparison be considered as too refined for the evidence on which
it rests, I may at least assert, that the words ‘“‘ newer red sandstone,” placed
under the colour representing the group of Dunnet Head, tend only to mis-
lead the reader, and do not correctly represent our opinions at the time the
section was published+. By these words, English geologists have generally
designated deposits of the age of the upper sandstone of St. Bees Head, with
which it was never our intention to bring the rocks of Dunnet Head into com-
parison}. It is true, that the upper limit of these rocks must remain in some
measure ambiguous ; but I have now little doubt that the whole of them ought
to be classed with the old red sandstone.
The relations of the red sandstone group of Shropshire to the carboniferous
series have been described during the past year in great detail by Mr. Mur-
chison ; and I believe his views agree perfectly with what is stated above
(pp. 399, 400.). I had few details to offer, and only alluded to the Shropshire
formations for the purpose of confirming conclusions drawn from certain
phenomena in the North of England.
and Flintshire. How many terms of the series are wanting it is impossible to tell without more
evidence; but this evidence is given in the Shropshire and Herefordshire sections described by
Mr. Murchison.
* Geological Transactions, Second Series, vol. ni. Plate XIV. fig. 2.
+ I am the more anxious to make this correction, because Mr. Conybeare has adopted and ex-
tended this error in his Memoir on the Progress of Geological Science, published in the first volume
of the Reports of the British Association for the Advancement of Science.
t Geological Transactions, Second Series, vol. it, pp. 157, 158.
Basin of the Hden and north-western Coasts of Cumberland, &c. 405
APPENDIX.
On the Demarcation of the New Red Sandstone Group, described in the preceding Memoir.
The northern line of demarcation, commencing near Brough and ending on the Scotch border, has
been already noticed (supra, p. 384, note). The remaining line may be traced as follows. Com-
mencing, as before, at the top of the flat lands near the bifurcation of the Belah, the line may be
drawn a little south of the left bank of the river, so as to leave out Caber. It then turns, about
south by west, till it just touches Winton, from which it ranges a little to the west of Hartley, just
under the road from Hartley to Naitby, which place it incloses within the area of the red sandstone;
thence, crossing the river, it enters the north end of Wharton Park, and ranging nearly due north,
passes along the brow of the hilljust above Kirkby Stephen. The range then appears to be about
north-west for more than a mile, when the line makes a bend, passing the rivulet about half a mile
south of Soulby; thence to the rivulet a little north of Crosby, from which a curve line may be
drawn skirting the high lands, so as to pass a little east of Musgrave; afterwards nearly parallel
to the Eden, so as to pass about a quarter of a mile south of Warcop Bridge, north of Birks
Chapel; half a mile south of Little Ormshead ; and from the last-mentioned point to the rivulet
just above Hoff. The line is then nearly defined by the left bank of the rivulet, and passes to
the north-west just above Colby, which it incloses.
Part of the preceding line is imaginary, the country being covered by enormous masses of red
diluvial gravel. But the conglomerates are seen at Belah Bridge, in the river under Winton, at
Naitby and Kirkby Stephen, and in the river above Soulby. Again, the red sandstone is seen on
both sides of the river near Warcop; and the conglomerates break out in the rivulet south of Little
Ormshead, and at Hoff and Burrels.
From Colby the line runs down close to the left bank of the Eden, under Beuley Castle ; thence,
through Bolton to the rivulet a little south of Walk Mill; afterwards nearly parallel to the rivulet,
and a little to the west of its left bank; thence, skirting the low lands, to a point about half mile
south of Cliburne. The remaining demarcation to the Eamont, is very obscure ; but it passes by
Clifton Dykes, and under Brougham Hall, into the alluvial flat of the river, and then enters Cum-
berland*.
For many miles, after it enters Cumberland, the line of demarcation is very ill defined. To
the east of the Petteril is a lofty ridge of new red sandstone hills, commencing with Penrith
Beacon. But on the road from Penrith to Hutton and Hesket Newmarket, we pass a very doubt-
ful country, which has always been coloured as new red sandstone. Some of the red sandstones in
that district (for example, at Catterlen, Hutton Park, &c.,) appeared to me, however, (when I ex-
SE ee: PP yy ST yet i tae SEE
* The area inclosed by the line above described is extremely covered with red gravel, formed,
in part, by the breaking up of the new red sandstone. Within the same area are also some places
where the new red sandstone has been washed off. Thus, near Warcop, there is in the bed of the
river an inclined micaceous red grit, probably belonging to the carboniferous series. Some very
remarkable red gritstones, associated with a magnesian limestone, are found on the hills west of
Soulby, and are clearly a part of the carboniferous system. I do not think the lower division of the
new red sandstone is found in this district; though I ought not to make the assertion with much
confidence, having never examined it since the year 1823.
362
A06 Prof. Sepewick on the New Red Sandstone Series in the
amined the district in 1823,) more to resemble the ferruginous coal grits, or the lower red sand-
stone; and I think it probable (after what has been stated above respecting Broadfield, supra,
pp- 391, 392,) that a spur of the older rocks, between the Petteril and the Caldew, encroaches con-
siderably on the line I am describing. I throw this out as a mere conjecture, confirmed, however,
by the fact, that inclined beds of a hard red gritstone are also found along the Petteril, at least as
far north as the Broadfield limestone.
Passing, then, this doubtful tract, we find characteristic beds of new red sandstone between
Macey Bank and Ivegill; and thence, south of Highhead Castle to the banks of Raw Beck, and
down both sides of that rivulet for more than a mile. Here, again, the demarcation is not only
obscure in many places from the want of good sections; but difficult also from the appearance of
lower grits, of a red colour (“lower red sandstone” ?), which break out in both the above-mentioned
rivulets.
No rock is visible for some way west of Raw Beck; but an imaginary boundary may be drawn
to the Caldew, a little south of Rose Bridge, and thence to Green Quarry, a little south of the Chalk
limestone above described (supra, p. 392). From that quarry the line sweeps round nearly by
toler)
able dislocated coal field of Rosley, now nearly deserted). From Tracing Tree it passes through
a wood, a little above the confluence of Silver Gill with the rivulet, and thence under Church Hill,
and on the north side of Islekirk to Parson Bridge ; from whence it may be traced near Cross Hill,
a little above Bridge Mill, and close to Low Blaithwaite ; from which place the line sweeps to the
south-west a quarter of a mile south of Elfield, and more than half a mile above Crook Dyke Mill;
Howrigg, Height, Brackenthwaite, Cragg Houses, and Tracing Tree (almost inclosing a remark-
and so after crossing the river in a direction about south-south-west, it turns west, ranging a little
north of the Leesrigg road, through the hill above King Gate, along the south side of Brayton Hall
Park, under the village of Aspatria, under Hayton, a little south of the road from Hayton to Al-
lerby, just under Crosby ; thence deflecting to the north-west, it passes north of Birkby, and down
by the right bank of the Ellen to the sea at Maryport.
We may pass over the coast from Maryport to St. Bees Head, as it is either occupied by the
>
coal measures, or by the “lower red sandstone,” in places already described. Across St. Bees
Head the range is defined by quarries, ending (as above stated) at Ben How*. On crossing the
valley, it reappears in Walton Wood, just above Linethwaite, and thence passes just under Bank
End, and at the base of an escarpment, from which it descends between Gill Foot and How Bank ;
and, inclosing Orgill, it disappears in the alluvial plain of Egremont.
Beyond this plain the line appears to range nearly east and west from New House to Grange ;
and from a quarry near the latter place it strikes about south-south-east into the valley of Kirk
Beck. It crosses above the mill, and then ranges above Head of Hail and Hall Garth to the
north end of Cold Fell near Side; from whence it descends into the valley of the Calder, in a di-
rection about south-south-east. It crosses below Thornholm, and then ranges east-south-east on
the way to Farmary, and is exposed in quarries at the hill-top. It then strikes across the Gill, and
is laid bare about a quarter of a mile above Hurrel Barrow; thence it ranges through Blaing Fell,
leaving Lockray and Whinray to the east, just touching Bank House, and forming the whole
escarpment of the hill above Gosforth.
We have no regular escarpment of the formation on the Cumberland coast south of Gosforth ;
but the rock is seen at the following places: Drig Cross, west of Gosforth; Brandreth Scar and
* The range of “ the lower red sandstone” over the coal field, as well as certain outliers of the
new red sandstone, will be given in a subsequent paper.
Basin of the Eden and north-western coasts of Cumberland, &c. AQT
Codlin Rock, two reefs to the south of Ravenglass, only seen at low water; on the Cross House
estate, half a mile north of Bootle; and, lastly, in wells and other excavations at Mopus, Hise
Moor, Well Bank, and Old Highton, all in the same neighbourhood, and on the north side of the
Bootle rivulet.
Crossing the estuary of the Duddon to the limestone of Roan Head, we find the superior rocks
concealed under blown sand ; but the new red sandstone breaks out south of Wet Flats, and may be
traced by Little Mill, Billing Coat, and Newton; and thence by Bousfield, Stank, and Hole Beck.
Beyond the last-mentioned place everything is buried under alluvial accumulations to the sea-side ;
but at low water the red sandstone is seen just to the north of Rampside. It appears also at the
north point of Old Barrow Island.
In the Cartmel promontory the new red conglomerates appear at Rougham Point, west of
Humphrey Head; and the red sandstone is said to have been reached by boring between Cannon
Winder and Ravend’s Winder, and close to Lower Hosker.
By help of the preceding notice, the demarcation of the new red sandstone may be laid down on
the large county maps with a near approach to accuracy. Had the Ordnance maps of the northern
counties been published, such details would have been perfectly useless, as the information would
have been more correctly conveyed by a superficial colour, than by any verbal description.
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VII.—On a portion of Dukhun, East Indies.
By Lizutenant-Cotoner W. H. SYKES, F.R.S. F.G.S. F.LS.
[Read January 23, 1833. ]
My personal observation of Dukhun (Deccan) and Konkun (Conean) *
is not confined to the boundaries laid down in the following geological
memoir ; but as the rock and mineral specimens remaining at present in my
possession are from Dukhun only, I have not thought it proper to extend
my details beyond the limits I here prescribe to myself, although I might
venture to do so from notes taken at different periods, without exposing my
accuracy to question. I will, however, in closing this paper, offer a few ob-
servations on the trap and other formations of India; the amazing extent of
the former not appearing to have been appreciated hitherto in European geo-
logical works. :
Boundaries.
My tract + is bounded on the west by the range of mountains usually deno-
minated by Europeans the “Ghats”, from a misinterpretation of the term
ghat, which simply means a pass, the proper name of this range being the
““Syhadree’”’; on the north by the Mool river, as far as Rahooreh; on the
east by a direct line from Rahooreh to the city of Ahmednuggur, and sub-
sequently on the north-east by the Seena river until its Junction with the
Beema river below Mundroop; on the south-east by a line from Mundroop
to the celebrated city of Beejapoor; on the south by a line from Beejapoor
to the town of Meeruj; and from this place the boundary in the south-west
is the Kristna and Quina rivers, to the hill fort of Wassota, situated in the
Ghats. The western boundary line extends, as the crow flies, about 144
miles; the northern 72 miles; eastern and north-eastern 159 miles; south-
eastern 41 miles; southern 80 miles ; and south-western 88 miles. Agree-
ably to observations made by myself and the officers of the revenue survey in
* With respect to the pronunciation of native words, the “u” is the w in “hut,” and the “a”
the a in “all.”
t+ See Map, Plate XXVI.
410 , Lieut.-Colonel Sykes on a Portion of Dukhun.
Dukhun, the tract lies between the parallels of north latitude 16° 45' and
19° 27', and east longitude 73° 30! and 75° 53’, and, roughly calculated, may
be said to comprise an area of about 26,000 square miles.
Stratification.
Previously to entering into descriptive details, I will state, in a few words,
that the whole of the country comprised within my boundaries is composed of
distinctly stratified trap rocks, without the intervention of the rocks of any
other formation. Whether at the level of the sea, or at the elevation of 4500
feet, in all and every part, beds of basalt and amygdaloid are found alternating,
whose superior and inferior planes preserve a striking parallelism to each other,
and, as far as the eye can judge, to the horizon. Barometrical measurements
and the course of rivers indicate a declination of the country to the east-south-
east and south-east. From the town of Goreh, latitude 19°03 and longitude
74°-05, on the Goreh river, following a mean course for the river until it falls
into the Beema, and subsequently, continuing a mean course for the Beema
until its junction with the Seena river, the distance is about 200 miles, and the
declination 671 feet : there may therefore be a trifling dip of the strata ; but
as a succession of low terraces occur in that distance, the apparent horizontal
position of the strata may be unaffected by the above difference of level.
Dr. MacCulloch, describing the overlying or trap rocks, says, “these
masses are generally irregular, but sometimes bear indistinct marks of strati-
fication *.””. As Dr. MacCulloch’s language implies the rare occurrence of
stratification, instead of its being a distinctive feature, at least of the Indian
branch of the trap family, I deem it necessary to quote the few authors who
have written on Indian geology, in confirmation of the fact I have stated +.
* Classification of Rocks, p. 466.
+ “These mountains (the Vindhya range), like every other in Malwa, appear to be distinctly
stratified, consisting of alternate, horizontal beds of basalt or trap and amygdaloid. Fourteen of
these beds may in general be reckoned, the thinnest at the top, and rapidly increasing in thickness
as they lower in position, the basalt stratum at the bottom being about 200 feet thick.” Again,
at page 327, he says: “In the upper plains of Malwa every point of view presents the same uni-—
form and distinctly streaked appearance noticed in the Vindhya range.”—Captain Dangerfield,
in Geological Notices of Malwa, in Appendix No. 2. to Sir John Malcolm’s Central India,
pp. 322, 327.
Dr. Voysey, in a paper on the Geological and Mineralogical Structure of the vicinity of Nag-
poor, says: “ From the summit of the hill of Sitabaldi the difference in the outline of the rocks
eastward is very perceptible. The flattened summits and long flat outline, with the numerous gaps
of the trap hills, are exchanged for the ridgy, peaked, sharp outline of the primary rocks.”—
Physical Class of the Asiatic Researches, p. 127.
In asecond paper in the same work, on some petrified shells in the Gawelghur range of trap
Lieut.-Colonel Sykes on a portion of Dukhun, All
Ghats.
The Dukhun rises, by a succession of terraces or steps, very abruptly from
the Konkun*. Its valleys and table-lands have a mean elevation above the sea
of about 1800 feet. The Konkun is a long strip of land from thirty to fifty miles
in breadth, lying between the Ghats and the sea; the mean elevation of this
strip is less than 100 feet ; but it is bristled with isolated hills, or short ranges,
some of which attain an elevation equalling that of the Ghats. Numerous
shoulders or salient angles are thrown out from the Ghats from the western or
Konkun side, and by means of these the ascent to Dukhun is effected ; with
what difficulty, will be understood when I state that the military road of commu-
nication between Bombay and Poona, up the Bore Ghat, rises nearly 600 feet
ina mile. The western portion of my tract along the crest of the Ghats is ex-
ceedingly strong : spurs of different lengths extend from the main range to the
eastward and south-east, leaving many narrow tortuous valleys between them,
some of which have the character of gigantic cracks or fissures ; other valleys,
although occurring less frequently, when looked at from the neighbouring
ranges, appear as flat and smooth as a billiard-table, even to the crest of the
Ghats, but when traversed are found to be cut up by numerous narrow and
deep ravinest. Stupendous scarps, fearful chasms, numerous waterfalls, dense
forests, and perennial verdure, complete the majesty and romantic interest of
the vicinity of the Ghats. As the spurs extend to the east and south-east they
diminish in height, until they disappear on approaching the open plains in
my eastern limits, between the Beema and Seena rivers. The area of the
table-land on their summit often exceeds that of the valley between them;
such is the case with the spur bordering the left bank of the Beema river for
forty miles from its source, occupying, in fact, the whole country between the
sources of the Beema and Goreh rivers. The spurs are rarely tabular for
their whole length, but narrow occasionally into ridges capped with compact
basalt, and subsequently expand into extensive table-lands. ‘The spur ori-
ginating in the hill fort of Hurreechundurghur affords a good example. The
fort is about eighteen miles in circumference: on the east it presents a salient
mountains, extending for 165 miles along the left bank of the Tapty river, from its source to the
city of Boorhanpoor, he describes the principal part of the range as formed of “ compact basalt
“ very much resembling that of the Giant’s Causeway. It is found columnar in many places, and
“ at Gawelghur it appears stratified ; the summits of several ravines presenting a continued stratum
** of many thousand yards in length.” —Physical Class of the Asiatic Researches, p. 189.
* See Plate XXVIII. + The valley of the Malsej Ghat, for instance.
VOL. 1V.—SECOND SERIES. 3H
A12 Lieut.-Colonel Sykes on a portion of Dukhun.
angle to the neighbouring mountain ; absolute contact, however, only com-
mences at about 400 feet from the top of the scarp, leaving a gap and an ex-
tremely narrow ridge, over which lies a difficult footpath of communication
between the valley of the Malsej Ghat and that of the Mool river. The spur
then widens ; some lateral ramifications shoot out, on one of which is situated
the fort of Koonjurghur ; at the Brahmun Wareh pass it narrows considera-
bly, but not into a ridge; it subsequently expands into the extensive and
well-peopled table-land of Kanoor and Parneir, twenty-four miles long by
twenty broad, having diminished in height, by a succession of steps, from
3894 feet in Hurreechundurghur to 2866 at Brahmun Wareh, 2474 at Par-
neir, and 2133 on the terrace of Ahmednuggur. From Ahmednuggur the
spur bends southward until it is finally lost in the neighbourhood of Sholapoor.
It is, in fact, the margin of a great plateau, which has a mean elevation of
about 300 feet above the valley of the Godavery river, and over which the
rivers Goreh, Beema, Seena, &c., take their course. The basaltic caps of
the ridges appear more or less columnar, from numerous vertical fissures ;
the weathering of these exposed rocks produces pillars, spires, towers, houses,
and other forms of works of art*. Another feature of these spurs is the occa-
sional occurrence on their table-lands of small hummocks or conical hills with
a truncated apex. Dr. Voysey{ mentions ‘‘ groups of flattened summits and
“ isolated conoidal frustra” in the Gawelghur trap mountains.
One of the longest of the spurs originates in the Ghats north-west of Sata-
rah, and runs nearly east-south-east, about 110 miles, towards Punderpoor.
The spur immediately south of Poona, on the ramifications of which are
situated the formidable fortresses of Singhur (4162 feet), Poorundhur (4472
feet), and Wuzeerghur, adjoining Poorhundhur (at nearly the same ele-
vation), has an extent of ninety-five miles. The accompanying section,
Plate XXVIII. fig. 2. represents this spur.
Valleys.
Much having been said respecting valleys of excavation, I think it may be
acceptable to offer a few observations on the valleys between the spurs. I
shall describe only those that present the greatest contrasts to each other.
Valley of the Mota River.—The valley of the Mota river, south of Poona, originating in a mass
of hills on the edge of the Ghats, is so exceedingly narrow, that for some miles the bases of the
opposite hills frequently touch each other, leaving, at intervals, little horizontal plots, of a pistol-
shot in width, ‘These plots occur in terraces, on lower levels as they extend eastward.
* See Plate XXVIII. fig. 1. and 2. on the Konkun; and Plate XXVII. fig. 1.
+ Physical Class, Asiatic Researches, p. 189.
Lieut.-Colonel Syxes on a portion of Dukhun. 413
Vale of the Sa le valley of the Under river, north-west of Poona, presents a perfect
contrast to the last. It is level for twenty miles, running east and west to the very edge of the
Ghats ; and a person can stand at the head of the valley upon the brink of a searp le almost
from the Konkun. Here, at the source of the river, it is nearly six miles wide. The river Under
runs down the valley 150 feet below the level of the cultivated lands.
Vale of the Baum.—The neighbouring valley of the Baum river, unlike that of the Under,
originates about seven miles from the crest of the Ghats, at a spot where the mountain masses
separate into two spurs. Hence it continues level for fourteen miles, gradually widening east-
ward. The Baum river, like the Under, runs at a level of 150 feet below the cultivated lands ;
these lands, in fact, being upon one terrace, the river upon a second and lower terrace.
Vale of the Beema.—The next valley on the north is that of the Beemariver. The river rises
on the elevated table-land above the Ghats, at 3090 feet, and within the first few miles it tumbles
over several terraces. The valley, for eighteen miles, is occasionally as narrow as that of the
Mota river.
Vale of the Goreh.—Next on the north occurs the valley of the Goreh river, which, from the
source of the river to Munchur, (twenty-nine miles,) is exceedingly narrow and tortuous. Here
it expands into the broad horizontal plain of Kowta, ten miles wide.
Vale of the Malsej Ghat.—In conclusion, as a contrast to the first part of the Goreh valley, I
must mention the valley of the Malsej Ghat, on the south of the Dukhun-base of the fort of Hur-
reechundurghur. It is several miles wide, and literally as level, even to the brink of the Ghats,
as if smoothed by art. Many of the valleys of the Ghats, particularly that of the Mool river, from
the continued scarped character of the marginal mountains, and the flatness of the bottom for miles
in extent, look like fosses to a Titan’s fortress.
If all these valleys be valleys of excavation, the present rivers could scarcely
produce such, were we to suppose their powers of attrition in operation from
the origin of things even to the end of time!
Those of a fissure-like character might have resulted from the upheaving of
the beds of trap from below the sea, and the consequent probable fracture of
the surface ; but the same explanation will not apply to those valleys associated
with the preceding, broad, flat, and margined by scarped mountains, which
valleys are as wide at their origin at the crest of the Ghats, and at the sources
of the rivers which run through them, as in any part of their length.
Terraces.
As the rise from the Konkun to the Dukhun is by terraces, so the declination
of the country eastward from the Ghats is by terraces; but these occur at
much longer intervals, are much lower, particularly in the eastern parts, and
escape the eye of the casual observer. In the neighbourhood of Munchur, on
the Goreh river, there are five terraces rising above each other from the east
to the west, so distinctly marked, that the parallelism of their planes, to each
other and to the horizon, gives them the appearance of being artificial. An
artificial character also pervades the form of many insulated hills: some of
which viewed laterally, appear to have an extensive tabie-land on the summit,
3H 2
414 Lieut.-Colonel Sykes on a portion of Dukhun.
but seen endways look like truncated cones. Conoidal frustra in the Gawel-
gurh range have been already noticed. Other insulated hills are triangular
in their superficial planes, as the forts of Teekoneh (three-cornered) and
Loghur.
Escarpments.
Stupendous escarpments are occasionally met with in the Ghats. In these
instances the numerous strata, instead of being arranged in steps, form a con-
tinuous wall. At the Ahopeh pass, at the source of the Goreh river, the wall
or scarp is fully 1500 feet high* ; indeed, on the north-west face of the hill
fort of Hurreechundurghur, the escarpment can scarcely be less than double
that height. On the other hand, the steps are sometimes effaced, and a hill
has a rapid slope. This criginates in a succession of beds of the softer amyg-
daloids, without any basaltic interstratification ; their superior angles disinte-
grate, and a slope results. But most usually three or four beds of amygdaloid
are found between two strata of compact basalt; the former disintegrates,
leaving a slope, which is not unfrequently covered with forest trees, forming a
picturesque belt: the basaltic scarp remains entire, or it may be partially
buried by the debris from the amygdaloids above; but its great thickness
usually preserves it from obliteration, and it rises from the wood below with
majestic effect, its black front being finely contrasted with the rich and lively
green of its sylvan associate. It is these strata, arranged in slopes and scarps
repeated three or four times, and so commonly met with in insulated and other
mountains in Dukhun, that constitute the amazing strength of the hill forts of
the country, leaving a succession of natural walls encircling a mountain. This
feature did not escape the observation of Captain Dangerfield in Malwa, who
says, “From the great difference in the resistance made to decomposition by
“these trap and amygdaloid beds, their exposed ends acquire a very distinct
“ degree of inclination and character ; the amygdaloid forming a great slope,
“and affording a loose mould covered with vegetation, the trap retaining its
“ original perpendicularity and dark bareness f.”’
In the alternation of the strata there does not appear to be any uniformity ;
but the general level, thickness, and extent of a stratum are preserved, as in
sedimentary rocks, on both sides of a valley ; the basalt and hardest amyg-
daloids being traceable for miles in the parallel spurs or ranges; but the im-
bedded minerals, and even the texture, vary in very short distances.
Columnar Basalt.
A great geological feature of Dukhun is the occurrence of columnar basalt.
* Plate XXVIII. fig. 1. ¢ Malcolm’s Central India, Appendix, p. 322.
Lieut.-Colonel Sykes on a portion of Dukhun. Ald
The basalts and hardest amygdaloids run so much into each other that the
line of separation is not always readily distinguishable, excepting of course
the lines of horizontal stratification. I observed the prismatic disposition more
marked and perfect in the basalt strata than in the amygdaloids, and the more
or less perfect development of determinate forms was dependent on the com-
pactness and limited constituents of the rocks. Basalts and amygdaloids, how-
ever compact, with many imbedded matters, rarely formed columns. Perfect
columns were generally small, of four, five, or six sides; but the prismatic
structure sometimes manifested itself in basaltic and amygdaloidal columns
many feet in diameter. A bare mention of the places where they occur will
testify to their extended localities.
On the low table-land of Kurdah, near Serroor, between sixty and seventy miles east from the
Ghats, columnar basalt occupies an area of many square miles. Small columns are seen in most
of the slopes of the very narrow sinuous valleys of the flanks of the platform, and frequently the tops
or terminal planes of columns are observed on the table-land forming a pavement. The perfect
columns in the flanks are generally small, four, five, or six-sided, and rest on a stratum of basalt
or amygdaloid. In some spots the columns are articulated, in others not. In amass of columns in
the face of the table-land towards Serroor the columns are of different lengths, but spring from the
same level. More articulations having been washed from the outer columns than from the inner by
monsoon torrents dashing over them, a pretty flight of steps remains. The columns of this table-
land are for the most part erect, but sometimes stand at various angles to the horizon, usually at
45°, In one instance, near the village of Kurdah, they lean from the east and west, towards a
central upright mass: these are about fourteen feet in length, and are not articulated. In a mass
of columns facing the west, and two miles south of the cavalry lines at Serroor, some are bent and
not articulated ; they are nevertheless associated with straight columns, which are articulated. At
Karkullah, thirty miles north-west of Poona, between Tellegaon and Loghur, a hill has been
scarped for the great military road. Very numerous small columns occur in the escarpment, and
they lie piled upon each other in a horizontal position ; the only instance of the kind within my
knowledge in Dukhun. Two or three hundred yards west of the village of Yewtee Purgunnah
Kurdeh, in the rocky banks ofa rivulet, imperfect columns are seen. On the right bank they are
so marked, as to have excited the attention of the natives (an unusual event) ; and they are daubed
with red lead, in the manner of Hindoo deities, and venerated.
At Kothool, twenty-two miles south of Ahmednuggur, there is a thick stratum of close-grained
gray homogeneous basalt in the face of the hill on which is seated the temple of Kundobah. Ver-
tical and horizontal fissures are seen in the lateral plane or exposed edge of this stratum, but
they are so far from each other as to leave huge blocks between them, giving the appearance of the
superstratum of the hill being supported by massive articulated pilasters. Parts of the exposed
edge are detached from its mass, leaving rude columns four or five feet in diameter, eight or ten
high, and composed of three or four weighty stones disposed to assume geometrical forms. In the
water courses near Kurroos Turruf Ranjungaon, columns are observable. The basalt is bluish
gray, compact, has a vitreous hue, and sharp fracture. The columns occur very abundantly in
the slope of the hills, on either side of a very narrow valley running westward from the village
of Ankoolner, Ahmednuggur Collectorate. They are five- or six-sided, articulated, and from a
foot to two feet and a half in diameter, and of various lengths; the lateral planes perfect, but in
416 Lieut.-Colonel Sykes on a portion of Dukhun.
some instances the sharpness of the angles has been affected by weathering. The texture is
close-grained, colour almost black, and they affect the needle.
At Jehoor, near the source of the Seena river, in an insulated hill, an obscure columnar disposi-
tion is met with in a rock, in which in other places I had not seen the slightest trace of it. A
stratum of red, cellular, amygdaloid fifteen feet thick has subcolumns in its exposed edges eight or
ten feet indiameter. In the banks of a water-course running into the Hunga river, half a mile east
of Parneir, on the elevated table-land between the cities of Ahmednuggur and Joonur, basaltic co-
lumns are very numerous ; they are five or six feet high, not articulated, and are not quite perpen-
dicular. This formation is evidently extensive, as the ends of columns, chiefly pentangular, appear
in the bed of the water-course for some distance, forming a pavement of geometrical slabs. The
ends of columns of different lengths also appear in the southern bank at intervals, forming flights
of steps. The basalt of which these columns are composed is very close-grained, almost black,
with shining specks of a metallic lustre. The rocky banks of the Kokree river at Jambut, in
the plain of Joonur, exhibit a strong inclination to a large columnar structure. In the hill fort of
Singhur, at an elevation of 4162 feet, at the western end of the fort, there is a sheet of rock which
has the appearance of a pavement of pentangular slabs. The slabs are no doubt the terminal
planes of basaltic columns. The same is observed in the hill fort of Hurreechundurghur, about
seventy miles north of Singhur; also in the bed of a water-course one mile north-east of Bar-
lonee, near the fortress of Purrunda, 112 miles east-south-east of Singhur ; and, lastly, in the bed
of the Mool river at Gorgaon, Poona Collectorate. These pavements extend to Malwa, as Captain
Dangerfield mentions their occurrence in the beds
2 lia dudigdieg ta of the Chumbul and Nerbuddah (Nermada) ri-
i TT if vers*. The other localities of basaltic columns, or
are a marked disposition to this structure, were in a
well at Kumlepoor, between the fortress of Pur-
rundaand Barlonee, near the left bank of the Seena
river ; at Kheir Turruf Rasseen, in the face of a
headland, abutting on the Beema river, on which
the town stands; in the ascent to the temple of
Boleshwur Turruf Sandus, Poona Collectorate ;
and, finally, in the scarps of a mountain running
down into the Konkun, and seen from the Naneh
Ghat, about three miles distant. Here the Giant’s
Causeway in Ireland is brought to mind; but the
scale of the mountain is infinitely more magnifi-
cent, being fully 4000 feet high. There is a dou-
ble row of columns ; but from their inaccessible
situation, I could only examine them through my
telescope, and cannot testify, therefore, to their
perfect development; but the accompanyingsketch
will give a just idea of their appearance to me,
Captain Dangerfield only once speaks of columns. They lie about a mile from the Ner-
buddah (Nermada), between Mundleysir and Mhysir, at 696 feet above the sea: they are either
* Malcolm’s Central India, Appendix, pp. 329, 330.
Lieut.-Colonel Syxts on a portion of Dukhun. Al7
vertical or highly inclined. General Hardwick has published a lithographic sketch of them*. I
have already stated that Dr. Voysey found columnar basalt in many places in the Gawelghur
range.
Schistose Structure.
Following the preceding formation, I may mention, that in some few places
a schistose structure was met with ; but its extent was limited to a few yards,
the lamelle were vertical, from an inch to three inches in thickness, being
perfect tables, with parallel bounding planes. The rock in which this struc-
ture occurs, is a simple, indurated, gray clay, which flies into fragments under
slight blows from the hammer. At Dytneh near Serroor some very perfect
specimens have led the inhabitants to connect mystic influences with so arti-
ficial a development of inorganic matter. The spot is daubed with oil and
red lead, and venerated.
Basalt en boules.
Another characteristic feature is the general diffusion of those rounded or
oval masses of compact basalt, with concentric layers like the coats of an
onion, which the French geologists denominate ‘ Basalt en boules’”’, and
ourselves, nodular basalt. :
These concretions are usually found at the base of hills, buried in the debris from the decom-
posing strata; but in the Konkun, between Choke and Campolee, (the latter at the foot of the
Bore Ghat,) two villages on the high road between Bombay and Poona, I met with them lying on
the surface over a considerable area. They occur in a similar manner on the table-land of the
ball-practice hill at Poona. At Koothool (already mentioned), in the slope of the hill, and in the
debris at its base, and along the edge of the table-land near Paubul, they are abundant ; but the
finest specimens are seen near the village of Karkullah, thirty miles north-west of Poona, associated
with horizontal basaltic columns. The hill has been cut away, to form the great military road.
In making the escarpment the balls were met with, and it being impossible to cut through the
nuclei in vertical sections, it was either necessary to leave them projecting or to remove them
altogether: in the latter case cavities remained equal to the hemispheres of the nuclei; and the
vertical sections display from ten to fifteen concentric layers of friable gray stone, which in some
instances I have found to affect the needle. I compared specimens of the nuclei; with a mass
brought by me from the Solfatara at Naples, and found them quite similar in aspect, colour.
hardness, and great weight. This formation excited the attention of those gentlemen who have
visited the northern and eastern parts of the great trap regiont; but Dr. Voysey was quite mis-
* Malcolm’s Central India, Appendix, p. 323.
+ Dr. Voysey says, ‘The nodular wacken or basalt is one of the most common forms of trap
** in the extensive districts composed of the rocks of the family south of the Nermada (Nerbuddah)
“river. It occurs perpetually in the extensive and lofty range of mountains, (the Gawalghur)
“ situated between the Purna and Tapti rivers, and appears to form their principal mass. It is
“ found equally abundant throughout the whole of Berar, part of the provinces of Hyderabad, Beder
“ and Sholapoor, and appears to form the basis of the great western range of trap hills which separate
“ the Konkun from the interior of the Dukhun.”—Physical Class, Asiatic Researches, pp. 126, 189.
418 Lieut.-Colonel Sykes on a portion of Dukhun.
taken in supposing it formed the basis of the Western Ghats. Captain Coulthard speaks of it
in Sagar*, Major Franklin also noticed it in the trap of Sagar, in lat. 23° 51’, and long. 78° 44’,
at 1933 feet above the sea, as “ frequently globular ; the nuclei of the decaying masses, varying in
“ size from an egg toa large bombshell, and their decomposing concentric lamellze being generally
“ very thin, and often very numerous” f.
Dykes.
I now pass to the basaltic dykes, several of which came under my notice
in different parts of the country. They are all vertical, and I did not observe
that they occasioned any disturbance or dislocation in the strata of basalt and
amygdaloid, through which they passed.
Two dykes run obliquely across the valley of Karleh, (35 miles north-west of Poona), and
intersect each other: they are about four feet thick and cut amygdaloidal strata. A prismatic
disposition is generally observable in the fracture, and from one of them I obtained a square
prism, which lay at right angles to the walls of the dyke. The texture is compact, The military
road running through this valley and down the Bore Ghat to Panwell, is frequently crossed by
ridges which I presume to be the outcrops of dykes. A dyke is seen on the southern slope of
an insulated hill, near the villages of Bosree and Digghee, 74 miles north of Poona}. It is
about four feet thick, has a transverse prismatic fracture, is compact, and runs from the bottom
to the top of the hill; but it is not discoverable in the northern slope. It is visible from the can-
tonments at Poona. A similar dyke occurs in the hill at Ombreh, twenty miles north-north-
west of Poona. But the most remarkable dyke runs vertically, from east to west, through the
hill fort of Hurreechundurghur. It is first seen, of a thickness of six or seven feet, in the ascent
of the mountain on the south-east from Keereshwur, about 400 feet below the crest of the scarp.
The path of ascent into the fort is intersected by it, and its prismatic fracture, at right angles to its
planes, offers a few available steps in the ascent. It is traceable for about 300 feet in perpen-
dicular height. On the top of the mountain, within the fort, about a mile to the westward, it is
discoverable at intervals, cutting through basaltic and amygdaloidal strata. J could not ascertain
whether or not it appears in the western scarp of the mountain, the point to which it directs its
course being wholly inaccessible.
The gentlemen whose geological memoirs I have quoted, rarely advert to the
subject of trap dykes, and their notices are very brief. Capt. Dangerfield says,
«'The trap of the southern boundary of Malwa is much intersected by verti-
“ cal veins of quartz, or narrow seams of a more compact heavy basalt, which
‘ appears to radiate from centres§.”’ Beyond the continuous trap region of the
peninsula, Dr. Voysey notices a basaltic vein in sienite, near the Cavary river
* « The base of the hills is invariably broader than the summit; and if the sides of a hill are
‘“‘ smooth and even, balled trap, often a concentric lamellar variety will be the principal component
“‘ matter, decomposing and decomposed into a predominating workable clay, still showing the
‘« narallel converging layers.” —Physical Class, Asiatic Researches, p. 78.
+ Physical Class, Asiatic Researches, p. 30. } See Plate XXVIII. fig. 1.
§ Malcolm’s Central India, Appendix, p. 330,
Lieut.-Colonel Sykes on a portion of Dukhun. AI9
at Seringapatam, which must have been propelled upwards, as it broke
through an oblique seam of hornblende in the sienite, and carried the pieces
up above the level of the hornblende vein*. “On the eastern coast,” Mr,
Calder says, “from Condapilli northward, the granite is often penetrated
“and apparently heaved up by injected veins or masses of trap, and dykes of
“ greenstone ft.”
Ferruginous Clay.
The next distinctive feature is the occurrence of strata of red ochreous
rock, in fact, Mac Culloch’s ferruginous clay underlying thick strata of basalt
or amygdaloid, precisely as is seen to be the case in the Giant’s Causeway in
Ireland. It passes through every variety of texture, from pulverulent, friable,
and indurated, to compact earthy jasper. The stratum is from an inch in
thickness to many feet. The rock makes a red streak on paper, with the
exception of the very indurated kinds, and does not affect the needle. It is
pulverulent near the basaltic columns at Serroor, friable under sub-columnar
red amygdaloid, near the source of the Seena river, indurated under basalt
at Kothool. Although hard, it is here so cellular as to have the appearance
of sponge, and reduced to powder, looks like brickdust.
In the scarps of the hill fort of Hurreechundurghur and a mountain near Joonur in which are
excavated numerous Boodh cave temples, it is found compact and homogeneous, and is, in fact,
an earthy jasper. In these localities it lies under from 300 to 600 feet of basalt. In the former
locality it is about three feet thick, in the latter one foot. At Nandoor, north-north-west of
Ahmednuggur, in the valley of the Godavery river, it is found as a porphyritic stratum many
feet in thickness, and is used as a building stone. The imbedded matter consists of very minute
crystals of lime. At Wangee, lying nearly in the latitude of Barlonee, but differing 18 miles in
longitude, and at Barlonee it occurs as an earth: as both places lie on the same level, I have no
doubt the stratum is continuous between them. It occurs abundantly in the Ghats, frequently
discolouring the rivulets, and giving a ferruginous character to the soil over a considerable area.
When thin, and under heavy beds of basalt or amygdaloid, the exposed edge of the stratum
projects, is rounded, and double the thickness of the stratum itself; as if it had once been in a
tenacious fluid state, and squeezed out by the superincumbent basalt. Such is the case at
Jehoor, and an illustrative specimen accompanies this paper.
Pulverulent Limestone.
Limestone is met with, in the Dukhun, only in three states: pulverulent,
nodular, and crystalline. The first occurs in thin seams on the banks of rivers
and water-courses and at the base of hills in debris. The seams are from an
* Physical Class, Asiatic Researches, part i. p. 22,
¢ Ibid., part i. p. 10.
VOL. IV.— SECOND SERIES, 31
420 Lieut.-Colonel Sykes on a portion of Dukhun.
inch to three feet in thickness, covered by a few feet of black earth. Some-
times in whiteness it resembles pounded chalk, and is then used by children
to smear their writing boards.
In this state it ocecurs at Jehoor and Islampoor near Ahmednuggur. At Kurkumb and at
Salseh, ten miles south of the fortress of Kurmaleh, it is met with under black earth in unusually
thick strata, and of a peculiar whiteness. Major Franklin notices “ a stratum of earthy limestone,
white as chalk, at Sagar, occurring under a stratum of amorphous trap *.”
Nodular Limestone.
The nodular limestone, which is the well-known kunkur f of India, (kunkur
being a native word for nodule,) occurs, like the preceding, disseminated or
diffused in the soil, and also on the surface. I have never seen the nodules
of a regular crystalline form. They vary in size from a marble to a twelve-
pound shot, and many of them are exceedingly irregular in shape, particularly
those dug from the banks of rivers. ‘They are sometimes obscurely lenticular.
They are so abundant in certain localities that they appear as if showered
upon the earth, and disguise its colour. Dr. Buchanan mentions the same
in Rajmahl. When upon black soil, they are usually minute and tolerably
uniform in size: on other soils their form is variable. In the Ghats neither
pulverulent nor nodular lime is met with. It is unnecessary to particularize
the localities of the nodular kind, as it is of common occurrence eastward
from the hilly tracts of the Ghats, and is the only source of lime for mortar, a
class of persons making a livelihood by collecting the larger nodules. When
carefully burnt, they make an excellent cement. Captain Dangerfield de-
scribes ‘ the occurrence (in Malwa) in some parts, particularly near the bottom
of the small hills and banks of the rivulets, of a thin bed of loose marl or coarse
earthy limestonet”’.
Captain Coulthard says, ‘“‘ In Sagar a white patch of this limestone moulder-
“‘ ing by the weather is the source from whence comes the particles of kunkur,
«mixed with the black basaltic earth of the neighbouring valley, in such pro-
“ portion as to add increased fertility to it; and if a rivulet meanders through
“ that valley (and such is generally the fact), patches made up of aggregated
“ particles of the same, will here and there be found ; and this it is which the
“« native families pick out and work into lime §”. Captain Coulthard refers the
origin of the nodules to limestone rock underlying basaltic strata, but I
* Physical Class, Asiatic Researches, parti. p. 30.
+ The Mahratta word is not spelt with an “a.”
+ Malcolm’s Central India, p. 328.
§ “Trap of the Sagar District,” Physical Class, Asiatic Researches, p. 60,
Lieut.-Colonel Sykes on a portion of Dukhun. AQ]
cannot trace them to such a source, not having seen strata of compact lime-
stone, properly so called, in the Dukhun. The only specimen of compact
limestone met with by me was in the bed of the Beema river near Pundur-
poor. It was an insulated, amorphous, gray mass, four or five feet in dia-
meter. I looked upon it as an aggregation of the pulverulent particles of
the lime disseminated in the neighbouring banks. A specimen of it ac-
companies this paper.
Crystalline Limestone.
Lime in a crystalline state occurs only as an imbedded mineral in the
amygdaloidal strata, in quartz geodes, and in the nucleus or compact part
of masses of mesotype or stilbite. It is rare compared with the preceding
varieties.
Loose Stones.
Another feature of Dukhun is the occurrence of immense quantities
of loose basalt stones, as if showered upon the land; also masses of rock
heaped and piled into mounds as if by the labour of man. Their partial
distribution is not less remarkable than their abundance. For the most part,
the stones have a disposition to a geometrical form, and it is by no means
rare to meet with prisms of three or four sides and cubes almost perfect:
stones with one or two perfect planes are very common. Their texture is
close-grained and the colour verging to black.
At Dehwuree, Hungawaree, Behloondee, Kothool, and Dytneh in the Ahmednuggur Collectorate,
they are very abundant. At the last place they cover fields several acres in extent, so thickly
that the black fertile soil on which they rest is not discoverable: they vary from an ounce to
several pounds in weight. Amongst these I picked up a perfect square prism. In neighbouring
fields, most unaccountably, there is not a stone to be seen: patches of sheet rock occur in their
vicinity. Other localities are the top of the Neem Durra Ghat near Ahmednuggur; the junction
of the Beema and Seena rivers below Mundroop; right bank of the Seena at Kurmaleh; between
Kurjut and Meerujgaon; and generally it may be stated that the precipitous slopes of the low
table-lands of the Desh (open or flat country) are very strong and rocky. For ten miles between
Jeetee and Soagaon, Ahmednuggur Collectorate, the fields, and even the road, are so thickly
strewn with large basalt stones as to render cultivation difficult and travelling penible.
Rocky Heaps.
The singular heaps of rocks and stones above noticed occur at Kanoor,
Patus, Kheir, between Kurjut and Meerujgaon, and at other places in the
Desh, but not in the Mawals, or hilly tracts of the Ghats. The heaps are
from twenty to seventy feet in diameter, and the same in height: when com-
posed of rocky masses without small stones, blocks of three or four feet in dia-
312
422 Lieut.-Colonel Sykes on a portion of Dukhun.
meter and with a disposition to determinate forms, are piled upon each other,
constituting rude pillars. In certain parts of the country from fifty to sixty of
these heaps are seen within the area of a couple of square miles, and it ex-
cites surprise that the intermediate ground is destitute of stones.
Sheets of Rock.
Mention must not be omitted of the constant recurrence of sheets of rock
of considerable extent at the surface, and totally destitute of soil: this is par-
ticularly the case in the Mawals, or hilly tracts along the Ghats, They
abound with narrow vertical veins of quartz and chalcedony. When of suffi-
cient thickness, the vein splits in the centre parallel to the surface of its
walls, the interior being drusy with quartz crystals: the walls consist of
layers of chalcedony, cachalong, hornstone, and semi-opal. These veins
supply the majority of the siliceous minerals so abundantly strewed over
Dukhun.
The localities where the sheets of rocks particularly struck me were Lakungaon, on the plain of
Joonur, and generally in the valley of the Goreh river; at Kothool, Pergunneh Kurdeh; at
Kheir and Raseen; in the hill fort of Hurreechundurghur ; most markedly between Kooldurrun
and Pairgaon on the Beema river. At Aklapoor, on the Mool river, they were very extensive ;
and at Angur, Mohol, Kurjut, and Patkool. Generally in the eastern and south-eastern parts of
my tract, much decomposing amygdaloid is found at the surface of the low table-lands or terraces,
which, in favourable monsoons, is equal to the support of Jowaree*; but a small deficiency in the
rains occasions the destruction of the crop.
Structure and Mineral Composition of the Trap Rocks.
The structure and mineral composition of the trap rocks in Dukhun vary
exceedingly in short distances, even in the same stratum ; nevertheless, the
predominant character does not disappear, although the basalt in a con-
tinuous bed may pass several times from close-grained, compact, and almost
black, to gray, amygdaloidal, and externally decomposing. The same ob-
servation applies to the amygdaloids. A variety of compact basalt, of an
intense green colour, is susceptible of a brilliant polish, and rivals the cele-
brated Egyptian kind. It is of great weight and remarkable hardness: the
natives use it to work into idols for their temples, pedestals to the wooden
columns in their mansions, and slabs for inscriptions. The bulls of the size
of life, always placed before the temples of Mahadeo, are cut out of this
variety at Raseen, Wurwund, and the renowned Boleshwur. Some of the
pedestals in the gateway of the Mankeswur palace at Teimboornee look like
* Andropogon Sorghum.
—
Lieut.-Colonel Syxes on a portion of Dukhun. 423
mirrors. In the temple at Pooluj south of Punderpoor, there is a slab six or
seven feet long and 23 broad, covered with an inscription in the Kanree
language ; and in Punderpoor the streets are paved apparently with the
same basalt. At Jehoor and near Ahmednuggur is found a compact kind
like the last, but not so heavy. It has a crystalline character and sharp frac-
ture, and has angular siliceous pebbles imbedded : an occasional pebble is
loose in its cell. In the Happy Valley near Ahmednuggur the basalt is com-
pact and smooth, with reddish flat transparent crystals imbedded. It opposes
a feeble resistance to the hammer, and flies into fragments, some of which
have right angles. The basalt, even of the true columns, is not of a uniform
texture in different localities : at times it is blackish or gray, and very small,
granular or compact ; at others, earthy and ferruginous, particularly exter-
nally. The basis of the amygdaloids is clay, with more or less hornblende
disseminated : they embrace the cellular, porphyritic, hard, friable, and de-
composing. I endeavoured to class them“agreeably to the prevalence of
quartz, chalcedony, lime, mesotype, or stilbite, as imbedded minerals, but
found the method of very limited application. Sometimes one mineral only
is imbedded, occasionally two, and often the whole.
In Hurreechundurghur quartz amygdaloid prevails: at Aklapoor on the
Mool river it is characterized by mesotype, that mineral being imbedded in
large masses, and the radii (six or seven inches) are the longest I have seen.
At Nandoor it is porphyritic with minute crystalline specks of lime: near
Ahmednuggur is seen a cellular, indeed spongiform kind, which is hard, and
the cells are empty. A small cellular and pisiform variety is found in the
wonderful cave temples of Ellora, and some of the sculptured figures appear
as if marked by the smallpox. This observation is partially applicable to
the Boodh and Hindoo cave temples of Elephanta, Salsette, Karleh, Joonur,
the Naneh Ghat, and the Adjunteh Ghat; all of which are excavated in
basaltic or amygdaloidal strata. The stilbite or Heulandite amygdaloid is of
very common occurrence ; but the most prevalent kind is that in which all
the minerals noticed above are associated. The stone usually selected for
building is of various shades of gray or bluish gray ; has hornblende dis-
seminated in very small crystals; works much easier than some of the com-
pacter basalts, but takes a good polish. The entire temples of Koorul and
Boleshwur, with their innumerable alto-relievo figures and laboured orna-
ments, are built of this variety of trap, which is, in fact, a greenstone,
although less crystalline than the European rock. There is a variety selected
carelessly, also used in building, which has the structure and nearly the
external characters of the last, but which, in weathering, exfoliates, and the
424 Lieut.-Colonel SyxEs on a portion of Dukhun.
buildings fall to ruin; such is the case with the great temple in Hurree-
chundurghur.
I must not omit mention of two remarkable rocks which, as far as my
reading extends, have not been noticed by authors on European geology.
The first is an amygdaloid in which compact stilbite is imbedded in a ver-
micular form. One of its localities is the insulated hill on which stands the
temple of Parwuttee in the city of Poona* ; and it is met with in many other
places. Captain Dangerfield observed the same peculiar stratum near
Sagar. He says, “There occurs an amygdaloidal or porphyritic rock con-
* sisting of a compact basis of wacké, in which are imbedded in great abun-
“dance small globular or uniform masses, but more usually long curved cy-
“ lindrical or vermiform crystals of zeolite +.”
The other rock occurs as a thick stratum of amygdaloid at the elevation of
A000 feet, in the hill forts of Hurreechundurghur and Poorundhur; and in
the bed of the Goreh river at #800 feet, near Serroor. The matrix resem-
bles that of the other amygdaloids, but the mineral imbedded is a glassy
felspar in tables resembling Cleavelandite, crossing each other at various
angles, and so abundant as to occupy a moiety of the mass. I have only
remarked it in the above localities, and it does not appear to have come
under the notice of the gentlemen I have so often quoted in other parts
of the peninsula.
Minerals.
Minerals are not uniformly dispersed in Dukhun. In one part quartz pre-
dominates, in another chalcedony ; and these are more or less associated with
jaspers, agates, hornstones, heliotrope, and semi-opal or cachalong. In other
places particular members of the zeolite family prevail, nearly to the exclusion
of the siliceous class ; and elsewhere there is a diminution of minerals amount-
ing almost to privation. Amethyst quariz is rare in Dukhun ; when met with
it constitutes the crystal, lining the interior of geodes of agate. I have not
seen it in veins. Pseudomorphous quartz is common; the most frequent
impression is that of rhomb spar. Lime occurs only in three crystalline
forms : rhomb, dog-tooth, and the dodecahedron. ‘The first is found on the
surface, and imbedded in masses of quartz and compact mesotype; the two
latter forms are associated with ichthyophthalmite in cavities in the amygdaloid
strata tf.
* See Plate XXVIII. fig. 2., near to the city of Poona.
+ Central India, p. 328.
{ That comparatively rare European mineral, ichthyophthalmite, is most abundant and of great
beauty in the neighbourhood of Poona.
Lieut.-Colonel Syxrs on a portion of Dukhun. A25
The following are a few of the mineral localities :
At Kothool, south of Ahmednuggur, the numerous quartz and chalcedony veins cover the
country with agates, colourless quartz-crystals, and chalcedony; some of the specimens are fully
a foot thick, including both walls of the vein. Here are met with some few crystals of calca-
reous spar inclosed in quartz. At Ahmednuggur, to the above siliceous minerals, some members
of the zeolite family are to be added, principally stilbite. At Nandoor, on the plain of the Goda-
very river, the zeolites disappear, and the siliceous minerals are limited in number. On the con-
trary, at Jamgaon, eighteen miles west of Ahmednuggur, on the upper terrace or plateau, in ad-
dition to all the minerals enumerated, bits of yellow and red jasper and heliotrope occur. As-
cending the Mool river from Nandoor, at Aklapoor, great masses of mesotype, with radii several
inches long, are found imbedded in friable amygdaloid. North of Aklapoor, at Gorgaon, a new
mineral occurs in a mass two feet in diameter. Its depth I do not know, as it lay partly buried in
the amygdaloid bed of the river: its colour green, and breaking into rhombs. Gorgaon is the
only locality known to me of this mineral. Its measurements are those of calcareous spar, but the
specific gravity is less. It is stated to be coloured by green earth. It is interesting from being
unknown in the cabinets in England.
A few miles further up the Mool river, at the village of Chas, in the shoulder of a hill formed
of numerous thin horizontal beds of decomposing amygdaloid, many specimens of cloudy calca-
reous spar, imbedded in stilbite, are found, and the siliceous minerals are rare. Ascending to the
source of the river the same scarcity prevails. Three miles south-south-west of Chas, at Brah-
munwareh, great masses of stilbite, of the radiating foliate kind, are imbedded in hard amygdaloid.
In the hill fort of Hurreechundurghur, although siliceous minerals are not abundant, crystallized
quartz of various colours is seen, a feature not characterizing the Desh or open country. South
of Ahmednuggur, as far as Soagaon on the Beema river, and Meerujgaon on the Seena river, the
Ahmednuggur minerals prevail; hence descending the Beema to its junction with the Seena, a
gradual diminution takes place, and at the junction they almost disappear; returning north, at
Ashtee, between Kurkumb and Mohol, a few are met with. At Oondurgaon, and up both banks
of the Seena river to Purrunda, numerous and very fine specimens of milk opal, with a flame-
coloured tinge in transmitted light, are found on the surface; and this is the only locality where I
met with opal as a distinct mineral; and here the members of the zeolite family are very rare. At
Tudwull, between Oondurgaon and Barlonee occur the only specimens of black calcareous spar
seen by me in Dukhun; it is associated with transparent calcareous spar. In excavating wells in
the cantonments at Poona, splendid specimens of ichthyophthalmite were brought to light; and
generally in the bed of the river Mota-Mola and the neighbourhood, fine specimens of heliotrope
and coloured quartz occur. The other minerals are nadelstein, analcime, chabasite, and laumo-
nite. Captain Dangerfield’s details prove that the minerals of Malwa are identical with those of
Dukhun.
Natural Salts.
Only two kinds of natural salt came under my notice, namely, muriate and
carbonate of soda.
With respect to the former, many of the wells at Ahmednuggur are brackish; and there is a
rivulet running into the Seena river about two miles north-west of the city, which has its source a
few miles distant, called the Salt Brook. It passes over a saliferous soil; and in its dry bed, or
426 Lieut.-Colonel Syxes on a portion of Dukhun.
on insulated stones standing in its stream, are incrustations of common salt intimately mixed with
carbonate of lime. No use is made of this salt. The saline impregnation of the soil extends to
some distance west and north-west of Ahmednuggur, as I found a handsome well at Kurjooneh,
eight miles distant, filled with water so brackish as not to be available for domestic use. At Wur-
gaon, between Kurjut and Pairgaon, a peculiar hoary appearance of a patch of ground in the midst
of withered grass, led me to examine it. The whiteness was occasioned by lime in minute particles,
mixed with a little muriate of soda.
The third locality of common salt was in the bed of a rivulet at Koond Mawlee, near the falls
on the Kookree river, between Serroor and Kowta. A little common salt, with a trace of carbo-
nate of soda, appeared, incrusting the rocky bed for a few feet near the water line. I did not
observe common salt elsewhere. My attention was first directed to carbonate of soda at Serroor, by
observing washermen digging for earth in the banks of a rivulet ; learning that they used it to wash
their clothes, I obtained a quantity; lixiviated the earth, boiled down the lixivium, and on cooling
obtained a large crop of crystals, which the usual tests indicated to be carbonate of soda. I only
met with one other bed, although I have no doubt they are numerous. At Kalbar Lonee, twelve
miles east of Poona and two miles south of the Mota-Mola river, within an area of 200 yards, a
constant moisture and partial absence of vegetation is observed. An efflorescent matter appears
on the surface every morning, which is carefully swept up and sold to washermen; it is carbonate
of soda. The occurrence of salts in the trap formation did not escape Captain Dangerfield’s notice.
He states that ‘“ the banks of the Nerbuddeh (Nermada) near Mundleysir, consist of an upper thin
bed of vegetable mould; a central bed, chiefly of indurated marle, strongly impregnated with mu-
riate of soda; and a lower bed, of a reddish hue, with much carbonate of soda, In the dry season
these salts form a thick efflorescence on the surface of the bank*.” Saltpetre is manufactured in
Dukhun, not from nitrated soils, but from the scrapings of old walls. I have also seen specimens
of muriate of ammonia obtained by the brick and tile makers in burning dung, stable and other
refuse matters in their kilns,
Ores.
No other ore than that of iron is found in Dukhun. It is only worked, to
my knowledge, at Mahabuleshwur, at the source of the Krishna river. It
occurs as a nodular hematite, associated, I understand (for I have not been at
the spot myself), with laterite. This ore produces the celebrated Wootz steel.
Organic Remains.
I did not meet with organic remains of any kind whatever. Captain Coult-
hardf in Sagar, Major Franklin in Bundelkand, and Captain Dangerfield in
Malwa, were equally unsuccessful. Dr. Voysey, indeed, mentions a bed of
freshwater shells in a stratum of indurated clay near the Tapty river in the
Gawelghur hills ; also at Medconta, 2000 feet above the sea, on trap; but
these may have been recent, as he does not say to the contrary+. Mr. Calder,
in his general observations on the Geology of India§, says, “ But hitherto the
* Malcolm’s Central India, p. 324. t Physical Class, Asiatic Researches, p. 81.
} Physical Class, Asiatic Researches, p. 194, § Ibid., p. 16.
Lieut.-Colonel Sykrs on a portion of Dukhun. A27
most striking phenomenon in Indian geology is the almost total absence of
organic remains in the stratified rocks and in the diluvial soil.” As this must
have been written with a knowledge of Dr. Voysey’s paper, it being in the
same volume with his own, it is probable he considers the shells recent.
Thermal Springs.
Thermal springs do not exist in Dukhun within my limits; but there are
three distant localities in the Konkun below the Ghats, where hot water
gushes up from numerous crevices in trap rocks over an extensive surface.
The first is at Vizrabhaee, forty-eight miles north of Bombay, where the principal springs are in
the bed of a river, and in the monsoon are consequently lost in the swollen stream; but in tra-
versing the jungle in the vicinity I have met with detached pools of hot water, which are unaffected
by the rains; their temperature is very high. The second locality is that mentioned by the late
Dr. White, of the Bombay army. The hot wells are called Devakl Unei, and are fifty miles south-
east from Surat*, at the foot of some hills; the temperature in the different springs ranges from 111°
to 120° Fahr. They are spoken of as being in the vicinity of Anaval and Veval, but as these
places, agreeably to the map of India, are only thirty miles from Surat, there is evidently some
mistake with regard to the distance. The third locality is at Mahr, on the Bancoot or Fort Vic-
toria river, about seventy-five miles south of Bombay. I know of these springs only from report.
The whole of the above springs, extending through 3° of latitude, lie nearly in the same parallel of
longitude (73°), and are within twenty-five miles of the sea,
In a manuscript report to the Government of Bombay, on the province of Khandeish, Colonel
Briggs has the following passage testifying to the occurrence of thermal springs above the Ghats $
‘Among the natural curiosities of Khandeish are the hot springs of the Satpoora hills, particu-
larly those of Soonup Deo and Oonup Deo, the former in the district of Arrawud, and the latter
in the deserted Pergunneh of Amba. The former is so hot that the hand cannot be borne in it;
the latter is less ardent, and is used as a hot bath; they are both said to possess medicinal quali-
ties, and are considered useful in the cure of cutaneous disorders,—amongst others leprosy.”
Dr. Buchanan speaks of hot springs at Rishikunda and Bhimband in the trap mountains of Raj-
mahl+; and the Rev. Mr. Everest mentions a thermal spring associated with a trap bed at Kat-
camsan, between the 23rd and 24th parallels of latitude, and longitude 86° and 87°¢. Dr. Adam
mentions that of Sitakhund near Monghyr on the Ganges§. Dr. Davy speaks of one at Cannina,
Ceylon ||; and I am informed they are to be met with in Canara. Mr. Crow, formerly commercial
agent of the Bombay Government in Sinde, in his manuscript reports, mentions a thermal spring near
Corachee on the Indus, of which the water is almost boiling hot. In Major Cruickshank’s manuscript
revenue map of part of Goojrat a hot spring is placed at Tooee, near Ruttenpoor on the Mhye
river, in latitude north 22°49', and longitude east 73° 30’; and there is another at Lawsoondra,
eighteen miles west-north-west of Tooee. These instances, which I am satisfied could be multi-
plied by diligent inquiry, afford ample proof of the wide occurrence in the peninsula of India of
those singular phzenomena, the satisfactory explanation of the causes of which is still a desideratum
in geology.
a
* Transactions of the Royal Asiatic Society, 1833. + Gleanings of Science, vol. i. p. 36.
+ Gleanings of Science, May 1831, p. 135. § Geol. Trans., 1st Series, vol. v. p. 349.
|| Geol. Trans., 1st Series, vol. v. p. 313.
VOL. IV.—SECOND SERIES. 3K
428 Licut.-Colonel Sykes on a portion of Dukhun.
Craters.
Volcanic products were not seen by me, nor any conformation of the hills that might be deemed
an extinct crater; although the porcelain and ferruginous clays, and the exterior coat of the various
quartz and jasper minerals indicate their having been exposed to igneous action. Captain Danger-
field did not meet with volcanic matters or craters in Malwa or the Vindhya range, but states
a tradition exists of the celebrated city of Oogein, and eighty other places having been destroyed at
a remote period by a shower of earth; and the people say that in the Vindhya range and Rajpeeply
hills there are hollows near their summits ‘sometimes filled with water, which may be craters*.”
As the old city of Oogein stood upon a river constantly overflowing its banks, it was probably
buried in alluvium. Mr. W. Hunter attributed its destruction to one of three causes,—earthquake,
overflowing of the Seeprah, or drift earth by high winds; and, although the least probable of the
three, inclines to drift earth. He states there are not any traces of volcanic agency in the buried
city, nor in the neighbourhood f. The remains of the city of Mhysir, on the banks of the Nerbuddeh
(Nermada), are found in alluvium. We may safely say, therefore, there are not any indications of
volcanic action of a comparatively recent date.
Extent of Trap Region, &c.
I will now offer a few observations on the amazing extent of the trap, la-
terite, nodular limestone, granite, and gneiss formations in the Peninsula,
limiting their application to 25° of north latitude. My personal knowledge
of the country extends from the sea on the western side, to Arungabad, in
75° 33', and Sholapoor, 75° 53! east longitude ; north, nearly to Kandeish, and
south, to Beejapoor and the Kristna river. Captain Dangerfield takes up the
country on the north, nearly where my knowledge of it terminates, and says,
«Tt (Malwa, including the Vindhya range) appears to constitute the northern
termination of a very extensive secondary trap formation, which extends from
the extremity of the Dukhun, and probably even Mysore, forming all the
country above the Ghats, and part of the plains below, on the western side of
the Peninsula, including the islands of Bombay, Salsette, Elephanta, &c.}”’
He carries the continuous trap north to Neemutch, in latitude 24° 27', at 1476
feet above the sea. Its western limit is at Dohud, longitude74°. Major Franklin
and Captain Coulthard take it up in the eastern limits of Malwa, and trace it
through Sagar; and it continues to an unknown extent towards Sohagpoor
and the source of the Nerbuddeh river, on the table-land of Amarakantah, in
longitude 82° east. Dr. Voysey describes its eastern limits at Nagpoor, lati-
tude 21°10' N., and longitude 79° 14’ E. at 1000 feet above the sea. Mr. Cal-
der states it passes from Nagpoor southward by the confines of Hyderabad,
as low as the 15th degree of latitude, and taking a north-west direction termi-
nates on the sea-coast at Bancoot or Fort Victoria, in latitude 18°. But speci-
mens of rock shown to me from the Kolapoor country above the Ghats, between
* Malcolm’s Central India, Appendix, p. 325. + Asiatic Researches, vol. vi. p. 39.
t Malcolm’s Central India, Appendix, p. 320.
Lieut.-Colonel Sykes on a portion of Dukhun, 499
the parallels of latitude 16° and 17° N., bear testimony to the trap extending
nearly a degree and a half further south along the Ghats than Mr. Calder
supposed. Indeed its southern limit in the Konkun, Mr. Fraser states to be
at Malwan, fifty miles north of Goa*. From the above evidence we have proofs
of a continuous trap formation covering an area of from 200,000 to 250,000
square miles, a phenomenon unexampled in any other country whose geolo-
gical structure has been examined. It appears to me, however, that the above
are not the absolute limits of the trap. Dr. Buchanant and Mr. Jonest+
describe the Rajmahl hills in latitude 25° and longitude 88° to 89° E. as
trap; the latter says the basalt is of amazing thickness. The Rev. Mr. Everest §,
in a journey from Calcutta to Ghazipoor, passed four distinct broad beds of
trap between the parallels of north latitude 23° and 24°, and longitude 84°
and 87°. He states these beds to have an inclination to a common axis, and
he thinks it probable they are connected beneath the granite and gneiss.
Mr. Royle travelling the same route, observed the same beds. Mr. Everest’s
diagram shows their longitudinal axis ona line between the Rajmahl hills and
the sources of the Nerbuddeh and Soan rivers ; and as the trap of the Vindhya
range and Sagar extends towards these sources, it is very probable the rami-
fications are connected with the beds (seen by Mr. Everest) and the Rajmahl
hills, forming a belt across India from the 73° to the 89° of longitude, ex-
tending, in fact, from near the mouth of the Nerbuddeh river to the Ganges
at Rajmahl. The southern limit of trap is much lower than is assigned to it
by Mr. Calder, as Dr. Voysey describes a basaltic dyke at Seringapatam, in
latitude 12° 26’; and Mr. Calder himself mentions partial deposits of over-
lying rocks as far south as Cotallum, at the extremity of the great western
range, between the parallels of latitude 8° and 9°. Mr. Babington, passing
through Mysore, describes all the black rocks he met with as hornblende pass-
ing into basalt. He evidently adverts also to nodular basalt].
Age of Trap.
With respect to the age of the great trap formation of India, it would ap-
pear from Major Franklin’s Memoir on Bundelkund, that its northern ex-
tremities rest on sandstone, which he considers identical with the new red
sandstone of England; the trap would therefore be posterior to the carboni-
ferous series and belong to the supermedial order. But the Rev. Mr. Everest 1
adduces valid reasons for questioning the correctness of Major Franklin’s
opinion ; and it may be inferred, that he is doubtful with respect to the exact
* Geol. Trans., 2nd Series, part 1. p. 153. + Gleanings of Science, vol. iii. Jan., 1831, p. 1.
+ Phys. Class, As. Researches, p. 165. § Gleanings of Science, vol. iil. p. 135.
|| Geol. Trans., 1st Series, vol. v. p. 325. q Gleanings of Science, vol. ili. p. 211.
3x 2
430 Lieut.-Colonel Sykes on a portion of Dukhun.
equivalent in Europe of the Indian sandstone, as it is much associated with
the primitive rocks *. In fact, where are the oolitic rocks above, and the mag-
nesian below the red sand, where the rock salt and gypsum, and where, above
all, the characteristic organic remains of the lias and magnesian limestone ?
It would be idle, therefore, to speculate on the era of a formation without a
standard of comparison to direct the judgement. The question of the manner
of the formation of the horizontal beds of trap with their vertical edges is very
interesting. It will be said they were ejected under the pressure of an incum-
bent ocean. If such had been the case, where are the marine remains, and
would not there have been sedimentary deposits upon them? Moveover, if
viewed as coulées from craters, would not the beds have thinned out, instead
of preserving the parallelism of their superior and inferior planes and their
vertical edges ?
Laterite.
Laterite is a ferruginous clay mottled red and yellowish. When first dug
from its bed, it is soft and is easily fashioned into the form of bricks or large
square masses for building ; and if my recollection serves me right, it consti-
tutes the material of the walls of the fort at Tellicherry and the jail at Calicut.
It rapidly indurates on exposure to the atmosphere. It is destitute of fossils,
as far as is yet known.
That curious and very extensive rock, aptly denominated laterite, (I learn from the information
of a friend,) occurs at the source of the Kristna river in latitude 17° 59', at an elevation of 4500
feet above the sea. It covers the low land between the sea and the great western range from the
southern Konkun to Cape Comorin, and, agreeably to Dr. Davy, passes into Ceylon. I casually
observed it at Tellicherry and Calicut, respectively 744 and 756 miles south of Bombay ; and at
Calicut granite rises through it. On the low land at the base of the great eastern range, Mr. Calder
says it reappears between the 11° and 12° parallels of latitude, and recurs in increasing patches
passing northwards, covering granite. The Rev. Mr. Everest speaks of laterite forming a fringe
to great part of the bay of Bengal and covering the edge of the granite of either peninsula f.
Nodular Limestone.
In addition to the evidence already adduced of the extensive occurrence of
nodular limestone, Dr. Buchanan mentions having met with it in Rajmahl
trap hills, in Bengal, and in Mysore. A writer in the ‘Gleanings of Science’ t
states that it occurred in repeated borings for water in Calcutta, at from 50 to
112 feet below the surface. Another writer§ says, it is “very extensively distri-
“ buted throughout Hindoostan,”’ and further asserts that it is a “most distin-
‘ guished feature of Indian geology.’’ The Rev. Mr. Everest and Mr. Royle
remarked it in their journey before adverted to. The few organic remains
* Gleanings of Science, vol. iii. p. 213. + Ibid., vol. ii. p. 135.
$ Ibid., vol. i. p. 169. § Ibid., vol. i. p. 365.
Lieut.-Colonel Sykes on a portion of Dukhun. 431
hitherto found imbedded, belong to living species. The following is the ana-
lysis of “‘ Kankar ’’* (nodular limestone) by Mr. Prinsep f.
Wister Of AbsOrptlonye. <<jcietn cle sle'selo'n a alele cialis’ 6 sie'aieictorn os 1*4
Carbonatelofilimeyy cic: cicte ocerohetoke¥orch ol enetierss ore areal ekeheve sic oreverctd 72°0
Carbonate off magnesiaig awe ls eitrecigers ae slates sissies «soc 0°4
Silesahis J 54: tars, SaaS eparora aver taie ata etatet dala tater are Ota e wietevere 15°2
Alumine) and: oxide ofanonwaesictetelersie crerenteiniel eieie'« ole) e) cls, o/c 11:0
100°0
Kunkur, or nodular limestone, has been likened to the cornbrash of the En-
glish strata ; but its geological position (principally superficial), and the absence
of characteristic fossils, present insuperable objections to their identity.
Granite.
The late Dr. Voysey states, that he “had reason to believe, partly from per-
“‘ sonal observation and partly from specimens obtained from other sources,
“ that the basis of the whole peninsula of India is granite; he had traced it
“ along the coast of Coromandel, lying under iron clay (laterite) ; also in the
‘“‘ hed of the Godavery river, from Rajamahendri to Nandair; and he had
“ specimens from the base of the Sitabaldi hills of Nagpoor, from Travankur,
“ 'Tinnevelli, Salem, and Bellari.””’, Mr. Stirling in his memoir on Cuttaek says,
“The granite where my specimens were principally collected appears to burst
“ through an immense bed of laterite (iron clay) rising abruptly at a consider-
“able anglet.”’ Major Franklin adds to the above quotation, “ the plains of
« Bundelkhund attest that granite is there the basis rock.’’ Ceylon is exclu-
sively granite and gneiss ; finally, I observed granite rising through laterite
at Calicut on the Malabar coast. With these facts before us, we can scarcely
question the truth of Dr. Voysey’s opinion ; an opinion involving the belief,
with reference also to the extent of trap, that the whole peninsula of India
and Ceylon, covering an area roughly calculated of 700,000 square miles, is
of igneous origin.
Sedimentary Rocks.
Iam not aware of the existence of any sedimentary rocks in Western India,
south of Baroach, excepting such as have probably originated in the conso-
lidation of comparatively recent alluvium.
Recapitulation.
I close this paper with a recapitulation of the characteristic geological fea-
tures of the peninsula; namely,—the amazing extent of the trap region, and
the horizontal position of its stratified beds the granitic basis of the whole
* Properly Kunkur. + Gleanings of Science, vol. i. p. 278.
{ Phys. Class, Asiatic Researches, p. 37.
A32 Lieut.-Colonel Sykes on a portion of Dukhun.
country ; trap veins in granite ; the absence, as far as is known, of that uni-
form series of rocks which constitutes the formations of Europe ; the extended
and peculiar nodular limestone and laterite formations; the occurrence of
pulverulent limestone in seams ; and finally, the non-discovery hitherto of the
fossil remains of extinct animals within the limits of the Peninsula.
London,
January 21st, 1833.
A few words are necessary in explanation of the sections which accompany
this paper. They represent two principal spurs from the Ghats, and con-
verge to the same point at the junction of the Goreh and Beema rivers. In
strictness they are not sections ;—ramifications of the spurs, and hills at short
distances north and south of the central vertical plane being inserted : they par-
take, therefore, of a slightly perspective character, but this does not affect the
general correctness of their geological features. Fig. 1. comprises the range
of hills between the Under and Beema rivers, and has a length of about
seventy-five miles. Fig. 2. shows the mountains between the Bore Ghat and
the source of the Mota river, and extends nearly eighty miles. The length
and elevation are expressed by different scales, and from this cause the out-
lines of the mountains are not rigidly correct. A bare outline is traced from
the Ghats westward to the sea, for the purpose of showing the curious forms
of the weathered basaltic caps and ridges of the mountains in the Konkun.
The elevations were determined either barometrically, or thermometrically.
Those marked “B.”’ are barometrical, and result from simultaneous observations
with previously-compared barometers ; all the necessary corrections having
been applied, for temperature, moisture, and latitude. Those marked “W.’
were obtained by ascertaining the boiling-point of water at different eleva-
tions with delicate thermometers : they are not to be relied upon within 100
feet, although in some instances, when tested by barometrical measurements,
they corresponded within a few feet.
Of the Panoramic Sketches, Plate XXVII. No. 1. is a distant view of the mountains, on
which are situated the celebrated hill forts of Jewdun, Hurreechundurghur, Koonjurghur, and
Sewneir, in which Sewajee, the founder of the Mahratta empire, was born. It is taken from the
hill N. of the town of Goreh.
No. 2. is a view of the hills, to the North and East, as seen from Lakungaon in the flat broad
valley of Jooneir (Sewneir).
No, 2*. is a continuation of the view No. 2., from the N. round to the West.
No. 3., a sketch of the hills, to the North and East, as seen from the summit of the armoury,
in the fort of Ahmednuggur.
No. 4. is a sketch of the northern flank of the plateau, or which the city of Ahmednuggur stands ;
as seen from Wamooree, in the plain of the Godavery river.
VIII.—On the Geology of the Environs of Bonn.
By LEONARD HORNER, Esg., F.R.SS. L. & E., F.G.S.
[Read March 13, 1833.*]
THE district about to be described lies on the Rhine, from the mouth of the
Sieg, below Bonn, to the town of Linz, a distance of about eighteen English
miles, and extends nearly five miles inland, on both sides of the river.
A short way above Bonn the Rhine leaves the mountainous land, through
which it has flowed with little interruption from its source, and enters a vast
plain that extends to the North Sea, the nearest shore of which is about a
hundred and thirty miles distant.
The SrespeNGesirce, or Seven Mountains, are the grand feature in the
district, and constitute a group of hills, of very graceful forms, on the right
bank of the river. Looking down from one of their higher summits, one sees
a numerous assemblage of conical hills and connecting ridges; but when
viewed from a distance, and in certain positions, seven peaks rise conspicu-
ously above the rest, and hence the group has received its name. Of these,
the most remarkable, as well from its individual form as from its fame in
legendary story, is the Drachenfels, with a ruined castle on its summit. But
the Oehlberg is the highest point, being 1369 English feet above the level of
the sea, or 1209 above the Rhine, the surface of which at Konigswinter, a
small town at the foot of the Drachenfels, is, at its mean height, 160 feet above
the seat. (A table of the principal heights will be found in the Appendix t.)
The Siebengebirge and adjacent country have been described with more or
less detail by several eminent geologists of Germany. The earliest memoir
on the volcanos of this district is probably that of “ Barrnotomaus Hempet-
MANN und Jon. Witn. Muenster, Ueberbleibsel erloschener Vulkane in
einigen Gegenden des Niederrheins.”” Bonn, 1785. There is a very copious
* Between the reading and the printing of this paper, an interval of three years has elapsed,
and during that time some new facts have come to my knowledge, both from my own observations,
and from those of other geologists, which will be found in an Appendix, p. 472.—March, 1836.
+ By the barometrical measurements of Professor Benzenberg of Dusseldorf, in 1824.
+t Appendix I. p. 472.
ASA Mr. Horner on the Geology of the Environs of Bonn.
work by Nose*, which was published in 1789, and, considering the time when
it was written, it possesses great merit, and evinces minuteness of obser-
vation. Professor Noggerath+ of Bonn has described some of the more
remarkable features of the district, and Messrs. Von Oeynhausen and Von
Dechent have given, in a periodical Journal, a general view of what Nose,
Noggerath, Steininger§, and others had written, adding many original ob-
servations||. But to the geologists of England this remarkable district is little
known; it is, however, particularly deserving of their attention, for, diver-
sified as is the mineral structure of the British isles, nothing analogous to
it occurs in them; and it affords this further attraction, that the Siebenge-
birge and the neighbouring country of the Eifel are the nearest points to
England where volcanic phenomena, at all approaching in character to those
of modern times, can be seen. ‘Those who are desirous of studying, on the
spot, the effects of volcanic action, by availing themselves of the facilities of
steam navigation, may, with great ease, in six days from leaving London,
reach the Mosenberg in the Upper Eifel, and there stand by the side of a
stream of lava, and, although the fires have been long extinguished, on the
edge of a crater covered with cinders. Nor is it to be forgotten, that these
numerous objects of geological interest present themselves in a country
renowned for the charms of its natural scenery and historical associations.
I have deposited in the museum of the Society a suite of 277 specimens in
illustration of this paper, with a descriptive catalogue. The accompanying
Map has been coloured in part from my own observations ; but as far as the
Siebengebirge are concerned, it is, with a few alterations which I have seen
occasion to introduce, a copy of one communicated to me by Professor
Noggerath, and which he kindly permitted me to make use of. In a coun-
try so covered with a luxuriant vegetation as this is, one cannot say that the
boundary linesof the different formations are exact{, or that all the phenomena
which bear upon the geological history of the country have been discovered ;
future observers will probably see reason to make alterations in these boun-
daries, and I have no doubt that much remains to reward further researches.
From my learned friends Professors Goldfuss and Noggerath I derived
* Orographische Briefe tiber das Siebengebirge, &c., 2 vols. 4to,
+ Das Gebirge in Rheinland-Westphalen, 4 vols., 1822—1826.
{ Hertha, 12th vol., 1828.
§ Die erloschenen Vulkane in der Eifel, und am Niederrheine, 1 vol. 8vo, 1820; and Neue Bei-
trage zur Geschichte der Rheinischen Vulkane, 1821.
|| Professor Noéggerath is now engaged in preparing a full account of the Siebengebirge.
{| See Appendix II. p. 472.
z
Mr. Horner on the Geology of the Environs of Bonn. 43!
~
much assistance in the course of my inquiry, not only in conversation, but
also by the liberality with which they laid open to me the valuable col-
lections in the museum of the University under their charge. Iam further
much indebted to the kindness of the Count von Beust, President of the
Council of Mines in the Prussian Rhenish Provinces, who made the exten-
sive geological library and the documents belonging to that establishment
freely accessible to me.
General Structure.
The lowest and the prevailing sedimentary deposit of the district is grau-
wacke, both in the form of sandstone and of slate, a continuation of the same
formation which covers so great an extent of country in the Lower Rhine and
in the Eifel; but here no limestone beds are associated with it. None of the
later secondary strata occur, and the grauwacke is covered unconformably by
a deposit of the tertiary period, consisting of a series of beds of sand, sand-
stones, clays, and lignites, which collectively constitute a brown-coal forma-
tion. This is covered by an extensive bed of gravel, and above the gravel is
a loosely coherent sandy loam, containing terrestrial and aquatic shells of ex-
isting species, called in the Rhine valley by the technical name of Loess. From
under the grauwacke a variety of unstratified rocks have been erupted, con-
sisting of various kinds of trachyte and trachyte tuff, basalt, dolerite, and
other modifications of trap; and in one place volcanic scorie. The main
body of the Siebengebirge is composed of these unstratified rocks.
The structure of the Siebengebirge was long considered to be different in
its character from that of any other group in Germany ; and it is so with
the exception of two analogous formations, the one in Nassau, near Monta-
baur, lately described by Stifft*; the other not far from Gratz in Styria, of
which an account was published by M. von Buch+ in 1820; and by Dr. Dau-
beny in 1826{. It is remarkable that the trachyte of Nassau had not been
previously examined by geologists : it is accompanied, as in the Siebengebirge,
by trachyte tuff and phonolite, and rises in the midst of a basaltic district of
vast extent, connected with that of the Westerwald. Professor Mitscherlich
visited that part of Nassau in 1832, and I saw him just after he had been
there. He described the trachyte as covering a space quite as great in extent
as the Siebengebirge, but not forming such elevated hills, the trachyte out-
bursts rarely exceeding a very moderate elevation above the surface. In
texture they very much resemble those of the Siebengebirge, and, like them,
present various modifications of the constituent parts.
* Geognostiche Beschreibung des Herzogthums Nassau, 1831.
¢ Ueber einige Berge der Trap Formation bet Gritz.
{ Description of Active and Extinct Volcanos.
VOL. IV.—SECOND SERIES. 3 L
436 Mr. Horner on the Geology of the Environs of Bonn.
I shall first describe the several formations in detail, in the following
order: Grauwacke, Trachyte, Trachyte Tuff, Basalt, Brown-Coal For-
mation, Loess; and shall then point out their several relations to each other,
drawing such conclusions as to their several ages, and the geological history
of the district, as the facts appear to me to warrant.
Grauwacke.
This rock varies considerably in mineral character, sometimes occurring as
a fine-grained clay slate, not distinguishable from that of Westmoreland ; in
others, as a coarse red sandstone, very like some beds of the old red sandstone
of Herefordshire and Shropshire. Although | found no opportunities of
forming a decided opinion on the subject, it is probable that the prevailing
rock in the neighbourhood of the Siebengebirge belongs to the later periods of
the grauwacke deposit. At Dottendorf, on the left bank of the Rhine, about
two miles from Bonn, there are beds of it of a loose texture containing
rounded pebbles of slate, with numerous vegetable impressions, which, in spe-
cimens, might be taken for a sandstone of the coal-measures. These impres-
sions are too indistinct in form to enable one to pronounce upon their nature ;
they are black, and when exposed to heat the blackness disappears. Impres-
sions of Terebratule and the stalks of Encrinites, although abundant in the
grauwacke of the adjoining country, are not very common within this district.
They are found in that near Rhéndorf, and in the neighbourhood of Unkel.
In some places it contains anthracite ; and I was informed by Mr. A. L. Sack
that at Bruckhausen six different beds of it were found, one of which was a
foot thick, but they were not continuous.
The strata are generally highly inclined, but they are found at all angles.
There is neither uniformity in the strike nor in the dip, but the former is
most generally from north-east to south-west, and the dip more frequently
south than north. In the immediate neighbourhood of the Siebengebirge the
strata are thrown up in all directions, which, at first sight, might be thought
to be caused by the eruption of the volcanic matter; but there are great de-
rangements of the grauwacke in the Kifel and Westerwald, at a distance from
igneous rocks. Sudden variations in the strike and dip, the latter from ver-
tical to horizontal, (if I may so speak of dip,) may be well observed between
Unkel quarry and Remagen, and on the opposite side of the Rhine between
Erpel and Orsberg.
The extent occupied by the grauwacke will be seen by an inspection of the accompanying Map.
It flanks the volcanic region of the Siebengebirge on the east and south, and appears in detached
spots on its western side, but it is wholly wanting on the north. On the left bank of the river it
constitutes the ridge from Remagen to Rolandswerth, but it is partially covered by the brown-coal
Mr. Horner on the Geology of the Environs of Bonn. A37
formation and by loess between these places ; and from Rolandseck northward, it is covered by the
brown-coal formation, except in a few places on the eastern side of the elevated plateau that runs
from Rolandseck in a north-west direction; as at Muffendorf, Friesdorf, Dottendorf, and Kessenich,
in all which places it appears in highly inclined strata.
Trachyte.
There are several varieties of this rock. Glassy felspar is the chief ingre-
dient in all, mixed with hornblende, occasionally augite, quartz, magnetic
iron, and sometimes, but rarely, mica. Distinct crystals of glassy felspar,
often of great size, are imbedded in the base of most of the varieties. The
different aspects which the rock presents depend mainly on the felspar of the
base being largely crystalline or small granular, upon the proportion of horn-
blende and size of its crystals, upon the size and proportion of the separate
imbedded crystals of felspar and hornblende, and upon the colours imparted
by the different states of the iron which enters into the composition of all.
Some varieties are also produced by the felspar being decomposed.
The places where the trachyte can be studied to most advantage are on the Drachenfels, the Wol-
kenburg, and the Stenzelberg, especially the two latter, where there are extensive quarries. The
trachyte of the Drachenfels is one of the most remarkable varieties: it is a gray stone, with a cry-
stalline base of felspar, and minute crystals of hornblende, including separate crystals of felspar,
often more than two inches long and an inch and a half in diameter. It has been for ages used as a
building-stone, and is upon the whole very durable, except that the separate crystals of felspar are
apt to fall out. The Cathedral of Cologne is built of it. The trachyte of the Stenzelberg contains
more hornblende, and has few imbedded crystals of felspar ; but those of hornblende often occur,
and are sometimes of a great size. In some places there are portions of the rock, separated by sharp
lines from the rest of the mass, of a dark fine-grained texture, so as to look like included fragments
of basalt; but it is probable that they are fragments of slate, altered by the heat of the melted tra-
chyte, as there are other similar portions about whose origin there can be no doubt, the slaty struc-
ture being quite distinct. In the quarry of the Stenzelberg a face of rock about sixty feet in height
is exposed: it is divided by vertical rents into large tabular masses of irregular forms, and in some
places they are rounded, standing out like the stems of gigantic trees, the rock separating into
curved layers parallel to the axis, a tendency to exfoliation which is often observable in small
specimens. This appearance has been particularly described by Professor Noggerath*, and Pro-
fessor Goldfuss, in his Geognostiche Tafeln, has given a print representing the face of the quarry
at that time: it is now a good deal altered, and the appearance of exfoliation on the great scale is
at present not so marked as it is in the print. The trachyte in the upper part of the quarry is vesi-
cular, and it resembles the lava stream which is quarried for millstones at Nieder Mendig near the
Laacher See; so much so, as to suggest the idea that the latter owes its origin toa melted trachyte.
Mr. Lyell, who visited this place with me, remarked the great resemblance of the trachyte to the
rock quarried above the Plateau de |’Aigle, not far from the baths of the Mont Dor in Auvergne.
The trachyte of the Wolkenburg resembles that of the Stenzelberg, including, although more rarely,
large separate crystals of hornblende, and occasionally large masses of quartz. It often contains
oS SO ee ee eee
* Das Gebirge in Rheinland-Westphalen, iv. 359.
3L2
438 Mr. Horner on the Geology of the Environs of Bonn.
calcareous spar, lining cavities, and in well-defined erystals. Here, also, a lofty face of rock is ex-
posed in the quarry, exhibiting the trachyte in large vertical tabular masses, without apparent cross
joints, although these exist, as the rock separates easily into huge blocks by natural fissures. It is
for the most part of a light fawn colour; but when the large masses are broken they show a bluish
gray nucleus, such as is often seen in trap rocks. The one colour, however, does not always gra-
duate into the other; on the contrary, there is sometimes a sharp line between them, and at the
separation the trachyte is of a vitreous texture. I observed the same thing in the trachyte of the
Keilsbrunnen quarry, with a tendency to globular decomposition. One of the most remarkable
varieties of trachyte is that of the Perlen Hardt, on the eastern side of the group. I nowhere found
such large imbedded crystals as here, but they are extremely brittle, and consequently good spe-
cimens are not easily obtained*. The base is much decomposed, the felspar being in some places
changed into a bright red earth: it contains small yellow crystals of sphene. At the Rosenau there
is a variety containing augite; I obtained a specimen at this place with a separate well-defined
crystal of that mineral; and close to this spot I found a sudden change into a variety with large
imbedded crystals of felspar, like that of the Drachenfels, a circumstance which, like many others,
shows under how many different forms the same materials may issue from a volcanic focus. At
the Klein Rosenau there occurs a variety of a light gray colour, very compact, with a conchoidal
fracture and ringing sound, a phonolite, composed of felspar and quartz, without any hornblende
or other ingredient; and it passes into another kind of a light fawn colour, still more compact, in
which the quartz predominates almost to the exclusion of the felspar, being infusible, while the
gray variety is readily acted upon by the blowpipe: the latter is in some places of a bright pale
green, apparently from an admixture of iron, and contains chalcedony, hyalite, and veins of ferru-
ginous opal }.
The Hummerich, the Mittelberg, and the Bruder-Kunzberg are three conical hills, which rise
out of an elevated plateau of grauwacke at some distance to the south of the main group of the
Siebengebirge. They are composed of trachyte, but of a kind bearing a strong resemblance to
some varieties of trap, particularly that of the Mittelberg and Bruder-Kunzberg. It is of a gray
colour, has a much smaller proportion of distinct erystals of felspar and hornblende, and has some-
what of a foliaceous structure. At the Hummerich it is rudely columnar, and has a tendency to
globular decomposition: at the foot of the same hill it has the character of an amygdaloid.
The affinity between trachyte and the trap family has been pointed out by
many geologists ; long ago by M. von Buch in his admirable essay on Trap Por-
phyry{. In the Siebengebirge it would be easy to form a suite of specimens,
showing a gradation from a white trachyte to a compact black basalt. The
analogy is further seen by the columnar form and tendency to globular de-
* Lavas, which probably belong to a much more modern period than these rocks, contain fel-
spar crystals of great size. In his description of the Ponza Isles, Mr. Poulett Scrope says, “I met
“* with some felspar crystals nearly three inches in diameter, and these are accompanied by augite,
‘ bearing the same proportion to them in size as the ordinary minute grains to the common-sized
“ felspar.’—Geological Transactions, Second Series, vol. ii. p. 215.
+ Mr. Poulett Scrope inthe same Memoir, describes a siliceous trachyte, which appears from
the description to be very similar to the rock found at the Klein Rosenau.—Geological Trans-
actions, Second Series, vol. ii. pp. 201, 208, 214, 229.
+ Transactions of the Royal Academy of Berlin, 1812.
Mr. Horner on the Geology of the Environs of Bonn. 439
composition. Near the Thier Garten, north of the Stenzelberg, there is a
variety of trachyte scarcely distinguishable from the base of an earthy amyg-
daloid ; and I found a block at the foot of the Drachenfels, of a green colour,
very like some kinds of serpentine. Nor is this intimate connexion between
these two classes of unstratified rocks différent from what might naturally have
been expected to happen, for the materials of both exist in the same spot ;
variations in the proportions of these not very numerous ingredients, in the
degrees of heat to which they were exposed, in the circumstances under
which they cooled, would perhaps account for all the shades of difference
we meet with. M. Von Buch states in the memoir above quoted, that
when trachyte passes into a black substance, the felspar and hornblende
have disappeared, and olivine and augite have taken their places. Much
light has been thrown on this subject by the interesting experiments of
Mr. G. Rose*, who has shown how intimately hornblende and augite are
connected: he obtained artificial crystals of the forms of augite by fusing
hornblende; and he conceives that hornblende may be formed by slow,
and augite by rapid cooling. Such gradations show how necessary it is to be
cautious in drawing geological inferences from mere mineralogical variations,
and that in giving new names to rocks merely on account of such differences,
much confusion and error may be introduced. Notwithstanding, however,
this connexion between the trachyte and basalt of this district, the basalt ap-
pears to have been, if not entirely, at least in great part, erupted at a distinct
and later period, and I have not discovered any evidence of trachyte having
been again ejected after the basalt had begun to flow ft.
There is only one place where I have seen the trachyte in the form of a
dike or vein, and [ have not been able to learn that it is so met with in any
other spot. This dike crosses the road from the Loéwenburg Tranke to the
Perlen Hardt. It is about five feet wide, and is much decomposed, but the
fresher parts resemble the trachyte of the Perlen Hardt. It traverses a tra-
chyte tuff, containing hard masses of trachyte and fragments of slate.
* Leonhard and Bronn’s Jahrbuch fiir Mineralogie, &c., 1832, p. 237.
+ Among the volcanic rocks of the Siebengebirge are varieties whose constituent parts are as
largely crystalline as any granites that have been met with. Von Buch states that in several places
in the neighbourhood of Clermont and Puy de Dome, a transition from granite into trachyte may
be traced, and thus we have the gradation extended from granite to basalt. Dr. Hibbert de-
scribes a gradual transition from basalt into granite in the Shetland Islands. (Brewster's Edinburgh
Journal of Science, i. 107.) Speaking with Professor Mitscherlich about the large imbedded
crystals of the Drachenfels and Perlen Hardt, he remarked to me, that in a mass which is only
viscid, crystals will be formed, but that it requires a very long time; that felspar becomes viscid
at a comparatively moderate heat, but that it requires a very high temperature to make it flow.
440 Mr. Horner on the Geology of the Environs of Bonn.
The substances which in Hungary and Central France accompany trachyte,
viz. pitchstone, obsidian, pearlstone, and pumice, do not occur in the Siebenge-
birge, if we except some portions of the latter that are met with occasionally
in the trachyte tuff. It has in no instance flowed as a stream, nor do any of
the hills in the Siebengebirge show any signs of a crater.
The ground is so covered with vegetation that it is very rarely that the different rocks can be
seen in contact. In one place only have I been able to discover the trachyte and grauwacke to-
gether: this is behind the village of Rhondorf, at the Bruckersberg, where trachyte rises under grau-
wacke strata, inclined at a high angle, bent and broken, and both are covered by a thick unstratified
mass of loess. The trachyte is much decomposed, but at a short distance it is tolerably fresh.
CSS
Trachyte. Grauwacke. Loess. Alluvial Soil.
When the water in the Rhine is low, trachyte rocks may be seen stretching from the foot of the
Drachenfels a considerable way across the river; but it has not been found in any part of this
district on the left bank of the Rhine, except at Borkum, about three miles west by south of Meh-
lem: there it is of a grayish white colour, is composed of white felspar and minute portions of green
hornblende, with imbedded crystals of glassy felspar. It forms a small hill, surrounded on all
sides by grauwacke slate, but the junction cannot be seen*.
Trachyte Tuff:
A considerable part of the Siebengebirge is covered with a tuff consisting
of angular fragments of trachyte, generally in an earthy state, especially as
* Von Oeynhausen and Von Dechen, in Hertha, xii. 432.
+ I adopt the term trachyte tuff in preference to that of conglomerate, by which it is usually
called by the German geologists, because, in England, conglomerate would generally be under-
stood to mean a congeries of water-worn fragments of various substances.
Mr. Horner on the Geology of the Environs of Bonn. 4A]
regards the felspar, for the most part loosely aggregated, but sometimes so
compact as to be quarried for various economical purposes. The fragments
are usually small, seldom larger than hazel-nuts or small beans, and sometimes
so fine, that when the stone is white and compact, it is very like a coarse chalk.
It occurs grayish white, yellow, and brown of various tints, and sometimes of a
reddish colour. It frequently contains masses or balls of hard trachyte, vary-
ing in diameter from a few inches to two feet and upwards, and fragments of
slate, usually angular, but sometimes rounded. Except in one situation, which
I shall afterwards mention, | never found any basalt fragments in the tuff,
an important fact as regards the history of these volcanic regions. They
were formerly stated to have occurred, but later observations have shown
that what was taken for basalt is a very compact black slate. I searched for
basalt in those places where it was said to occur, but never found any.
The trachyte tuff generally occupies the intervening valleys, and is found at considerable ele-
vations, but none of the higher summits are composed of it: they are either of trachyte or basalt.
Its extent and mode of surrounding the trachytic and basaltic hills will be best understood by an
inspection of the Map, but I shall mention some of the spots where it may be most distinctly seen.
The road from Konigswinter into the Wintermihlen-thal goes across the extremity of a ridge,
which descends from the Drachenfels, apparently wholly composed of trachyte tuff, and at a place
called the Holle it is cut through to the depth of forty feet. Here it is of a brown colour, and
seems to contain much iron. It is traversed in all directions by lines like the decomposing crusts
of two surfaces united, which sometimes give a false notion of stratification: in many places it is
decomposed in concentric layers, like basalt, and it contains numerous masses of trachyte and
slate. It is traversed by basalt dikes, which will be afterwards described. A tuff similar to this
occurs between the Lohrberg and Scheerkopf, where it is traversed by the trachyte dike, men-
tioned p. 439, and it is here at an elevation of about 900 feet. The tuff in these two places is
different from any that occurs elsewhere in the district. After passing the Holle, and arriving at
Quegstein, at the entrance of the vailey, a white, very loosely coherent tuff, including fragments of
slate, rests on a compact sandstone of the brown-coal formation, and is covered by loess: specimens
may be obtained of the junction of the tuff and sandstone. In the museum of the University of
Bonn there are specimens of tuff from this place with impressions of the leaves of trees similar to
those which are found in the brown-coal formation. In the immediate vicinity of this spot there
was a knoll of basalt, which contained fragments of slate converted into jasper, of which several
specimens may be seen in the museum; but the hard rock has been entirely removed for mending
the roads. Higher up the valley, the tuff, preserving its white colour, becomes more compact, and
at the Ofenkulenberg, a ridge descending from the Wolkenburg, it is quarried. It is much used
for building ovens, from its property of resisting heat, and is thence called Backofenstei , and from
being easily worked, masses are hollowed out to form troughs. In the road leading to the quarry
;t is traversed by a dike of basalt; and Mr. Noggerath* says, that at this place impressions cf
leaves have been found in the tuff. In the Keilsbrunnen Steig, near the Ofenkulenberg, a similar
tuff is traversed by dikes of basalt.
‘Pit wll teaksl ete Ul s t
* Rheinland-Westphalen, 1. 125.
442 Mr. Horner on the Geology of the Environs of Bonn.
The trachyte tuff is well seen in the Haisterbacher-thal, the other great valley which runs up
into the Siebengebirge from Ober-Dollendorf, to the Stenzelberg and to Haisterbacherroth. At
the Langenberg it is loosely coherent, white, and pale red, contains much pumice, fragments of
slate; and portions of mood, ina soft state and of a brown colour, are not uncommon. Small
crystals of glassy felspar may be picked out of the earthy base, and the ruts in the road are often
coated with magnetic iron-sand, left by the rain that has washed the tuff. It contains numerous
masses of trachyte, many of which are quite fresh, and resemble those of the Drachenfels, Rosenau
and Stenzelberg; others unlike any found i situ. The tuff in this place lies in beds which are
nearly horizontal, but it exhibits that partial and irregular deviation from horizontality in short
distances, so often seen in sections of beds of gravel where there are alternations of sand, indi-
cating the deposition of the tuff to have taken place under the surface of water. Ascending the
valley at the foot of the Wirlberg to the Stenzelberg Kreuz, another section of the tuff is seen
covered by loess; and Professor Noggerath states* that the tuff here was traversed by a vein of
opal jasper from two to three inches thick, and nearly vertical, very like the wood opal of Hungary °
it has long since been carried all away. Immediately above Ober Cassel a tuff is found which
differs considerably from any other in the district I have met with, in as much as it contains frag-
ments of basalt and scoriz, together with balls of clay ironstone. From its situation it is not im-
probable that this may be an after deposit of trachyte tuff, along with clay of the brown-coal for-
mation.
Behind the village of Honnef a small knoll, called the Schwarzenerdenkopf, is formed of a con-
glomerate or rather breccia, to which I have found nothing like in any other part of the district.
It contains fragments of trachyte of different kinds, scoriaceous basalt, compact basalt, quartz,
crystals of felspar and hornblende. It is surrounded on all sides by grauwacke, and is of very
limited extent. It is altogether a very singular occurrence, and not very intelligible as to its
origin.
Between the villages of Dambruch and Rott, on the northern slope of the Siebengebirge, con-
siderably within the region of the brown-coal formation, and four miles from the nearest point
where trachyte occurs, there are distinct beds of trachyte tutf lying between beds of clay and clay
ironstone. The same association of tuff with the brown-coal formation is found at Scheurn, Ut-
weiler, and Oehlinghoven. It is generally composed of smaller fragments than the tuff nearer to
the trachyte, but it contains masses of fresh hard trachyte. At Scheurn it contains impressions of
the leaves of trees, similar to those found in the brown-coal formation.
The only spot on the left bank of the Rhine where I have found trachyte tuff is in a lane behind
the village of Muffendorf, between that place and Godesberg ; it is very similar to that near the
Drachenfels, and contains large masses of trachyte f.
It has been remarked by some who have described the Siebengebirge,
that the trachyte tuff always corresponds in composition with the trachyte
nearest to it, as if it were derived from a disintegrated trachyte, and were
thus a recomposed rock. I have looked for this correspondence of structure,
but could never satisfy myself that such is the fact. In the first place the tuff
is, in almost every case, in too earthy a state to enable one to say of what
particular species of trachyte it is composed ; and in the next place, it occurs
generally surrounded by trachytes of various kinds ; and lastly, the masses or
* Rheinland-Westphalen, i. 139. + See Appendix III. p. 472.
Mr. Horner on the Geology of the Environs of Bonn. AAS
balls of trachyte which it contains are very often entirely different from any
variety that now exists en masse. In addition to all these objections to its
being derived from preexisting trachyte, I think there is every reason to sup-
pose that the ejection of the tuff preceded that of the solid trachyte, just as in
existing volcanos showers of ashes often precede streams of lava.
Basalt.
Although all the rocks [am about to describe under this head do not strictly
correspond in mineralogical character with the black compact substance to
which the term is usually applied, I shall not convey any erroneous idea by
employing it, as by far the greater proportion of the trap rocks of the district
are true basalt, characterized by the presence of olivine, and the rest have a
great resemblance to it.
Basalt occurs in different parts of the district on both sides of the Rhine. In the Siebengebirge
it forms entire hills, and dikes of it traverse grauwacke, trachyte, and trachyte tuff; it is also as-
sociated with the beds of the brown coal formation. The three highest hills in the district are
composed of it, viz. the Diisberg near Linz, the Oehlberg, and the Lowenburg in the Siebengebirge ;
and, by a reference to the Table of Heights in the Appendix, it will be seen that it constitutes one
half of the separate hills in the group. The extent of their united surfaces is also fully equal to
that occupied by trachyte.
There are two important differences as regards the manner in which the
two classes of rocks have been ejected: the trachyte, except in a single in-
stance, is not found in veins traversing other rocks, and the basalt is never
associated with basaltic tuff except at Siegburg, to be afterwards described,
and that hill is not within the Siebengebirge group.
The summit of the Lowenburg is composed of a rock that would be called
dolerite by most geologists, its constituent parts, augite and felspar, being in
much larger grains than in basalt: it contains magnetic pyrites, and it sepa-
rates in some places into slender irregular columns.
The upper part of the Oehlberg is a close-grained black basalt in large tabular or rudely columnar
masses, highly magnetic, and possessing polarity; it contains in some places numerous reddish
brown grains, which are probably hyacinth, as that mineral is not unfrequently met with in the
basalt of the district: among the specimens which accompany this paper is one from Papelsberg
near Ober-Cassel, with a well-defined crystal of hyacinth*. The ridge between Ober-Cassel and
Ramersdorf is wholly composed of basalt, containing much common calcareous spar and arrago-
nite, but no zeolite, a substance which seems to be of very rare occurrence in the Siebengebirge.
Numerous quarries have been opened in this ridge; in the most considerable of them the rock has
I sk is Mae Fi re A ea ee ne
* Sassenberg, the intelligent guide of the Siebengebirge at Ober-Dollendorf, told me in July 1833
that a specimen of basalt had been found in the quarry at Unkel containing sapphire.
VOL. IV.—SECOND SERIES. 3M
444 Mr. Horner on the Geology of the Environs of Bonn.
the remarkable appearance of a gigantic globular concretion, an ellipsoid, the shorter axis of which
is at least seventy feet, composed of concentric layers. Professor Noggerath* has described this
spot; and although by the operations of quarrying the appearances are a good deal altered since
his drawing was made, the concentric arrangement of the rock is quite distinct. In a quarry north
of this the basalt is split into tabular masses like stratification ; and these again into smaller portions
by cross rents, so that the face of the rock looks like a dry-built wall of squared stones, an appear-
ance not at all uncommon in modern lavas. In a quarry under Fovaux’s Hauschen, a little further
north, the basalt presents the appearance of a pile of globular concretions so squeezed together as
to assume the form of flattened lenticular masses.
In the southern part of the district the sharp cone which rises from the grauwacke plateau above
Honnef, called the Leyberg, is composed of rudely columnar basalt; and between it and Linz are
four other conspicuous hills, rising in a like manner from the grauwacke ; the Gross Diisberg,
1325 feet above the Rhine, the Klein Diisberg, the Hummelskopf, and the Mendenberg, all com-
posed of basalt. On approaching the Mendenberg from Erpel or Linz, one is surprised to see
the quantity of fragments of the most regular slender basaltic columns, which are applied to all
sorts of purposes, as building-stones; pig-styes are constructed of pillars which would be prized
as beautiful specimens in a public museum. The quarry from which these are procured is situated
immediately under the summit of the Mendenberg; it forms at present an oval space of about
fifty feet by thirty, the entrance to which is by a narrow passage, and it is surrounded by walls
twenty feet high, of the most regular slender columns, standing nearly erect, and packed close
together like the cells of a honeycomb, but easily separable and without cross joints, so that single
columns are sometimes obtained of the whole height: I saw one lying on the ground, a hexagon
of nine inches diameter and sixteen feet long. The most regular columns are pentagons and hexa-
gons; in these the angles are very sharp. It is a very compact black basalt, which breaks into
very sharp fragments that ring like glass, and contains few imbedded minerals: I obtained, how-
ever, a good specimen of slender prismatic mesotype. ‘The ends of the columns reach the surface,
and are not covered by amorphous basalt ; but they are an inferior bed, for higher up, at the very
summit, there is a mass of columns less regular in form, lying in an inclined position, and detached
from each other. Such is the profusion of basaltic columns in this neighbourhood, that the walls
of the town of Linz are wholly built of them, laid on their sides, with the ends projecting outwards;
and the streets are paved with the smaller columns set on end, a miniature representation of the
Giant’s Causeway. The walls of Bonn and Cologne are in the same way built of fragments of
basaltic columns laid with brick; and the posts by the sides of the roads and streets in this part
of the country are generally made of the same ready-shaped stones.
All round Linz basalt breaks out from the grauwacke at detached points. One of the most con-
siderable of these eruptions is the Erpeler Lei, which rises to a very considerable height from the
edge of the river. These basalt knolls are of very frequent occurrence towards the east and south-
east of this district, and they form a continuation of the eruptions around Siegen, in the Wester-
wald and near Frankfurt; and these are connected with the greater masses of the Vogelgebirge
Rhongebirge, and Habichtwald. It breaks out, too, at several detached points on the left bank
of the Rhine within this district. The Landskron in the lower part of the Ahr valley, a hill about
800 feet high, is composed of grauwacke for two thirds of its height; but the upper part is basalt,
showing some tolerably regular jointed columns. Opposite to the town of Unkel a considerable
face of rock is exposed in an extensive quarry: here the whole mass of basalt is columnar, the
* Rheinland-Westphalen, ii. 250. See also Dr. Daubeny on Volcanos, p. 67.
Mr. Horner on the Geology of the Environs of Bonn. AAD
columns lying in an inclined position, and separated frorn each other as if there had been an in-
termediate part reduced to an earthy state by decomposition. The basalt itself is very fresh, and
contains many simple minerals, especially olivine in rounded granular masses, sometimes as large
as a turkey’s egg, calcareous spar, hornblende, mesotype, hyacinth, and magnetic iron. In the
upper part of the quarry there is a basalt conglomerate which includes fragments of wood, and
above that a pretty thick bed of loess. When the water in the Rhine is low the columnar basalt
is seen extending a considerable way into the stream, and before a great part of it was removed
it rendered the navigation here difficult and dangerous. Eruptions of columnar basalt may also
be seen at Rolandseck, at Dechelsberg near Nieder Bachem, at Liihnsberg near Muffendorf, and
near Kessenich ; and the conical hill of Godesberg, which, crowned with its ruined castle, forms
so conspicuous a feature in the landscapes of this neighbourhood, is composed of the same rock.
Basalt Dikes.
These are of frequent occurrence in the Siebengebirge.
In the Keilsbrunnen quarry, not far from the Lowenburg, a dike of amygdaloidal trap, about
twelve feet thick, traverses trachyte; and one traversing the trachyte tuff in the immediate neigh-
bourhood, from its composition and direction, seems to be a prolongation of the same. Not far
from hence, at the Lowenburg Tranke, the trachyte is traversed by a dike of amygdaloidal trap
about two feet wide, the trachyte being much decomposed. In the lane leading from Konigswinter
to the Keilsbrunnen quarry, between the Hirschberg and Wolkenburg, the trachyte tuff is traversed
by four dikes in a space of about seventy-five feet. They are narrow, but their dimensions and
their relations to the substance they cut through cannot be well seen from the covering of soil.
Near the Stenzelberg Kreuz the trachyte tuff is cut by a dike which probably is connected with the
basaltic hill, the Wirlberg, close by, and which probably has also sent out the dike in the opposite
direction, which is seen near the Thier Garten. In aroad leading over the hills due east of Hon-
nef, near Steinsbusch, a dike of basalt cuts the grauwacke strata; there is no change produced in
the latter either in regard to disturbance of the regularity of the stratification or the texture of the
stone; but at no great distance, at the Goldnen Kistchen, a mass of basalt in contact with the
grauwacke changes it into a hard substance like jasper, which splits into prismatic fragments.
In the Kénigswinter valley, and in the road to the Ofenkulenberg quarry, and not far from it, a
white trachyte tuff is traversed by a trap dike about six feet wide; the tuff is considerably har-
dened at and near the junction, and splits into prismatic fragments. The dike is a dark amygda-
loidal basalt with olivine; but there seems to have been an intermixture with the tuff towards the
sides, where it is so changed as scarcely to be recognisable from basalt in detached specimens.
Where it is of a dark colour it separates into thin plates like a coarse slate, parallel to the direction
of the dike. The tuff in the Kénigswinter Holle, described p. 441. is traversed by two dikes of
about two feet in width, which intersect each other; the one being thrown considerably out of its
direction by the other, but the point of intersection is concealed by the road. The substance of
these dikes is so much decomposed that it would be impossible to recognise them for basalt except
by their resemblance to what occurs in other instances, where the rock is partly fresh and partly
decomposed ; indeed one of the dikes is changed into a substance very like a dun-coloured friable
sandstone. Besides these two dikes there are two others in the same situation, but they do not
present anything requiring particular notice.
3M 2
446 Mr. Horner on the Geology of the Environs of Bonn.
One of the most remarkable volcanic eruptions of this neighbourhood
occurs at Siegburg, a small town in the northern part of the district. The
small river Sieg winds through an extensive alluvial plain, and in the midst of
this, entirely detached from the adjoming hills, three conical eminences rise up,
one of them quite insulated, the other two connected together by a low ridge.
At the foot of the insulated cone, which is 211 feet high, the town of Sieg-
burg is situated, and on its summit there is a vast building, formerly a mo-
nastery, now a public Lunatic Asylum, which forms a very conspicuous object
for many miles round. The principal mass of these three hills is a tuff of a
yellowish brown colour, in some places compact, but more usually of a loose
texture ; in point of structure very like trachyte tuff, but substituting the con-
stituent parts of basalt for trachyte as the material ; and it is used for similar
purposes, viz. the construction of ovens and fireplaces. Its component parts are
for the most part decomposed basalt, hut sometimes the fragments are fresh ;
many are in the state of scoria, and there are numerous fragments of grau-
wacke slate. It is often penetrated by calcareous spar, seemingly introduced by
subsequent infiltration ; and it contains numerous fragments of dicotyledonous
wood, generally brown like lignite, sometimes fossilized by calcareous spar, at
others highly charged with iron; balls of clay ironstone are not unfrequent.
Mr. Lyell, who visited this spot with me, remarked the great resemblance of this
tuff to the volcanic tuff of the Phlegraeean Fields and of Ischia. The two con-
nected hills are called the Grimprich and Wolsberg, and are 189 and 230 feet
high. From the former stands out a mass of basalt at the summit, a part of a
dike from the sides of which the tuff has been washed away, portions of it
being still left adhering ; the main part of the dike is a compact black basalt,
but towards the sides it becomes scoriform ; it may be traced to the bottom of
the hill. On the south-east side the tuff lies in beds dipping from the hill,
that is, with a slope nearly parallel to its present surface. The basalt contains
nests of arragonite in well-defined crystals. In the Wolsberg there are large
quarries where the tuff may be seen in all its varieties, being sometimes so
hard as to require to be blasted. On the south side, and just above the Sieg,
it is traversed by a double dike of basalt, each branch about a foot wide, the
tuff between being very different from that on the outside, appearing like
cinders that had run together, part being in a twisted form, as is often seen
when a viscid ropy stream of lava has cooled; the basalt of the dikes is also
scoriform. No place can show in a more distinct manner the similarity of an
undoubted lava to basalt occurring in situations where none of the usual ap-
pearances of active volcanos exist ; for the basalt of these two cones could not
Mr. Horner on the Geology of the Environs of Bonn. AAT
be distinguished in specimens from the Rowley Rag of Staffordshire, or the
Castle Rock of Edinburgh.
The only remaining point of volcanic eruption which I have to notice is
the Roderberg, a hill above the village of Mehlem, on the left bank of
the Rhine. From a distance, and even near at hand, one would not suspect
that the hill had anything volcanic in its nature; it is not conical, but looks
like a smooth rounded prolongation of the adjoining hills that belong to the
brown-coal formation. But at the beginning of the ascent from Mehlem
loose black cinders appear, and on arriving at the summit there is found a
circular depression of about a hundred feet deep, and a quarter of a mile in
diameter, once the crater of a volcano, but now occupied by corn-fields sur-
rounding a farm-house. It is on the north and north-east side chiefly that the
volcanic materials are seen, for in the ascent from Nieder Bachem there are
few traces of them, till one comes to the edge of the crater, even although the
road is cut several feet deep into the hill in some places. On the north and
north-east the edge of the crater is composed of a spongy scoriaceous rock,
with marks of fusion, identical with the productions of active volcanos. At
the south-west side of the crater, however, grauwacke appears, but whether iz
situ or in detached blocks it is difficult to determine ; it is of that brighter red
colour from oxidation of iron which is produced when a portion of grauwacke
is exposed to a strong heat. Upon this lies a yellow gravel, the same as that
which covers the brown-coal formation throughout the district, and containing
no fragments of volcanic matter; and upon the gravel lies a black tufaceous
semi-indurated substance, disposed in layers which slope outwards from the
crater *.
Brown-Coal Formation.
This formation consists of an assemblage of beds of siliceous sand, sand-
stone, quartzose conglomerate, clay of different qualities, clay ironstone in
layers and detached masses in the clay, and of lignite cf various qualities, in
distinct beds and intermixed with the clay.
It occupies a great extent of country on both sides of the Rhine. On the right bank it covers
the northern slope of the Siebengebirge, as it falls to the plain through which the Sieg flows, oc-
cupying an area of about seven miles from east to west, and five from north to south. It occurs
again north of the Sieg, in detached spots along the sides of the hills forming the eastern boundary
of the Rhine valley, as far as the immediate vicinity of Bensberg, nine miles east of Cologne. On
the left bank of the river it forms a long broad ridge of low hills, or rather plateau, lying between
the valleys of the Rhine and the Erft, from the town of Meckenheim, nine miles south-west of Bonn,
* See Appendix IV. p. 472.
448 Mr. Horner on the Geology of the Environs of Bonn.
to the south of the town of Bergheim, between Cologne and Juliers, a stretch of about thirty miles ;
and Professor Néggerath informs me that he has traced the lignite beds at intervals from Bergheim
to Aix la Chapelle. The breadth of the plateau varies from three to five miles. Its greatest ele-
vation is about 200 feet above the plain on the eastern side; and from the foot of the plateau near
Briihl to the Rhine, a distance of about five miles, there is a fall of fifty feet*. These two districts,
on the right and left banks of the Rhine, are the chief deposits; but the formation occurs at several
places further south, on both sides of the river, and also within the volcanic regions of the Sieben-
gebirge and Lower Eifel.
A. The Siliceous Deposits.
The lowest member of the formation seems to be the loose siliceous sand ;
with this is associated, and generally covering it, a sandstone of various de-
grees of coherence, sometimes so friable as to be easily rubbed between the
fingers, at others as compact as a granular quartz rock. At Tanzchen and
Quegstein, in the valley above Kénigswinter, all these varieties may be seen
together. Here also are found thick beds of a quartzose conglomerate, the
pebbles of which are for the most part small, but sometimes as large as a
pigeon’s egg, and so associated with the fine-grained quartzose rock, that
specimens may be obtained of both united, sometimes showing a gradual
transition from the coarse to the fine, at others a sharp line of separation.
In specimens no one could distinguish this sandstone conglomerate of fresh-
water formation from rocks of constant occurrence in the grauwacke and
older secondary strata. ‘The conglomerate is traversed by yellow and brown
semi-opal, which occasionally assumes the mammillary structure of chalcedony,
and in which traces of vegetable structure may be detected.
In the neighbourhood of Rott and Geistingen, on the right bank of the
Rhine due east of Bonn, there are found, associated with a thin leafy bitu-
minous lignite which has obtained the name of Papierkohle (Paper-coal),
lamine of a flinty substance, seldom above an inch thick, and usually accom-
panied with thin friable siliceous plates, earthy, and bearing some resemblance
to the Polierschiefer that is found in the brown-coal formation of the Ha-
bichtwald. Between the plates of the Papierkohle siliceous concretions, of
the form and size of beans, are sometimes found.
B. The Argillaceous Deposits.
These consist of beds of clay of various qualities and colours, according to
which they are used for making bricks, tiles, and pottery ; and some is sent
into Holland for making tobacco-pipes. In many places the clay is much
* Von Dechen, Beschreibung des Kuhlen und Tummelbau in dem Briihler Braunkohlenrevier,
in Karsten’s Archiv., vol. iii. 1831.
Mr. Horner on the Geology of the Environs of Bonn. 449
mixed with earthy lignite, is in many places very pyritous, and when that is
the case, works have been established for the manufacture of alum, as at
Friesdorf on the left bank, and Holtorf on the right bank of the Rhine, both
near Bonn. The clay, intermixed with earthy lignite, which also contains
pyrites, is piled up in lumps, forming heaps of many yards in length; and
after being for some time exposed to air and moisture, decomposition takes
place, evolving much heat ; sulphate of iron and sulphuric acid are formed,
which last unites with the alumine of the clay, and by repeated solutions and
evaporations, and the addition of potash, crystallized alum is obtained in the
usual way. This spontaneous heating, often extending to inflammation, some-
times takes place in the pits where the brown coal is worked. Between the
layers of the alum slate crystals of gypsum are often found, and large detached
crystals of gypsum occur in the clay, as in the London clay, in both cases
most probably produced by the decomposition of pyrites.
Clay ironstone is of frequent occurrence in the clay, both in the form of
layers and in detached lenticular and irregular masses. In the neighbourhood
of Rott thirteen different layers were found, varying from an inch to a foot
in thickness, and making together nine and a half feet of ironstone*. Mas-
sive portions of crystalline spathose iron have been found at Scheurn near
Rott.
C. The Brown-Coal or Lignite.
This is found in various states.
a. A dark brown or black earthy substance, friable, sometimes pulveru-
lent, generally occupying the upper part of the lignite beds, and
rarely showing a stratified structure.
b. A concreted mass, in which fragments of wood and leaves are visible,
with a mixture of earthy matter.
c. Wood in different stages of bituminization, of all shades of colour,
from light brown to black, and the latter sometimes approaching
to the nature of jet.
d. Papierkohle, highly bituminous, burning with a bright flame, leaving
a white ash, separating readily into leaves as thin as writing-paper;
a deposit of finely comminuted vegetable matter and earth.
The wood is generally in fragments of inconsiderable size ; but sometimes
large stems of trees are found, and if lying horizontal, as they usually are, very
often flattened. Trees have been met with in an upright position with their
roots attached, and the stem passing through different beds, into which the
* Noggerath, Das Gebirge in Rheinland-Westphalen, iv. 388.
450 Mr, Horner on the Geology of the Environs of Bonn.
lignite deposit is separable. Professor Néggerath mentions* two instances
at Friesdorf; in the one the tree was seven feet in diameter, and from the
beds it penetrated must have been about ten feet high; in the other the tree
was eleven feet thick, but how high could not be ascertained. At Zisselsmaar,
on the western side of the plateau, an upright mass of root and stem, of four
feet in length, was foundf. I do not, however, mention these instances as
any proof of the trees being in the situation in which they grew, for if they
were floated, the heavy root might keep them in an erect position, and the
rarity of the occurrence is a strong presumption against the idea.
The wood is sometimes so fresh, so little changed, as to have been used at
Viernich for timbers in the mines}. Pyrites is of frequent occurrence in all
the beds; and sometimes, as at Friesdorf and Holtorf, wood, in which the
texture is preserved, is highly charged with a granular carbonate of iron. A
specimen which accompanies this paper is a portion of a tree which I found
in a thick bed of lignite at Friesdorf; it was about four feet long, and a foot
and a half in diameter. The interior was converted into carbonate of iron
to the almost total disappearance of the woody texture, but this last was still
entire on the outside, where the iron was in the state of a yellow oxide. I
have mentioned, p. 446, that I found a portion of wood highly charged with
oxide of iron in the basaltic tuff of Siegburg ; and it is important to remark,
with reference to the relative age of the brown-coal formation, and the vol-
canic eruption of Siegburg, that in addition to this fact I found a specimen of
bituminized wood in the basaltic tuff identical in appearance with a specimen
which I obtained from the brown-coal beds at Geistinger Busch.
M. Von Dechen mentions that at Lieblar a lignite is found with a thin
powdery coating of amber. From the smell which this coal gives out when
burnt, the workmen call it edeler Weihrauch, frankincense.
D. Organic Remains of the Brown-Coal Formation.
These consist of vegetables, fish, insects, and reptiles: no shells of any sort
have ever been found, except in one particular spot, which I shall afterwards
notice ; and no remains of quadrupeds, except in two very doubtful cases§.
a. Remains of Vegetables.
The brown-coal or lignite beds consist of wood and of leaves, and wood and impressions of leaves
are also found in the siliceous and argillaceous beds of the formation. As the woods occur in
* Beschreibung der Braunkohlen Ablagerung auf dem Putzberge, in Von Moll’s Jahrbuch,
vol. ii. Nuremberg, 1815.
t Von Dechen, uti supra. ¢ Ibid. ~§ See Appendix V. p. 473.
Mr. Horner on the Geology of the Environs of Bonn. Abl
broken masses to which leaves are never attached, no decision can be pronounced as to the general
to which they belong more exact than that of resemblance. Faujas St. Fond, in a description of
a visit he made to the brown-coal mines at Lieblar, published in 1802, says that he obtained spe-
cimens of fruits found in the brown coal which Jussieu and other eminent botanists pronounced to
belong to the palm tribe*. The impressions of leaves are most distinct in the Papierkohle, the
sandstone and clay ironstone, and the leaves belonged, doubtless, to the stems which are associated
with them.
In sinking a pit some years ago in the clay at Bruch near Ober Cassel, there was found a bed
of fragments of silicified wood four feet thick. Professor Néggerath made a very close exami-
nation of an extensive suite of specimens of the wood from this place, in the possession of Pro-
fessor Leonhard of Heidelberg, with Mr. C. Bernhard Cotta, the author of an excellent work
on fossil woods, and the result was, that without a single exception they were all dicotyledonous.
There exist, however, in the museum of the University of Bonn, two specimens from this place of
a doubtful character. They are from three to four inches long, and about an inch and a half
thick, and are silicified. They were long imagined to be fir tops, but Professor Nees von Esen-
beck, Sen., who at the request of Professor Noggerath examined them with great care, was
of opinion that they are most probably portions of the root of a species of Fern{. Among the
specimens I obtained from this place is one in which the silicified woody fibres separate like some
kinds of glassy actinolite ; this variety is not uncommon; some are found passing into the state of
semi-opal. At Alter Roth, near Haisterbach, I found in a friable sandstone a portion of a branch
of a tree, which is remarkable in this respect, that while the form of the branch with a knot in it
is perfectly preserved, the substance of the wood has been replaced, not as in the other instances
by silica in a state of minute division, but by a somewhat coarse quartzose sand. ;
It does not appear that the vegetable remains contained in the brown-coal formation of this
district have as yet been described by any botanist of acknowledged authority. My friend Pro-
fessor Lindley has been so kind as to examine the specimens I have sent in illustration of this
paper, and the following communication from him contains the result of that examination.
‘The principal part of the impressions of leaves is in a state which renders it impossible to de=
“termine, with any certainty, the nature of the plants to which they have belonged. They consist
generally of casts of portions of dicotyledonous foliage, of so common an appearance that no one
could have determined them with precision, even if they had been newly gathered and possessed
“of all those characters of texture, surface, colour, and odour, by which a botanist would be
* obliged, in the case of such fragments, to form his opinion.
* “ On trouve quelquefois dans les mines de terre d’Ombre de Liblar, des fruits qui ont au pre-
‘* mier aspect la forme des noix ordinaires enveloppées de leur brou, mais en les examinant avec
* attentions l’on voit qu’ils en différent totalement. Les botanistes les plus exercés, tels que de
* Jussieu, Desfontaines, Thouin, aprés avoir examiné et comparé ces fruits ont trouvé qu’ils avoient
“un trés grand rapport avec les noix du palmier Areca. [Ils n’ont pas cru devoir affirmer que
“ces fruits fussent directement ceux de l’Areca, mais ils ont une opinion unanime qu’ils ont ap-
‘* partenus a des arbres du genre palmier.”—Annales du Museum d’ Hist. Nat. 1. 459.
t Die Dendrolithen in Bezichung auf ihren inneren Bau. Dresden, 1832. 4to.
t M. Alex. Brongniart says, in treating of lignite, in 1823, “On n’y cite encore aucune fougére
‘* evidente, ni aucune des feuilles ou tiges des plantes de cette méme famille.”—Dict. des Sciences
Naturelles, vol. xxvi. p. 360.
VOL. IV.—SECOND SERIES. 3N
A452 Mr. Horner on the Geology of the Environs of Bonn.
** Among them are, however, three species, the existence of which is sufficient to determine with
“certainty the relative age of the formation; and, with great probability, the nature of the climate
“of the North of Germany at the time of their deposit.
“ Messrs. Murchison and Lyell found in the tertiary formation of Aix in Provence, remains of a
« Cinnamon, and of a kind of coniferous plant called Podocarpus, figures of which are given in the
«“ Edinburgh New Philosophical Journal for 1829, p. 298. Both of these occur in the present col-
“ection, and along with them distinct traces of the leaf of some kind of Palm, which was also met
‘‘ with in the deposit at Aix.
“The Cinnamon I formerly thought identical with C. dulce, a species now inhabiting China, and
‘there is nothing in the impressions from Bonn to render it necessary to modify that opinion. At
‘the same time it must be confessed that this identification may be erroneous, and that better
“« specimens may prove it to be even a species of T'etradenia or Camphora.
“The Podocarpus was referred, with some doubt, to P. macrophylla; and if not actually that
“species, or P. coriaceus, a West Indian species, may at least be considered as certainly belonging
“to the genus.
“Of the Palm very imperfect fragments only remain. They consist of strap-shaped impressions,
“truncated at each end, with some of the parallel veins slightly thicker than the others, at rather
‘‘ unequal intervals, and also with traces of parallel ribs; the lateral veins diverge from the ribs at
‘an angle of about 40°, and are remarkably well preserved.
“Imperfect as are these data, they seem at first sight to lead to the conclusion that the climate of
“‘ Bonn was tropical at the time of this deposit, because the Cinnamon is characteristic of the Flora
‘of the Indian Archipelago; Podocarpus is found in the West Indies and at Sincapore, while the
‘Palm might reasonably be considered in its natural station in such situations,
“ But it may also be supposed, from the same evidence, that the climate of Bonn approximated
‘to that of the northern provinces of China, and the valleys of Nipal; for Cinnamomum dulce, to
‘which the cinnamon-like leaf may have belonged, is, as has already been stated, Chinese; while
“the genera Tetradenia and Camphora range as far to the north as the mountains of Nipal, and
“even Japan: and Cinnamomum itself finds its most northern limit only in the upper mountains of
“ Nipal, near the river Cosa. Podocarpus macrophylla itself has certainly been found in’ Nipal,
“and probably near Nagasaki; and although it is impracticable to determine positively from
‘such materials as we have here preserved, to what species of palm the impressions belonged, yet
“there is nothing in them at variance with the leaves of the modern Chamerops, one species of
“ which, the Chamerops Palmetto, now inhabits the South of Italy and Barbary, and another the
“valleys of Nipal.
“It may, therefore, be safely concluded that the climate of Bonn, at the period of the brown coal
“ deposit, ranged between that of the Indian Archipelago and Nipal*.”
b. Remains of Fishes.
Professor Broun}, in a paper on the fossil remains of fish, found in the papierkohle of this
district, states that he examined some hundred specimens, and that, with the exception of one, of
which the remains were very indistinct, all belonged to one species. They are usually from two
to three inches long, rarely exceed three quarters of an inch in depth, and the head forms a fourth
* See Appendix VI. p. 474.
t Ueber die fossilen Reste der Papierkohle vom Geistenger Busch im Siebengebirge, in Leon-
hard’s Zeitschrift fiir Mineralogie, 1828.
Mr. Horner on the Geology of the Environs of Bonn. A53
part of the entire length*. Nothing of the substance of the fish remains, but there is occa-
sionally a dark coaly matter marking the contour of the body: there is even no appearance of
the fragments of scales, nor of fins, ribs, vertebra, or bones of the head, but the forms of all are
impressed on the Papierkohle with remarkable exactness, and they are for the most part quite
entire. He considers them to belong to the genus Cyprinus, but to be dissimilar from any known
species, and he has named it Cyprinus papyraceus. These impressions have been examined
since that time by M. Agassiz +, and are mentioned in one of the memoirs he published, pre-
paratory to his more extensive work on fossil fishes. He confirms the opinion of Professor
Bronn, naming the species, however Leuciscus papyraceus, in conformity with a new division of
the genus Cyprinus}. Professor Bronn describes also a small crab, and Professor Goldfuss, in a
recent memoir§, says that besides this specimen of the remains of Crustacea, there are three
remarkable animals belonging to the Branchiopoda, the largest of which is more than an inch in
diameter.
c. Remains of Insects.
These and the remains of some reptiles have been described by Professor Goldfuss in the
memoir above quoted. Insects have been found in the papierkohle of Stésschen at the foot of
the Mendenberg, at Orsberg near Linz, and at Friesdorf near Bonn. Sometimes nothingr emains
but the impression of the form of their bodies ; at other times the bodies form a thin, compressed,
coaly scale, shining, and sometimes having a metallic lustre. They seem to belong to the genera
Lucanus, Meloe, Dytiscus, Buprestis, Cantharis, Cerambyx, Parandra, Belostoma, Cercopis, Lo-
custa, Anthrax, and Tabanus.
d. Remains of Reptiles.
Professor Goldfuss describes a species of Frog, Salamander, Triton, and Ophis. These were
found at Orsberg in the papierkohle. In this case, as in that of the fishes, the organized matter
has almost wholly disappeared: very perfect impressions, however, remain, not only of the
skeleton, but a dark shade in the coal marks the entire form of the animal, as in those ana-
tomical plates where the skeleton is contained in a shaded form of the entire body. After a very
careful examination, which he minutely describes, Professor Goldfuss satisfied himself that these
remains belong to an extinct species of frog, which he has called Rana Diluviana. The sala-
mander, which is about two inches long, also exhibits a structure somewhat distinct from existing
species, and he has named it S. Ogygia. So with regard to the impression of a triton, about two
inches long, and which he has named 7’. Noachicus. The remaining reptile he describes as being
of a singular nature, the specimen exhibiting the appearance of two portions of a coiled snake,
* Lord Cole informs me that he and Sir Philip Egerton obtained specimens from this place,
of impressions of a fish of much larger dimensions, and I have seen that which is in the pos-
session of Sir Philip Egerton. It is an impression of the skeleton of the tail end, and is pro-
bably not more than a half of the fish: it measures seven inches in length, and rather more than
two inches in the broadest part.
+ Untersuchungen iiber die fossilen Siisswasser Fische der tertiéiren Formationen, in Leonhard
and Bronn’s Jahrbuch fiir Mineralogie, 1832.
t+ See Appendix VII. p. 474.
§ Beitriige zur Kenntniss verschiedener Reptilien der Vornelt in the Transactions of the Kaiser-
liche Leopoldinisch-Carolinische Akademie der Naturforscher, vol. xv.
3N 2
AbD4 Mr. Horner on the Geology of the Environs of Bonn.
one of which is the end of the tail: there are no traces of bones, but there are impressions of
scales arranged in a diverging form downwards, on each side of a ridge: he calls it Ophis
dubius*.
e. Remains of Quadrupeds.
Professor Noggerath, in describing the eighteen different beds composing the brown-coal
formation at Putzberg near Friesdorf+, speaking of the ninth bed from the surface, says that there
was once found in it a large tusk of a wild boar ; and of the eleventh bed, that there was found ~
in it the bone of the leg of an ox in a very complete state of preservation, together with some
other fragments of bones. An occurrence so important in the history of this formation led me to
call the attention of Professor Noggerath to these passages in his memoir ; when he informed me
that in drawing it up several years ago he had inserted several things on the authority of others :
that he has a distinct recollection of having seen the bones in the collection of a, private indi-
vidual in Bonn, which has since been dispersed, but that he did not see them himself in situ.
Faujas St. Fond, in the memoir above quoted, says that a very old miner at Lieblar had told him
that he had fifteen years before that time found a stag’s horn in the brown coal beds.
Such is the whole result of my inquiry as to the existence of the remains of quadrupeds in the
brown-coal formation; and unsupported as the facts are by any subsequent discoveries, very
little reliance can be placed upon their accuracy. .
The sandstone clay and lignite deposits above described constitute what
may properly be termed the brown-coal formation of this district, but there
is a small local deposit which I have yet to notice, and which, if it belongs to
the same formation, is highly important as regards the question of age. In
a valley behind Godesberg lies the old monastery of Marienforst, and going
from thence to the village of Muffendorf, the path crosses the summit of the
plateau; and here, about half way between the two places, there are strewed
upon the surface of the ground small blocks of a white siliceous stone, con-
taining casts of freshwater shells, with jointed stalks of a plant. Mr. Brassard,
late keeper of the University Museum at Popplesdorf near Bonn, conceived
that he had found the rock zn sztu at the same spot where the loose blocks occur,
and I accompanied Professor Noggerath and him to ascertain whether he was
right in his conjecture, by digging round the mass. Although the ground was
cleared away for some distance, and there was an excavation made in the rock
to the depth of two feet, it is possible that it may still be only a large block.
The stone is of a dull white colour, sometimes smoke gray like flint, generally
of an earthy, but often of a crystalline translucent texture: in some places it
* Dr. Hibbert, in his History of the Extinct Volcanos in the Basin of Neumied, has given
a short account of the brown-coal formation of the Lower Rhine, which he says is drawn up from
the writings of the German geologists. He appears not to have seen the memoir of Professor
Goldfuss above mentioned, for he says, p. 86, that the brown-coal contains the remains of frogs
and lizards “ still ling”.
+ In Von Moll’s Jahrbuch, uti supra.
Mr. Horner on the Geology of the Environs of Bonn. 455
contains yellow, brown, semi-opal, not to be distinguished from that which IL
have described as occurring in the quartzose conglomerate at Tanzchen, and
like it passing into the mammillary structure of chalcedony. It contains
numerous casts of Planorbes, Lymnei, and Paludinz, and jointed stalks of a
plant. I have examined above a hundred fragments, to try to discover Gyro-
gonites, but have found none. Mr. Lyell informs me that M. Deshayes, to
whom he showed some of these specimens, found in them the three freshwater
shells above named: he said that they do not look like modern tertiary shells,
that the Planorbis appears, as far as can be determined by a cast, identical
with P. rotundatus ; that the Lymneus seems to be longiscatus, both occur-
ring in the Paris basin. The plant is described by Professor Lindley to be
fragments of dicotyledonous wood ; and, in one of the specimens, there is a
fragment of some organic body, which may have been the fruit of the palm,
of which the nucleus is left entire, and the fleshy integuments half broken
away.
This Marienforst siliceous rock has not been noticed by any previous
writer on this district, probably because it has not been long known, as
nothing of the kind exists in any other part of the district. If it had been at
one time an extensive deposit, subsequently broken up, one could hardly fail
to find fragments of it in the vast mass of gravel which covers the plateau ;
but this is not the case. Onthe other hand, I know of no rock in the ad-
joining country from which these blocks could have been derived; and had
they come from a distance, it is not probable that they would have been
confined to so small a spot. Although I do not mean to adduce it as a proof
of identity, I would point out the almost identical semi-opal found in this
rock and in the quartz conglomerate at Tanzchen. Upon the whole I am
inclined to consider this as a small local deposit belonging to the same period
as the brown-coal formation, and very possibly produced by some hot spring
in the volcanic region holding silica in solution.
The brown-coal formation is covered by a mass of gravel almost through-
out its whole extent, there being very few places where it is wanting. It is
of very variable thickness, sometimes being only a thin covering, at others
as much as eighty feet deep; and M. Von Dechen, in the memoir already
quoted, describes a mass of sand which he considers as belonging to the
gravel in the neighbourhood of Ichendorf, near Bergheim, of 125 feet in
thickness. The gravel consists of rounded fragments of grauwacke and
quartz, the latter greatly predominating, the pebbles generally small, about
the size of a walnut ; but very often large blocks, both of grauwacke, quartz,
and basalt are imbedded in it. The pebbles are united by an argillaceous
456 Mr. Horner on the Geology of the Environs of Bonn.
sand containing much iron, so that the general colour of the gravel is yellow,
very like that round London. I have never found any other fragments than
those above named in the places where I have examined the gravel, but
Professor Noggerath informs me that he has found in it trachyte, transition
limestone, and bunter sandstein. To trace the history of this vast accumu-
lation of gravel would be an interesting inquiry; but it would require a
very extensive series of observations, a minute acquaintance with the rocks
of the Upper Rhine and the adjoining lands, and an accurate knowledge of
the forms and levels of the country, before any satisfactory conclusions could
be attained.
The gravel often lies immediately upon the lignite deposit, but frequently
a bed of clay is interposed. The following section is constructed from the
description given by Professor Néggerath of the beds at Putzberg.
Ft. In.
1. Loam and marl (loess) of an average depth of ......+-.--- 55 270
2. (Gravel «cists bin oie 0 alstele wie ulelele of bie's dielv Oe skilctelele ie ols cvwleld ele 13 0
3:{ Sandy loam. ¢.. «isie\r oe ashe ictile stajaiein oro die afd cliaier Stas ots, o/s /ajejcliev fas 0 6
4, Earthy lignite and bituminized wood, lower part mixed with clay 3 0
5. Gray bituminous clay, bituminized wood, and clay iron stone... 4 6
6. Earthy lignite and bituminized wood .........-eeseeeeee oes 0 6
7. Bituminous brown clay........++ Moree liaise ofevclers weteinlemiaions.ozs 1 0
8. Earthy lignite and bituminized wood .........-e++eeee0> ees 0 6
9. Gray plastic clay «6.000 sccsdecct ns cescveccersccssecesces 5 0
10. Earthy lignite and bituminized wood........seesereesveces 8 0
11. Highly bituminous and pyritous clay .......--+++.- esevcces 5 0
12. Leafy mass; chiefly bituminized stems, branches and leaves .. TG
13. Bituminized Wood... 0.0 ccc cccccccrcccccsccenscevscvsces 1 6
14°’ Same'as INO. 10.) crderstae te eielasistete ste sl e' c's o 1c wie ove etaitle mieianaie 3 0
15, /Same.as No, 12:0 sees ee ee sie Lsla lel» cioleie\ers ale Waieletdere cletenshe 2 6
UGS Same as No. 1Ojand aie cote sacisisle <'el> inj om «14 iyi ete a eis Li
U7. Same as No. 12 sane monies treritelelalerelels's sles «)'s 01 6idiele feel iateteiete 2 6
18. Same as No. 9., bored into to the depth of ..........-eceeee- 24 0
79 6
Of which the lignite beds constitute ........ sis ole choleistte ote sheks 24 6
In most places the lignite rests upon clay, and below that come the sand-
stone and loose sand, the latter being generally the lowest. At Roisdorf, near
Bonn, the sandstone is covered by bituminous clay ; and at Frechem, near
Brihl, thick beds of clay and lignite lie upon loose sand. In many places
the sandstone occupies the surface, so that the clay and lignite have
either never been deposited upon it, or have been carried away by sub-
Mr. Horner on the Geology of the Environs of Bonn. A457
sequent denudation. At Friesdorf the clay and lignite beds rest imme-
diately upon the ends of highly inclined strata of grauwacke. I have
already noticed, p. 442. the alternation of trachyte tuff with the beds of the
brown-coal formation ; and at p. 441. I have described the occurrence at
Quegstein of trachyte tuff lying upon sandstone. I have also said, p. 443.
that basalt occurs in connexion with the brown-coal formation: the place
where this has been most distinctly seen is at Utweiler, on the north-eastern
border of the district, about four miles from the centre of the trachytic and
basaltic eruptions of the Siebengebirge, but situated in a valley between two
knolls of basalt, the Rother Hardt, nearest to it, and the Hinzberg, not very
far off. I visited this place in 1832 with Professors Néggerath and Mit-
scherlich, to see the workings in a new shaft which had been sunk to obtain
the coal. The former has lately published in Karsten’s Archiv fiir Bergbau,
&c., an account of his observations, together with some subsequently made
by M. Augustus von Strombeck, on this occurrence of basalt in the lower
ground. M. von Strombeck drew up the following account of the different
beds sunk through in the new shafts :
Ft. In.
Soil, «2... aie n pip wives bisie aise pleeo aie STORE >> 9e ipa laieep emai 4-0.pi 9.0) ¥,0)0 sp 2 6
2S LDCS 05 vc nce sw cnnerccwsereces pxspohe ioneje b =yphnbenia pinion eis seeees sis ps>.o 0 vhs ops 9 5
B. Prasat sre ncn tees ¢ owes 0.0 0 00 sete aps e]sj ols ip aie MiEate’slele aie ohe’salerote ohn ike cots] se ~ |, 30.6
The upper part consists of globular masses in some degree decomposed ; then
comes a dark gray compact basalt, containing olivine, augite, and magnetic iron
ore, but not regularly columnar.
The lower part of the mass is formed of
4, A compact bluish gray argillaceous stone, a decomposed basalt or tuff, similar to
what usually accompanies volcanic masseS......-essceeccescccscvcecsces . Les
5. Here begin the brown-coal beds properly so called; an indurated clay of a black
colour from a mixture of coal, which splits into prisms about three inches long,
and from eight to ten lines in diameter, the interstices filled with crystallized dolo-
mite; a structure probably occasioned by the heated mass of basalt covering it al
6. Dark-coloured clay, containing much coaly matter ‘and pyrites, but neither slaty
HOF COWMMMUAL . 206s. 6 oe ceeeeeseceee eveioi sie’ oe maida teidietel eaves etal covesesne 0 6
It is remarkable that this bed should show no indication of that columnar
structure which is so marked in the beds which lie immediately above and
below it. A similar fact has been observed in the Meisner.
Then come the lignite beds, consisting of
7. Black pitch coal, separating into prisms of from an inch to an inch and a half in
diameter, standing perpendicular to the face of the basalt bed, with the inter-
stices lined with crystallized dolomite .. ....ccseeceesrseesecesecesseece
This passes gradually into
8. AP mala: 0's. on Ds cls iala ole Do vec sev oesesvacece eereereee eee eeeee vee
458 Mr. Horner on the Geology of the Environs of Bonn.
x
Ft. In
9, Unaltered brown coal or bituminized wood, preserving the woody texture ....., 8 6
Total thickness of coal 13 feet 8 inches.
In the lower part of this last bed occur kidney-shaped masses of compact clay
iron stone.
58 10
Then comes a trachyte tuff, with portions of hard trachyte, into which they
had sunk to the depth of two feet. It is here the usual underlier of the
brown-coal beds, but it is also found lying between them, so that it is very
possible if the shaft were sunk deeper, that this tuff would be gone through,
and other brown-coal beds be found below it.
M. Von Dechen states* that in the district of Briihl the beds lie con-
siderably above the Rhine valley, and this seems to be equally the case on the
right bank. It is worked at several places on the right bank, but by far the
most considerable mines are on the other side of the river, and in the district
immediately around Briihl. The united thickness of the lignite beds in dif-
ferent situations in the plateau is very various, often too inconsiderable to
be worth working. It has not been ascertained by actual trial whether they
stretch quite across the plateau, the mines being situated on the east and
west sides, but this is very probably the case. The following table will show
the thickness of the brown-coal beds at different points on each side, lying
east and west of each other. The thickness includes the clay beds that may
be interposed between one layer of brown-coal and another,
West Side. East Side.
Feet. Feet.
Walberberg near Bruhl ....From 12 to 30
Wine lane reistetatetelelelalelele icles From 6 to 66 Metzmacher....-+.-scegsrscee 26 to 49
An der ‘Gabgay fyi tecciaetel. 43
Bingsdortete se cretelelete ite tetele . 364
ZISSCISTMAAL veleils 1 ste). siecle Tee 16 to 63 Hennersgrube ......ss+cereres 40 to 52
Aurich einen erevelors ieielt epee 10 to 60 Altstadter Berg” =). <1s pis cieihommt 6 to 60
Gleneler Beng elie citer teeter 18 to 70
_ Schlenderhany-6..1. ses eo 14 to 40 Frechemer Berg... 25.0005. 19 to 55
The various mines of brown-coal in the district give occupation to about
1200 persons. The coal is consumed almost entirely by the poorer classes,
as its strong peculiar odour, and sometimes sulphurous vapours, render its use
disagreeable. Some of the harder kinds are used as they are taken from the
pit; but these form a small proportion, and are, moreover, not so valuable for
fuel: the greatest part is used after it has been artificially prepared. It is
* Karsten’s Archiv, uti supra, p. 417.
Mr. Horner on the Geology of the Environs of Bonn. A59
beat and trodden after being well mixed with water, and is formed in shapes
like the crown of a small hat, which are laid out to dry like bricks, and these
when dry are preserved for use by being piled up under cover. In this state
they are called Alitten, and are sold on the ground for about nine groschen
per hundred ; and as each of the kliitten weigh about five pounds when dry,
the price is equal to about four shillings per ton *.
The beds of the brown-coal formation are generally either horizontal or
deviate only a few degrees from it. In the immediate neighbourhood of Ut-
weiler, however, under a bed of loess about fourteen feet thick, there is a se-
ries of about twenty distinct strata of clay, distinguished by various colours,
and containing four layers of lignite, each about six inches thick, which have
an inclination about 60°S. This elevation was probably occasioned by the
eruption of basalt which is in the immediate neighbourhood. On the left
bank of the Rhine, and near Brithl, near which no unstratified rocks appear,
there have been also considerable disturbances subsequent to the deposition
of the beds. At Hennersgrube, near the old monastery of Beuten, the lignite
beds are suddenly cut off by a fault to the depth of forty-nine feet}.
By referring to the Map, it will be seen that the brown-coal formation exists to a considerable
extent within the volcanic region of the Siebengebirge, especially in the valley of Haisterbach. It
is found in two small patches in Kénigswinter valley, one at a place called Kuckstein, pretty high
up in the ascent to the Drachenfels, where clay beds are found; the other in the bottom of the
valley at Quegstein and Tanzchen, as already mentioned. Here the sandstone members of the
series only occur, the quartzose conglomerate occurring in great detached masses, seemingly piled
together. These probably formed indurated portions in a deposit of sand, which has been since
washed away, as has been often noticed in sandy beds of the plastic clay and other tertiary de-
posits.
In the southern parts of this district the brown-coal formation occupies much higher situations.
The Papierkohle of Orsberg, near Erpel, which contains the impressions of reptiles and insects, is
372 feet above the Rhine ; and continuing the ascent towards Bruckhausen, there is a plateau of
about a mile square, which seems to be entirely composed of the brown cval formation. At the
very foot of the Mendenberg, at Ehl and at Stésschen, there is a very extensive deposit of lignite
on the slope of the mountain, very high above the adjoining valleys, which has long been worked
for the purpose of making alum, the clay and lignite being highly pyritous. The latter splits into
thin plates, and contains numerous impressions of leaves, and occasionally those of insects, and is
about sixteen feet thick. The beds occur close to the basalt ; and the workmen told me that they
rise towards it, but that the actual contact is not seen. It appears that formerly four different beds
eee ee ee eee eee
* The pigment called Cologne earth is prepared from an earthy lignite. It is said that a great
quantity of the light pulverulent varieties is sent to France and Holland, to be used in the adul-
teration of snuff.
t+ Von Dechen, in Karsten, uti supra.
VOL. IV.— SECOND SERIES. 30
460 Mr. Horner on the Geology of the Environs of Bonn.
of lignite were worked, separated from each other by clay and friable sandstone *. The Menden-
berg is 1198 feet above the Rhine, and the lignite beds occur within 300 feet of the summit.
Loess.
The substance to which this name is applied is a sandy calcareous loam of
a yellowish brown colour, slightly coherent, and absorbing water with great
avidity. It is a deposit which has been generally considered to be peculiar to
the Rhine valley +, and it is found, to a great extent, at detached points on
both sides of the river, from Basle to Bonn. It has not been noticed by pre-
vious writers on the district described in this paper with that attention to which
its geological importance entitles it. Loess is specially noticed by Leonhard
in his Charakteristik der Felsarten, published in 1824, who has adopted this
trivial name, given to it in the neighbourhood of Basle {; but a fuller account
of it has more recently been given by Professor Bronn§, in his description
of the environs of Heidelberg, and from which I have put together the fol-
lowing particulars.
It is found on the sides of the hills next the Rhine valley, and penetrating into the side valleys,
such as that of the Neckar, Mayn and Lahn, and occurs chiefly in those situations where the form
of the land presented a barrier against its being washed away by a descending stream. It is, for
example, more abundant near Worms and Oppenheim than near Heidelberg, because the force
of the Rhine is chiefly directed there against its right bank. It is found at various distances from
the plain of the Rhine, as much as nine miles, and it is in some places 600 feet above the level of
the sea.
One hundred parts of that near Heidelberg yielded 50 per cent. of siliceous sand, 164 of
* Von Oeynhausen and Von Dechen in Hertha, vol. xii. 1828.
+ In the synopsis of the successive deposits in the basin of Vienna, given by Mr. Murchison,
the uppermost is described to be “ Alluvial loam, called Zéss, with terrestrial shells of existing
‘‘ species, (of the genera Pupa, Helix, and Succinea,) mixed with bones of elephants of extinct spe-
“cies. The average thickness of this deposit is about 60 feet, but at some places the thickness is
“much greater.” Further, “It is greatly expanded near Krems and St. Polten, reaching occasion-
“ally the thickness of 140 feet, and having, near these places, the exact appearance of the old allu-
‘vial hillocks in the valley of the Rhine, which have been described by M. Voltz.”—Geological
Transactions, vol. iii. pp. 402, 405.
Loess is said to occur also in the valleys of the Garonne and the Allier.—Rozet, Journal de
Géologie, i. 57.
t It is mentioned by the name of Britz by Steininger in his Neue Beitrége zur Geschichte der
Rheimschen Vulkane. 1821. 8vo.
\ § Gea Heidelbergensis, oder Mineralogische Beschreibung der Gegend von Heidelberg. 1830.
See also Voltz, Uebersicht der Mineralogie der beiden Rhein-Departemente; and Rozet, Sur le
Diluvium de la Vallée du Rhin, in Journal de Geologie, vol. i.
Mr. Horner on the Geology of the Environs of Bonn. 461
argillaceous earth, nearly 32 of carbonate of lime, a trace of magnesia, and it was coloured by iron
and manganese.
In the immediate vicinity of the primary mountains it has a somewhat different character, being
more sandy, and containing mica.
The loess does not contain what can properly be called petrifactions, but a vast number of cal-
cined land-shells of living species, more usually in the upper than in the lower parts of the deposit,
and they seem to belong to particular horizontal beds. There have been found near Heidelberg
the following species: Helix pomatia, H. nemoralis, H. hortensis, H. hispida, H. ericetorum, Bu-
limus radiatus, B. lubricus, Lymneus ovatus. Some years ago, the lower part of an elephant’s tusk
was found near Weinheim, at an elevation of 100 feet above the Rhine, and some fragments of
elephants’ grinders had been previously found at a little distance from the same spot.
It is found lying on granite, porphyry, red sandstone, muschelkalk, keuper, and lias, and near
Oppenheim on grobkalk (calcaire grossier).
The greatest elevation at which I have seen loess in the district described
in this paper is near Erpel, above Orsberg, where it lies upon the brown-coal
formation, a height which is fully 400 feet above the Rhine*; and it occurs,
at about 200 feet high, near Steinsbusch, above Honnef.
A very extensive deposit of it may be seen at the Bruckersberg, near Rhondorf, immediately south
of the Drachenfels, where it forms an irregular mass from three to twenty-five feet thick, and covers
trachyte and grauwacke, as represented in the wood-cut, p. 440. It is found at Quegstein in the
valley of Konigswinter, covering trachyte tuff, and near Paffroth and Ober Dollendorf, on the slope
of the Petersberg, covering grauwacke. Between Ober Dollendorf and Haisterbach it lies upon
grauwacke, covering the summit of a ridge over which the road passes, in the side of the valley
leading to the Stenzelberg, and at Roth Kreuz, covering trachyte tuff. It is found in the narrow
valley which opens at Ober Cassel, and covering basalt at a considerable elevation on the Raben-
lei. It occurs also, to the depth of fourteen feet, near Utweiler, covering basalt. These are the
places where I have seen it on the right bank of the Rhine; but it is met with, no doubt, in many
others. On the left bank a narrow ridge of it runs in a south-east direction from Bonn for about
three miles ; and it is seen in the high bank of the river, covering the gravel of the Rhine plain,
the surface of which is deeply channelled, the loess filling up the furrows. It is seen on the north-
western slope of the Kreuzberg, in the valley between the Kreuzberg and Venusberg; in a valley
behind Godesberg, near Marienforst ; to 4 considerable extent near Lannesdorf, where very deep
clefts are cut in it; and it skirts the northern and eastern sides of the volcano of the Roderberg.
Above Rolandseck there is a quarry of grauwacke, and upon the ends of the elevated strata of
that rock lies gravel covered by loess. The basaltic columns in the quarry opposite to Unkel are
covered by it at a very great height above the river, and where it is nearest to the basalt it con-
tains rounded fragments of that rock. It is here, as elsewhere, an unstratified mass, which seems
to have filled up deep furrows and irregularities of the preexisting surface. The absence of all
signs of stratification is universal in this district. At Unkel it contains a considerable quantity of
calcareous concretions.
* Dr. Hibbert says that at Monrepos, in the neighbourhood of Neuwied, about ten miles seuth
of this spot, and on the same side of the river, loess occurs at a height of 600 feet above the Rhine ;
—History of Extinct Volcanos, &c., p. 205.
302
462 Mr. Horner on the Geology of the Environs of Bonn.
The following are the shells which I have found in it in this district: they
were named by Professor Goldfuss. Helix pomatia, H. nemoralis Linn.,
H. arbustorum Linn., H. hispida Linn., H. pulchella Drap., H. incarnata
Drap., H. glabella Pfeiff., Lymneus mimutus Drap., Pupa muscorum Linn.,
P. unidentata Pfeiff., Bulimus radiatus Drap., Clausitia obtusa Pfeiff.
Bones of Elephas primigenius and Rhinoceros tichorhinus have been found
in the loess which covers the basalt in the Unkel quarry. In that near
Lannesdorf I found a fragment of a rib belonging to an animal of the size of
a horse or ox, and I obtained from the neighbourhood of Ober Dollendorf a
few bones, which upon showing to my friend Dr. Miiller, Professor of Ana-
tomy at Berlin, he considered to belong to the lower jaw of a young individual
of a species of deer.
It is remarkable that such a deposit should be almost devoid of all vegetable
remains. ‘They are not noticed by Professor Bronn and other writers, and I
have never found any*.
Valley of the Rhine.
The Rhine, from Linz downwards, flows through a deep deposit of gravel,
with the exception of about three miles on the left bank, between Remagen
and Rolandseck, where the hills come nearly to the water’s edge, and the
grauwacke strata appear in the side and channel of the river. The gravel is
composed for the most part of grauwacke and quartz, but the former predo-
minates. It is very distinct in its character from that which covers the brown-
coal beds on both sides of the river, in which quartz is the prevailing material,
and which is usually of a bright yellow colour, from an admixture of oxide of
iron, which I have never found to be the case in the gravel of the plain, deep
sections of which are shown in pits in several places distant from the river. It
is of an unknown depth; wells which have been sunk sixty feet have not
passed through itf.
The plain which spreads out on both sides from the gorge near Rolandseck,
has by no means an uniform flat surface: there are long low ridges in the
direction of the stream, but not parallel to its present bed, which seem to indi-
cate that the Rhine, previous to the historical epoch, had occupied a different
channel from that in which it now flows: that at one time its course was very
near the foot of the ridge from Ober Cassel to Kiidinghoven, and at another
time close under the brown-coal plateau on the left bank, westward of Bonn.
The situation of Cologne, founded in the early part of the first century, proves
that it has flowed in its present course for at least eighteen hundred years.
* See Appendix VIII. p. 474. + See Appendix IX. p. 478.
Mr. Horner on the Geology of the Environs of Bonn. 463
Mineral Waters.
There are three springs of some celebrity ; at Roisdorf and Godesberg near
Bonn, and at Heppingen near Landskron, in the valley of the Ahr. They are
cold, and contain a considerable quantity of carbonic acid gas. Their con-
tents, according to analyses which have been published, are as follow :
Roisdorf*, 1°37 volume of carbonic acid gas :
Carbonate! ofisoda eajjients ato: iccctiera cliniors oierd storie’ 7°86
Sulphate Of Sodaracerpeitemssits << ep<'as ameuile « evipis 4°78
Muriate'of soda) ey .e+.5. Mictaterecst ahaa s of a) cletens 19°01
Phosphate Of SOda icicces cuscccccss cece eseees 0°06
Carbonate Of lime ntact nce cleseisie.e.s:0 «ccs oiSere ore 2°81
Carbonate of magnesia........... oh Coane we 3°98
Iron, alumina, and silica, about ............-e. 27
58°77 in 10,000 parts.
Godesberg +, about 16 cubic inches of carbonic acid gas in a pound of the water, and
Carbonate: Of sodas eparsreycvels eis: arevsyenavele oistovaletstone’s 7°00 grains.
Carbonate of magnesia .........0+0% hoon hee 3°32
Carbonate ofelime cin lelacin ofareter corsteleteterste tele sis 2°70
Miuriate, Of SOGAY si. sh<'> se els ple ls civic! hate sisi sisi otclers.g 1°33
Garbonaterof irom. pe siecle nels © seve cit CISL CRO 75
15°10 in 1 |b.
Heppingen f, 80 cubic inches of carbonic acid gas in 100 cubic inches of water, and one pound of
water yielded
Carbonate of soda ........e+++-: aetebtsies sisere sit) OF20
Carbonate of magnesia ....... s aaetsarist cher eRe isteretate 2°40
Muriate of soda ....... Mee tiie BU leiete s: 3 Soper. 3°00
Sulphate of soda....... SCO GIE O CODER eereoe 2°10
Carbonate, of lime ngeretesctels c)siefs)r1s, 01+ ofare © si slievencie ele 1°30
15°00
No mineral waters appear to have been found within the region of the Sie-
bengebirge § ; and no water from which any calcareous deposit has been pro-
duced exists in any part of the district: there seems, indeed, to be an entire
absence of limestone in any form,
* Bischof, Die Mineralquellen zu Roisdorf. Bonn, 1826.
+ Wurzer, in Harless, Gesundbrunnen in Grosherzogthum Nieder Rhein. 1826.
¢ Funke, in Harless, uti supra.
§ Harless, uti supra.
464 Mr. Horner on the Geology of the Environs of Bonn.
Of the relative Ages of the Sedimentary Rocks.
The oldest of these is the grauwacke, and, as If have already said, it has
every appearance, in the more northern part of the district at least, of belong-
ing to the latest periods of that formation. The whole series of the secondary
rocks, from the grauwacke to the chalk, inclusive, is wanting ; not a trace of
them is to be found én situ in any part of the district *.
This brown-coal formation has been hitherto held by those who believe in
the universality of tertiary formations, according to the types in the Paris ba-
sin, as belonging to the plastic clay ; but on what grounds I have not seen
stated. 'The clays, sands, sandstones, clay ironstone, pyrites +, gypsum, and .
the lignite itself, when without a recognisable organic structure, prove nothing
as to age, for all these are found in formations much earlier and much later
than the plastic clay. We can found no safe reasoning upon any other ground
than upon a comparison of the organic remains with those in other deposits.
The Flora of the several brown-coal or lignite deposits has not yet been
explored by a botanist of authority, with the exception of the short notices we
have received from M. Adolphe Brongniart. It is to be hoped that in the
future progress of his valuable general work he will direct his special attention
to this branch of his subject. In his Prodrome d’une Histoire des Végétaux
Fossiles, published in 1828, he says, “‘ From all I have yet seen I do not be-
«lieve that a single distinctly dicotyledonous leaf has ever been found in any
“formation older than the chalk. Future researches may prove the existence
“ of such vegetable productions in the secondary periods, but it is at least cer-
“tain that they are extremely rare, and that they did not begin to be very nu-
“¢ merous until the period which succeeded the deposition of the chalk.” (p. 148.)
In speaking of the lignite formation, including those of the molasse and plastic
clay, he says, “This formation is one of the richest in vegetable remains, but
“it is however very rare to find them in such a state of preservation that they
“can be determined with any degree of precision ; or they belong to classes of
* M. Alex. Brongniart has been much misinformed when he says, ‘ Les masses immenses de
“lignite terreux de Bruhl et de Liblar, ne peuvent étre placées que sur la craie tufau, qui est la roche
“« fondamentale de ce pays.” —Descr. Min. des Environs de Paris, 345; and Dict. des Sciences Natu-
* relles, art. LicnirE, p. 386.
+ M. Alex. Brongniart says, “ Les terrains thalassiques ne contiennent méme au dessus des ar-
“ giles plastiques aucun sulfure métallique en quantité notable.” — Tableau des Terrains, p. 129. Were
there no exceptions to this rule, the existence of pyrites would become a valuable document for
the determination of the ages of deposits ; but the London clay abounds in pyrites.
Mr. Horner on the Geology of the Environs of Bonn. A65
** plants in which the power of determination becomes much more difficult.’
(p. 205.) He only alludes to the brown-coal of this district, by naming among
the Palms “ Cocos Fauasi,”’ and under Monocotyledons of uncertain families
“ Endogenites ”; both from Liblar. M. Alex. Brongniart, who has entered
more fully into the subject of lignite than any other systematic writer I have
met with, both in a special article on lignite in the Dictionnaire des Sciences
Naturelles, and in his Tableau des Terrains, assigns this deposit to the plastic
clay ; but it is obvious that he has not visited the spot himself, and that what
he says about it, as well as the above notice of it by his son, is taken in great
part from the memoir of Faujas St. Fond, above quoted, who thirty years ago
visited the Liblar mine only, and in whose memoir everything that relates to
organic remains is far from satisfactory, in so far as regards observations on
the spot by the author himself.
Now although the leaves of dicotyledonous trees may settle the question of
this lignite deposit being superior to the chalk, they do not fix it to any parti-
cular epoch of the tertiary period, unless it can be shown that they have an
equally limited range ; and it has not yet been ascertained what species of di-
cotyledonous leaves are peculiar to the earlier, what to the later beds of the
tertiary series, and whether there be any common to all. So far, therefore,
the present state of our knowledge of the fossil botany of the deposits above the
chalk does not afford any sure criterion for determining the age of a bed.
The usual and most exact medium of identification, by the remains of mol-
luscous animals, entirely fails in this case; for, with the exception of the sili-
ceous mass or blocks at Marienforst, not a single shell of any description has
been found in any part of this brown-coal formation*. Now these are abun-
dant in the lignite deposits of the Paris basin, of Soissons, of those in the mo-
lasse of Switzerland, and in the great deposit in the valley of the Inn at Hi-
ring, which may be taken as types for comparison ; and, moreover, in all of
these, marine shells are more or less mixed with those of fresh water. So far,
therefore, all proofs of similarity fail; nor do we derive any aid from superior
beds, as these are entirely wanting in this district. We are thus limited to
the evidence which can be derived from the remains of fish, insects, reptiles,
and the Marienforst shells.
Although found in considerable abundance, one species of fish only has
been met with in this brown-coal formation, the Leucescus papyraceus of
Agassiz, and that belongs to fresh water. Now in none of the-great lignite
deposits above mentioned have the remains of fish of any kind been yet
* See Appendix V. p. 473.
466 Mr. Horner on the Geology of the Environs of Bonn.
stated to have occurred ; but Mr. Agassiz mentions that several species of the
genus Leuciscus are found in the beds of Giningen.
With regard to the remains of Frogs, they do not appear to have been
known to exist in a fossil state previous to the memoir of Professor Goldfuss
on those found in the papierkohle of this district; for Cuvier says, under the
head Des Ossemens de Batraciens, ‘‘ Je crois qu’il n’y a de certain que ceux
“des carriéres si problématique d’C&ningen* ;”’ and here he does not allude to
Rane. Mr. Murchison, however, in his late memoir on Giningen, when
speaking of the collection of fossils from that place in the museum at Carlsruhe,
says, “I observed specimens of Rana and Testudo.” I have had no means
of ascertaining whether the same species of Salamander exists at Giningen
with that found in our papierkohle; but Professor Goldfuss informs me that
the Salamander Ogygia is scarcely to be distinguished from the living species,
The insects in the papierkohle are another distinctive character of this
brown-coal formation, for no such occurrence has been mentioned in any of
the other great lignite deposits above alluded to, and two of those found in
the papierkohle also occur at Giningen, viz. Anthrax and Cerambyx.
It is impossible to decide whether the siliceous mass of Marienforst belongs
to the lower or the upper part of the brown-coal formation, but the quartzose
sandstones are always found in the lower part. As far as casts enable one to
decide, and these only are met with, the species Planorbis rotundatus and
Lymneus longiscatus have been made out by M. Deshayes. Mr. Lyell
enumerates them in his Tables of shells, constructed on the authority of
M. Deshayes, as occurring in his Eocene and Miocene periods, and not in the
Pliocene.
It thus appears that there is no evidence to prove that this brown-coal for-
mation belongs to the period of the plastic clay, and all the phenomena seem to
assign it to a more recent period, and they prove it to be of purely lacustrine
origin. It seems to have been deposited in a vast inland lake of fresh water, fed
by some great river or rivers, which brought the sand and clay and wood, that
subsided gradually to the bottom ; and the perfect state of preservation of some
delicate leaves shows also that the lake was surrounded by trees or shrubs.
I have been thus particular in endeavouring to fix the age of the brown-coal
formation, not only on account of the great extent and importance of the
deposit in itself, but because it affords, as I shall presently show, a criterion
for judging of the period when the unstratified rocks of the Siebengebirge
were ejected.
* Cuvier, Ossemens Fossiles, tom. v. p. 385.
Mr. Horner on the Geology of the Environs of Bonn. 467
Of the relative Ages of the Volcanic Rocks to each other and to the Sedimen-
tary Rocks.
The trachyte tuff appears to me to be the oldest of the volcanic eruptions,
for it has nothing of the character of having been derived from preexisting
trachytes, and it is traversed by a dike of trachyte, as I have described at
p. 439. This is quite in accordance with what takes place in active volcanos,
where nothing is more common than for an eruption of ashes to precede that
of a stream of lava; and it is also in accordance with what has taken place in
another part of this district, at Siegburg, where dikes of basalt traverse basaltic
tuff. The masses of solid trachyte contained in the tuff are not fragments,
but, as was observed to me by Professor Mitscherlich while we were ex-
amining together the trachyte tuff of the Konigswinter Holle, are similar to the
bombs we had found in such abundance in the ashes of the volcanos of the
Eifel, and which are of frequent occurrence in the ashes of active volcanos *.
They often, it is true, resemble, nay, are almost identical with, the trachyte of
the adjoining hills, but they are very frequently of a kind unlike any found en
masse. That there may be some secondary trachyte conglomerates is very
probable ; indeed I am inclined to consider that variety at Ober Cassel, con-
taining portions of basalt and balls of clay ironstone, as having been derived
from preexisting trachyte and trachyte tuff.
Previous writers on this district have said that they were unable to point
out any difference of age between the trachyte and the basalt. I presume,
therefore, that the dike of amygdaloidal basalt which traverses the trachyte in
the Keilsbrunnen quarry must have been only lately exposed, for that is de-
cisive of the question. Another proof of the basalt being more modern than
the trachyte is, that the trachyte tuff, except in the case of that at Ober Cassel
above alluded to, never, as far as my observations and information go, con-
tains any detached masses of basalt. There is, besides, no instance of a tra-
chyte dike traversing basalt, but many of the latter traversing trachyte tuff.
That the trachyte and basalt are later than the grauwacke requires scarcely
* Mr. Poulett Scrope in describing the trachyte tuff of the Ponza Isles (which he calls conglo-
merate,) mentions the occurrence of numerous “ fragmentary blocks” in it, and says, “ None of the
fragments are water-worn, and they all have evidently been enveloped in the base immediately upon
their ejection by the volcanic impetus.” He also shows that eruptions of solid trachyte have taken
place subsequently to the ejection of the tuff: “this rock [prismatic trachyte] bears on most points
the appearance of having forced its way upwards by cutting through the incumbent conglomerate
in various directions, and occasionally of having spread laterally over it.”—Geological Transac-
tions, Second Series, ii. 203 and 206.
VOL. IV.— SECOND SERIES. 3 P
468 Mr. Horner on the Geology of the Environs of Bonn.
to be mentioned ; the numerous fragments of it included in the volcanic rocks,
and the basalt rocks traversing it, remove all doubt. The great disturbance
of the grauwacke strata in the neighbourhood of the trachyte and basalt may
have been produced by their eruption.
It is clear that volcanic eruptions took place during the deposition of the beds
of the brown-coal formation.
Trachyte tuff covers the sandstone at Quegstein, alternates with clay and
clay ironstone in the neighbourhood of Rott and Utweiler, contains fragments
of wood at the Langenberg, and leaves of trees, identical with those found in
the papierkohle and sandstones, at Scheuern and Ofenkulenberg*. The basalt
tuff of Siegburg contains fragments of wood, bituminized and penetrated by
iron, not to be distinguished from that found in the lignite deposits. In con-
formity with what has been said of the more modern age of the basalt, we
find it at Utweiler lying over the brown-coal beds to the depth of thirty feet;
and no fragments of basalt occur in any of the beds of the brown-coal forma-
tion, as far as I have been able to ascertain. Besides the instance of alternate
beds mentioned above, the trachyte tuff in many places shows an arrangement
that could only have been produced by the materials being moved under the
surface of water.
All these facts seem to me to prove that volcanic eruptions were going on
in a freshwater lake, in the same manner as we have submarine eruptions at
the present day, during the time that the brown-coal beds were in the course
of being deposited. It is probable, however, that all the volcanic rocks we
now see were not ejected at that period, but that subsequent eruptions took
place which heaved up the Siebengebirge and the cones to the south, carrying
up the brown-coal beds along with them, in some instances, as at Stdsschen,
to the height of nine hundred feet above the present surface of the Rhine ;
the same action, probably, heaving up the plateau on the left bank of the river,
although with a less degree of force, as the basaltic outbursts on that side are
comparatively on a limited scale. The great fault in the brown-coal beds,
described p. 459, indicates a powerful and sudden disturbing force. It would
appear, also, that the great mass of gravel which covers the brown-coal beds
had been strewed over them previous to this elevation, for it is found on both
sides of the Rhine at a great height, and never in the intermediate plain, the
gravel of which, as far as my observations go, has quite a distinct character.
I have endeavoured to obtain some distinct evidence as to the relative age
vf the volcanic eruption of the Roderberg, described p. 447, the whole cha-
racters of which are very different from anything in the Siebengebirge. I
* See Appendix X. p. 478.
Mr. Horner on the Geology of the Environs of Bonn. 469
have not been able to find anything more precise than that the loess at its
base contains portions of scoriaceous basalt, and that a mass of the same gravel
which covers the brown-coal formation, occurring at the edge of the crater,
lies under a dark volcanic tuff, or indurated mud. Dr. Hibbert states that in
the road from Andernach to Frauenkirchen he saw a section where a bed of
pumice, twenty-one feet thick, lies over a fine loess from forty-five to forty-
eight feet thick, and a coarser loess eighteen feet thick: he mentions other
places, which show that the volcanos in the Lower Eifel were in activity
subsequently to the deposit of the loess, and it is probable that this was
also the case of the Roderberg*.
Of the relative Age of the Loess.
This remarkable deposit, abounding in terrestrial and fluviatile shells of ex-
isting species, and containing in many places, some of which are more than
two hundred feet above the Rhine, bones of extinct species of the elephant
and rhinoceros, rests at Bonn, as it does at Strasburg, upon a deep mass of
that same gravel through which the Rhine flows in the greater part of its
course from Basle. It is the latest deposit found in this district prior to the
commencement of the recent period.
It is difficult to conceive how it should have been produced, except by some
vast flood, which, if no elevations or subsidences of the land have since taken
place, must have been of the depth of at least six hundred feet, and several
miles in breadth, and so densely charged with mud as to leave behind, at an
elevation of two hundred feet, masses covering hundreds of acres, two hundred
and fifty miles distant from the spot where its first traces are to be seen, simi-
lar masses occurring at intervals not far asunder during the whole of that
course. That it was a sudden inundation, and that the loess was not gradually
and tranquilly deposited from stagnant water is probable, from there being no
signs of stratification, by its containing the remains of land and fluviatile shells,
and of land animals only, and by the great rarity of vegetable remains in it.
That plants and trees were not swept along by such a flood is extremely im-
probable; but they would obviously not sink in so dense a fluid, hurried along
with such a velocity as that with which it must have moved. Had there been
a gradual subsidence, not only would there have been stratification, but beds
of lacustrine and fluviatile shells, and abundance of leaves and other vegetable
remains. We must ascribe such a flood to the sudden bursting of the barrier
of a vast lake, the volume of water rushing over a great extent of land, and
* See Appendix XI, p. 478.
3P2
470 Mr. Horner on the Geology of the Environs of Bonn.
becoming charged as it rolled along with the earthy contents it afterwards de-
posited in the lower part of its course. We know that in the upper part of
the Rhine valley, between the lake of Constance and Basle, there must have
existed at one time a vast freshwater lake, where the great deposits of lime-
stone and marl at GEningen took place, forming a mass of horizontal beds,
six hundred feet thick, counting from the present bed of the Rhine. That
the discharge of the waters when these (iningen beds were laid bare was
that which brought down the loess is, perhaps, even a conjecture too hazardous
from one who has never been near the spot. To give a history of the loess in
the valley of the Rhine, by a careful examination of its composition, organic
remains, its form of deposition and levels, and to trace it, if possible, to its
source, would be a most interesting subject of inquiry, and could not fail to
prove a valuable contribution to geological science.
It was my intention to have compared this district with the great trachytic
eruptions of Hungary and Central France, but I found that to do so to any
useful purpose, I must have entered into details which would have extended
this paper beyond all reasonable bounds*.
Table of Heights.
The following heights are extracted from a Table of barometrical mea-
surements, by M. Moliere of Saarbruch, Civil Engineer, a manuscript belong-
ing to the Council of Mines at Bonn.
The measurements are in Paris feet+, above the mean height of the surface
of the Rhine at Bonn, which, according to Van der Wyck, is 193 English
feet above the level of the sea. I have classed them according to the nature
of the rock at each place.
* See Appendix XII. p. 479.
+ 1 Paris foot = 1:0658 English; so that adding th part of the height in Paris feet gives
very nearly the exact height in English feet.
Mr. Horner on the Geology of the Environs of Bonn.
Grauwacke.
Feet.
Greatest height to which it rises on south
slope of Mendenberg .......+++++ 908
Ditto between the Hummerich and Mit-
telberg wescccsescsececvees coooe 841
Ditto on west slope of Petersberg .... 658
Trachyte.
Drenkelberg .....ceecceeseeeesees 1188
Briingelsberg .....ececeecesessees 1131
WGHE Pre ae oo 0:0 + wiv nn oon vs sie ese pe asl
Scheerkopf ....... a ciaiaidin sieiaisieb\ denen eC
Bruderkunzberg ....+.-eeeseeeeeees 1022
Hlummierich ...,cecccsesssccvesscs 996
Gross Mittelberg ....+seccceseesses 936
Buckeroth ....2csceccscsssesescoes 927
Wasserfall ....ccccccccosccccsvess 919
Perlen Hardt <2 .c--cnesccedcaceess 917
Gross Rosenau .cccesscoecescesees 883
Gross Geisberg ....-.ccccoeccseee 871
Jungfer Hardt....+seeeeceeeseesee 865
Wolkenburg .....ccccccescccesess 865
Gross Breiberg ...ccccescccescceee | 846
Schallenberg ....scccccesceescecces 818
Klein Mittelberg.....ceccccseccess 199
Drachenifels...012 J scccicciceccaccicaci, 100
Stenzelberg ...sceccccssccccseceee 760
Hirschberg ..cccccscscccsesescces O19
Trachyte Tuff.
Rises to height of :
On west slope of Oehlberg ........+. 933
At Margaretha Kreuz.....seeeseees 834
On south-east slope of Geisberg...... 776
On north slope of Nonnen Stromberg.. 638
Basalt Dikes.
Keilsbrunnen, through trachyte...... 785
Lowenburg Tranke, through trachyte 949
AT)
Feet.
Between Drachenfels and Hirschberg,
through trachyte ..ssecescsceeees 443
Steinsbusch, through grauwacke...... 216
Siegburg, through trap tuff.......... 211
Wolsberg, through trap tuff.......... 230
Grimprich, through trap tuff......... 189
Konigswinter Holle, through trachyte
HEE. wiaseieternie Sietst stata/siols] sles sion) efere!« 184
Basalt.
Diisberg, neat EiMzZjecsicece sce css s we lioge
Gross Ochi bergy). sss cise claus s:> «0,0 1289
Lowenburg .cccsccccccsseesersees 1272
Mendenbergicn aie « cles aieisinicie ce nraais = 1198
Klein OchIbere “032. seis cera. s © « 974
Ley berg paar. Sat ws seine em toue een o7
Petersbers: 22.) io aie sete cists sr er 904
Nomen Stromberg)... 00.05.0000 - 818
Ober Dollendorf Hardt ............ 619
Limberg “7.12... <% Bid a ateinlntedni sts eans ooo
Grose WirlBer. Peele Sloe ewewenes O97
Steinringsberg ...s.cccccccscvess «+ 565
Hartenberg ....cscccccscccesessee 050
Gross Scharfenberg .....00000++008 560
Whomasberg .'ss0 0 ccc ceccsecccccens 541
aICMDENS /cfoiec ccntasia vee sce ets 538
Rabenlelscicct sccvccccenncssccess A420
Hinzberg ocescccciecccccens succes 429
Finkenberg, -o.0 00,016.00 010 90 selec clnle ee 210
Brown-Coal Formation.
Stoschen, at foot of Mendenberg...... 913
At village of Vinxel .....cesesee. - 400
At Orsberg, near Erpel .......++0-- 372
Between Drachenfels and Wolkenburg. 445
Auf dem Stein, near Ober Cassel, where
a bed of silicified wood was found .. 402
At Rott, where fish arefound........ 298
At Tanzchen, sandstone beds........ 226
472 Mr. Horner on the Geology of the Environs of Bonn.
APPENDIX.—Marcu, 1836.
See Page 433.
I. Page 433.
M. van per Wycx makes the mean height of the surface of the Rhine at
Bonn 188 Rheinland feet (193°6 English feet), and at Konigswinter 192
Rheinland feet (197°72 English feet) above the level of the sea. Barometer-
Hohen—Messungen des Rheinstroms, in Leonhard and Bronn’s Neues Jahr-
buch fiir Mineralogie, &c. 1835, p.260. One Rheinland foot = 1:0298 En-
glish.
II. Page 434.
From the smallness of the scale to which my map has been reduced for
publication, it is scarcely possible to define the boundaries of the several mi-
neral formations with precision. ‘Those who wish to examine the Sieben-
gebirge will do well to provide themselves with a copy of a geological map
published at Bonn in 1835 by Henry and Cohen.
III. Page 442.
M. Tuomas, in the memoir cited in the next note, mentions the occurrence
of trachyte tuff in the lane leading from Nieder Bachem to Liessem, p. 48.
IV. Page 447.
A very detailed account of the Roderberg has been recently published,
entitled Der Vulkanische Roderberg bei Bonn. Geognostische Beschreibung
semes Kraters und seiner Umgebungen, von Cart Tuomas. Bonn, 1835.
Those who wish to examine and understand the structure of this interesting
geological feature of the district should take this memoir as a guide. I ex-
tract the following particulars in this place, and I have refered to it in other
parts of this Appendix.
The highest point of the crater is 330 Rheinland feet (339°8 English feet)
above the surface of the Rhine. He estimates the longest diameter of it at a
thousand paces, and the shortest at seven hundred paces.
The lava at the north-east side of the crater was at one time quarried, in
Mr. Horner on the Geology of the Environs of Bonn. A73
the hope of obtaining millstones, like those of Nieder Mendig; but it decom-
poses readily when exposed to the air, and masses of sufficient size without
rents could not be had.
Fragments of grauwacke and of quartz are common in the lava; they are
fast imbedded in it, and their surfaces are frequently vitrified. These vitrified
pebbles are met with abundantly among the scoriz on the sides of the hill,
varying in size from a foot to the tenth of an inch in diameter. “ Any one,’
says M. Thomae, “who had not picked them up himself on the spot from
“among the brown cinders, might swear they came out of a porcelain furnace.”
p- 17. Volcanic bombs are sometimes found, and some which M. Thomae
“ broke presented the following remarkable appearance. “ Three almost per-
“ fectly round balls, the largest of which might be about the size of a man’s
‘ head, contained in the interior rapilli, small rounded portions of porous lava,
“ vitrified and non-vitrified quartz pebbles, and small fragments of grauwacke,
“some friable, others vitrified, and some unchanged. The bodies, which were
“ of the size of nuts, filled the whole interior space of the bomb ; they lay chiefly
“loose, often five or six were adhering together, or single ones were fixed to
“the sides of the bomb, so that in breaking the porous lava shell, which was
“ about a finger’s breadth in thickness, great caution was necessary to prevent
“the contents falling out. In the interior of one of the bombs there was a
“‘ small detached crystal of augite.” p. 21.
V. Pages 450 and 465.
In Leonhard and Bronn’s Neues Jahrbuch fiir Mineralogie, &c., for 1835,
p. 678, there is the following communication from Professor Noggerath to
the Editors. ,
“ Bonn, 30 October, 1835.
“Hitherto no shells have been found in our Rhenish brown-coal. Recently
“‘ some freshwater shells were brought to me from a bed which seems to be in-
“termediate between earthy brown-coal and bituminous (brown-coal) clay.
“'This bed, which is of inconsiderable thickness, covers the alternations of
“‘ compact clay ironstone, which occur near Rott, eastward of the Siebenge-
birge, an account of whichis given in my Rheinland Westphalen, iv. p. 388.
“« You will see by the specimens sent herewith that the shells are changed into
“a kind of brown-coal, and are almost quite flat. If M. Bronn will venture to
“‘ pronounce an opinion upon these, I should wish you to insert it along with
“this notice in your journal.”
M. Bronn adds, “ All these shells belong to the genus Planorbis, but they
“are so crushed as to be almost wholly unrecognisable. The largest and best-
ATA Mr. Horner on the Geology of the Environs of Bonn.
« preserved specimen nevertheless appear to be Planorbis carinatus ; the rest
‘seem to belong to the same species.”
VI. Page 452.
I visited the lignite deposit at Friesdorf in September 1835, in company
with Mr. Robert Brown, when he collected several specimens of the vegetable
remains. He informs me that all the wood he found is coniferous, which,
taken along with the evidence derived from the leaves already noticed, might
point rather to a temperate than an equinoctial climate.
VII. Page 453.
M. Agassiz examined the specimens accompanying this paper, in a late
visit to England. Besides the Leuciscus Papyraceus, he found another spe-
cies, which he named Leuciscus Macrurus.
VIII. Page 462.
Since this paper was read, J have seen the loess in three situations, which
are remarkable as connected with the geological events which, in compara-
tively recent times, have occurred in this district.
I learned in the summer of 1833, that, in the preceding spring, the pro-
prietor of the farm in the bottom of the crater of the Roderberg, in sinking a
well near his house, had passed through a bed of loess. I went there, accom-
panied by Mr. Lyell, and we ascertained that, after a few feet of scoriz, they
had found loess, and had penetrated it to the depth of 62 Rheinland feet
(632 English feet), but without passing through it. Part of that which had
been dug out was on the ground near the well, the rest had been scattered
over the adjoining field. It had the usual characters, and several of the cal-
careous stony concretions were lying about.
In the left bank of the Rhine, a short distance below Neuwied, and near
Andernach, I observed the loess lying under a bed of volcanic scorie, and that
covered by a considerable thickness of alluvial soil.
On a visit to the Laacher See in September 1835, I observed a section close
by the edge of the lake, and within a quarter of a mile of the monastery,
where loess, containing its characteristic shells, is covered by a succession of
beds of volcanic sand, scoriz, and pumice, and altered fragments of grau-
wacke.
In a paper on the solid contents of the Water of the Rhine, which was read
before the Geological Society in March 1834, and published in the London and
Edinburgh Philosophical Journal for January 1835, p. 102, I showed that the
Mr. Horner on the Geology of the Environs of Bonn. 475
sediment obtained from a large quantity of the water has the same appearance,
and is of the same composition as loess.
In the Edinburgh Philosophical Journal for July 1834, there is a paper by
Mr. Lyell on this peculiar deposit: he has treated of it very fully in his
“Principles of Geology,” vol.iv. p. 44, 4th edition; he read some addi-
tional observations upon it at the Geological Society in December 1835, an
account of which is given in the Society’s “ Proceedings,” vol. ii. p. 221, and
he again refers to it in his Address at the Anniversary of the Geological Society,
in February, 1836. M.Thomae, in the work above cited, has recorded several
interesting facts respecting the loess which lies around the Roderberg. We
learn, from the observations of these gentlemen, the following particulars in
addition to those mentioned in my paper.
Of the shells found in the loess near Bonn the terrestrial predominate
greatly over the aquatic; the same rule holds good, though not to the same
extent, with respect to the shells now drifted down by the Rhine, and con-
tained in the mud and sand of its shores; and the greater proportion of these
last agree specifically with those buried in the loess.—Lyell, Memoir of 1834,
p. 3.
The loess absorbs water with great avidity, and where exposed to the action
of water is often carried away in great masses. It affords a very fertile soil ;
but the husbandman is sometimes doomed to see his hopes blasted by a violent
storm of rain washing away the whole soil from his field, laying the roots of
his vines bare to the sun.— Thomae, 26.
On the east side of the Roderberg there are five round-back ridges, co-
vered with vegetation, which seem to radiate from the lower part of the hill
towards its base. ‘These are composed of loess; and, at their inferior ex-
tremity, are in some places laid open, exhibiting a vertical section from twenty
to thirty-five feet in height, resting upon a mass of gravel, identical in com-
position with that forming the present bed of the Rhine, and from four to eight
feet in thickness. —Thomae, 29—31.
“On the north-north-west side of the Roderberg a valley separates the
volcano from the Zilliger Haidchen, heathy hilly ground composed of loess,
which is furrowed in several places to a great depth. ‘These excavations are
called in German schluchten, meaning hollow ways. In some of these the loess
is seen to be intermixed with volcanic products, and containing detached ac-
cumulations of scoriz in amorphous masses. In several places there are con-
tinuous beds of scoria lying upon and covered by loess. In one of the
schluchten a section is exposed, exhibiting alternate layers of scorie and tuff,
resting on the fundamental grauwacke, and covered by loess; in another a
VOL. IV.— SECOND SERIES. 3 Q
A76 Mr. Horner on the Geology of the Environs of Bonn.
volcanic breccia, composed of fine blackish grey sand, including small frag-
ments of clay slate and grauwacke five feet thick, rests upon loess, and is
covered by another deposit of loess fifteen feet thick, identical in composition
with the lower deposit. The flat surfaces of the slate and grauwacke frag-
ments, and numerous scales of mica, lie horizontal, producing a slaty structure,
and indicating their having assumed that position under the surface of water.
The schlucht, which opens towards the village of Lannesdorf, exhibits a
similar intermixture of scoriz in the loess, and it is about two miles and a half
distant from the crater of the Roderberg.—Thomae, 36—A43.
I shall now point out some of the more important observations of Mr. Lyell
on the loess in the higher parts of the Rhine valley and the adjacent country,
contained in the memoirs above mentioned, which throw light on the history
of this remarkable deposit.
He observed it near Andernach, alternating with volcanic scorie, &c.,
and in one place ‘‘ covered with beds of pumice, trassy pumiceous sand,
and small dark volcanic cinders, forming upon the whole a mass from ten
to fifteen feet in thickness,”—ejections from the neighbouring volcanos of
the Lower Eifel. In an excursion through part of the duchy of Darmstadt
by Mayence, Oppenheim, Alzey, Flonheim, Eppelsheim, and Worms, he
found the loess spread almost everywhere over the country. On the oppo-
site side of the Rhine, in the elevated table land above the Bergstrasse be-
tween Wiesloch and Bruchsal he observed the loess attaining a thickness of
200 feet. Near Strasburg large masses of it are seen at the foot of the
Vosges mountains on the left of the great plain of the Rhine, and at the base
of the mountains of the Black Forest on the other side. It occurs in con-
siderable force at Basle, and still higher up the Rhine at Waldshut, and
it is said to terminate between that place and Schaffhausen. In the hills
called Bruder Holz, about two miles south of Basle, it rests upon nearly
horizontal beds of molasse, and it has here an elevation of more than 1100
feet above the sea, which is more than 900 feet above that ridge of loess that
stretches between Bonn and Riungsdorf. In a section exposed at Bruder
Holz, he found the usual terrestrial and aquatic recent shells, and along
with them two vertebra, which M. Agassiz says belong decidedly to a small
species of the Squalide, or Shark family, perhaps to the genus Lamna. Mr.
Lyell has been so good as to allow me to have figures taken of these organic
remains, the first ichthyolites hitherto found in the loess and so remarkable in
a freshwater deposit*. |
* See Plate XXIX.
Mr. Horner on the Geology of the Environs of Bonn. ATG
Ascending the valley of the Neckar, he found a section near the Manheim
gate of Heidelberg, exhibiting alternating layers of loess and gravel, to the
thickness of 12 feet. He saw it near Heilbronn at an elevation of 500 feet
above the level of the sea, and was informed that it lies on the hills in that
neighbourhood, 300 feet higher. Further up the Neckar, at Canstadt, near
Stutgardt, it overlies a freshwater formation of tuff travertine and marl, and
south-east of Stutgardt, between Géppingen and the little watering-place of
Boll, he found it in a valley watered by a small tributary of the Neckar.
From Géppingen his route lay eastward hy Weisenstein and Heidenheim to
Nordlingen, and between Weisenstein and Heidenheim he crossed elevated
land, on the west side of which the waters flow to the Rhine, on the east to
the Danube, and eastward of this ridge no more loess was to be seen.
Returning again to the tributaries of the Rhine, in proceeding westward
from Bamberg in Bavaria, he found the loess at Dettelbach, a small town on
the Mayn, eastward of Wiirtzburg ; and not only in the valley, but on the
neighbouring hills of muschelkalk, at a height of five or six hundred feet
above the valley. It was here of a somewhat redder tint than in Wiirtem-
berg, and Mr. Lyell conjectures that the colouring-matter may have been
derived from the neighbouring red bunter-sandstein. Lower down the
Mayn, he again saw the loess at Hochst below Frankfurt, and at Soden,
where it abuts against the elevated grauwacke ridge of the Taunus.
Crossing the Taunus to the valley of the Lahn, he again found the loess at
the village of Elz near Limburg. ‘On the north of this village,” he says,
“is a hill, which forms one boundary of the valley of the Lahn, and here
loess is seen with all its usual characters, with many land and freshwater
shells, and alternating, as at Heidelberg, with gravel. I observed, in par-
ticular, a horizontal layer of white quartz pebbles, a foot and a half in thick-
ness, resting on a mass of loess fifteen feet thick, and covered by loess five feet
in thickness, the loess, in both situations, including in it entire shells. Follow-
ing the road, I found the slope of the hill above to consist of horizontal beds
of quartz pebbles, which have a base of loess. Hence it appears that the valley
of the Lahn, which is excavated through highly inclined greywacke, has, at
some period since its excavation, been partially filled up with beds of gravel al-
ternating with loess, a great part of which has since been removed by de-
nudation.”’
It is material to observe that all the above-mentioned places, where Mr.
Lyell observed the loess, have a direct communication with the main valley
of the Rhine ; that is, form part of one hydrographical basin. The quantity
left bears but a small proportion to the mass which we must suppose to
3Q2
478 Mr. Horner on the Geology of the Environs of Bonn.
have been originally deposited. It has been shown that the great avidity
with which it absorbs water, renders it liable to be easily washed away ;
and accordingly, wherever it is not protected by the form of the land, or by
a dense covering of vegetation, it is carried off by every shower; and this
is in a great degree the cause of the yellow colour and the muddy state of
the Rhine after heavy rains.
IX. Page 462.
In a gravel-pit near Bonn, I found a tooth of the Ahinoceros tichorinus.
The gravel is not that yellow alluvium which lies over the brown-coal forma-
tion, but resembles that of the present bed of the Rhine, and which I have
shown to be older than the loess.
X. Page 468.
Trachyte tuff is intermixed with the upper beds of the brown-coal forma-
tion in the lane between Nieder Bachem and Liessem, on the left bank of
the Rhine.—Thomae, p. 49.
XI. Page 469.
We have seen that from the volcanic focus of this district, limited though
it be in extent, products have been erupted which differ very much in their
nature, and that these different products must have been ejected at distinct
periods. The trachyte tuff appears to have been the first eruption, then
trachyte, then basalt, and lastly, the lava and scoriz of the Roderberg, which
resemble the ejections of the neighbouring Eifel, and partake very much of
the characters of those of active volcanos whose productions have more of an
augitic than a felspathic nature.
That there was an eruption from the Roderberg subsequently to the com-
mencement of the deposit of the loesss, is proved by the thick beds of scorize
which are incumbent upon loess near Lannesdorf; and that it had become
extinct prior to the termination of that particular deposit is shown by beds of
loess covering the volcanic ejections, and still more conclusively by its accu-
mulation to so great a depth in the very bottom of the crater; for had the
volcano been subsequently in activity, the loess must have been blown into
the air. That the edge of the crater must, in part at least, have been under
the surface of the water which transported the loess, is manifest, and that
collected at the bottom is probably the amount of the solid contents of the
fluid which filled the cavity. All the phenomena seem to lead to the con-
clusion, that the Roderberg was a subaqueous eruption during the period of
Mr. Horner on the Geology of the Environs of Bonn. A79
the loess, and that it was subsequently raised up gradually, en masse, into its
present position.
XII, Page 470.
The additional facts which have come to my knowledge since this paper
was read, the most important of which are narrated in the preceding notes,
have led me to modify in some degree the opinions I had formed relative to
the history of the loess.
Its origin remains as uncertain as before; but it is very evident that it
came from above Schaffhausen ; and as it is so uniform in its nature through-
out, with the exception of the somewhat redder tint of that at Dettelbach on
the Mayn, which may have been produced by some local intermixture, it is
fair to presume that it was derived from one source.
Do its characters indicate that it was brought down by the water of the
Rhine, and was deposited gradually during a long period ; or, that it sub-
sided in a vast lake, into which the Rhine then entered, as the Rhone now
does into the lake of Geneva, and whose waters ran up into all those sinu-
osities of the land where remains of the deposit are still to be found? or, do
they point to the sudden rush of a muddy torrent, occasioned by the bursting
of a barrier which drained a vast lake, as I have already suggested ?
The generally homogeneous unstratified nature of the loess, even though
in masses between 200 and 300 feet in thickness, always appeared to me to
be strongly presumptive evidence that it was deposited from a flood of water
densely loaded with mud, and moving with a velocity sufficient to transport its
solid contents to a distance so great as that from Basle to Bonn, before they
had time to fall to the bottom ; but the alternations of loess with gravel in the
valleys of the Neckar and the Lahn, and with volcanic ejections around An-
dernach, the Laacher See, and the Roderberg, show that, if it was a flood,
there must have been more than one.
Were the idea of a lake at all admissible, there would be nothing extra-
vagant in supposing that the loess near Basle, which is more than 1100
feet above the level of the sea, and that of Bonn, which is less than 200
feet, might have been deposited in one and the same lake ; for it is only sup-
posing the water at the latter place to be 900 feet deep; and the lake of Geneva,
according to Mr. De la Beche, is in some places 984*. But if the loess
were a gradual deposit from the waters of a lake, there would surely have
been indications of successive layers in the structure of the loess itself; the
shells would have been found more frequently in something like a similar
* Manual, 3rd edit. p. 22.
480 Mr. Horner on the Geology of the Environs of Bonn.
mode of arrangement, in place of being scattered, as they generally are,
without order through the mass; and vegetable remains would not have
been entirely wanting ; or so rare, if they do exist. ‘Then there must have
been a barrier to contain the waters of the lake, at the head of the delta of
the Rhine near Bonn, and that barrier must have been wholly swept away ;
but a country with forms more unlike those which we might expect, had
such a barrier ever existed, can hardly be imagined.
All the appearances of the Rhine valley favour the supposition that, at the
time of the deposit of the loess, there was a free river communication be-
tween Basle and the sea, and the vertebra of the Lamna certainly render that
supposition more probable. ‘It may seem very extraordinary that the first
remains of fossil fish obtained from this freshwater silt should belong to a
marine genus, but M. Agassiz has informed Mr. Lyell that both in the Se-
negal and the Amazon certain species-of the Shark and Skate families (Squa-
lus and Raia, Linn.) have been known to ascend to the distance of several
hundred miles from the ocean, and analogous facts are referred to in Mar-
grave and Pisa’s Natural History of India *.”’
In a work descriptive of Bonn and its neighbourhood +, there is the fol-
lowing statement. ‘The chronicle of Bonn further informs us of a visit to
“our river from an animal of the remote north; a sea monster, whose appear-
“ance may be brought forcibly before our imagination by the steam-boat of
** modern days, as it works its way through the waters of the Rhine. In the be-
*‘ ginning of the year 1680, a Sea Cow, or Walrus, more than fourteen feet in
“length, was seen swimming up the Rhine past Bonn. A violent and unheard-
“ of agitation of the water was observed, accompanied bya loud noise, and by
“ two lofty jets of water spouting from the forehead of the monster. The whole
**town rushed to the river to see the great beast, the very name of which was
“then unheard of bythem. The centinel on the Alten Zoll fired at it several
‘times but missed it, and the animal proceeded on its way upwards undis-
“turbed, and is said to have got above Strasburg. ‘Two months afterwards, it
“‘was cast ashore dead, near the village of Niel, about three miles below Co-
*‘logne, with four wounds from bullets below the head ; but it was not known
“by whom or where it had been killed.”’
In the present imperfect state of our knowledge, there seems to be no
explanation, upon the whole, so rational as that suggested by Mr. Lyell in
the Address above alluded to, who says, “ Instead of supposing one continuous
* Geological Society’s “ Proceedings, ” vol. ii. p. 222.
+ Hundeshagen, Die Stadt und Universitit Bonn am Rhein, mit ihren Umgebungen. Habicht,
Bonn, 1882, p. 15.
Mr. Horner on the Geology of the Environs of Bonn. 481
“lake of sufficient extent and depth to allow of the simultaneous accumulation
“ of loess at all heights and throughout the whole area where it now occurs, I
“ conceive that subsequently to the period when the countries now drained by
“the Rhine and its tributaries, acquired nearly their actual form and geogra-
“ phical features, they were again depressed gradually by a movement like that
“now in progress on the west coast of Greenland. In proportion as the whole
«« district was lowered, the general fall of the waters between the Alps and the
“ ocean was lessened, and both the main and lateral valleys, becoming more
“ subject to river inundations, were partially filled up with fluviatile silt con-
“ taining land and freshwater shells. After this operation, when a thickness of
“many hundred feet of loess had been thrown down slowly,and in the course of
“many centuries, the whole region was once more upheaved gradually, but
“ nerhaps not equally, throughout the whole region. During this upward move-
<«‘ ment most of the fine loam was carried off by denudation to such an extent that
_ the original valleys were nearly re-excavated. The country was thus restored
* toits pristine state, with the exception of those patches of loess still remaining,
“and which, from their frequency and their remarkable homogeneousness of
“composition and fossils, attest the original continuity and common origin of
“the whole. By introducing such general fluctuations of relative level, we may
“dispense with the necessity of erecting and afterwards removing a great
“barrier more than 1200 feet high, sufficient to exclude the ocean from the
“valley of the Rhine during the accumulation of the loess.”
Sweden has afforded the most unequivocal proofs that upward and down-
ward movements of the land may take place in countries where no ordinary
volcanic action is to be seen ; and that so gradually, as to be imperceptible to
all who are not watching the phznomenon : and, as there are so many in-
dications of volcanic action in early times, on both sides of the Rhine valley,
it does not seem to me to be stretching theory beyond the limits of just phi-
losophical reasoning, to suppose that such oscillations may have taken place in
this district, during the gradual accumulation of the loess, and subsequently to
its deposition.
END OF VOL. IV.
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AARAU, pisolitic iron ore of, 350.
Afton Down, Isle of Wight, section at, 200.
Agassiz, M., on the fishes of the Wealden, 180.
, examination of Mr. Horner’s speci-
mens of fishes from the environs of Bonn by,
474,
Aketon, notice of carboniferous rocks within area
of new red sandstone near, 393.
Aldbury, Shropshire, account of section of new
red sandstone near, 400.
America, deposits in lakes of, compared to the
Wealden, 325.
Ammonites, fragment of, found in the Weald clay,
Isle of Wight, 205.
Amygdaloid of the Dukhun described, 423.
, remarkable varieties
of, 424.
Anticlinal lines in Kent and Surrey, 142, 143, and
note.
in South Wiltshire, 244.
- in the vicinity of Bristol, 244, note.
Aptychus: see Trigonellites.
Aqueous action, degradation by, of the solid por-
tions of the earth, in a certain sense constant, 67.
Araucaria, cone approaching to, found on the
shore of Portland Island, 349.
Argillaceous deposits of brown coal formation in
the environs of Bonn described, 448.
Arkendale and Swaledale, general account of me-
talliferous hills between, 94.
Arran, observations on red sandstone systems of,
402,
Axes of coal fields of Bristol Channel, not parallel,
57.
Aylesbury Vale, strata of, 284.
B.
Babington, Mr., on trap in the Mysore referred
to, 429.
Bacon-hall, near Lulworth Cove, good section of
the lowest Purbeck strata there, 223.
Barbon coal-pits, section in shaft of, 76, note.
“ Bargate-stone ” of Surrey, a calcareous conglo-
merate, 146.
Barkin to Casterton High Fell, notice of section
from, 95,
Barker, Mr., on chalk in Rutlandshire, 308, and
note.
Barrowmouth, notice of new red sandstone series
near, 395, 396; of magnesian conglomerate,
395.
Barytes, sulphate of, found near Caxton, 306, note.
— in the Fuller’s earth of Nutfield, 141.
Basalt of the environs of Bonn described, 443-
445,
, age of, with re-
ference to the trachyte, 467.
, ho fragments of,
found in the brown-coal deposit, 468.
Dukhun, varieties described, 414—
423,
en boules, very
generally diffused, 417.
» resembles
that of the Solfatarra, 417.
oe ees a » columnar, 414,
» remarkable
natural pavement of, at Singhur, &c., 416,
———, compact, of a
green colour, 422.
—E———————— ——— Statesand
other pieces of sculpture formed of it, 422.
3R
484
Basalt of the Dukhun, extraordinary heaps of
loose masses of, described, 421.
—-— dykes in the Dukhun described, 418.
— in general transversely prismatic,
——_——_—-, remarkable one at Hurreechun-
durghur described, 418.
—_———-—— common in the Siebengebirge, 445.
Basterot, M. De, on the vicinity of Folkstone, 106.
Baw Fell, notices of structure of, 88, 96.
to the Howgill Fells, account of section
from, 96.
Beaumont, M. Elie de, reference to his memoir on
the boundaries of the Paris and London basins,
530.
Beck, Dr., of Copenhagen, on a deposit in the
Isle of Bornholm containing plants like those
of the Wealden, 330.
Bedfordshire, beds below the chalk in, 269.
—_—_—__-—_____—___,, fossils of, 296, 316.
Belemnites, enormous deposits of, in the lias in
Dorsetshire, 31.
Bell, Thomas, Esq., F.G.S., observations by, on
a new fossil species of Chelydra, 379.
Bembridge Down, Isle of Wight, section at, 187.
Ben How Quarry, notice of, 396.
fault by which it is
traversed, 396.
Benett, Miss, Cycadedidea procured by, from
Tisbury, 15.
ee » notice of catalogue of Wiltshire
fossils by, 255, 256, 257.
——, specimens of gum or resin ob-
tained from the gault near Crockerton, 257.
Bere Head, Devon, section of the coast at, 234.
Berkhampstead, Vale of, its general altitude, 283.
Berkshire, beds below the chalk in, 269, 270, &c.
Berthier, M., analysis by, of green particles, 109,
note.
Birds, bones of, found in the Hastings-sand at
Tilgate, 180; distinguished from those of Pte-
rodactyles, 382*,
Bishopstone, near Aylesbury, section at, 287.
Black glossy slate of Cumberland contains no
organic remains, 48, 66; probable cause of
their absence, 66.
INDEX.
‘«‘ Black land”, Gault so called, in Surrey, 141.
Black limestone group between Kirby Stephen
and Penigent described, 73.
distinguished by regu-
larity of stratification, 73.
—— —
, organic remains found
yields a fine black marble,
where found, 73.
Blackdown Hills, Devonshire, description of, 235.
, fissures from dislocation at,235.
——,, list of quarries
, Sithestone pits, section of, 236.
, Sithestones, mode of preparing,
2318
Blackdown-sands, list of fossils from, 239.
—_—____—__———,, fossils of, well preserved, why,
238.
» principally converted into
chalcedony, 239, note.
Blackgang Chine, Isle of Wight, section at,
194.
Blackstone Edge, notice of great saddle of mill-
stone grit at, 60.
Boblaye, M., notice of his memoir on the beds
below the chalk in the North-west of France,
330.
Bonn, Leonard Horner, Esq., on the geology of
the environs of, 433.
, district little known to geologists, 434.
, general structure of the environs of, 435.
» grauwacke, 436.
——, trachyte, 437.
——, basalt, 443; volcanic eruptions, 446.
— —., brown-coal formation, 447, 473.
, loess, 447, 469, 474, 479.
——, mineral waters, 403.
, relative ages of the sedimentary rocks of,
464.
the volcanic, 467.
——_——$<_$—_——___—______ volcanic rocks to each
other, 467.
, table of heights, 471.
——, Appendix, 472.
————-— to
INDEX.
Bornholm, Isle of, affords plants like those of the
Wealden, 330.
Bothenhampton and Bridport Harbour faults, 40.
Boughton quarries, in the lower green-sand, 132.
» remains of Iguanodon found at, in-
cluding new portions of the skeleton, 132, note.
Boulonnois, strata connecting the Kimmeridge
clay with the Oxford oolite, well disclosed on
the coast of, 332.
, Portland-stone in, 326.
, nodules of grit in the Portland sand,
283.
Bowstead, Rev. James, notice of his observations
on the north-eastern demarcation of new red
sandstone series in Cumberland, 384, note.
Bray, Pays de, (near Beauvais, ) equivalent in, of the
Wealden, 326.
Portland-stone, 328.
a of the
Portland-sand, 328.
Breccia, in Dorsetshire, accumulations of, analo-
gous to those of Normandy, 8.
of the
, tertiary, siliceous accumulations of, in
Dorsetshire, described, 5.
Bredy, physical features of the Vale of, 32; geo-
logical structure of, 32.
Bridport, occurrence of oolitic breccia near, 31.
—— Harbour and Bothenhampton faults,
40.
Brill, Bucks, strata at, 279, 280.
Bristol Channel coal fields, axes of, not parallel,
Dive
, elevation of the car-
boniferous system of, less than that of the
North, 59.
, form and direction of
dislocations in the, have little resemblance to
those in the North, 58; disturbing action pro-
bably not contemporaneous, 58.
which
gave final configuration to, probably posterior
to deposition of lower new red sandstone, 58.
——_—-—., movements
Bristol coal-fields, overlying deposits of, analogous
to series in the North of England, commencing
with magnesian conglomerate, 58.
A85
Bristol Institution, collection of Blackdown fossils
belonging to, 239.
Broadfield, notice of a mass of carboniferous lime-
stone within the area of new red sandstone,
near the middle of, 391.
Brongniart, M. Adolphe, on Cycadedidea, 218.
——_—_—————— on the fossil plants of
Hoer in Scania, 330.
Brook Chine, Isle of Wight, section at, 194, 200.
Brough, account of the fault near, 62.
, coal measures near, sometimes resemble
new red sandstone in colour, 387, and note.
, new red sandstone conglomerate near,
described, 385.
Brown coal formation of the environs of Bonn, 447.
le
scription of the argillaceous deposits, 448.
———--——_—— .,, of
the siliceous, 448.
oo HOt
the lignite beds, 449.
—-= more
recent than the plastic clay, 466.
——_ — — —, its
age a criterion of the period of the ejection of
the unstratified rocks of the Siebengebirge,466.
, thick-
os
ness of, near Brihl, 458.
— —— ——
exists
extensively in the volcanic region of the Sie-
bengebirge, 466.
— —
» vege-
table remains of the, examined by Prof. Lin-
dley, 451.
> ore
ganic remains of described, 450; vegetables,
450-452, 464; fishes, 452; insects, 453; rep-
tiles, 453; quadrupeds, 454.
eS ee
ie
see
Lignite.
Broun, Prof., fossil fishes in the brown-coal for-
mation of the environs of Bonn described by,
452.
Brown, Robert, Esq., his specimens of vegetable
remains from the lignite of Bonn, referred to,
474.
3R2
486 _ INDEX.
Brown, Robert, Esq., silicified wood of Portland
examined by, 222.
, examines a cone approach-
ing to an Araucaria, from Portland, 349.
—, his observation respecting
the Conifer and Cycadee of Portland,
225%
Buchanan, Dr., referred to, on various points of
Indian geology, 420, 427, 429, 430.
Buckinghamshire, beds below the chalk in, 269.
, fossils
of, 296.
Buckland, Rev. Dr., on bones of the Iguanodon
near Swanage, 207.
, on Cycadee in the Dirt-bed
of Portland, 14, 218.
, notice of his memoir on the
Valley of Elevation in North Wiltshire, 263.
Buckland, Rev. Dr., V.P.G.S., and De la Beche,
H. T., on the geology of the neighbourhood
of Weymouth, 1.
, paper referred to,
217, 233.
Burrels, notice of new red sandstone conglome-
rate near, 386.
C.
“ Caillard,” or crow-limestone, description of, 74.
owes its existence
to shells, 75.
Caithness schist, proved to belong to the old red
sandstone, 402, 406.
, ichthyolites of, placed on the pa-
rallel of the Herefordshire cornstones, 404.
Calcareous grit formation, near Weymouth, 25.
Calcareous slate and limestone, band of between
the green slate and grauwacke of Cumberland,
described, 49; range of, 50.
eee , faults which affect
it, 50, et seq.
Se ——— generally
marked by valleys, 52.
» Notice of the for-
mations associated with, 48.
—— ——, order of
their succession, 48.
Calcareous slate and limestone of Cumberland,
order of beds associated with, first determined
by Mr. Otley, 48.
sometimes passes into strong beds
of limestone, containing many fossils, 68*.
the limestone breaks with faces
parallel to the cleavage of the slates, 68*.
exhibits without exception true
cleavage planes, 68*.
lines of stratification often almost
obliterated by the cleavage planes, 68*.
, cleavage planes dip N. W., 68*.
sometimes strike
with the beds, sometimes obliquely, 68*.
——— nowhere coin-
cide with the planes of the beds, 68*.
rs cut off by Shap granite and por-
phyry, near Wastdale Head, 54, 68*.
_—— reappear as calcareous conglo-
merates imbedded in greywacké, 68*.
Calder, Mr., referred to on points of geology of
India, 419, 426, 428.
Cambridgeshire, beds below the chalk in, 303.
$$ —___ _—____. ; fossils
of, 316.
Cam Dod, top of, a peat moss, 91.
Cam Fell, nature of beds forming flanks of, 91.
Candern in the Brisgau, marine beds there, sup-
posed to be coeval with the Wealden, 330.
“Cap”, a remarkable bed in the lower Purbeck
strata, so called, 222.
, section of, at ‘* Bacon-hall”, 223.
Carbonaceous shale and fissile gritstone, group
consisting of, described, 75.
, subdi-
visions of, 75,
contains
a bed of coal, 75.
Carbonate of lime, fibrous, in the Purbeck beds
on the coast of Dorset, 11.
Carboniferous chains of Cumberland, Professor
Sedgwick on the dislocations which have sepa-
rated them from the Cumbrian mountains, 47,56.
, physical
features of, contrasted with those of the slate
district, 47.
INDEX. 487
Carboniferous formations of the North of En-
gland, deposited during a long period of com-
parative repose, 56.
Sanne succeeded by one distin-
guished by remarkable convulsions, 57.
effects of, 57.
—_—--————— first elevation of, suc-
ceeded by the deposition of lowest members of
new red sandstone, 58.
movements which gave
the chief impress to the, anterior to principal
dislocations of the south-western coalfields, 58,
59, note.
Carboniferous chain between Penigent and Kirby
Stephen, Prof. Sedgwick on the, 69.
forms a mineralogical link
between High Peak of Derbyshire and region
of Cross Fell, 69, 98.
general section of the forma-
tions composing the, 70, 83.
contains six bands of lime-
stone, 70, 73, 75, 76, 78, 79.
ee divisible
into three groups, 99.
-, lowest,
almost identical with mountain limestone of
Derbyshire and Bristol, 99.
» middle,
conforms to portion of Cross Fell carboniferous
system, 99.
$< —_ —__—______—., third, or
millstone grit, common to carboniferous system
of England, 99.
, conclusions drawn from
structure of, 99.
between Penigent and Kirby
Stephen, causes disturbing the formation of
the limestone beds, were in full action in the
valley of Tweed, during the whole carboni-
ferous period, 99.
————— in York-
shire had produced considerable effect before
complete development of the formation, 99.
in Der-
byshire, and the south-western coalfields pro-
duced but small modification, 99.
Carboniferous chain between Penigent and Kir-
by Stephen, beds of, slowly deposited in a sea
of considerable depth, 100.
contains no freshwater
shells, 100.
» fossils of distinct species,
not confined to particular beds, 100.
, sudden change
in, accompanied by change in mineral cha-
racter, 100.
, Trilobites, Ammonites,
and Orthocera not found above the scar lime-
stone, 100, note.
, bottom beds of the calca-
reous groups impure, 101.
contain few
fossils, which are small, 101.
do not ge-
nerally alternate extensively with shale and
sandstone, 101.
, top beds of calcareous
groups; fossils numerous and large, alter-
nate universally with shale and sandstone,
101.
—_—___—_—___——_-——, inferences _respect-
ing, 101.
» grit and sandstone groups
of mechanical origin, and less continuous than
the limestone, 101.
, valleys in the carbonifer-
—
ous chain are valleys of denudation, 101.
group, opinion of the Germans,
that it forms only a part of a great system, in-
cluding the new and old red sandstones, advo-
cated, 401.
series, detached masses of, within
the area of the new red sandstone in Cumber-
land, 391—393.
—___- ______——, causes which may account
for the appearance of detached portions of,
within area of new red sandstone, 391.
strata in Cumberland not always
distinguishable from the new red sandstone by
colour, 387, and note.
Carrock Fell syenite, boulders of, on shores of
Solway Firth, 388.
488
Carrock Fell syenite, mixed with boulders from
Dumfriesshire, 388.
“ Carstone” of Norfolk, what; places of its oc-
currence, 313.
Casterton High Fell, account of beds forming the
flank of, 96.
oe to Barkin, section from, 95.
Caumont, M. de, notice of memoir on beds below
the chalk in Normandy, 330.
Caxton, sulphate of barytes, found near, 306, note.
Central carboniferous chain, account of the dis-
locations by which the Cumbrian mountains
became separated from the, 56.
Chalcedony, veins of, frequent in the sheets of
bare rock in the Dukhun, 422.
Chalk Beck, notice of mass of carboniferous lime-
stone within area of new red sandstone in, 392.
Chalk, cavities in, filled with chalk flints, clay,
and sand, at White Nore, 6.
— and Oxford oolite, general composition of
strata between, in the South-east of England, 104.
on , arrange-
ment and list of, 105.
—, decline of its summits from Bedfordshire
to Norfolk, 303, &c.
-, its thickness in the South-east of En-
gland estimated, 318.
-, remarks on its distribution and charac-
ters in the South-east of England, 322.
—, fossils of, in West Norfolk, 312.
— —-, inclination of, atthe Hogsback, Surrey,145.
— on the coast of Dorsetshire described, 8.
— near Dunstable, 293.
—-— from Dunstable into Norfolk, 305.
, its course through Hertfordshire, 296.
——- cut through at Diss in Norfolk, 311.
— at Mildenhall in Suffolk, 310.
—- in West Norfolk, 311;
Cliff, 314.
— in Oxfordshire, 270, 271.
-, supposed outlier of in Rutlandshire, 308.
at Hunstanton
—, the red strata at Speeton, in Yorkshire,
referred to it, 315, note.
—, red, at Hunstanton Cliff, 314.
———~ in Lincolnshire, 310, note.
- on the north-east of Swindon, 264, 270.
INDEX.
Chalk, fragments of, at Sywell in Northampton-
shire, 308.
—, lower, near Tetsworth, fossils of, 296.
in the Vale of Wardour, 245.
— in the Isle of Wight, 182.
** Cheesecakes ”, beds locally so called in Bucks,
289. ;
Chelydra Murchisonii, a new fossil species from
(Eningen, memoir upon by Thomas Bell, F.G.S.
(Pl. XXIV.), 379,
——_—____—___—, detail of its proportions,
Serpentaria, comparison of with C.
Murchisonii, 380.
, its habits described, 380.
Chemical combination may be cause of volcanic
combustion, 68.
» each successive action of,
would tend to ultimate quiescence, 68.
Chert, concretions of, in sand, of subsequent for-
mation, 121.
Wi 75 WAU.
, in the lower green-sand,
-——, following lines of false stra-
tification, 120.
,hotice of beds ofshivered, near Weymouth, 7.
Chideock Hill, notice of loose breccia in the in-
ferior oolite on the summit of, 7.
Chichester, earthquake around, in 1834, 155, note.
Chicksgrove, in the Vale of Wardour, section at,
251.
Clapham to Penigent, notice of a section from, 94.
Clay, ferruginous, beneath basalt in the Ghats of
the Dukhun described, 419.
, remarkably tabulated, in the Dukhun de-
scribed, 417.
see Gault; Kimmeridge-clay; Oxford-
clay; Weald-clay.
**Clunch” of Cambridgeshire, what, 305.
Coal-formation, resemblance of part of the Weal-
den to, 333.
Coal, gritstone and shale, group consisting of, near
Penigent, described, 79 ; subdivisions of, 79.
Coal measures of Whitehaven were disturbed in
part anterior to the new red sandstone series,
397.
INDEX.
Coal seams, persistence of, in the Valley of Dent,
101, note.
* Cologne earth” prepared from an earthy lig-
nite, 459, note. - --
Combe-Wood, Oxfordshire, oolite containing
freshwater shells found there, 275, 276.
Composition of strata between the chalk and Ox-
ford oolite, general remarks upon, 332, 333.
Concretions, formation of, 121.
, an accident illustrating,
121, note.
of chert, near Sandgate, following
lines of false stratification, 120.
, coproid, of phosphate of lime, in the
Gault, 111, and note.
Cone, approaching to an Araucaria, found on the
shore at Portland, 349.
of an unknown species, from the Hastings-
sand, (Plate XXII.-fig. 10.), 181. -
—_—_—— from the Isle of Pur-
beck, (Plate XXII. fig. 9.), 230.
Conglomerate of new red sandstone near Brough,
Kirby Stephen, Burrel, &c., described, 385.
-— forms lower part of series, 386.
not to be distinguished from the
dolomitic conglomerate of Mendip Hills, 385,
399.
Conglomerates of the lower green-sand in Kent,
of what composed, 118.
Concan :—see Konkhun.
Coniferz, silicified trunks of, found in the “ Dirt-
bed” of Portland, 13, 222, 230.
es —, wood-cut of a re-
markable trunk, found in Portland, 221.
, some microscopic characters not con-
fined to them, 222. :
accompanied in Portland by Cycadez,
a nearly related family, 14, 225, 230.
at Swindon, above the Portland stone,
269.
, petrified, found in the Lower green-
sand, 131.
229.
Coniston Water Head, account of faults between,
and Windermere, 52, 67*.
Hastings-sands,
A89
Contortions and faults in the Weymouth district,
35.
Contraction produced by diminished temperature
may explain some of the great parallel corru-
gations, 67.
Conybeare, Rev. W; D., indicates the group pro-
posed to be called Portland-sand, 210.
» his account of the Ox-
ford oolite referred to, 274.
Coprolite, masses resembling, found in the Gault,
111 and note, 368 note.
green-
sand, over Weald-clay, 181.
Copt Point, Kent, its composition, 107.
-, view of, from the east, (Pl. X. b.
fig. 1.), 106.
Coral rag, Professor Sedgwick on the, 26, note,
213, note.
Coralline or Oxford-oolite, near Weymouth, de-
scribed, 23; its composition, 25; its extent,
27.
, very ferruginous cha-
racter of the upper beds, near Weymouth, 27.
Cordier, M., reference to his notes on the Pays de
Bray, 327.
Cornbrash, notice of, near Weymouth, 28.
‘© Cornstone” beds, locally so called in Bucks, 288.
Coulthard, Capt., referred to, on points of Indian
geology, 418, 420, 426, 428.
Cowleaze Chine, Isle of Wight, section of the
Weald clay at, 197, 198.
Crow-limestone, or caillard, description of, 74.
-_________...___.___. owes its existence to
shells, 75.
Craven fault, description of, 90.
, under Baw Fell, 97.
, at Clapham Beck, 95.
, at Short Gill, 96.
——— ———————, near Fhornton Force,
95.
89.
, near Wild Boar Fell,
, account of effects produced by,
60.
, intersection of, with the Cross Fell
Fault, 63.
490
Craven fault, notices of Mr. Phillips’s account of,
60, 95, 98.
Cross, mountain so called, not to be confounded
with Cross Fell, 92, note.
Cross Fell, notice of fault near base of, 62.
— fault, effects produced by intersection
of, with the Craven fault, 63.
Crystalline structure of primary slates, not al-
ways effect of igneous action, 65.
-_——_—— of secondary rocks some-
times due to chemical action, unaided by ig-
neous cause, 65.
—_—____-—__-, instances of, stated, 65.
Cumberland, order of beds associated with band
of limestone and calcareous slate in, 48.
——, Professor Sedgwick on the new red
sandstone series on the north-western coast of,
383.
, position and peculiar structure of
the schists of, due to causes in action prior to
old red sandstone, 49,55, 65.
Cumbrian mountains, Professor Sedgwick’s in-
troduction to an account of the general struc-
ture of the, 47.
, parallelism of, to the chains
of Cornwall, North Wales, &c., 56.
, central portions composed
of rocks anterior to the old red sandstone, 47.
, outskirts covered by de-
posits chiefly of the carboniferous order, 47.
» notice of formations consti-
tuting the central portion of the, 48.
, order of succession of the
stratified deposits, 48.
— ———~ , first determined
by Mr. Otley, 48.
, older and newer systems of,
entirely unconformable, 55.
» no gradations be-
tween, but abrupt transitions, 55.
——
, Mineral axis consists of un-
stratified crystalline rocks, 49.
——_——_—_——__—————__., formations on the
sides of, arranged symmetrically, 49.
» general strike of formations
composing the chain, 49.
INDEX.
Cumbrian mountains, great dislocations by which
they became separated from the central carbo-
niferous chain, 50.
oe
, elevation of the old slates
of, produced by protrusion of granite and sy-
enite, 67.
» elevation, sudden, 55; suc-
ceeded by a long period of comparative re-
pose, 56.
» crystalline slates of, pro-
bably owe their structure in part to igneous
action, 65.
—_—_————,, northern and southern cal-
careous zones of, cut off from the central
chain, by the same fault, 61.
, inferences deduced respect-
ing, from the phenomena accompanying the
band of limestone and calcareous slate, 54.
——, as concerns the
valleys, 54.
———————,, boulders from, occur in
South Lancashire, Cheshire, and Denbighshire,
390, note.
Cycadez, in the ‘ dirt” above the “Cap” of Port-
land, 220, 222.
found also in a second bed of dirt, below
the “Cap”, 223; a large specimen described,
ibid., note.
not hitherto found at Chicksgrove or
Wockley, 254.
Cycadedidez of Dr. Buckland, two species, found
in Portland, 230; found by Miss Benett at
Tisbury, 15.
Cypris Valdensis, (P]. XXI. fig. 1.), why separated
from Cypris Faba, 344.
, the genus, perhaps not distinguishable, in
the fossil state, from Cytherina, 345.
, other species of, 177, 260, 345.
Cytherina, a marine genus of Crustacea, near to
Cypris, 333, note; 345.
D.
Dangerfield, Capt., on a tradition respecting a
shower of earth, by which Oogein was de-
stroyed, 428.
INDEX.
Dangerfield, Capt., on various points of Indian
geology, referred to, 410, 414, 416, 418, 420,
424, 425, 426, 428.
the great extent of the trap
formation in the Peninsula of India, 428.
Davy, Dr., notice of a hot spring in Ceylon, 427.
, on laterite in Ceylon, 430.
Deccan: see Dukhun.
De la Beche, H. T., F.G.S., reference to his me-
moir on the green-sands of Devonshire, 234.
on the coast of Nor-
mandy, 330.
on marine equivalents
of the Wealden, 329.
nd er buckland,
on the vicinity of Weymouth, 1, 217,
Dent, persistence of coal seams in the valley of,
101, note.
Denudation producing valleys, account of, in Dor-
setshire, 41.
Deposits, siliceous, of the brown-coal formation
near Bonn, 448.
Depressions, geological, in the Weymouth district,
84.
Desnoyers, M., notice of memoir on beds below
the chalk in the North-west of France, 330.
Devakl Unei, hot wells so called in the Konkun,
427.
Devonshire, beds below the chalk in, 233, &c.
, subdivisions of the green-sand se-
ries not discernible in, 233.
Diluvium, deposits of,in the vicinity of Weymouth,
44,
in the, 44.
Dinton, Bucks, quarries at, 285.
Dinton, Vale of Wardour, S. Wiltshire, 248.
‘“‘Dirt-bed” near the bottom of the Purbeck
series, in the Isle of Portland described, 13,
220.
, organic remains occurring
of the Isle of Portland affords a mea-
sure of the duration of the Portland stone in
the state of dry land, 16.
, notice of near Upway, 15.
Portisham, 15.
Thame, 15.
VOL. IV.—SECOND SERIES.
491
“ Dirt-bed ”, silicified coniferous trunks found in,
13, 218, 220.
, Cycadez found in, 14, 224.
, notice of, in the Boulonnois, 15, note.
» a second and lower bed of, also con-
tains Cycadez, 223.
“Dirt, black,” on the Dorsetshire coast, what,
287.
“Dirt, black and grey,” clays, so called in Bucks,
290.
Dislocations in the coal-fields of Bristol Channel,
little resemblance of, to those in the North, 58.
, disturbing
action probably not contemporaneous with that
of the North, 58.
, Prof. Sedgwick on the, which have
separated the Cumbrian Mountains from the
neighbouring carboniferous chains, 47, 56.
Diss, Norfolk, section quite through the chalk at,
311.
Distribution, local, of the strata between the chalk
and the Oxford oolite, in the South-east of
England, 321.
Disturbances of strata in Buckinghamshire, 285.
near Hazeley, Oxfordshire,
286: see “Gulls”.
in Portland, 218.
near Sevenoaks in Kent,
134, 135.
Disturbing forces, their effects, on the coast of
Dorsetshire, 32.
Dolphin Sty, notice of fault at, 90.
Dorking, and Leith Hill, Surrey, tract between
described, 143.
Dorsetshire, Mr. Webster on, referred to, 1, 206.
coast, fossils of, 228.
, enumeration of authors on the coast
of, 1.
, geology of the coast of, 1, 206.
eee
, the subdivisions of the green-sand
strata seen in Hants, Sussex and Kent, not re-
cognisable in, 9.
, description of tertiary deposits of
the coast of, 4.
, description of puddingstone in, re-
sembling that of Hertfordshire, 5.
358
492
Dorsetshire, greensand formation of, 9.
, Hastings sand on the coast of, 11.
, Purbeck beds on the coast of, 11.
, description of inferior oolite in, 30.
—_—
—., succession of changes in the coast of,
45.
Down Cliff, notice of a conglomerate in the infe-
rior oolite, formed of fragments of that rock,
$1.
Duddon, notice of a fault in valley of the, 51.
Dufrénoy, M., notice of his memoirs on the beds
below the chalk in the South-west of France,
330.
Dukhun, portion of, described by Lieut.-Col.
Sykes, 409. ;
it sboundanes 1400:
—_—_—_——_—_—_ —_—_—. , Stratification of, 410.
Ss therGhats orale
, the valleys of, 412.
———_—_——_—_—__—_——_——,, not produced
by rivers, 413.
— eee
, terraces, 413.
po te eee ee , escarpments of the Ghats in,
described, 414,
, columnar basalt a great geo-
logical feature in, 414.
, basaltic and amygdaloidal
columns in, 415.
, places of their occurrence,
415, 416.
, schistose, indurated clay as-
sociated with basalt, 417.
, basalt en boules (or nodular
basalt) of, 417; its localities, 2b.
, basaltic dykes of, 418 ; their
localities, 2b.
, prismatic character of, 418.
, ferruginous clay associated
with basalt described, 419; its localities, 2b.
——_—_———-——, limestone, three forms of,
419,
——_——__—_——_—_—_—,, pulverulent, 419;
its localities, 420.
—_—_—__—_———_—,, nodular, 420; its
great abundance in certain localities, 420, 430.
, crystalline of, 421.
INDEX.
Dukhun, portions of, limestone, specimen of com-
pact found by Colonel Sykes in, 421.
, loose basaltic stones occur
in immense quantities, 421.
» heaps of rocks and stones
in the, 421.
— , occurrence of sheets of rock
in the, 422 ; description of them, 2b. ; their loca-
lities, 2b.
—, structure and mineral com-
position of the trap rocks of, 422.
—, a variety of green compact
basalt found in, 422; description of it, 423.
, prevalence of amygdaloids
in certain localities in, 423.
-—- ———_--—— , amygdaloid with vermicular
stilbite, 424.
————-_—-—-—,, minerals found in the trap
rocks of, 424; their localities, 425.
——_ natural saltssoimA2ommanens
localities, 425, 426.
———, ores of, 426.
a , No organic remains met with
by Colonel Sykes, 426.
——_—— —_ ——_—_— , the absence of remarkable,
—_———, great extent of the trap re-
gion in, 428.
, absence of volcanic products
——., age of the trap formation of,
———— —— lateritesolm4oOnmitsmlaea=
lities, ib.
—_____—_—__——_., granite of, 431.
—_____—_—_——,, sedimentary rocks of, 431.
» mode of determination of
the elevations of, 432.
——, explanation of the sections
accompanying Col. Sykes’s paper on, 432,
Dunnose, in the Isle of Wight, its true position,
191, note.
Dunscombe Hill, notice of pits in the chalk of,
filled with flints, 6.
Dunstable, Bedfordshire, section through, 292.
Dunton, Bucks, quarries of Portland stone at,272.
INDEX.
Dykes, basaltic, in the Dukhun described, 418.
, aremarkable one at Hurreechun-
durghur, 418.
-, of the Siebengebirge, 445.
E.
Earthquake around Chichester, in 1834. 155,
note.
Eden, account of cleft, called Span of, 385.
, description of a longitudinal section from
Penigent to the plains of the, 84.
——, Professor Sedgwick on the new red sand-
stone series in the basin of the, 383, et seq.
—-, sterile sandstone in valley of, the parallel
of forest sand of Nottinghamshire, 387.
Elevation, effects and phenomena of, in the
neighbourhood of Weymouth, 32—34.
of the northern carboniferous chain,
dislocations produced by, 59.
marked by asystem
of longitudinal faults, 59.
—, great changes of
level among the strata during, 63.
—_—_—__—________—_—, fractures produced
by, sometimes inclined to each other, 63.
probably produced
by protrusion of the Cheviot porphyries, the
Charnwood syenite, &c., acted on by volcanic
agents, 63, 64.
——_—__—____————— produced by vio-
lent action, and of short duration, 64.
Elephants’ teeth, occurrence of, in the diluvium
of Dorsetshire, 44.
Elie de Beaumont, his theory of epochs of ele-
vation supported by position of the older for-
mations in British Isles, 56, 65.
——, coal-fields of
Bristol Channel, exceptions to, 57.
Endogenites erosa, found in the Hastings-sand
near Hastings and St. Leonard’s, 167, 168.
—, its external forms, (Plates XIX.
and XX.,) 172; internal structure, 175.
England, general comparison of the red sandstone
series of, with that of Scotland, 402.
—, probable appearance of, if laid dry im-
mediately after the carboniferous period, 56.
3f
493
England, South-east of, Dr. Fitton on the strata
between the chalk and Oxford oolite in, 103,
et seq.
, succession of geological
events in, 45, 320.
Eruptions, volcanic, of the Siebengebirge, 468 ;
of the Roderberg, 2b.
Everest, Rev. Robert, on trap between Calcutta
and Ghazipoor, referred to, 429.
Exeter conglomerate may be equivalent of upper
part of lower red sandstone of Yorkshire,403.
Exogyra (Gryphza) virgula, found in the Kim-
meridge-clay of Buckinghamshire, 273.
F.
Farlton Knot, dislocation near, not leading branch
of Craven fault, 60.
Farnham, Surrey, section near, 144,
Faults, account of, on coast between Parton and
St. Bees Head, 393, et seq.
at Bothenhampton and Bridport Harbour,
40.
— and contortions in the Weymouth di-
strict, 35.
— at Osmington and Ringstead Bay, 39.
, notice of, respecting the band of lime-
stone and calcareous slate of Cumberland, 50,
et seq.
——_—_—_————_——— generally marked
by valleys, 52.
Felspar, glassy, resembling Cleavelandite, in amy-~
gdaloid, in the Dukhun, 424.
Fenny Stratford, section through, 292.
Firestone, (Upper green-sand,) section of, near
Godstone, 137.
near Merstham, 140.
at Reigate, 137.
First millstone grit, description of, between Peni-
gent and Kirkby Stephen, 81.
Fishes, fossil, of the Gault, 203, 259.
Weald clay, 180, 206.
examined by
——
M. Agassiz, 180.
~ Hastings sand, 180, 206.
Purbeck strata, 230, 260,
298.
352
AO
Fishes, fossil, of the Portland stone, 261, 300.
Portland sand, 231.
Kimmeridge clay, 232, 303.
Fissile gritstone and carbonaceous shale, descrip-
tion of beds of, between Strong Post and
Mosdale limestones, 75.
——_—, Mosdale
Moor and Four-fathom limestones, 77.
, most important of the groups al-
ternating with the limestone series, near Pe-
nigent, 77. E
—, subdivisions of, 77.
—______-—_—, used as roofing-slate, 78.
—_——,, contains two beds of coal, 78.
Fitton, William Henry, M.D. P.G.S., “ On Strata
between the Chalk and Oxford-oolite in the
South-East of England,” 103.
——_—__—___—_—__——__——__, objects and
plan of his paper, 104, 105.
, table of its
contents, 384*.
—___________._______ finds the
“ dirt-bed” of Portland in the Boulonnois, 15,
note.
Fitton, W. J., remarkable specimen of Ammonites
found by, 152.
Flints, accumulations of, due to the action of
water, 6.
Flinty slate, fragments of, in the conglomerates of
the Lower green-sand, 117.
Flookborough Spaw, conglomerate of new red
sandstone unconformable to mountain limestone
near, 589.
Flora of the lignite of Bonn, not yet explored,
451, 464.
Fog, remarkable appearance in, from the Hogs-
back, Surrey, 149, note.
Foliated-sand, and clay, remarkable alternation
of, 168.
Folkstone, vicinity of, strata described, 105.
» coast near, view of, (Plate VIII.),
106.
Forest marble, description of, in the Vale of Wey-
mouth, 28; fossils of, 29; its extent, 29.
and cornbrash closely united in
the Weymouth district, 3, note.
INDEX.
Fossils of strata from chalk to Oxford-oolite, lists
of explained, 112, note.
—_-—_—_—_—_, local
distribution of: see the Names of Counties,—
Kent, Surrey, Sussex, &c.
oe ,-
scribed in Dr. Fitton’s paper, deposited in the
Geological Society’s Museum, 334, note.
» new
species of, (Plates XI.to XXIII.), Mr. Sowerby’s
descriptive notes upon, 375.
» col-
of, general inferences not safely deducible from,
334.
, Varia-
tion of, within short distances, 334.
, syste-
matic and stratigraphical Tables of, 351—368.
, explanation of the Tables, 350.
Fossil remains of the Loess of Bonn, 461, 462.
Fossil trees in the Isle of Portland, 13,217, et seq.
Foundations of geology, are accurate mineralogi-
cal distinctions, and order of superposition, 67.
Four-fathom limestone, description of, 78.
—_—_—___—_—_— variable in thickness, 78.
———__—_—__—___—_— abounds in. encrinital
—_—_—__—__—____—_—,, some cherty beds of, con-
tain casts similar to the screwstones of Derby-
shire, 78.
Fovant, Vale of Wardour, section at, 246.
Franklin, Major, referred to, on points of geology
of India, 418, 420, 426, 428, 429, 431.
Fraser, Mr. on the extent of trap in India, 429.
Freshwater deposits in England, publications
upon, 324, note.
, limestone, beds resembling, at the top
of the Portland strata; but including marine
shells, 333.
shells, in oolite, at the bottom of the
Purbeck series, in Oxfordshire, 275—276.
Fuller’s-earth near Aylesbury, 287.
——_——-— of Bedfordshire, described by Hol-
loway, in 1723, 295.
INDEX.
Fuller’s-earth at Nutfield, Surrey, 141, includes
sulphate of barytes, 141.
— near Woburn, section of a pit, 294,
—————_ , grey clay on the coast of Dorsetshire,
probably the equivalent of the, near Bath, 29.
G.
“ Gault,” a local term in Cambridgeshire ; its
meaning, 306.
Gault, general remarks on the distribution and.
characters of, in the South-east of England,
323.
———, its thickness estimated, 319.
, its constancy remarkable, 323.
incloses nodules containing phosphate of
lime, 111, and note.
, bed supposed to resemble, in the Lower
green-sand, 142, note.
, the red beds at Hunstanton supposed to
represent, 312; doubtful, 365, note.
, coproid masses found in, examined by
Dr. Prout, 111, note.
near Aix-la-Chapelle, 323.
in Berkshire and Oxfordshire, 271.
in the Lower Boulonnois, 323.
in Buckinghamshire, 291, note.
near Cambridge, its general relations, 306.
— not found onthe coast west of Weymouth,
on the coast of Kent, described, 109.
near Liege, 323.
near Leighton and Wing, 294.
in Norfolk, 312.
———— near Swindon, 265.
near Thame, 279.
in the Vale of Wardour, 247.
in the Isle of Wight, 184.
, fossils of, in Bedfordshire, 296.
in Cambridgeshire and Norfolk,
316.
———— on the Dorsetshire coast, 228.
near Folkstone, 112.
in the interior of Kent and part
of Surrey, 152.
in the Isle of Wight, 203.
in South Wiltshire, 258.
495
Garsington, Oxfordshire, stratification at, 270.
» quarries of Portland-
Strata at, 277.
Geology, foundations of, are accurate mineralogi-
cal distinctions, and order of superposition, 67.
Germany, central, proofs of identity of new red
sandstone system of, with that of England,
399.
Ghats, true meaning of the term explained, 409.
~ of the Dukhun, general description of, 411.
, escarpments of described,
414,
—, sections respecting, (Plate XXVIII.) ex-
plained, 432; have a slightly perspective cha-
racter, ib.
-, some heights in, determined by boiling
point of water, 432.
Glaisher & M’Lauchlan, Messrs., heights in
Cambridgeshire ascertained by, 370.
Glennie, Rev. J. D., drawing by, of the coast
near Hythe, (Plate VIII.) 106.
, drawing by, of Copt Point,
from the east, (Plate X. b. fig. 1.) 106.
Godalming, Surrey, section at, 146.
Godstone, Surrey, section through, (Pl. X. a.
No. 2.), 137.
—, sectional list of firestone pits near, 137.
Goldfuss, Prof., remains of insects in the brown-
coal formation of Bonn have been described by,
453.
, fossil remains of reptiles in the
environs of Bonn described by, 453.
Goodhall, H. H. Esq. (deceased), a fossil species,
of Nerinea named after, 348.
Grauwacke of the environs of Bonn, 436; its lo-
calities and extent, 2b.
Granite and gneiss regions, in the Peninsula of
India, of amazing extent, 428, 431,
, its great extent in India mentioned by
Dr. Voysey, 431.
———, fragments of, found in the gravel at
Muswell Hill, Middlesex, 293, note.
of Skiddaw Forest overlaid by crystalline
slates, 48.
Gravel, angular, account of beds of, near Wey-
mouth, 7; referred to the tertiary period, 6,
496 INDEX.
Gravel, containing chalk flints, over green-sand,
within the Wealden tracts, 153.
, remarkable accumulation of, at Muswell
Hill near Highgate, Middlesex, 293, note.
, superficial, in Bedfordshire, a very exten-
sive deposit, 293.
——— of Bucks and Bedfordshire, some fossils
of, 296.
of Cambridgeshire, of two kinds, 304,
note.
much conceals the strata in the eastern
counties, 304-805.
———., mass of, over the brown-coal formation,
in the environs of Bonn, 455.
Graystone House, account of the limestone near,
50, and note.
Graves, M., “Marbre a Paludines”, in the Pays de
Bray, 328.
Great Colm (in Cumberland), enumerationof beds
composing sides of, 87.
— to Ingleton, notice of a section from,
95.
Great Ridgeway fault (in Dorsetshire), descrip-
tion of the, 36.
Great scar limestone, description of, 70; full of
fissures, 71.
—-—_ ——__ —_—__.-_—_——_ caverns, 71.
, not formed by the
mere long continued action of water, 71.
—
SS ,» how some were
probably formed, 71.
———— between Penigent and
Kirkby Stephen, contains no bands of coal, 72.
—, beds of reddish sandstone
alternate with, in the lower part, 72.
passes upwards by alter-
nations into a group of sandstone and shale, 72.
Great upper shale, description of, between Peni-
gent and Kirkby Stephen, 81.
Green matter of the Lower green-sand, analysed
by M. Berthier, 108, 109, note.
of the green-sands, analysis of,
by Dr. Turner, 108, and note.
— the same in several different strata,
of sand, 108.
of the beds above the chalk, 333.
Green matter of the Portland-sand, 108.
Greenock, Lord, fossils of the Kentish coast col-
lected by, 112.
Green quartzose slate of Cumberland, notices of,
48.
dislocated,
but not contorted, 55; and why, 55.
Green quartzose slate of Cumberland, contains no
organic remains, 48.
continuous bed of limestone, 48.
—_—_——--——,, supposed
origin of the, 55.
Green-sand, the term objectionable; but adopted ;
why, 105, note.
822.
in Devonshire, no subdivisions, 233,
——,, list of fossils, 239.
in Dorsetshire, described, 9.
—_—______—__—_ reposes_ successively
on the Purbeck beds, Portland stone, Kimme-
ridge clay, Oxford clay, inferior oolite, lias and
red marl, 10.
——_—__—__———___-_-—— in Normandy,
on Kimmeridge clay, coral rag, and Oxford
clay, 11.
Green-sand, Lower, mineralogical nature of the
pebbles composing the conglomerate beds, 116,
Mr
117, 118.
———___————— easily removed by water,
197, note.
includes concretions of chert,
, eroded cavities on its surface,
containing gravel, 144.
, chalk-flint gravel on its sur-
face, within the Wealden denudation, 153.
, general remarks on its cha-
racters and distribution in the South-east of
England, 323.
a , in contact with Kimmeridge-
clay at Little Brick Hill, Bedfordshire, 295.
with sand of the
Portland strata, at Swindon, 265.
, its thickness in the South-.
east of England estimated, 319.
INDEX. A97
Green-sand, Lower, near Folkstone, subdivided
into three, 115.
a » Ast, or up-
per subdivision described, 116, 118.
Bo eee » 2nd, or
middle subdivision, 121 ; detail of beds, 123.
—__—_—__—__,, 3rd, or low-
est, subdivision, 124, 125; contains beds of
limestone, 126, 127.
» subdivisions of, near God-
stone, 137.
subdivisions of, near Pulbo-
rough, like those of Folkstone, 155.
, ridges of, between Seven-
oaks and Godstone, 133.
near Aylesbury, 285.
— in Oxfordshire and Bedford-
shire, 271.
—_—. in the east of Bedfordshire,
295; subdivisions probably exist there, 295.
at Brill, 280.
————— in Cambridgeshire and Nor-
folk, 306.
at Long Crendon, 282.
near Farnham, its thickness
and probable subdivision, 145.
at Hunstanton, 314.
near Leighton, 294.
——_—__—_—_—_—_—_—_——— near Merstham, 141.
in Norfolk, 313.
in the Pays de Bray, 327.
at Quainton, 289.
in Surrey, advances by pa-
rallel steps, or ranges, 143.
near Swindon, in contact
with sand of the Portland strata, (wood-cut),
265.
near Thame, 279.
at Tilburstow Hill, near
Godstone, (wood-cut), 138.
at Whitchurch, 291.
in the Vale of Wardour, 248.
in the Isle of Wight, 184, 188,
TOT 19552005
» fossils of, in Bedfordshire,
297.
Green-sand, Lower, fossils of, near Folkstone,
OK
in the interior of
Kent and Surrey, 152.
ae in Hampshire, 157.
in Norfolk, 317.
—_—_——_—____—— inthe Isleof Wight,
in North Wiltshire,
268.
— in Oxfordshire and
Bucks, 297.
Green-sand, Upper, remarks on its distribution,
and characters in different places in the South-
east of England, 322. ;
, its thickness estimated, 318.
not prominent between the
coast and Godstone, 131.
, the firestone beds near God-
stone, a part of, 137.
in Cambridgeshire, 306.
near Folkstone, 107.
near Godstone, 137.
in Hampshire, 154.
at Hunstanton, 314. m1
in West Norfolk, 312.
in Oxfordshire, 270.
in the Pays de Bray, 327.
in the Vale of Wardour, 246.
, fossils of, in Dorsetshire,
near Folkstone, 108.
in Hampshire, 156.
in Oxfordshire, 296.
in Western Sussex, 156.
in the Isle of Wight, 202.
in South Wiltshire, 257.
in North Wiltshire, 267.
Greenstone, large masses of, found on the sur-
face near Hunstanton, 314, note.
, worn fragments of, in the superficial
|
gravel of Cambridgeshire, 304.
‘“*Greenstone,” beds locally so called in Bucks,
288.
Greywacke of Cumberland contains beds of im-
pure limestone full of organic remains, 48.
498
Greywacke of North Devon and part of South
Wales, probably elevated after completion of
carboniferous series, 57; does not conform to
the range of other greywacke chains, 7b.
Gritstone shale and coal, description of a group
of beds of, between the first and second mill-
stone grits, 82.
—., between the twelve-and
four-fathom limestones, 79.
, between the second and
upper millstone grits, described, 82.
Growth of plants, on former surfaces of the globe,
limitation of inferences from, 321, note.
Grypheea Virgula—(see Exogyra,) 273.
Guildford, Surrey, description of Upper green-
sand, &c., near, 144.
“Gulls” (or Gullies), cavities so called, in the
Portland strata at Great Hazeley, 276.
, wood-cut of one, 276.
evidently the effect of disturbance, 276.
, surface over, not irregular, 276.
analogous to cavities in the lower Pur-
beck strata, in Portland, and Buckinghamshire,
286; and in the Pays de Bray, 328.
Gypseous marls of central England, wanting almost
entirely in new red sandstone of valley of the
Eden, 387.
H.
Hailstone, Rev. Mr., on the vicinity of Cambridge,
303, 304, notes.
Hamites, remarks on a spiral portion of, by the
Rev. Gerard E. Smith, 337.
Hampshire, geological features of part of, 153.
** Hardstone,” bed locally so called in Bucks, 290.
— contains Paludine, 290.
Harter Fell to Wild Boar Fell, account of a sec-
tion from, (Plate VI. fig.9.), 97.
** Hassock” of the Kentish quarries, what, 127.
Hastings, view of cliffs on the east of, by Mr.
Webster, (Geol. Trans. 2nd Ser. ii. Pl. V.),
163.
—, cliffs on the west of, great recent altera-
tions in, 165, &c. 382*.
————, sectional sketch of (Plate X. b.
fig. 3.), 164,
INDEX.
Hastings, ledges of rock on the coast near, 168,
and note.
—, great disturbance of the strata near,
169, note.
Hastings-sand, a member of the Wealden group,
103.
, Junction of, with the Purbeck
strata, 208.
, ledges of, in the sea, in the Isle
of Wight, 186; and near Hastings, 168, note.
a , probable outliers of, in Bedford-
shire and Bucks, 294, and note.
fossils of, (supposed,) in Bucking-
hamshire, 297.
in Kent, Surrey, Sussex,
and Hampshire, 176.
near Hastings, contains numer-
ous specimens of Endogenites erosa, 172.
,cone of unknown species found
in, 181.
in Kent, Surrey, Sussex, and
Hampshire, 176.
on the Dorsetshire coast, 11, 229.
in the Vale of Wardour, 248.
Haute Sadne, a marine deposit coeval with the
Wealden occurs there, 329, 330.
** Hazel-mould,” soil over upper green-sand so
called in Surrey, 141.
Hazeley, Great, Oxfordshire, quarries at, 276.
Headington, Oxfordshire, section at, 278, 279.
‘* Heath,” beds locally so called in Bucks, 289, 296.
Heaps of rock, remarkable, in the Dukhun, de-
cribed, 421.
—, places of their occurrence, 421.
Height of the surface of the Rhine at Bonn, 472.
Heights, in the Ghats of the Dukhun, (Section,
Plate XX VIII.), 411,432; some determined by
boiling point of water, 432.
—, in the environs of Bonn, table of, 471.
in the South-east of England, many
well determined by the recent levelling for
railroads, 375.
, list of, in the South-east of England,
3871—381*.
explanation of, and reference to
authorities for, 369—371.
INDEX.
Helsingburg, in Scania, probable existence there,
of a deposit analogous to the Wealden, 330.
Hematite of Mahabuleshwur in the Dukhun pro-
duces the Wootz steel, 426.
Henslow, Rev. Prof., his observations on the strata
containing stratified trunks in Portland, 16,
note; referred to, 218, 220.
, notice of the temperature of
springs in the neighbourhood of Weymouth, 44,
note.
Herschel, Sir John, examines the colouring mat-
ter of the green sands, 109.
—, sectional drawings, and lists
by, of the strata on the south of the Isle of
Wight, referred to, 186.
High Pike to the top of Great Colm, notice of the
beds from, 87.
Hill forts in the Dukhun, their great strength due
to trap, 414.
Hills, Mr. of Court-at-Street, Kent, numerous
fossils collected by, 112, 127, note, 128, 339.
Hindhead, Surrey, stratification at, 144.
, sands near, described, 147.
Hockliffe, in Bedfordshire, section through, 292.
Hoer, in Scania, fossil plants there analogous to
those of the Wealden, but probably belonging
to the oolite series, 330.
Hog’s-back, Surrey, a ridge of chalk strata highly
inclined, 145.
Hole Beck near Stank, beds of cellular magnesian
limestone, form base of red sandstone, 389.
Hollows, which may have been craters, in the
Vindhya range, mentioned, 428.
Holworth Cliff, notice of the spontaneous com-
bustion of the Kimmeridge clay in, 23.
Horner, Leonard, Esq., on the geology of the
environs of Bonn, 433.
—_—_—_—_—_—_.— geological specimens de-
posited by him in the museum of the Society,
454.
—_—————-—., his coloured map of the
environs of Bonn, 434.
, his notice of Mr. Ly-
ell’s observations on the loess, 475, 476.
, modification of his opi-
nions respecting the history of the loess, 479.
VOL. IV.—SECOND SERIES.
499
Hot springs of the trap mountains of Rajmahl,
427.
Howgill Fells to Baw Fell, account of a section
from the, 96.
Hunstanton Cliff, Norfolk, sectional lists of strata
at, 313, 314.
, Sections of, by different
geologists compared, 315, note.
—___—_——_—__. » red stratum between
the chalk and the Lower green-sand there, 314,
315, note.
Hunter, Rev. Joseph, notes by, on the word
Hurst, 162, note,
Huntingdonshire, not yet described geologically,
303, note.
Hurreechundurghur, hill fort of, its situation de-
scribed, 411.
, remarkable basaltic dyke at,
418.
, glassy felspar, resembling
Cleavelandite, found there in amygdaloid, 424.
“ Hurst”, the word of frequent occurrence in the
names of placesin Kent, Sussex, and Surrey,161,
note.
, Its meaning explained, 162, note.
Hyleosaurus, a new fossil of the Wealden, dis-
covered and described by Mr. Mantell, 179.
i
Ichthyophthalmite in the amygdaloid of the
Dukhun, 424.
at Poona, 425.
Ichthyosiagones, a name given to a species of
Trigonellites, by Dr. Riippell, 348.
Iguanodon, new portions of the skeleton found
near Maidstone, in the Lower green-sand, 132,
, splendid specimens of, found
note.
India, age of the trap formation of, undetermi-
nable, 429.
, Peninsula of, its characteristic geological
features recapitulated, 431.
» granite, its basis, 431.
Indus, mouth of the, phenomena there like those
which produced the strata in Portland, 226.
aT
500
Inferior oolite, description of, on the coast of Dor-
setshire, 30.
Ingleborough, succession of beds on the flanks of,
Sor
Ingleton to Great Colm, notice of a section from,
(Pl. VI. fig. 6.) 90%
Insects, fossil, of the environs of Bonn, notice of
Prof. Goldfuss’s description, 453.
Iron ore, hematite, of the Dukhun produces the
Wootz steel, 426.
— SS
fragments of, found in the
Lower green-sand, 117.
, pisolitic, found in the Hastings-sand near
Hastings, 166, and note.
probably not confined to Hastings, 335.
, found on the Continent, in ma-
rine deposits supposed to be coeval with the
Wealden, 329, 330.
, titaniferous, at Hunstanton, Norfolk,
313.
K.
Kankar: see Kunkur, 431.
Kent, coast of, beds below the chalk on, described,
105.
: see Copt Point, Folkstone, Sand-
gate, Hythe, &c.
, ancient cliffs of, now separated
from the sea by Romney Marsh, 161.
, general section of (Plate X. a.
No. 6.), 163, and note.
, another section, on the true scale
of height and distance, (Plate X. a. No. 6. lower
line), 163, note.
, near Folkstone, view of, by the
Rev. J. D. Glennie (Plate VIII.).
, East, Packe’s Map of, 1743, 106.
, interior of: see Boughton, Maidstone, &c.
Kimmeridge Bay, described, 21, 212.
Kimmeridge clay and Weymouth beds, in the Isle
of Purbeck, 212.
ee —— pass insen-
sibly into Oxford oolite, 331.
——_____—___, its thickness in the South-east
of England, estimated, 320.
INDEX.
Kimmeridge clay, the substratum of the Isle of
Portland, 22.
near Aylesbury, 292.
at Little Brickhill, in contact
with Lower green-sand, 293.
in Cambridgeshire, 307.
at Headington, Oxfordshire,
278.
near Muswell Hill, 283.
in Oxfordshire and Bucks, 273.
—__—___—, a portion of, wanting near Ox-
ford, 274.
near Swindon, 267.
in West Norfolk, 315.
near Weymouth, 21.
——— at Whitchurch, 291.
, fossils of, in Bedfordshire,Cam-
bridgeshire, and Norfolk, 317.
in Dorsetshire, 231.
in Oxfordshire and
—— ——— ——— ——
Bucks, 302.
——_—— the marly sandstone
of, in Ringstead Bay, 21.
at Swindon, 269.
———, notice of its occurrence in
France, 22.
—
—=—
——-—, spontaneous combustion in, at
Holworth Cliff, near Weymouth, Dorset, 23.
Kirkby Lonsdale, dislocation near, not the leading
branch of the Craven fault, 60.
Kirkby Stephen and Penigent, Prof. Sedgwick on
the carboniferous chain between, 69.
, description of a longitudinal sec-
tion from Penigent to the plains of the Eden
near, 84,
, new red sandstone conglomerate,
near, described, 385.
Konkun, (East Indies), general description of, 411,
, thermal springs of, 427 ;
their localities, 2b.
——_———, widely diffused
there, 427.
Kunkur, (nodular limestone), signification of the
word, 420, 430.
, its characters in the Dukhun de-
scribed, 420.
INDEX.
Kunkur, analysis of by Mr. Prinsep stated,
431.
, not the cornbrash of England, 431,
L.
Lancashire, Prof. Sedgwick on the new red sand-
stone series on the north-western coast of,
883.
Langcombe, Oxfordshire, section at, 278.
Laterite of a portion of Dukhun, described, 430,
, places of its occurrence, 430,
associated with hematite, said to occur at
the source of the Krishna river, 430.
——— region, in the Peninsula of India, of very
great extent, 428.
——.— passes into Ceylon, 430.
Leighton Buzzard, vicinity of, 293,
Leith Hill, Surrey, 142, 143,
“ Lets,” eroded cavities in the strata, so called,
at Tisbury, 255: (see ‘“ Gulls.”)
Lias formation of Dorset, 31; enormous depo-
sits of Belemnites in, 31,
Lignite: see Brown-coal.
deposit of Bonn superior to the chalk,465.
—— » no remains of mollus-
cous animals to be found in, 465.
, only two species of fish
hitherto met with in, 474.
Lime, phosphate of, coproid masses composed of,
frequent in the Gault, 111, note,
examined by
Dr. Prout, 111, noée.
Limestone, three states of, in the Dukhun, 419.
, crystalline, in amygdaloids, of the Duk-
hun trap, described, 421.
, nodular, (Kunkur) of the Dukhun, de-
scribed, 420.
——_—_—___—_—_——- occurs very exten-
sively in India, 430.
—
— , analysis of by Mr,
Prinsep stated, 431.
, pulverulent in the Ghats of the Duk-
hun, described, 419.
—————, description of the bed called ‘ Strong
Posto.
501
Limestone, range of the bed called “ Strong Post,”
(ie
and calcareous slate, account of a band
of,in Cumberland, between green slate and grey-
wacke, 49.
—_—__—_—_———— full of organic remains,
separated by enormous
masses from other calcareous strata, 49.
——, most western appear-
ance of, at Beck, 49.
» great faults which af-
fect the band, 50, et seq.
————_—_--—-——_————— generally
———— — ————_—_—_——., exception
at Pool Beck Scar, 52.
» notice of the forma-
tions associated with, 48.
, order of their suc-
cession, 48.
SERRE » first esta-
blished by Mr. Otley, 48, and note.
———_—— —, cut off by the Shap
granite of Wastdale Head, 54.
—, reappears beyond
the granite, 68*,
Lincolnshire Wolds, structure of, 310, note.
Lindley, Prof., examination by, of specimens of
the vegetable remains of the brown-coal forma-
tion near Bonn, 451.
Loess of the environs of Bonn, description of, 460;
its localities, 460, 461 ; its composition, 460, 461;
fossil remains of, 461 ; its greatest elevation, 461.
absence of vegeta-
ble remains in, 462.
— — around the Roderberg, 474, 475,
—-— intermixed with volcanic products, in ex-
cavations near the Roderberg, 475.
, hotice of Mr. Lyell’s writings on the, 475,
480, 481.
, terrestrial shells greatly predominate over
aquatic in the, 475.
—— absorbs water with great avidity, 475.
, modification of Mr. Horner’s opinions re-
specting its history, 479-481.
372
502
Loess, relative age of the, 469.
. probably the production of some vast
flood, 469.
Lonchopteris Mantelli, said to have been found at
Wansford in Northamptonshire, 309; doubtful,
383*.
Lonsdale, William, F.G.S., notice of his examina-
tion of the Oolitic series, near Bath, 261.
—— , lines of sections by,
in Geol. Trans. 2nd Series, vol. ili.; Map,
Plate IX., 261, note.
near
ee , sections by,
Calne, Plate X. a. No. 15 and 16, 261.
Lower new red sandstone, overlying Whitehaven
coal-field, compared with that of the Yorkshire
and Durham coal-fields, 397.
——_——,, of Yorkshire and Dur-
ham, in some places conformable, in some un-
conformable to coal measures, 397, 401.
—, near Whitehaven, ex-
cavated prior to the deposition of the magne-
sian conglomerate, 398.
——- conformable
to the coal measures on the coast; unconform-
able in the interior, 397.
Lulworth Cove, section of, east side, 216.
—, inclined strata near, 14.
——, inference from,
—
respecting the trees of the dirt-bed, 15.
Lunn, Francis, Esq., on the confines of part of
Huntingdonshire and Cambridgeshire, 303,
note.
Lydden Spout, near Folkstone, Kent, issues from
the lowest chalk, 106.
Lyell, Charles, Esq., P.G.S., observations by, on
the effect of earthquakes at the mouth of the
Indus, 226.
——— ——__—_-_—_______, observations on the
loess in the higher parts of the valley of the
Rhine, 475, 477.
Lynn, West Norfolk, deep well at, in the Kim-
meridge and Oxford clays, 310.
M.
M’Lauchlan, Mr., observations by, on the chalk of
Bedfordshire and Cambridgeshire, 303, 304.
INDEX.
M’Lauchlan, and Glaisher, Messrs., list of heights
by, in Cambridgeshire, 370.
Magnesian conglomerate and limestone, descrip-
tion of near Barrowmouth, 395.
————— ————— of the coast near White-
haven compared with that of Nottinghamshire,
Yorkshire, and Durham, 398.
of Bristol coal-field equi-
valent of magnesian limestone and not of rothe
todte liegende, 399, 400.
Mahr, in the Konkun, hot springs at, 427.
Maidstone, remains of Tguanodon found near,
132, note.
, large Scaphites found near, 339.
“Malm,” a mass so called at Garsington, Oxford-
shire, belonging to the Purbeck series, 277.
“ Malm-land”, and “ malm-rock”, in Surrey, what,
154, note.
rock”, in Hampshire, supposed to be di-
stinguished by its fossils, 154.
Man-of-War Cove, section at, 217.
Mantell, Gideon, F.G.S., Hyleosaurus, a new
genus of reptiles, discovered by, 179.
, his observations on
remains of the Iguanodon found near Maid-
stone, 132, note.
ascertains that bones
of birds exist in the Hastings-sand, 382*.
Mantell, Mr. Walter, anew fossil species of Unio
found by, 179.
Marshes of Huntingdonshire and Cambridgeshire,
remarks upon, 304.
Martin, P. I., F.G.S. The term ‘ Wealden”
proposed by, 103.
, his observations on West-
ern Sussex, 155.
—_— on the drainage of the
Wealden Valleys, 150.
, beds subordinate to the
Weald clay carefully traced by, 160.
, section by, through West
Sussex (Plate X. a. No. 5.), 155.
Maryport to St. Bees Head, country almost
wholly composed of coal measures, 388.
Menzalé, description of the lake of, 12, note.
Merian, M., marine deposit of pisolitic iron ore,
INDEX. 503
described by, supposed to be coeval with the
Wealden, 330.
Merstham, Surrey, section at, 140.
Mesotype in the amygdaloid of the Dukhun, 424.
, great masses of, found at Aklapoor in
the Dukhun, 425.
Meyer, M. Von, on Aptychus, referred to, 348.
Miller, Mr., late of Bristol, (deceased, ) his collection
of Blackdown fossils, 239.
, a fossil species of Pecten, named after,
342.
Millstone grit, description of the group called the
first millstone grit between Penigent and
Kirkby Stephen, 81.
, called the second
millstone grit, 82.
- upper mill-
stone grit, 82.
Mineral, new, green, breaking into ‘‘ Rhombs,”
found at Gorgaon in the Dukhun, 425.
Minerals in amygdaloid, ofthe Dukhun, mentioned,
425.
Mineral axis of Cumberland mountains, unstra-
tified crystalline rocks, 49.
formations on the sides of, arranged sym-
metrically, 49.
—-—_—_———, general strike of, 49.
Mineral waters of the environs of Bonn, 463;
analysis of, 7b.
Mineralogical] distinctions, and order of superpo-
sition, the foundations of geology, 67.
Mosdale, notice of the beds in, 93.
Mosdale moor or wold limestone described, 76;
range of, 2b.
Mota River, the valley of, on the south of Poona,
exceedingly narrow, 412.
Murchison, R. I., F.G.S., his observations on part
of Hants referred to, 153, 156.
ee sketch and description by, of
Hunstanton Cliff, (Pl. X. b. fig. 12. b.,) 313.
description by, of the
geological place of a new species of Chelydra,
referred to, 380.
Murchison, Mrs., fossils of the Green-sands of
Hampshire, collected by, 156.
Muswell Hill, Bucks, section at, 279.
Muswell Hill, near Highgate, Herts, superficial
deposit there, containing fragments of several
different strata, 293.
N.
Nautilus plicatus, wood-cut of, 129.
New red sandstone series, Prof. Sedgwick on
the, in the basin of the Eden, and on the north-
western coasts of Cumberland and Lancashire,
383.
———, geographical distribu-
tion of in Cumberland, and part of Lancashire,
384, 405.
employed in Westmore-
land and Dumfriesshire for roofing-slate,
386.
connected with the car-
boniferous rocks in Cumberland by a lower
red sandstone, 387, 4.00.
——, great degradation of,
388, 389.
of Cumberland differs from
that of the Bristol and South Wales coal-field,
by passing into the coal measure through an in-
termediate sandstone, 391.
in some parts of Cumberland
is concealed by enormous masses of drifted
materials, 388, 389.
» probable extension of, at a
former period from the coast of Cumberland,
to Cheshire, 389.
at Hole Beck, base of, is
cellular magnesian limestone, 389.
, the gypseous marls of central
England wanting almost entirely in the, of the
valley of the Eden, 387.
, carboniferous beds some-
times resemble it in colour, 387, and note.
, conglomerates of, near
Brough and Kirkby Stephen, described, 385.
, not to be di-
stinguished from the dolomitic conglomerates of
the Mendip Hills, 385, 399.
of England, proofs of
the identity of, with that of central Germany,
399.
504
New red sandstone series,description of the suc-
cessive deposits which compose the, from Par-
ton to St. Bees Head, 393.
, lowest member of, in
the North of England, probably produced by
the dislocations which immediately followed the
carboniferous period, 58.
» deposition
of, followed by movements of elevation anterior
to the magnesian limestone, 58.
, once extended in Cum-
berland over a greater surface than at present,
389,
—_—_____—_—__,, perfectly analogous to
the corresponding series of Yorkshire and Dur-
ham, 399.
———__-———., section of, near Ald-
bury, 400,
——_—_— ——_—_—-——,, though sometimes con-
formable to the carboniferous system in Cum-
berland, is not conformable on a great scale,
387, 388.
unconformable among
last ramifications of the Eden, 390,
—
Furness, 391,
in Low
, near Ros-
ley, 387, note.
between Appleby and
Maryport, generally conformable to carbonifer-
ous series, 391.
near St. Bees Head,
both conformable, and unconformable, 391.
Nicol, Mr., of Edinburgh, slices of fossil wood
prepared by, 222, note.
Nilsson, Professor, of Lund, his Petrifacta Sue-
cana referred to, 350.
—— , observations by,on
a deposit resembling the Wealden at Helsing-
burg, in Scania, 330.
Nodular limestone, (Kunkur,) forms a remarkable
feature in the geology of India, 430.
———
, organic remains in,
belong to living species, 431.
—
region of, in the
Peninsula of India, of very great extent, 428.
INDEX,
Noggerath, Prof., bed of silicified wood at Bruch
near Ober Cassel, examined by, 451.
, fossil remains of quadrupeds
in the environs of Bonn, mentioned by, 454.
—, on the shells of the brown-coal
formation of the environs of Bonn, 473.
Nomenclature of strata, notto be taken from mere
external character, 105, note.
Norfolk, West, general sketch of the geology
of, 309.
, fossils of, in beds below the chalk,
316, &e.
North Devon and part of South Wales, grey-
wacke series of, elevated probably after com-
pletion of carboniferous series, 57.
, axes of, parallel,
57. ,
North Wales, no obvious centre of dislocation in,
67.
, Strata thrown into vast parallel un-
dulations, 67.
—, probably not produced
by shocks succeeding after long intervals, 67.
Northern carboniferous chain, account of the ef-
fects produced by the elevation of, 59,
————— marked by a system
of longitudinal faults, 59.
Nutfield, Surrey, Fuller’s earth pits there, 141.
contain sul-
phate of barytes, 141.
O.
(Eningen, new fossil species of Chelydra from,
described by Thomas Bell, F.G.S., 379.
Old red sandstone conglomerates of, North of
England, often havea much newer appearance
than those of the new red sandstone, 390, note.
—__—_—__—_—__—_—_———~— in Westmoreland
occur at several points where the carboniferous
chain is in contact with greywacke, 69.
—— -_ —_—____———__ near
Hebblethwaite Hall Gill, 97.
——, peculiarities of structure
and position of the schistose rocks of Cumber-
land originated in causes anterior to existence
of the, 49, 55.
INDEX.
Oogein, city of, said to have been estroyed bya
shower of earth, 428.
Oolite, containing freshwater shells, in the Pur-
beck bed, at Combe Wood, Oxfordshire, 275.
-, Oxford, phenomena presented by, at
junction with the Kimmeridge clay, near Ox-
ford, 274.
its thickness, in the South-east of
England, estimated, 320.
at Blackthorn hill, Bucks, 274.
beyond Haddenham, Cambridge-
shire, 507.
- at Headington, 279.
, at Upware on the Cam, 307.
, fossils of, in Cambridgeshire, 316.
near Oxford, some fossils of,
303.
Oolitic stone, at the top of the Portland series ;
somewhat like that of Bermuda, 224.
Opal, milk, found at Oondurgaon in the Dukhun,
425,
Order of superposition and accurate mineralogical
distinctions, foundations of geology, 67.
Organic remains help to unite disconnected base
lines, 67.
» none found in the Dukhun, 426.
Osmington and Ringstead Bay, Dorsetshire,
faults at, 39.
Otley, Mr., order of stratified deposits of central
Cumbrian mountains, first determined by, 48.
Oxford clay, in West Norfolk, places of its oc-
currence doubtful, 316.
in Dorsetshire, 28.
_
Oxford oolite, or coralline, near Weymouth, de-
scribed, 23; its extent, 27.
, difference of characters of, in Ox-
fordshire and Dorsetshire, 26 and note, 27.
Oxfordshire, beds below the chalk in, 269.
» fossils of, 296.
Oysters, their occurrence a proof of the presence
of salt water, 321 note.
P.
Packe, Christopher, M.D., his map and memoir
on East Kent, (1743); 106 and note.
505
Paludine, found in the “ hard stone” of Quainton,
Bucks, 290.
Papierkohle in the environs of Bonn, frogs and
insects found in, 466.
Parkinson, Mr., his name Trigonellites, retained,
348.
Parton and St. Bees Head, account of the coast
section between, 393.
ne , faults
by which it is affected, 394, et seq.
Passy, M., notice of his work on the structure of
the Pays de Bray, 327, 331.
“Pendle,” fissile freshwater limestone so called,
in Bucks, 287, 289, 290.
Penigent and Clapham, notice of the country be-
tween, 94.
- to Stags Fell near Hawes, account of a
section from, 91.
- to the plains of the Eden, near Kirkby
Stephen, description of a longitudinal section
from, 84.
-, account of the beds composing the sum-
mit of, 84,
Peppingford, in Ashdown Forest, Sussex, fossil
Cone found at, 181.
Petersfield, fossils from neighbourhood of, 156.
Petrifactions, siliceous, amidst calcareous frag-
ments, 332.
of trees and Cycadez in
Portland, 225, 332.
——— of shells at Blackdown
in siliceous sand, 332.
Pewsey, Vale of, stratification described, 262.
———, Dr. Buckland upon, referred
to, 263; a “valley of elevation,” 263.
Phillips, John, F.G.S., notices of his account of
the Craven fault, 60, 95, 98.
et —— paper ona
group of slate rocks between the rivers Lune
and Warfe, referred to, 95, 98.
—, on Belemnites Listeri, in
red chalk, 315, note.
—_——-, his Geology of York-
shire, referred to, 214.
Phillips, William, F.G.S., on the chalk near
Dover, referred to, 107.
506
Pisolitic iron ore, in the Hastings sand, near
Hastings, 166.
, probably not confined to Hast-
ings, 353.
on the Continent, in deposits
supposed to be coeval with the Wealden, 329,
330.
Plastic clay, description of, near Weymouth, 5.
Farnham, 190.
Pleurotomaria (Trochus), note upon, 153,
Poland, marine deposits in, supposed to be coeval
with the Wealden, 329.
Pool Beck Scar, fault at, not marked by a valley;
52.
Poorundhur, glassy felspar found at, in amygda-
loid, 424.
Pope, Rev. W. L., a new species of Sphenopteris
found by, in the Hastings sand, 181.
Portland Ferry and Weymouth Harbour, com-
position of the cliffs between, 24.
— formation, its interrupted deposition in
England, 19.
Portland, Isle of, summary of publications on,
217%.
——— | int-bed ofthe lis.
, detailed section of
upper beds in, 219.
, fossil trunks of Co-
niferee and Cycadee in, 13, 225.
, phenomena of, analogous to
those produced by earthquakes at the mouth of
the Indus, 226.
—$—— , hypothesis,
explaining them, 226.
, quarries of, ought to be fre-
quently examined, 227.
, Strata pervaded by fissures,
proving disturbance, 218.
, strike of the strata well ascer-
tained, 214, note.
Portland Sand, group of strata proposed to be so
called, 20, 210.
—-— abounds in green particles, 210.
a stage of transition, from the
Kemendoe clay to the Portland stone, 21,
331.
INDEX
the Portland
stone, throughout the coast of Dorset, 19.
» concretional nodules in, near
Thame, (wood-cut,); 283; at Shotover, 273,
278; at Swindon, 273;
Portland Sand, coextensive with
in the Boulonnois,
273, 328.
designated by Mr. Conybeare,
210.
, importance of distinguishing it,
$3.
, probable occurrence of, at Shot-
over Hill, near Oxford, 21.
, notice of, at Whitchurch, 21.
, notice of, at Swindon, 21.
in the Boulonnois, 21.
, thickness of, in the South-east
of England estimated, 320.
near Aylesbury, 291,
——_—_——_——-. at Brill, 280.
———__———— at Long Crendon, 282,
——— at Emmet’s Hill, Isle of Purbeck,
———— at Muswell Hill, Bucks, 283.
—_—_————_ in Oxfordshire and Bucks, 273.
———_-———_— in the Pays de Bray, 328.
————_————_ in the Isle of Purbeck, 210.
——__-_— at Swindon, 266, 267.
———_—_——__ near Stewkley, 292.
———_———-_ near Thame, 282.
—_—_—_-—+_——. Vale of Wardour, 255.
at Whitchurch, 291.
, fossils of, in Dorsetshire, 20, 231.
at Swindon, 269.
in Oxfordshire
and
Buckinghamshire, 301.
in the Vale of War-
dour, 261.
Portland stone, its thickness in the South-east of
England estimated, 320.
, passing into sand, in contact with
Lower green-sand, 265.
near Aylesbury, 286.
in the Lower Boulonnois, 328.
at Great Hazeley in Oxfordshire,
276.
in Oxfordshire and Bucks, 272.
INDEX.
Portland stone in the Isle of Purbeck and Dor-
setshire, 17, 210.
at Quainton, Bucks, 290.
—____—_—_—— near Stewkley, 291 and note.
—_—_—_————- at Swindon, 265.
—_____—_——_ in the Vale of Wardour, 254.
in the Pays de Bray, 328; in
Burgundy and the vicinity of Angoulesme, 19.
in other parts of France, 330, 331.
, fossils of, in Dorsetshire, 260.
in Oxfordshire and
Buckinghamshire, 299.
at Swindon, 268.
in the Vale of Wardour,
260.
Portland strata, remarks on their distribution and
characters in the South-east of England, 331.
, their junction with the Purbeck
strata, a point of great geological interest, 331.
, less extensive at present than the
Kimmeridge clay, 332.
, their equivalents in France, 19,
227; and on the Continent in general, 222.
Prestwich, Joseph, F.G.S., on alternations of
marine and freshwater remains, 321, note.
Prevost, Constant M., observations by, on the
Isle of Wight, 185 note.
———— —— notice of his memoir on the
coast of Normandy, 331.
Primary and secondary stratified rocks, broad
mineralogical distinction between, 66.
tertiary stratified rocks, a_ still
broader distinction, 67.
Prout, Dr., coproid masses from the Gault,
examined by, 111, note.
finds the petrified trunks of Portland,
and of the Vale of Wardour, to be almost
wholly siliceous, 225, 254, note.
Pudding-stone, numerous large blocks of, like
that of Hertfordshire, occur in some of the
chalk combs, Dorsetshire, 5.
Pulborough, vicinity of, subdivisions of the Lower
green-sand in, 155.
, derangement of strata near, 155.
Purbeck beds on the coast of Dorset, notice of,
11; occurrence of an oyster bed in, 12.
VOL. IV.—SECOND SERIES.
507
Purbeck Isle, distant view of, 206, note.
, east coast of, section, 206.
-, general view of the south coast of,
212.
, general view of the coast west of,
215; numerous sections of beds below the
chalk, 215, and note.
Purbeck strata, their junction with the Hastings
sands, in the Isle of Purbeck, 208.
Portland
formation, very remarkable, 225, 331,
near Aylesbury, 287.
at Combe Wood, in Oxfordshire,
in part oolitic, 275.
at Long Crendon, 2&2.
at Dinton, Bucks, 285.
at Garsington, Oxfordshire, 277;
there called ‘* Malm,” 277.
in the Isle of Portland, 218.
in the Isle of Purbeck, 208, 209.
at Swindon, N. Wilts, 266.
in the Vale of Wardour, 249,
PHOS
——_—— ~—— near Whitchurch, Bucks, 289.
—_——— ——,, fossils of, in Dorsetshire, 229.
a in Oxfordshire and
Bucks, 297.
—_—__.__—___.._-___.. jn the Vale of Wardour,
259.
Pusch, M., notice of his memoir on the beds below
the chalk, in Poland and Silesia, 329.
Putzberg, near Bonn, section of the beds at,
456.
Q.
Quadrupeds, fossil remains of, in the environs of
Bonn, mentioned by Prof. Noggerath, 454.
Quartz (Amethyst), in the trap rocks of the
Dukhun, 424.
, varieties of, in the trap rocks of the
Dukhun described, 424.
, forms a large portion of the Lower green-
sand conglomerates in Kent, 116.
Quartzose green slate of Cumberland, notices of
the, 48.
3 U
508 INDEX.
R.
Radipole Barracks, Weymouth, notice of the Ox-
ford clay near, 28.
“Rag,” Kentish, described, 117.
Rail-roads in England have determined the heights
of numerous points of small elevation, 375.
, list of heights derived from
the sections of, 375—381*.
Raven Crag, notice of a fault at, 51.
Ravenglass, coarse red gravel of the cliffs south
of, consists apparently of debris of new red
sandstone, 389.
Ravenstone Dale, account of the dislocations in
the calcareous hills of, 61.
Red marl and gypsum of St. Bees Head, very
nearly on parallel of the lower red marl and
gypsum of Yorkshire, 398, and note.
Red sandstone of St. Bees Head, exact equiva-
lent of upper red sandstone of Yorkshire, 398.
series of Scotland and England,
general comparison of, 402.
Reigate, Surrey, section at, 142.
Remarks, general, on the strata between the chalk
and Oxford oolite, 318.
Reptiles, fossil remains of, in the environs of
Bonn, described by Prof. Goldfuss, 453.
, of the Lower green-sand, 153.
Weald clay, 179.
Hastings sand, 179, 206,
—_______..._——.. Purbeck strata, 230, 298.
= Portland=stone 30.
— Portland sand, 269.
— Kimmeridge clay, 303.
————-— Oxford oolite; 16;
Resemblance, notice respecting the, of deposits of
different epochs, 333.
Rhine, height of its surface at Bonn, 433, 472.
-, Valley of the, physical features of, 462.
Rhinoceros tichorinus, tooth of, found by Mr.
Horner in a gravel pit near Bonn, 478.
Ridge, Vale of Wardour, section at, 247.
Ridges, anticlinal, of curved strata, near Seven-
oaks, Kent, described, 133, and note.
of small extent, supposed mode of their
formation, 136.
Ridges, another hypothesis explaining, 136,
note.
Ridgeway fault, in Dorsetshire, description of the
great, 36.
—, no indications of
ruin and violence throughout its line, 42.
Ringstead Bay and Osmington faults, 39.
Risell, notice of beds on sides of, 87.
River gorges, of the Wealden, remarkable, 151.
Rivers, their mode of egress from the Wealden
tract wi32s
, their course transverse to the chalk, fa-
voured by the stratification, 151.
Rock, extensive sheets of bare, frequent in the
Ghats of the Dukhun, 422.
Rocks, sedimentary, of Bonn, relative ages of,
464—466.
, of the Dukhun, remarks on
, volcanic, of the environs of Bonn, 467;
their ages in relation to each other, and to the
sedimentary rocks, 467.
Roderberg, an eruption from, subsequently to the
commencement of the deposit of the loess,
478.
-————., alternation of volcanic ejections with
the loess near, 475.
—, recommendation by Mr. Horner of a
recently published account of the, by M. Carl
Thomae, 472.
—, voleanic eruption of the, 447, 468.
Rose, R. C. Esy., of Swaffham, his account of
West Norfolk, referred to, 309.
, section by, from Swaffham to
Lynn, (Plate X. a. No. 25); 510.
Rosley, new red sandstone not conformable to
coal strata near, 387, note.
Rothe todte liegende of Germany, not repre-
sented by the magnesian conglomerates near
Bristol, 400, 403.
Riippell, Dr., on Ichthyosiagones, referred to, 348.
So
“ Salt Brook,” stones in a rivulet so called, in-
crusted with common salt and carbonate of
lime, 425.
dk
ee
INDEX.
Saltom, notice of faults at, 395.
Saltpetre in the Dukhun, manufactured from
scrapings of old walls, 426. ;
Sand: see Bagshot-sand ; Green-sand ; Hastings-
sand ; Portland-sand.
and clay, foliated, in very thin beds, re-
markable alternation of, 168.
Le 45 Le ehy-
pothesis to explain it, 168.
, white and green, remarkably disposed, at
Tilburstow in Surrey, and other places, 139.
Sandgate, coast near, view of, (Plate VIII.) 106.
—, indications of disturbance near, 124, 126.
Sandown Bay, Isle of Wight, 187.
Sandstone, new red, immediately below the green-
sands of Blackdown, 238.
resemblance of to the Weal-
den, 333.
of the valley of the Eden, the
parallel of forest sand of Nottinghamshire, 387.
been ex-
posed to great denudation, 387.
and shale, lowest group of, between
Penigent and Kirby Stephen, described, 72.
, subdivisions of, 72.
, Shale, and calcareous grit group be-
tween second and Strong Post limestones, de-
scribed, 74.
stinguished by beds of calciferous grit, 74.
, lead-
ing subdivisions of, 74.
, fissile gritstone, and shale, between
Mosdale Moor and Four Fathoms, described,
tho
——_——_______—_—_—_—__ ——_,, most re-
markable of groups alternating with limestone
of Cumberland carboniferous system, 77.
, contains two beds of
coal, 78.
ee — ———
’
subdi-
———_—__—__—__—_—_————_,, the grit-
stone used for roofing-slate, 78.
Sadne Haute, equivalent of the Portland strata
and Wealden found in, 329, 330.
509
Satpoora Hills, Col, Briggs’s description of hot
springs of, 427,
Scaphites Hillsii, specimens of, from the Lower
green-sand near Maidstone, (Pl. XV. f. 5), 128,
339.
Schistose deposits, remarks on their ancient se-
paration into two groups, the upper containing
organic remains, the lower none, 66.
, line of separation difficult to
determine, 66.
rocks of Cumberland owe their pecu-
liarities of structure and position to causes in
action anterior to the existence of the old red
sandstone, 49.
Scotland, general comparison of red sandstone
series of, with that of England, 402.
—, red sandstone and conglomerates of,
assigned principally to old red sandstone, 402.
Second millstone grit, description of, between
Penigent and Kirkby Stephen, 82,
or black limestone group, between Kirkby
Stephen and Penigent, described, 73.
Secondary rocks, from the south coast to latitude
of Derby, have a direction parallel to grey-
wacke chains, 59; reasons why, 59.
beyond Derby, the direction is
parallel to great central carboniferous chain of
the North, 59.
and primary stratified rocks, broad mi-
neralogical distinction between, 66.
Sedgwick, Professor, F.G.S., description of a se-
ries of longitudinal and transverse sections
through a part of the carboniferous chain be-
tween Penigent and Kirkby Stephen, 69.
, Introduction to an
account of the general structure of the Cum-
brian mountains, 47. ‘
———_—_______1____, hissection between
Portland Ferry and Weymouth Harbour, 24.
, on the coral rag,
26, note.
———_____—_—__—___—1_——-,, on the vicinity of
Weymouth, 24, 213, note.
reference to his ac-
count of the Kimmeridge strata near Scarbo-
rough, 214,
3u 2
510
Sedgwick, Professor, F.G.S., notes by, on the
geology of Cambridgeshire, 303, note.
, on the new red
sandstone in the Basin of Eden, and the coasts
of Cumberland and Lancashire, 383.
Sedimentary rocks of Bonn, relative ages of, 464—
466.
, stated not to exist in Western
India, South of Baroach, 431.
Serroor, inthe Dukhun, glassy felspar found near,
in amygdaloid, in the bed of the Goreh river,
424,
, occurrence at, of carbo-
nate of soda, 426.
Shale, carbonaceous and fissile gritstone, group
of, between the Strong Post and Mosdale Moor
limestones, described, 75.
——————_— — —_ —___—________--, most im-
portant bed of the group is the coal in the shale,
7K
fc.
—, gritstone and coal, group of, between
the four and twelve fathom limestones de-
scribed, 79.
— and sandstone, lowest group of, between
Penigent and Kirkby Stephen, described, 72.
— sandstone, and calcareous grit, group of,
between the second and Strong Post limestones,
described, 74.
-——, calcareous
grits the characteristic beds of the group, 74.
—-—-, sandstone, and fissile gritstone, group of
between Mosdale Moor and four fathom lime-
stones, described, 77.
-, most re-
markable of the groups alternating with the
limestone series near Penigent, 77.
——-, a system of, wanting at bottom of lime-
stone series in Cumberland, 71.
Shanklin Chine, Isle of Wight, numerous fossils
found near, 192.
Shap granite, boulders of, in detritus of new red
sandstone of the valley of the Eden, 388.
of Wasdale Head, cuts through the
band of limestone and calcareous slate, 54, 68*.
assumed its present position after
the formation of transition limestone, 54.
INDEX.
Shap granite, veins of, penetrate greywacke near
Wasdale Head Farm, 68*.
Shap Wells, mineral waters of, spring from a cal-
careous conglomerate, 68*.
Shells, list of, found in the loess of Bonn, 462.
—, fossil, from the beds between the chalk
and Oxford oolite, Systematic Tables of, 350—
364.
, descriptive notes of new species,
by Mr. J. De Carle Sowerby, 335—348.
, alphabetical list of; Upper green-
sand, 108, 156, 202, 228, 257, 267, 296.
—— Gault, 112, 152,
203, 228, 258, 296, 316.
of the sands of Blackdown, De-
—
von, 229.
, of the Lower green-sand, 127,
152; 157, 204, 268, 297, 317.
———.-— Weald clay, 176, 228.
Hastings sand, 176, 228, 297.
Purbeck strata, 228, 259, 297.
260,
268, 299.
——_____._—.— Portland sand, 231,261, 269,
—-- Portland stone, 230,
—— Kimmeridge clay, 231, 261,
269, 302, 317.
—— ——— Oxford oolite,
817.
Shotover Hill, Oxfordshire, section at, 274.
232, 503,
Shropshire, account of a section of new red sand-
stone near Aldbury in, 400.
, continuity between the coal measures
and red sandstone series of, effected by lower
red sandstone, 401.
Shunner Fell, account of the beds composing the
flanks of, 93.
, description of a section from Whern-
side to, 92.
Siebengebirge, description of, by Mr.Horner, 453.
, basalt dykes frequent in the, 445;
their localities, 445.
, brown-coal formation of the,
447.
, crystalline volcanic rocks of the,
439, note.
ee
INDEX. 511
Siebengebirge, different in structure from other
groups in Germany, except one in Nassau, and
another near Montabaur, 435.
, absence in, of substances which
in Hungary and Central France accompany
trachyte, 440.
, Mon-occurrence of basalt frag-
ments in the trachyte tuff of the, 441.
, notice of a geological map of, 472.
, notice of authors who have de-
scribed the, 433.
, the, the nearest point to En-
gland where volcanic phenomena nearly re-
sembling those of modern eruptions are to be
seen, 434.
, trachyte tuff of the, (wood-cut),
440—443; its localities and characteristics,
441, 442.
, volcanic eruptions of, 468.
Silesia, Prof. Pusch on the beds below the chalk in,
329.
Siliceous deposits of the brown-coal formation
in the environs of Bonn, 448.
Siliceous stone in sand, concretion of, formed sub-
sequent to deposition of the sand, 232.
, white, containing casts of shells
and vegetable stems, occurrence of, at Marien-
forst in the environs of Bonn, 454.
Similarity of deposits of different epochs ;—
of Wealden, to new red sandstone, and to beds
above, and below, the chalk, 333;—of green-
sand, above, and below, the chalk, to that of the
Portland series, 333; of part of the Wealden
to the coal formations, 333.
, inference from this similarity, 333.
Sithe-stones, mode of preparing at Blackdown,
237.
, workmen said to be consumptive, 238.
Skiddaw Forest, granite of, overlaid by crystal-
line slates, 48.
-, slates of, probably owe their
structure to action from below, 65.
S'ate, siliceous, pebbles of, in the Lower green-
sand conglomerate of Kent, 117.
Smith, Rev. Gerard E., fossils of Kent, collected
and drawn by, 112.
Smith, Rev. Gerard, E., examines the Wealden
cliffs in Kent, 161.
-, remarks by, on the spiral
termination of certain Hamites, 337.
Smith, William, his map of Kent referred to, 107.
—— , his statement respecting “sand in-
“cluding the Portland-stone,” explained, 265,
note.
Soda, carbonate of, at Serroor in the Dukhun, its
form and mode of occurrence described, 426.
and at other places,
426.
——, muriate of, impregnates many of the wells
at Ahmednugeur, 425.
Samia also
a rivulet called the Salt Brook at Ahmednug-
gur, 425.
, streams impregnated with, at
other places described, 426.
Solway Firth, boulders of Carrock Fell syenite,
on the shores of, 388.
South Wales and North Devon, greywacke series
of, probably elevated after completion of car-
boniferous:series, 57.
- does
not conform, in direction, to other greywacke
chains, 57.
axis
of, parallel to that of the coal basin of South
Wales, 57.
South Western coal, notice of total break between
coal measures and red sandstone series of the,
401.
Sowerby, James, F.LL.S. (deceased), observations
by, (1812), on the probable existence of fresh-
water formations, 324, note.
Sowerby, James De Carle, F.L.S., fossils of beds
between the chalk and Oxford oolite, drawn
and engraved by, 105.
——_-—_____.__ , descriptive notes by, on
the shells figured in Plates XI. to XXIII. of
this volume, 335—348.
Sphenopteris gracilis, a new species of fern from
the Wealden, (wood-cut,) 181.
Springs near Weymouth, temperatures of, 44,
note.
512
Springs, thermal, in the Konkun, described, 427.
Spurs of the Ghats in the Dukhun described,
412.
Stags Fell near Hawes, account of the structure
of, 91.
—, section from Penigent to, 91.
Stainmoor, Craven-fault stops near the mountain
pass of, 61.
St. Bees Head, account of the coast section be-
tween, and Parton, 593.
, comparison of strata of, with new
red sandstone series of Yorkshire, 398.
, faults by which it is affected,
393, et seq.
, red sandstone of, dips conform-
ably to the coal measures, 388.
0 separated from
coal measures by intermediate sandstone, mag-
nesian limestone and conglomerate, 388.
, notice of structure of, 396.
-—— to Maryport, coast almost wholly
composed of coal measures, 388.
Stilbite and other zeolites, found at Ahmednuggur
in the Dukhun, 424, 425.
——.-, great masses of, found in amygdaloid, at
Brahmunwareh, in the Dukhun, 425.
Stirling, Mr. on Cuttaek in India, referred to, 431.
St. Leonard’s, near Hastings, detailed account of
the cliffS and strata, 163, 165, 169, 171.
Stone, village of, (Bucks,) pits of Lower green-
sand, at, 285.
Stone, formation of, amidst deposits originally
consisting of sand and gravel, 332.
Stourhead (South Wiltshire), section at, 256.
Strata below the chalk, their variation of cha-
racter in different parts of the South-east of
England, 322.
Stratification, false, near Folkestone, 120.
-———-, fissures of, adopted by masses
of chert of subsequent formation to the sand
which includes them, 120.
Strombeck, M. Von, his account of beds sunk
through at Utweiler, in the environs of Bonn,
457.
Strong Post limestone, description of, 75.
, range of, 75.
INDEX.
Stutchbury, Mr. Samuel, a fossil species of Pec-
ten named after, 342, 360.
Summary of observations on the strata below the
chalk in the South-east of England, 318, &c.
Superficial deposits of Cambridgeshire, extensive
and important; their contents, 304; of two
kinds, ‘‘ white” and “red” gravel, 304, note.—
(see Gravel.)
— —-————— _ resemble
those of Bedfordshire, and the East of En-
gland generally, 305.
Surrey: see Godstone; Reigate; Hind-Head ;
Leith-Hill; Guildford, &c.
, strata below the chalk in, described, 137.
Sussex, Western, strata of, described, 153.
Swanage, remarkable appearances on the shore
near, 209, note.
Swath Fell, structure of the top of, 89.
Sweden, marine deposits coeval with the Wealden
in, 330,
Swindon (North Wiltshire), stratification at de-
tailed, 264--267.
———___ — , fossils of, 267.
, nodules in the Portland sand at, 267.
Sykes, Lt.-Col. W. H., F.G.S., on a portion of
the Dukhun in the East Indies, 409.
—__—-—__—_—_—_——,, recapitulation of
the characteristic geological features of the
peninsula of India, 431.
-————___—___—___—__—— — , explanationof the
sections accompanying his paper on the Duk-
hun, 432.
408
Table of heights in the environs of Bonn, 470.
3039;
Taylor, R.C., F.G.S., his section at Hunstanton,
and publications on Norfolk, referred to, 315,
note.
-—— South-east of England,
Temperature, diminution of in the earth, may ac-
count for some of the great parallel corruga-
tions, 67.
Terraces of the Dukhun described, 413.
Tertiary deposits of the coast of Dorset de-
scribed, 4.
INDEX.
Thame, Oxfordshire, strata there, 279, 282.
Thermal springs of Konkun in the East Indies,
427,
Thirria, M., on beds below the chalk in the De-
partment of the Haute Sadne, 330.
Thomae, M. Carl, on the lava of the Roderberg,
473; on the loess around the Roderberg, 475,
476.
Tilburstow Hill, Surrey, list and sketch of beds
composing the section, (wood-cut,) 138, 139.
Tisbury, Vale of Wardour, quarries at, 255.
Titaniferous iron ore, found in the Lower green-
sand at Hunstanton, 313.
Tonbridge Wells, strata there resembling those of
the coast near Hastings, 170, note.
Trachyte and basalt of the environs of Bonn,
age of, 467.
and grauwacke, instance of a junction
of, in the neighbourhood of Bonn, 440.
of the environs of Bonn, 437 ; its loca-
lities and varieties, 437, 438.
Trachyte, its affinity with the trap family, 438.
Trachytic tuff, its correspondence in composition
with adjacent trachyte nearest to it, 442.
of the Siebengebirge, 440-443 ;
its localities and characteristics, 441, 442.
, the oldest of the volcanic pro-
ducts of the environs of Bonn, 467.
Trap region, in the Peninsula of India, of amaz-
ing extent, 428.
, extent not yet appreciated, 409.
, authorities upon its stratification
referred to, 410, note.
its age uncertain, 420; probably
not identical with that of the new red sandstone,
429.
rocks in the Ghats of the Dukhun, charac-
ters of described, 422.
Tree, fossil, a remarkable specimen of, found in
clay at Brill, 280.
Trees, coniferous, silicified found at Portland, 13,
BOA:
—____1+—_————,, ascertained by
Dr. Prout to be almost wholly siliceous, 225.
in the lowest
Purbeck strata of the Vale of Wardour, 256.
—— i ——
518
Trees, coniferous, silicified, wood-cut of a re-
markable specimen, 221.
Trigonellites of Parkinson (Pl. XXIII. f. 2.), the
name retained, why, 348.
found in the Kimmeridge clay in
Cambridgeshire, 273; and near Aylesbury,
Bucks, 292.
Troutbeck, account of fault in the valley of, 53.
Tucksbury Hill, (or Farnham Beacon,) near
Farnham, Surrey, section through, 149.
Tuff of Siegburg, its great resemblance to that of
the Phlegraean Fields and Ischia, 446.
Turner, Edward, M.D., Sec. G.S., analysis by,
of the green matter of green-sands, 108, note.
Turna Fell coal works, section of beds at the, 93,
note.
Twelve-fathom limestone, description of, 79;
abounds with encrinital remains, 80.
U.
Upper millstone grit, description of, between Pe-
nigent and Kirkby Stephen, 82.
Upware, on the river Cam, quarries there of the
Oxford oolite, 307 ; fossils obtained there, 317.
Vi
Vale of Bredy, geological formations of the, 32.
Wardour, geological structure of, 244.
Weymouth, physical features of the, 3.
Valley, remarkably narrow, on the Mota river,
south of Bonn, 412.
Valleys in the limestone band of the Cumbrian
mountains, scooped out upon lines of fracture,
52, O4,
in Dorsetshire produced by denudation,
41.
of the Dukhun in India described, 412.
Vegetable remains of the environs of Bonn, ex-
amined by Professor Lindley, 451.
—____\___—,, absence of, in the loess of
Bonn, 462.
Vegetables, fossil, of the Upper green-sand, 157,
203.
Gault, 115.
Lower green-sand, 131,
153,
514
Vegetables, fossil, of the Weald clay, 181, 228.
——_ _.__— Hastingsisand ld lenote,
725 US 2068229-
SE = Punbeckstratawlone2 il,
230, 298.
Portland stone, 269.
Portland sand, 269.
Kimmeridge clay, 269.
|
Volcanic action, cause of, not known, 64.
not reducible to laws of any con-
stant force as respects its effects, 65, 67.
may be an effect of chemical
combination, 68.
———.-, produced by
the penetration of water to highly heated matter,
68.
must diminish in force by the
earth’s refrigeration, 68.
Se ee and
by each successive chemical combination, 68.
has not acted during all geologi-
cal periods with equal intensity, 65.
-——, no indications of its recent oc-
currence in the Dukhun, 428.
Volcanic craters, none seen in the Dukhun, 428.
— eruptions in the neighbourhood of Bonn,
446, 447.
——-— eruptions of the Siebengebirge, 46S.
took place
during the deposition of the brown-coal beds,
468.
Roder-
berg, 447, 468.
Volcanic forces, provision for an eternal and
uniform circulation of, not compatible with
known laws of chemical action, 67.
have modified the earth in two
ways, 68.
—— by violent
paroxysms, producing lines of volcanic vent,
68.
—— - os by local
action producing volcanic cones, &c., 68.
——— rocks of the environs of Bonn, their ages
relative to each other and to the sedimentary
rocks, 467.
INDEX.
Voysey, Dr., on various points of Indian Geo-
logy, referred to, 410, note, 412, 417, and note,
418, 426, 428, 431.
W.
Wardour, Vale of, general structure of, 244; strata
described, 244; Chalk, 245; Upper green-
sand, 246; Gault, 247; Lower green-sand,
248; Wealden, 249-254; Portland stone,
254; Portland sand, 255; Kimmeridge clay,
256.
—-——————., anticlinal line of, 244.
—_—_— , fossils of, 257—261.
Warminster, Vale of, described, 257.
————., fossils of, 257,
Wasdale Head Farm, granite veins penetrate
the greywacke near, 68*.
——, the Shap granite of, cuts through
band of limestone and calcareous slate, 54, 68*.
, limestone and
slate reappear beyond the granite, 68*.
Water Blain limestone, notices of, 50, and note.
Waters, mineral, of the environs of Bonn, 463;
analysis of, 463.
Weald clay, a member of the Wealden group,
103.
earefully traced in W. Sussex by
Mr. Martin, 160.
——_——-—_,, beds of sand and stone subordinate
to, in Sussex, 159; in Surrey, 160; and in
Kent, 161.
, Cavities in, at its junction with the
Lower green-sand in W. Sussex, 156.
near Guildford, 148.
near Hindhead, Surrey, 148.
in the Isle of Wight, 185; detail of
its beds near Cowleaze Chine, 198.
» fossils of, in Kent and Surrey, Sus-
sex and Hampshire, 176.
in the Isle of Wight,
on the Dorsetshire coast,
Wealden, adopted as the general name of the
strata between the Lower green-sand and the
Portland stone, 103,
INDEX.
Wealden, acceptation of the term extended,
why, 159.
——_—— characterized by its fossils, 104.
probably the deposit of an estuary, 104,
324.
—_—
—, resemblance of part of, to the New
red sand-stone; to some of the beds above the
chalk ; and to the coal formation, 333.
, sudden change from marine fossils,
beneath it, and above, 324.
, its stratification conformable to the for-
mations above and below, 324.
, formations immediately below it much
connected, 331.
, theory of its formation, 324.
, analogy of, to deposits now in pro-
gress, 325; as in the lakes of North America,
325.
, its distribution and general characters
in the South-east of England, 323, and note.
, its original and remaining extent in
England, undetermined, 324.
, junction of, with the Lower green-sand,
in the Isle of Wight, 189; in Western Sussex,
remarkable, 156.
, thickness of, in the South-east of En-
gland, estimated, 319.
not found beyond the limits of the Port-
land formation, 332.
in Buckinghamshire, indications of,
288, 289, 290.
on the Kentish coast, described, 161.
in Kent, Surrey, and Sussex, 159, et
seq.
in Oxfordshire, traces of, 272.
at Shotover Hill, Oxfordshire, 274.
in the Vale of Wardour, 249.
, supposed indications of, at Wansford,
in Northamptonshire, 309 ; doubtful, 383*.
in the Isle of Wight, 184, 190.
, deposits of the same date and character
in other districts, 326 ; in Scotland, 326; in the
Lower Boulonnois, 326; Pays de Bray, 326.
equivalents of, in the Isle of Bornholm,
and near Helsingburg, in Sweden, 330; in
Poland, Switzerland, and France, 326, 330,
331.
VOL. IV.—SECOND SERIES,
515
Wealden, marine deposits coeval with, probable
@ priori, 329.
, consequences of their
existence, 329.
not to be expected, ge-
nerally, in England, $29.
, places in which they
have been found, 329, 330.
-—_———,, remains of plants in, 181.
» fossil shells of, in Kent, Surrey, Hants,
and Western Sussex, 176.
in the Isle of Wight,
205.
» reptiles of the, 179.
————, fishes of, examined by M. Agassiz,
180; list of them, 367, 368.
Wealds, Valley of the, in Kent, Surrey, and Sus-
sex, 160.
, drainage of, on the north-
west, remarkable, 150.
—_———_——,, tortuous course of rivers
in, 150; hypothesis thence deduced, 150.
ee » section across, from West
Sussex to Surrey, (Plate X. a. No. 6); 155.
Webster, Thomas, F.G.S., his work on the Isle
of Wight, referred to, 8, 182.
——___—. on fossil trees in Port~
land, 13, 217.
on the Purbeck and
Portland strata, 11, 206, 210.
, view by, of the coast
near Hastings, 163.
on freshwater shells in
the Hastings and Purbeck strata, 324, note.
Well, 600 feet in depth, at Lynn, Norfolk, 320.
Wells, hot, called Devakl Unei, 50 miles south-
east of Surat, 427.
Wendover hill, its height, 284.
Wey river, its course near Farnham in Hamp-
shire, and in Surrey, 151.
Weymouth, Dr. Buckland and De la Beche, H.T.,
on the geology of the neighbourhood of, 1.
— district, an important geological tract,
, the general physical features
of, 2.
—, physical features of the Vale of, 3.
3x
516
Weymouth strata form the transition from the
Kimmeridge clay to the Oxford oolite, 331,
332.
—-——— at Langcombe, Oxfordshire,
278.
vary, much in different places,
332.
, well seen in the Boulonnois, 332.
: see Kimmeridge clay.
Whernside, description of a section from, to
Shunner Fel], 92.
, notice of beds forming the flanks of,
85, 86.
Whewell, Rev. W., sketch by, of part of Hun-
stanton Cliff, (Plate X. b. fig. 12, ¢.); 313.
Whitehaven coal-field, notice on, 293.
, faults affecting, on the
coast, 393, et seq.
White Nore, Dorsetshire, pits in the chalk, at,
filled with flints, 6.
-, chalk cliffs of, 8, 9.
White-rock, Hastings, section at, 168.
recently destroyed or re-
moved, 165, note, 382*.
Wight, Isle of: see Blackgang, Shanklin, Cow-
leaze, &c.
, proofs of its repeated submersion
and elevation, 185,
» resemblance in, between the beds
above and below the chalk, 185.
» general structure of, 182.
, south coast, sectional sketches of,
by Sir John Herschel, 186.
, sectional list of strata, from Bem-
bridge Down to Sandown Bay, 187.
—_ -——_——___——_——— from Bon-
church Cove to Sandown Bay, 191, &c.
—.—_— from Black-
gang-chine to Brook-chine, 194.
INDEX.
Wight, Isle of, sectional list of strata, from the
shore under Afton-down to Brook-chine, 200.
, fossils of the beds below the chalk
in, 202.
Wild Boar Fell, structure of, 89, 98. -
to Harter Fell, account of a sec-
tion from, 97.
Wiltshire, North: see Swindon.
—, South: see Vale of Wardour, and of
Warminster.
Windermere, valley of, scooped out upon a line
of fracture, 52.
and Coniston Head, notices respect-
ing faults between, 67 *.
Woburn, section through, 292.
—, Fuller’s earth pit, near, 294.
Wockley-quarry, Vale of Wardour, section of,
Dole
Wold or Mosdale Moor limestone, described, 76;
range of, 76.
Wood, fossil, lignitized, a remarkable specimen
found in clay, at Brill, 280.
, coniferous, silicified, found in the
“Dirt Beds,” in the Isle of Portland, 13, 217,
221, 222; in the Vale of Wardour, 254; at
Swindon, 269.
, silicified, bed of, in the environs of
Bonn, 451; examined by Professor Noggerath
and M, B. Cotta, 2b.
, Slices for the microscope, prepared by
Mr. Nicol of Edinburgh, 222, note; mode of
preparing them, described, 222, note,
Woodward, Mr. Samuel, on the fossils of West
Norfolk, 309, note, 315.
Worbarrow Bay, section at, 208.
Z.
Zinc, layer of carbonate of, in the new red sand-
stone series near Barrowmouth, 396.
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List of Donations.
BOOKS.
On the Connexion between Geology and the Pentateuch,
by Dr. Cooper; also the Defence of Dr. Cooper before
the Trustees of the South Carolina College.
On the Insecurity of Sir Humphry Davy’s Lamp, and
the perfect Security of Messrs. Upton and Roberts’s
New Safety-Lamp.
Canal Navigation. On the Resistance of Water to the
Passage of Boats upon Canals and other Bodies of
Water, being the Results of Experiments, by John Mac-
neill, M.R.I.A., &c.
Travels in the United States of America and Canada, to
which is added an Essay on the Natural Boundaries of
Empires, by J. Finch, Esq. 8vo. London, 1833.
Bulletin de la Société Géologique de France, tome 3émey
feuilles 17—24, 1833.
Mémoire sur la Constitution Géologique de la Province
de Liége; quia remporté le Prix au Concours de
l’Académie de Bruxelles en 1830, par M. A. Dumont,
4to. Bruxelles, 1832.
Géologie Populaire a la Portée de tout le Monde, appli-
quée a l’Agriculture et a |’Industrie, par M. Nérée
Boubée, 18mo. Paris, 1833.
Tabelle iber die Geologie zur Vereinfachung derselben,
und zur Naturgemassen Classification der Gesteine, von
Hermann von Meyer, 8vo. Niirnberg, 1833.
Catalogue of German Books and Maps, which have been
published from January to June 1833, by Black, Young,
and Young, 12mo. London.
Deux Promenades au Mont Dore pour I’Etude de la
Question des Cratéres de Soulévement, formant la 1ére
livraison de la 4éme Série d’Itinéraires du Cours com-
plet d’Etudes Géologiques par des Lecons et par des
Voyages, par M. Nérée Boubée, 18mo. Paris, 1833.
Nixus Plantarum. Auctore Johanni Lindley, 8vo. Lon-
dini, 1833.
Notice sur le Bradford-clay de Bouxwiller et de Bavil-
lers, par M. P. L. Voltz, 4to, Extrait des Mémoires
de la Société d’Histoire Naturelle de Strasbourg.
Mémoire sur les Groupes du Cantal, du Mont Dore, et
sur les Soulévemens auxquels ces Montagnes doivent
leur Relief actuel, par MM. Dufrénoy et Elie de Beau-
mont, 8vo. Paris, 1833. Extrait des Annales des Mines,
8éme Série, tome 3.
Transactions of the Zoological Society of London, vol. 1,
part 1, 4to. London, 1833.
Proceedings of the Royal Society of Edinburgh, No. 2,
April and May 1833.
Mémoires de l’Académie Royale des Sciences de 1’In-
stitut de France, tome 12éme, 4to. Paris, 1833.
DONORS.
Dr. Cooper.
Messrs. Upton & Roberts.
Frederick Page, Esq. F.G.S.
The Author.
The Geological Society of
France.
The Author.
The Author.
The Author.
Messrs. Black, Young, and
Young.
The Author.
The Author.
The Author.
The Authors.
The Zoological Society.
The Royal Society of Edin-
burgh.
The Royal Institute of
France.
4s
1833.
Oct. 29.
Nov. 6
11.
13.
COS)
v9
List of Donations.
BOOKS.
Comentarios a las Ordenanzas de Minas, dedicados al
Catholico Rey, Nuestro Sefior Don Carlos III. (que
Dios guarde) siempre magnanimo, siempre feliz, siem-
pre augusto, por Don Francisco Xavier de Gamboa,
folio, Madrid, 1761.
Annales des Mines, ou Recueil de Mémoires sur |’Exploi-
tation des Mines et sur les Sciences et les Arts qui s’y
rapportent; rédigées par les Ingénieurs des Mines, et
publiées sous |’Autorisation du Conseiller d’Etat, Di-
recteur Générale des Ponts et Chaussées et des Mines,
3éme Série, tomes 3 et 4, 1833.
. A Geological Manual, by Henry T. De la Beche, Esq,
F.G.S. 3rd Edit. 8vo. London, 1833.
Résumé Préliminaire de ’Ouvrage sur la Théorie des
Volcans, par le Comte de Bylandt, 8vo. Naples,
1833.
Memorie sopra due casi di Alienazione Mentale osser-
yati nel R. Stabilimento de’ Matti di questa citta,
composte da Giovanni Silvestri, 8vo. Palermo, 1833.
General Observations upon, and Sailing Directions for,
the English and Irish Channels and Channel Islands
by Capt. Martin White, R.N.
Descriptions of the Inferior Maxillary Bones of Masto-
dons in the Cabinet of the American Philosophical
Society, with Remarks on the Genus Tetracaulodon,
&c., by Isaac Hays, M.D. Extracted from the Trans-
actions of the American Philosophical Society, vol. 4.
New Series, 4to. Philadelphia, 1833.
A Catalogue of a valuable Collection of Books, in the
French, Spanish, Portuguese and Italian Languages, on
sale by John Bohn, 8vo. London, 1833.
Verhandlungen der Gesellschaft des Vaterlindischen
Museums in Bohmen in der eilften allgemeinen Ver-
sammlung am 10 April 1833, 8vo. Prag, 1833.
. Journal of the Franklin Institute of the State of Penn-
sylvania, devoted to the Mechanic Arts, Manufac-
tures, General Science, and the recording of American
and other patented Inventions, edited by Thomas P.
Jones, M.D. New Series, vol. 10, Aug. 1832, No. 2,
8vo. Philadelphia, 1832.
Proceedings of the Royal Society of London, No. 13,
1832-1833.
A descriptive Catalogue of the Minerals, and Fossil Or-
ganic Remains of Scarborough and the Vicinity, inclu-
ding the Line of Coast from Hornsea to Mulgrave, and
extending into the Interior as far as Malton, 8vo. Scar-
borough, 1816.
Memoirs of the Royal Astronomical Society of London,
vol. 6, 4to. London, 1833.
DONORS.
Henry Brookes, Esq. F.G.S.
L’ Administration des Mines.
The Author.
The Author.
Comte de Bylandt.
The Lords Commissioners
of the Admiralty.
The Author.
Mr. Bohn.
Count Sternberg.
Petty Vaughan, Esq.
The Royal Society.
John Willimott, Esq.F.G.S.
The Royal Astronomical
Society.
1833.
Nov. 22.
Dec. 3.
16.
20.
List of Donations.
BOOKS.
Experimental Researches in Electricity, (Fourth Series, )
by Michael Faraday, D.C.L. F.G.S. From the Phi-
losophical Transactions, 4to. London, 1833.
The Horticultural Register and General Magazine of all
useful and interesting Discoveries connected with Na-
tural History and Rural Subjects, conducted by Joseph
Paxton, for the year 1833.
The London and Edinburgh Philosophical Magazine and
Journal of Science, conducted by Sir David Brewster,
K.H. LL.D. F.G.S. &c., Richard Taylor, Esq. F.G.S.
&c., and Richard Phillips, Esq. F.G.S., for the year
1833.
The Magazine of Natural History and Journal of Zoo-
logy, Botany, Mineralogy, Geology and Meteorology,
conducted by J. C. Loudon, Esq. F.G.S. &c., for the
year 1833.
The Penny Cyclopeedia of the Society for the Diffusion
of Useful Knowledge, vol. 1,A—Andes, 8vo. London,
1833.
Catalogue of Fellows, Candidates and Licentiates of the
Royal College of Physicians, 8vo. London, 1833.
Observations of Nebulze and Clusters of Stars made at
Slough, with a twenty-feet Refiector, between the Years
1825 and 1833, by Sir J. F. W. Herschel, Knt. Guelp.
F.G.S. From the Philosophical Transactions. 4to.
London, 1833.
On the Absorption of Light by coloured Media, viewed
in Connexion with the Undulatory Theory, by Sir
J. F. W. Herschel, K.H. From the London and
Edinburgh Philosophical Magazine and Journal of
Science, December 1833.
Etablissement Géographique de Bruxelles. Annuaire
Industriel et Administratif de la Belgique, Année 1833,
2éme Année, 8vo. Bruxelles, 1833.
Dictionnaire Géographique de la Province de Namur,
8vo. Bruxelles, 1832.
Dictionnaire Géographique de la Province de Hainaut.
8vo. Bruxelles, 1833.
Mémorial de l’Etablissement Géographique de Bruxelles,
fondé par Ph. Vander Maelen, 8vo. Bruxelles, 1831.
Recueil de Documens Statistiques. Belgique, 8vo. Brux-
elles, 1833.
Journal of the Geological Society of Dublin, vol. 1,
part 1, Dublin, 1833.
An Encyclopedia of Gardening, containing the Theory
and Practice of Horticulture, Floriculture, Arboricul-
ture, Landscape Gardening, &c., conducted by J. C.
Loudon, Esq. F.G.S., Specimen Number, 8vo. Lon-
don, 1833.
DONORS.
The Author.
The Conductor.
The Conductors.
The Conductor.
Mr. Knight.
The Royal College of Phy-
sicians.
The Author.
The Author.
M. Ph. Vander Maelen, Fon-
deur de 1’Etablissement.
CC
ee ee ereseeesneseeeoe eens
The Geological Society of
Dublin.
The Conductor.
10.
14,
List of Donations.
BOOKS.
. M.A. Nattali’s Catalogue of a Collection of Books in
General Literature, English and foreign, 8vo. Lon-
don, 1834.
The American Journal of Science and Arts, conducted
by Benjamin Silliman, M.D. vol. 24, No.2. and vol. 25,
No. 1. 8vo. New Haven, 1833.
. The Nautical Almanac and Astronomical Ephemeris for
the Years 1834 and 1835, published by Order of the
Lords Commissioners of the Admiralty, 2 vols. 8vo.
London, 1833.
Address delivered at the Anniversary Meeting of the
Royal Society on Saturday, November 30th, 1833, by
His Royal Highness the Duke of Sussex, K.G. &c.,
The President, 4to. London, 1833.
Descriptive and illustrated Catalogue of the Physiolo-
gical Series of Comparative Anatomy, contained in the
Museum of the Royal College of Surgeons in London,
vol. 1, including the Organs of Motion and Digestion,
4to. London, 1833.
Bulletin de la Société Géologique de France, tome 4éme,
feuilles 1-5, Paris, 1833.
Proceedings of the Royal Society of Literature, vol. 1,
No. 4, 1833.
Histoire des Végétaux Fossiles, ou Recherches Bota-
niques et Géologiques sur les Végétaux renfermés dans
les diverses Couches du Globe, par M. Adolphe Brong-
niart, Séme livraison, 4to. Paris.
A New System of Mineralogy in the Form of Catalogue,
by William Babington, M.D.
. Experimental Researches in Electricity, (Fifth Series,)
by Michael Faraday, Esq. F.G.S. From the Philo-
sophical Transactions, 4to. London, 1833.
Transactions of the Society instituted at London for the
Encouragement of Arts, Manufactures and Commerce,
with the Premiums offered for the Years 1832-1833
and 1833-1834, vol. 49, London, 1833.
. Studien des g®ottingischen Vereins, Bergmannischer
Freunde, im Namen desselben herausgegeben, von
Joh. Friedr. Ludw. Hausmann, 3ter band, 8vo. Got-
_ tingen, 1833.
Eloge de M. le Baron Cuvier, par. C. L. Laurillard.
Discours couronné par l’Académie des Sciences, Belles
Lettres et Arts de Besancon dans sa Séance du 24 éme,
Aott 1833, 8vo. Paris, 1833.
Proceedings of the Royal Asiatic Society, December
1833, and January 1834, 8vo.
Manvel Géologique par Henri T. De la Beche. Traduc.
tion Frangaise, revue et publiée par A. J. M. Brochant
de Villiers, 8vo. Paris, 1833.
DONORS,
M. A. Nattali.
The Conductor.
W.S. Stratford, Esq.
The Royal Society of Lon-
don.
The Royal College of Sur-
geons.
The Geological Society of
France.
The Royal Society of Lite-
rature.
Frederick Page, Esq. F.G.S.
B. G. Babington, M.D.
F.G.S.
The Author.
The Society of Arts.
M. F. L. Hausmann.
The Author.
The Royal Asiatic Society.
Henry T. De la Beche, Esq.
F.G.S.
—
1834.
Jan. 25.
28.
ole
Feb. 4
io.
20
cr
List of Donations.
BOOKS.
A Catalogue of Modern and Standard Works, principally
of the Duplicates of Hookham’s Library, 8vo. 1834.
Tide Tables for Plymouth, Portsmouth, Ramsgate, Sheer-
ness, and London for the Year 1834, 8vo. London,
1834.
A descriptive Catalogue of the Collection illustrative of
Geology and Fossil Comparative Anatomy in the
Museum of Gideon Mantell, Esq. F.G.S. 8vo. Lon-
don, 1834.
Proceedings of the Royal Society, No. 14, November 1832.
Philosophical Transactions of the Royal Society of Lon-
don, for the Year 1833, part 2. London, 1833.
On the Former Extent of the Persian Gulf, and on the
comparatively recent Union of the Tigris and Euphra-
tes, by Charles T. Beke, Esq. 8vo. From the London
and Edinburgh Philosophical Magazine and Journal.
Messrs, Black, Young, and Young’s Catalogue of German
Books and Maps which have been published from
July to December 1833, 18mo.
Mémoires de la Société Géologique de France, tome lére,
lére partie, 4to. Paris, 1833.
Contributions to Geology, by Isaac Lea, Esq. 8vo.
Philadelphia, 1833.
Report of the Scarborough Philosophical Society, for
1833.
. Proceedings of the Royal Asiatic Society, January 4th,
1834.
. The Architectural Magazine and Journal of Improvement
in Architecture, Building and Furnishing, and in the va-
rious Arts and Trades connected therewith, conducted
by J. C. Loudon, Esq. F.G.S. vol. 1, No. 1, March 1834,
. Aide-Mémoire du Voyageur, ou Questions relatives a la
Géographie Physique et Politique, 4 l’ Industrie et aux
Beaux-arts, &c., a Usage des Personnes qui veulent
utiliser leurs Voyages, ou acquérir la Connoisance exacte
du Pays qu’elles habitent, 12mo. Paris, 1834.
. Sketches in Spain during the Years 1829, 1830, 1831
and 1832, containing Notices on some Districts very
little known; of the Manners of the People, Govern-
ment, recent Changes, Commerce, Fine Arts, and
Natural History, by Capt. S. E. Cook, R.N. K.T.S.
F.G.S. 2 vols. 8vo. London, 1834.
Entomological Magazine, vol. 1.
. Journal of the Royal Geographical Society of London,
vol. 3, part 2.
Des Causes de la plus Grande Taille des Espéces fossiles
et humatiles comparées aux Espéces vivantes, par
M. Marcel de Serres. Extrait de la Revue Encyclo-
pédique, Avril—Mai 1833, 8vo.
DONORS.
Mr. Hookham.
The Hon. The Court cf Di-
rectors of the East India
Company.
Gideon Mantell, Esq. F.G.S.
The Royal Society.
The Author.
Messrs. Black, Young, and
Young.
The Geological Society of
France.
The Author.
The Scarborough Philoso-
phical Society.
The Royal Asiatic Society.
The Conductor.
Colonel Jackson.
The Author.
F. Walker, Esq. F.G.S.
The Royal Geographical So-
ciety.
The Author.
8 List of Donations.
1834. BOOKS.
Mar. 13. De la Simultanéité des Terrains de Sédiment Supérieur,
par M. Marcel de Serres. Extrait du tome 5éme de la
Géographie Physique de I’Encyclopédie Méthodique,
Ato. Paris, 1830.
April 3. Considérations sur les Ossemens Fossiles la plipart in-
connus, trouvés et observés dans les Bassins de |’Au-
vergne, par M. Geoffroy St. Hilaire.
8. Report on the Geology, Mineralogy, Botany, and Zoo-
logy of Massachusetts; made and published by Order
of the Government of that State, with a descriptive List
of the Specimens of Rocks and Minerals collected for
the Government, by Edward Hitchcock, 8vo. Am-
herst, 1833.
14. Thirteenth Report of the Council of the Leeds Philoso-
phical and Literary Society, at the close of the Session
1832-1833.
Bulletin de la Société Géologique de France, tome 4€me,
feuilles 6-9, 8vo. Paris, 1833.
Proceedings of the Royal Society of Literature, vol. 1,
No. 5, January to March 1834.
Proceedings of the Royal Society, No. 15, December
1833, to March 1834.
Lettre sur le Déluge de la Samothrace 4 M. A. M.
Létronne, par M. Théodore Virlet, 8vo.
Notes Géologiques sur les Isles du Nord de la Gréce, et
en particulier, sur un Terrain de Calcaire d’ Eau douce
a Lignites, par M. Théodore Virlet. Extrait des
Annales des Sciences Naturelles, tome 30éme, 8vo.
Asiatic Researches. Transactions of the Physical Class of
the Asiatic Society of Bengal, part 2, 4to. Calcutta,
1833.
16. Proceedings of the Committee of Science and Correspon-
dence of the Zoological Society, for May, June, July,
August, September, October, November and Decem-
ber 1833, with a List of Contributors.
Prospectus of a Joint Stock Company for the Improve-
ment of Ireland, 8vo. London, 1834.
Gedrangte Uebersicht der Ergebnisse einer geogno-
stischen Erforschung des Odenwaldes und einiger an-
grenzenden Gegenden, mit besonderer Riicksicht auf
Andeutung der Verbreitungsgebiete der Formationen,
von Dr. A. Klipstein, 4to. Heidelberg, 1829.
History of the Berwickshire Naturalists’ Club, instituted
Sept. 22nd, 1831, 8vo. Edinburgh, 1834,
25. The History of the Royal Society of London for the Im-
proving of Natural Knowledge, by Thomas Sprat,
4to. London, 1667.
Transactions of the Royal Society of Edinburgh, vol. 12,
part 2, 4to. Edinburgh, 1834.
DONORS.
The Author.
The Author.
The Author.
The Leeds Philosophical and
Literary Society.
The Geological Society of
France.
The Royal Society of Lite-
rature.
The Royal Society.
The Author.
eeeeeeeeee
The Asiatic Society of Ben-
gal.
The Zoological Society.
Lt.-Col. Colebrooke, F.G.S.
The Author.
The Berwickshire Natura-
lists’ Club.
Roderick I. Murchison, Esq.
V.P.G.S.
The Royal Society of Edin-
burgh.
1834.
April 25
26
29.
May 4%
8.
10.
14,
16.
June
.
List of Donations.
BOOKS.
Proceedings of the Royal Society of Edinburgh, Nos. 1
and 2, December 1832 to May 1833, and No. 3, De-
cember 1833 to January 1834.
Catalogue des Livres de la Bibliotheque de Feu M,
T* **** *, 8vo. Paris, 1834.
M. A. Nattali’s Catalogue of Books, for May 1834.
The Transactions of the Linnean Society of London,
vol. 17, part 1, 4to. London, 1834.
Mr. T. Rodd’s Catalogue of Works on Arts and Sciences,
and Natural History.
Studi Geologici sulla Toscana del Professore Paolo Savi,
8vo. Pisa, 1833.
An Inaugural Lecture on the Study of Botany, read in
the Library of the Botanic Garden, Oxford, May 1st,
1834, by Charles Daubeny, M.D. F.G.S. Professor
of Chemistry and Botany in the University of Oxford,
8vo. Oxford, 1834.
Annual Report of the Council of the Yorkshire Philo-
sophical Society, for 1833, presented to the Annual
Meeting, February 4th, 1834, 8vo. York, 1834.
Outline of the Geology of the Neighbourhood of Chelten-
ham, by Roderick Impey Murchison, Esq. V.P.G.S.
&c. 8vo. Cheltenham, 1834.
Annual Report of the Committee of the Athenzeum
for the Year 1833, dated May 12th, 1834.
An Account of the Caves of Ballybunian, County of
Kerry, with some Mineralogical Details, by William
Ainsworth, Esq. 8vo. Dublin, 1834.
- Memoirs of the Royal Astronomical Society, vol. 7,
4to. London, 1834.
. Origines Biblicz, or Researches in Primeval History, by
Charles Tilstone Beke, Esq. vol. 1st, 8vo. London, 1834.
- Note ona Paper by Dr. John Davy, entitled, ‘‘ Notice on
the Remains of the recent Volcano in the Mediterra-
nean,” by Charles Daubeny, M.D. F.G.S. From the
Philosophical Transactions for 1833, 4to. London,
1833.
On the Quantity and Quality of the Gases disengaged
from the Thermal Spring which supplies the King’s
Bath in the City of Bath, by Charles Daubeny, M.D.
F.G.S. From the Philosophical Transactions for
1834, 4to. London, 1834.
Hoéhen Messungen inund um Thiringen, Gesammelt,
Verglichen und mit einigen Bemerkungen begleitet,
von K. E. A. von Hoff, 4to. Gotha, 1833.
Proceedings of the Royal Society, No. 16, April and
May 1834.
3. Bulletin de la Société Géologique de France, tome 4éme,
feuilles 10-14, 8vo. Paris, 1833.
9
DONORS.
The Royal Society of Edin-
burgh.
M. Silvestre.
Mr. Nattali.
The Linnean Society.
Mr. T. Rodd.
The Author.
The Author.
The Yorkshire Philosophical
Society.
The Author.
The Committee of the Athe-
nzeum.
The Author.
The Royal
Society.
Astronomical
The Author,
The Author.
The Author.
The Royal Society.
The Geological Society of
France.
Last of Donations.
BOOKS.
. Table des Matiéres et des Auteurs pour le troisiéme
Volume du Bulletinde la Société Geologique de France,
par M. Clément-Mullet.
Researches in Theoretical Geology, by Henry T. de la
Beche, Esq. V.P.G.S. 12mo. London, 1834.
. M. A. Nattali’s Catalogue of Books, for June 1834.
Magazin for Naturvidenskaberne. Udgives af den phy-
siographiske Forening i Christiania, Anden Reekkes,
Iste Binds, 2det Hefte, 8vo. Christiania, 1833.
. Journal of the Royal Geographical Society of London,
vol. 4, part 1, 1834,
. Transactions of the Cambridge Philosophical Society,
vol. 5, part 2, 4to. Cambridge, 1834.
. Experimental Researches in Electricity (Sixthand Seventh
Series), by Michael Faraday, Esq. D.C.L. F.G.S.
From the Philosophical Transactions for 1834, 4to.
London, 1834. -
. The American Journal of Science and Arts, conducted
by Benjamin Silliman, M.D. vol. 26, No. 1, 8vo.
New Haven, 1834.
. Descriptions of some new Species of Cuvier’s Family
of Brachiopoda, by W. J. Broderip, Esq. V.P.G.S.
Ato. From the Transactions of the Zoological Society,
vol. 1, part 2, 1834.
On the Anatomy of the Brachiopoda of Cuvier, and more
especially of the Genera Terebratula and Orbicula,
by Richard Owen, Esq. Assistant Conservator of the
Museum of the Royal College of Surgeons in London,
4to. From the Transactions of the Zoological Society,
vol. 1, part 2, 1834.
. An Address delivered at the third Annual Meeting of
the Geological Society of Dublin, on the 13th of Fe-
bruary 1834, by the Rev. Bartholomew Lloyd, D.D.
President of the Society ; to which is subjoined the
Annual Report, &c. 8vo. Dublin, 1834.
Journal of the Geological Society of Dublin, vol. 1, part 2,
8vo. Dublin, 1834.
. Premiums of the Society for the Encouragement of Arts,
Manufactures, and Commerce, for the Sessions 1834—
1835, 1835-1836, 8vo. London, 1834.
Annalesdes Mines, ou Recueil de Mémoires sur l’Exploi-
tation des Mines, et sur les Sciences et les Arts qui s’y
rapportent, rédigées par les Ingénieurs des Mines, et
publiées sous }’ Autorisation du Conseiller d’Etat, Direc-
teur Général des Ponts et Chaussées et des Mines, 3eme
Série, tome 6, 4éme livraison, 1834, 8vo. Paris, 1834.
9. The Athenaum Journal of English and foreign Litera-
ture, Science and Fine Arts, from January to June
1834, 4to. London, 1834.
DONORS,
The Geological Society of
France.
The Author,
Mr. Nattali.
H. C. Strém, Esq.
The Royal Geographical
Society.
The Cambridge Philosophi-
cal Society,
The Author.
The Conductor.
The Author.
Wm. J. Broderip, Esq.
V.P.G.S.
The Geological Society of
Dublin.
The Society of Arts.
L’ Administrationdes Mines.
The Editor.
1834.
July
11.
13
17.
19.
List of Donations.
BOOKS.
Transactions of the Royal Asiatic Society of Great
Britain and Ireland, vol. 3, part 3, 4to. London,
1834.
The Journal of the Royal Asiatic Society of Great Bri-
tain and Ireland, No. 1, 8vo. London, 1834.
Notice of Fossil Bones found in the Tertiary Formation
of the State of Louisiana, by Richard Harlan, M.D.
Read October 19th 1832. From the Transactions of
the American Philosophical Society held at Philadel-
phia, vol. 4.
Annales des Mines, ou Recueil de Mémoires sur l’Ex-
ploitation des Mines et sur les Sciences qui s’y rap-
portent, rédigées par les Ingénieurs des Mines, et
publiées sous ]’Autorisation du Conseiller d’Etat, Di-
recteur Général des Ponts et Chaussées et des Mines,
3éme Série, tome 5éme, 11éme livraison de 1834, 8vo.
Paris, 1834.
Report of the Third Meeting of the British Association
for the Advancement of Science, held at Cambridge in
1833, 8vo. London, 1834.
. Philosophical Transactions of the Royal Society of Lon-
don, for the Year 1834, part 1, 4to. London, 1834.
. A Manual of Mineralogy, comprehending the more re-
cent Discoveries in the Mineral Kingdom, by Robert
Allan, Esq. F.G.S. 8vo. Edinburgh, 1834.
Mémoire sur la Position Géologique des Principales
Mines de Fer de la Partie Orientale des Pyrénées ;
accompagné de Considérations sur Epoque du Sou-
lévement du Canigou, et sur la Nature du Calcaire de
Rancié, par M. Dufrénoy. Extrait des Annales des
Mines, 3éme Série, tome 5éme, 8vo. Paris, 1834. °
Transactions of the Zoological Society of London, vol. 1,
part 2, 4to. London, 1834.
. Quelques Observations de Physique Terrestre, par MM.
Auguste de la Rive et F. Marcet, 4to.
. Bulletin de la Société Géologique de France, tome 4éme,
feuilles 15-19, 8vo. Paris, 1834.
. Mémoire sur la Formation Jurassique dans le Nord de la
France, par M. E. Puillon Boblaye. Extrait des
Annales des Sciences Naturelles, Mai 1829, 8vo.
Paris, 1829.
Recherches sur les Roches designées par les Anciens
sous les Noms de Marbre Lacedemonien et d’Ophites,
par M. E. P. Boblaye, folio.
. Bulletin dela Société Géologique de France, tome 4éme,
feuilles 20-24, 8vo. Paris, 1834.
Verhandlungen der Gesellschaft des vaterlandischen Mu-
seums in Bohmen in der zwélften allgemeinen Ver-
sammlung, am 2 April, 1834, 8vo. Prag, 1834,
11
DONORS.
The Royal Asiatic Society of
Great Britain & Ireland.
The Author.
L’ Administration des Mines.
The British Association.
The Royal Society.
The Author.
The Author.
The Zoological Society.
The Authors.
The Geological Society
France.
The Author.
The Geological Society of
France.
The President of the Mu-
seu of Prague.
12
1834.
Aug. 14
18.
30.
Sept. 1.
18.
20
Oct. 16.
24
Nov. 95.
List of Donations.
BOOKS.
. Nautical and Hydraulic Experiments, with numerous
Scientific Miscellanies, by Colonel Mark Beaufoy,
F.R.S. vol. 1, 4to. London, 1834.
Résumé des Progrés des Sciences Géologiques pendant
V’Année 1833, par M. Ami Boué. Lu aux Séances
des17et 24 Février, et 7 Avril 1834, tome 5éme du
Bulletin de la Société Géologique de France, 8vo. Pa-
ris, 1834,
Contents of parts 2 and 3 of the Proceedings of the
Royal Society of London, 1831-1833.
Black, Young and Young’s Catalogue of German Books
and Maps which have been published from January
to June 1834, 12mo.
Abhandlungen der Kéniglichen Akademie der Wissen-
schaften zu Berlin, aus dem Jahre 1832 nebst der Ge-
schichte der Akademie in diesem Zeitraum, 4to. Ber-
lin, 1834.
Principles of Geology, being an Inquiry how far the
former Changes of the Earth’s Surface are referable to
Causes now in Operation, by Charles Lyell, Esq. For.
Sec. G.S. 3rd Edition, in four volumes, 12mo. Lon-
don, 1834.
Transactions of the American Philosophical Society,
held at Philadelphia, for promoting Useful Know-
ledge. New Series, vol. 4, part 3, 4to. Philadelphia,
1834.
. ACollection of Geological Facts and practical Observa-
tions intended to elucidate the Formation of the Ashby
Coal Field, by Edward Mammatt, Esq. F.G.S. 4to.
Ashby-de-la-Zouch, 1854.
The American Journal of Science and Arts, conducted
by Benjamin Silliman, M.D. For. Mem. G.S. vol. 26,
No. 2, July 1834, 8vo. New Haven, 1834.
. Memorie della Societa Italiana delle Scienze residente in
Modena, tomo 20, fascicolo secondo delle Memorie
di Fisica, 4to.
Sul Problema dell’ Equilibrio delle Volte. Memoria del
Signor Dottore Vincenzo Amici, Coronata dalla Societa
Italiana delle Scienze residente in Modena, 4to. Mo-
dena, 1833.
A Treatise on the Epidemic Cholera; containing its Hi-
story, Symptoms, Autopsy, Etiology, Causes and
Treatment, by Alexander Turnbull Christie, M.D.
8vo. London, 1833.
Elements of Chemistry, including the recent Disco-
veries and Doctrines of the Science, by Edward
Turner, M.D. Sec.G.S. Fifth Edition, 8vo. London,
1834.
DONORS.
Henry Beaufoy, Esq. F.R.S.
The Author.
The Royal Society.
Messrs. Black, Young and
Young.
The Berlin Academy.
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cal Society.
The Author.
The Conductor.
The Society.
The Author. .
George Turnbull, Esq.
The Author.
14,
18.
ale
List of Donations.
BOOKS.
. Observations on the Genus Unio, together with Descrip-
tions of new Genera and Species in the Families
Naiades, Conche, Colimacea, Lymnzana, Melaniana
and Peristomiana ; consisting of Four Memoirs read
before the American Philosophical Society, from 1827
to 1834, and originally published in their Transac-
tions, by Isaac Lea, Esq. 4to. Philadelphia, 1834.
Recherches sur les Ossemens Fossiles, découverts dans
les Cavernes de Ja Province de Liége, par le Docteur
P. C. Schmerling, 2éme partie, complétant le premier
volume, 4to. Liége, 1833.
Mémoires de la Société de Physique et d’Histoire Na-
turelle de Genéve, tome 6éme, parties 1 et 2, 4to. Ge-
neve, 1833.
The American Journal of Science and Arts, conducted
by Benjamin Silliman, M.D. LL.D. vol. 27, No. 1,
Oct. 8vo. New Haven, 1834.
The Fourteenth Report of the Council of the Leeds Phi-
losophical and Literary Society, at the close of the
Session 1833-1834, 8vo. Leeds, 1834.
A Catalogue of the Fellows, Candidates and Licentiates of
the Royal College of Physicians, 8vo. London, 1834.
. Nouveaux Mémoires de la Société Impériale des Natu-
ralistes de Moscou, dédiés 4 S. M. l’Empereur Ni-
cholas I. tome 3, 4to. Moscou, 1834.
Bulletin de la Société Impériale des Naturalistes de Mos-
cou, tome 6, 8vo. Moscou, 1833.
A Treatise on Nautical Surveying: containing an Out-
line of the Duties of the Naval Surveyor ; with Cases
applied to naval Evolutions and miscellaneous Rules
and Tables useful to the Seaman or Traveller, by Com-
mander Edward Belcher, R.N. 8vo. London, 1835.
. Observations Géologiques sur les deux Isles Baleares,
Majorque et Minorque, par le Chevalier Albert de la
Marmora, 4to. Turin, 1834.
Transactions of the Geological Society of Pennsylvania,
vol. 1, part 1, 8vo. Philadelphia, 1834.
A descriptive Catalogue of the Collection illustrative of
Geology and Fossil Comparative Anatomy, in the
Museum of Gideon Mantell, LL.D. F.G.S. 3rd Edi-
tion, 8vo. London, 1834.
The Magazine of Natural History and Journal of Zo-
ology, Botany, Mineralogy, Geology and Meteorology,
conducted by J. C. Loudon, Esq. F.G.S. &c., for the
Year 1834, 8vo.
The London and Edinburgh Philosophical Magazine and
Journal of Science, conducted by Sir David Brewster,
K.H. LL.D. F.G.S. &c., Richard Taylor, Esq. F.G.S.
&c.,and R. Phillips, Esq. F.G.S. &c., for the Year 1834.
15
DONORS.
The Author
The Author.
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story of Geneva.
The Conductor.
The Leeds Philosophical and
Literary Society.
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sicians.
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turalists of Moscow.
The Author.
The Author.
The Geological Society of
Pennsylvania.
Gideon Mantell, LL.D
F.G.S.
The Conductor.
The Conductors.
Whe
12.
17.
List_ of Donations.
BOOKS.
_ The Horticultural Register and General Magazine of
all useful and interesting Discoveries connected with
Natural History and Rural Subjects, conducted by
Joseph Paxton, for the Year 1834.
. A Guide to Geology, by John Phillips, Esq. F.G.S.
Professor of Geology in King’s College, London, 12mo.
London, 1834.
Transactions of the American Philosophical Society held
at Philadelphia, for promoting Useful Knowledge,
vol. 3, part 2. New Series, 4to. Philadelphia, 1834.
Rules and Regulations for the Government of the Athe-
neum, with an Alphabetical List of the Members,
&c. 12mo. London, 1834.
Transactions of the Medico-Botanical Society of London,
for 1832 and 1833, 8vo. London, 1834.
Experimental Researches in Electricity (Eighth Series), by
Michael Faraday, Esq. F.G.S. &c. From the Philoso-
phical Transactions, part 2, for 1834, 4to. London,
1834.
A Journey from Sydney to the Australian Alps, by Dr.
John Lhotsky.
Geschichte der durch tberlieferung nachgewiesenen na-
tiirlichen Veranderungen der Erdoberflache ein Ver-
such, von Karl E.A. von Hoff, 3te Theil, 8vo. Gotha,
1834.
Lethza Geognostica, oder Abbildung und Beschreibung
der fir die Gebirgs-Formationen bezeichnendsten
Versteinerungen, von Dr. H. G. Bronn, 1ster Lie-
ferung, Stuttgart, 1834.
Canal de Jonction entre le Rhin et le Danube, par Ch.
Th. Kleinschrod. Traduit de |’Allemand, 8vo. Munich,
1834.
Bulletin de la Société Géologique de France, tome 4éme,
feuilles 28 et 29, 8vo. Paris, 1834.
The Philosophical Transactions of the Royal Society of
London, for the Year 1834, part 2, 4to. London, 1834.
Proceedings of the Royal Society of London, No. 17,
May and June 1834, 8vo.
The Repertory of Patent Inventions, and other Disco-
veries and Improvements in Arts, Manufactures and
Agriculture. New Series, for the Year 1834, 8vo. Lon-
don, 1834.
Annales des Mines, ou Recueil de Mémoires sur l’Ex-
ploitation des Mines, et sur les Sciences et les Arts
qui s’y rapportent, rédigées par les Ingénieurs des
Mines, et publiées sous ]’Autorisation du Conseiller
d’Etat, Directeur Général des Ponts et Chaussées et
des Mines, 3eme Série, tome 6, 5éme livraison, 8vo.
Paris, 1834.
DONORS.
The Conductor.
The Author.
The American Philosophi-
cal Society.
The Committee of the Athe-
nzeum.
The Medico-Botanical So-
ciety.
The Author.
The Author.
The Author.
The Author.
The Author.
The Geological Society of
France.
The Royal Society.
The Editor.
L’ Administration des Mines.
1835.
Jan. | 3:
9.
26.
Feb. 1
List of Donations.
BOOKS.
M.A. Nattali’s Catalogue of Books in various Languages,
for the Year 1835, 8vo. London, 1834.
T. Rodd’s Catalogue of Books for the year 1835, 8vo.
Descriptive and illustrated Catalogue of the Physiologi-
cal Series of Comparative Anatomy contained in the
Museum of the Royal College of Surgeons in London,
vol. 2, including the Absorbment, Circulating, Respi-
ratory, and Urinary Systems, 4to. London, 1834.
Transactions of the Society for the Encouragement of
Arts, Manufactures and Commerce, for the Session
1833-1834, being part 1 of vol. 50, 8vo. London, 1834.
Records of General Science, by Robert D. Thomson,
M.D. with the Assistance of Thomas Thomson, M.D.
F.G.S. Regius Professor of Chemistry in the Univer-
sity of Glasgow, No. 2, February 1835, 8vo. London,
1835.
On the Structure of the Teeth, in the “ Edentata,” fossil
and recent, by Richard Harlan, M.D. Read April 28th,
1834. From the Transactions of the Geological So-
ciety of Pennsyivania, vol. 1.
Critical Notices of various organic Remains hitherto
discovered in North America, by Richard Harlan,
M.D. Read May 21st, 1834. From the Transactions
of the Geological Society of Pennsylvania, vol. 1.
Bohn’s Catalogue of Ancient and Modern Books in all
Classes of Natural History, Agriculture, Gardening,
Mining, Hunting, Hawking, Fishing, &c. 8vo. Lon-
don, 1835.
Arboretum Britannicum ; or the Hardy Trees of Britain,
native and foreign, pictorially and botanically deli-
neated, and scientifically and popularly described, &c.,
by J.C. Loudon, Esq. F.G.S. Nos. 1 and 2, 8vo. Lon-
don, 1835.
Dictionnaire Géographique de la Province d’Anvers, et
Dictionnaire Géographique de la Province de la Flan-
dre Orientale, par M. Ph. Vander Maelen, 2 vols. 8vo.
Bruxelles, 1834.
Proceedings of the Royal Society of London, No. 18,
Nov. 1834.
Journal of the Royal Geographical Society, vol. 4, part 2,
8vo. London, 1835.
A Letter to James Jameson, Esq., by Charles Waterton,
Esq. of Walton Hall, 8vo. Wakefield, 1835.
On the Freshwater Limestone of Burdiehouse, in the
Neighbourhood of Edinburgh; with Supplementary
Notes on other Freshwater Limestones, by Samuel
Hibbert, M.D. F.G.S. From the Transactions of the
Royal Society of Edinburgh, vol. 13, part 1, 4to.
Edinburgh, 1835.
15
DONORS.
Mr. M. A. Nattali.
Mr. T. Rodd.
The Royal College of Sur-
geons.
The Society of Arts.
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eeeeeeeeee
Mr. John Bohn.
The Author.
M. Ph. Vander Maelen.
The Royal Society.
The Royal Geographical So-
ciety.
The Author.
The Author.
16
1835.
List of Donations.
BOOKS.
Feb. 1. The Analyst, a monthly Journal of Science, Literature
Mar.
and the Fine Arts, No. 7, February 1835, 8vo.
London, 1835.
Asecond Copy of the same Number was presented by the
Editor, March 7th.
Analysis of Coprolites and other organic Remains im-
bedded in the Limestone of Burdiehouse, near Edin-
burgh, by Arthur Connell, Esq. From the Transac-
tions of the Royal Society of Edinburgh, vol. 15, 4to.
Edinburgh, 1835.
On the Satellites of Uranus, by Sir J. F. W. Herschel,
Knt. Guelp. F.G.S. From the Memoirs of the
Royal Astronomical Society, vol. 8, 4to. London,
1834,
A List of Test Objects, principally double Stars, arranged
in Classes, for the trial of Telescopes in various Re-
spects, as to Light, Distinctness, &c., by Sir J. F. W.
Herschel, Knt. Guelp. F.G.S. From the Memoirs
of the Royal Astronomical Society, vol. 8, 4to. Lon-
don, 1834.
A Second Series of Micrometrical Measures of double
Stars, chiefly performed with the seven-feet equatorial,
at Slough, in the Years 1831, 1832 and 1833, by Sir
J. F. W. Herschel, Knt. Guelp. F.G.S. From the
Memoirs of the Royal Astronomical Society, vol. 8,
4to, London, 1834.
Transactions of the American Philosophical Society, held
at Philadelphia, for promoting Useful Knowledge,vol.5.
New Series, part 1, 4to. Philadelphia, 1834.
Bulletin de la Société Géologique de France, tome 6,
feuilles 1-4, 8vo. Paris, 1835.
Raccolta di Osservazioni Cliniche sull’ Uso dell’ Acqua
Termo-Minerale Vesuviana-Nunziante, Fatte da varii
Professori del 1832, fascicolo primo, 8vo. Napoli,
1833.
Raccolta di Osservazioni intorno gli Effetti Terapeutici
e le Cure per Acqua Termo-Minerale Vesuviana-
Nunziante corrente l’Anno 1833. Preceduta da una
Memoria scritta dal Professore Guiseppe Ricci, fasci-
colo secondo, 8vo. Napoli, 1834.
. A History of British Fishes, by William Yarrell, F.L.S.
part J, 8vo. London, 1835.
3. The West of England Journal of Science and Literature,
edited by George T. Clark, No. 1, January 1835,
8vo. Bristol, 1835.
Journal of the Academy of Natural Sciences of Philadel-
phia, vol. 7, part 1, 8vo. Philadelphia, 1834.
List of the Members of the Zoological Society of London,
June Ist, 1833, 8vo. London, 1833.
DONORS.
Hugh E. Strickland, Esq.
F.G.S.
The Author.
The Author.
The Author.
enreeseeeee
The American Philosophical
Society.
The Geological Society of
France.
Charles Daubeny, M.D.
F.G.S.
ee eeee reese ae ee eter oeee
The Author.
The Editor.
The Academy of Natural
Sciences of Philadelphia.
The Zoological Society.
1835.
Mar. 7.
26.
April 3.
6.
List of Donations.
BOOKS.
Supplement to the List of the Members of the Zoologi-
cal Society, June 1834.
List of the Members of the Royal Asiatic Society of
Great Britain and Ireland, 1834. 8vo.
List of the Members of the Royal Society of London,
Ist Dec. 1834, 4to.
Report on the Adjudication of the Copley, Rumford, and
Royal Medals; and appointment to the Bakerian,
Croonian, and Fairchild Lectures. 4to. London, 1834.
List of the Members of the Society of Antiquaries of
London. 4to. 1834.
List of the Members of the Linnean Society of London.
4to. 1834.
List of the Members of the Horticultural Society of Lon-
don. 4to. 1834.
. The American Journal of Science and Arts, conducted
by Benjamin Silliman M.D. LL.D., vol. 27, No, 2.
8vo. New Haven, 1835.
Transactions of the Royal Society of Edinburgh, vol. 13,
part 1. 4to. Edinburgh, 1835.
Proceedings of the Royal Society of Edinburgh, No, 4,
January to April, 1834. 8vo.
23, Bibliographia Paleonthologica Animalium systematica.
Auctore Gotthelf Fischer de Waldheim. Editio altera,
aucta, jussu Societatis Czesareze Nature Scrutatorum
impressa. 8vo. Mosque, 1834.
The Journal of the Royal Asiatic Society of Great Bri-
tain and Ireland, No. 2. 8vo. London, 1834.
Voyage dans ]’Amérique Méridionale commengant par
Buénos Ayres et Potosi jusqu’a Lima, par Antoine-
Zachaire Helms, traduit de l’Anglais. 8vo, Paris, 1815.
The Entomological Magazine, Nos. 6-9 for January to
October 1834, and Nos. 10 and 11 for January and
April 1835. 8vo. London.
Illustrations of the Botany and other Branches of the
Natural History of the Himalayan Mountains, and of
the Flora of Cashmere; by J. Forbes Royle, Esq.,
F.G.S., &c. parts 1 to 5. fol. London, 1834, 1835,
Memoirs of Ichthyosauri and Plesiosauri, extinct Mon-
sters of the Ancient Earth; by Thomas Hawkins, Esq.
F.G.S. fol. London, 1834.
Transactions of the Zoological Society of London, vol. 1,
part 3, 4to. London, 1835.
A memoir on Clavagella; by W. J. Broderip, Esq.,
V.P.G.S. From the Transactions of the Zoological
Society, vol. 1. 4to.
Descriptions of some New Species of Calyptreide; by
W. J. Broderip, Esq., V.P.G.S. From the Transac-
tions of the Zoological Society, vol. 1. 4to.
17
DONORS.
The Zoological Society.
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The Royal Society.
The Society of Antiquaries.
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The Horticultural Society.
The Conductor.
The Royal Society of Edin-
burgh.
The Author.
The Royal Asiatic Society of
Great Britain and Ireland.
John Willimott, Esq. F.G.S.
F. Walker, Esq. F.G.S.
The Author.
The Author.
The Zoological Society.
The Author.
eseeeeee00
is List of Donations.
1835. BOOKS. DONORS.
April 27. Views in Ethnography, the Classification of Languages,
the Progress of Civilization, and the Natural History
of Man; by Charles T. Beke, Esq. From the Edin-
burgh New Philosophical Journal for April 1835.
8vo. The Author.
Report of the Directors of the Manchester Mechanics’
Institution, and Proceedings at the Annual Meeting
of the Members held in the Theatre of the Institution |The Manchester Mechanics’
on Thursday, 26th February, 1835. 8vo. Institution.
A Catalogue of the Library of the Manchester Mechanics’
Institution, with the Rules anda Sketch of the Objects
and Advantages of the Institution. 8vo. Manchester,
1834.
28. The Chemical Catechism, by the late Samuel Parkes,
F.G.S. &c. &c. Thirteenth Edition; revised and
adapted to the present state of Chemical Science by
E. W. Brayley, Jun. 8vo. London, 1834. The Editor.
29. Illustrations on the Botany and other Branches of the
Natural History of the Himalayan Mountains and of
the Flora of Cashmere; by John Forbes Royle, Esq.
F.G.S. &c. part 6. folio. London, 1825. (he Authoe:
Proceedings of the Royal Society of London, No. 19
December 1834 to March 1835. 8vo.
May 1. Experimental Researches in Electricity (Ninth Series) ;
by Michael Faraday, Esq. D.C.L. F.G.S. &c. From
the Philosophical Transactions, part 1. for 1835, 4to.
London, 1835.
Arboretum Britannicum, or, the Hardy Trees of Britain
Native and Foreign, pictorially and botanically deli-
neated, and scientifically and popularly described ; by
J.C. Loudon, Esq. F.G.S. No. 5, May. 8vo. London,
1835. The Author.
Ueber Terebrateln mit einem Versuch, sie zu classificiren
und zu beschreiben; von Leopold von Buch, Eine in
der K6niglichen Akademie der Wissenschaften gele-
sene Abhandlung. fol. Berlin, 1834. The Author.
Nouvelles Annales du Muséum d’Histoire Naturelle, ou
Recueil de Mémoires publiés par les Professeurs de
cet Etablissement et par d’autres Naturalistes sur L’Administration du Mu-
The Royal Society.
The Author.
V'Histoire Naturelle, Anatomie, et la Chimie, tomes séum d’ Histoire Naturelle
143. 4to. Paris, 1832-1834. de Paris.
4. Mr. M. A. Nattali’s Catalogue of Books for May 1835.
8vo. Mr. Nattali.
A Guide to Geology; by John Phillips, Esq. F.G.S.
Professor of Geology in King’s College, London. 2nd
Edition. 12mo. London, 1835. The Author.
Sketch of the Geology and Mineralogy of New London
and Windham Counties in Connecticut ; by Wm. W.
Mather. 8vo. Norwich, U.S., 1834. The Author.
Fast of Donations. 19
1835. BOOKS. DONORS.
May 12. An Address delivered at the Fourth Annual Meeting of
the Geological Society of Dublin, on the 11th of Fe-
bruary, 1835, by Richard Griffith, Esq. F.G.S. Pre-
sident of the Society: to which is subjoined the Annual T. H. Holdsworth, Esq.
Report, &c. &c. 8vo. Dublin, 1835. F.G.S.
Notice as to the supposed Identity of the large Mass of
Meteoric Iron now in the British Museum, with the
celebrated Otumpa Iron described by Rubin de Celis
in the Philosophical Transactions for 1786 ; by Wood-
bine Parish, Jun., Esq. F.G.S. From the Philoso-
phical Transactions, part 1. for 1834. 4to. London,
1834. The Author,
21. The American Journal of Science and Arts, conducted
by Benjamin Silliman, M.D. LL.D. vol. 28, No. 1,
April, 1835. 8vo. New Haven, 1835. The Conductor.
27. Notices on the Bolivian Andes, and Southern Affluents
of the Amazons, communicated to the Royal Geogra-
phical Society by J. B. Pentland, Esq. and Woodbine
Parish, Jun. Esq. F.G.S. From the Journal of the
Royal Geographical Society. 8vo. 1835. The Communicators.
* How to Observe” Geology; by H. T. De la Beche,
Esq. For, Sec. G.S. 8vo. London, 1835. The Author.
20. Synopsis of the Organic Remains of the Cretaceous
Group of the United States; by Samuel George
Morton, M.D. 8vo. Philadelphia, 1834. The Author.
The Repertory of Patent Inventions, and other Disco-
veries and Improvements in Arts, Manufactures and
Agriculture. New Series for the Year 1835. 8vo.
London, 1835. The Editor.
June 2. Revelation and Science: the Substance of a Discourse
delivered before the University of Oxford at St. Mary’s,
March 8th, 1829, with some additional Remarks oc-
casioned by the publication of the Bampton Lectures
for 1833 and other recent Works; by the Rev. Baden
Powell, M.A. Savilian Professor of Geometry inthe The Rev. James Yates,
University of Oxford. 8vo. Oxford, 1833. F.G.S.
4. Instructions for making and registering Meteorological The South African Literary
Observations in Southern Africa, and other countries and Philosophical Institu-
in the South Seas, as also at Sea. 8vo. tion.
The Cyclopedia of Anatomy and Physiology; edited by
Robert B. Todd, M.B. part 1, published by Sherwood
and Co. 8vo. London, 1835. The Publishers.
5. Arboretum Britannicum, or, the Hardy Trees of Britain,
Native and Foreign, pictorially and botanically deli-
neated, and scientifically and popularly described, by
J. €. Loudon, No. 6, June. 8vo. London, 1835. The Conductor.
Volcanic Geology, by Professor Daubeny, M.D. F.G.S,
From the Encyclopedia Metropolitana 4to. The Author.
1834.
Jan.
Mar. 25
April 14
Nov. 5
14
25.
List of Donations.
BOOKS.
. Revue Critique des Poissons Fossiles figurés dans !’Ittio-
litologia Véronese ; Rapport sur les Poissons Fossiles
decouverts en Angleterre; par M. L. Agassiz.
The Horticultural Register and General Magazine of all
Useful and Interesting Discoveries connected with
Natural History and Rural Subjects ; conducted by
Joseph Paxton, from January to June 1835. 8vo,
London, 1835.
The Magazine of Natural History and Journal of Zoo-
logy, Botany, Mineralogy, Geology and Meteorology ;
conducted by J. C. Loudon, Esq. F.G.S. From
January to June 1835. 8vo, London, 1835.
DONORS.
The Author.
The Conductor.
The Conductor.
II. Donations to the Collections of Maps, Drawings, &c
MAPS, &c.
. Carte de I’Ile et Dé partement de la Corse, et une Carte et
Plan de Constantinople et du Canal du Bosphore. 2
sheets.
An Impression of the engraved Portrait of the Rev.
Prof. Sedgwick.
Series of Charts containing Surveys mostly executed in
the Indian Seas by Officers in the East India Com-
pany’s Marine Service.
Sheet No. 45 of the Ordnance Map in continuation of
the Trigonometrical Survey of Great Britain.
Sixteen Charts of part of the Mediterranean, the Coast
of Portugal, &c.
. Head of an Ichthyosaurus, painted with Fossil Sepia.
» Sheet No. 62 of the Ordnance Map in continuation of
the Trigonometrical Survey of Great Britain.
- Sheets Nos. 53 and 57 of the Ordnance Map, in con-
tinuation of the Trigonometrical Survey of Great
Britain.
. Copy of the Lithographic Plate accompanying M. Jules
de Christol’s “Recherches sur les Caractéres des
Grandes Espéces de Rhinoceros Fossiles.”
19, The Ordnance Townland Survey of the County of
1835.
Mar. 31
Tyrone.
- An Impression of a Lithographic Drawing of Calymene
arachnoides.
DONORS.
M. Donati.
Thomas Phillips, Esq. R.A.
The Hon. the Court of Di-
rectors of the East India
Company.
The Master-general and
Board of Ordnance.
Capt. Beaufort, R.N. Hon.
Mem.G.S., by orderof the
Lords Commissioners of
the Admiralty.
H. T. De la Beche, Esq.
F.G.S.
The Master-general
Board of Ordnance.
and
M. Jules de Christol.
Lieut.-Col. Colby, by order
of His Excellency the
Lord Lieutenant of Ire-
land.
M. F. Wm. Hoeninghaus.
1835.
ad 13.
19;
21.
1833.
July 1
Sept. 19.
30.
List of Donations.
MAPS, &c.
An Outline Map of the World on Mercator’s Projection,
drawn by C. Bradbury.
No. 46 of the Ordnance Map in continuation of the
Trigonometrical Survey of Great Britain,
Ordnance Townland Survey of the County of Down, in
59 sheets.
The N.E. quarter sheet of the 63rd sheet of the Ordnance
Survey, coloured geologically by H. Still, Esq. em-
ployed in the Ordnance Survey.
21
DONORS.
Mr. Bradbury.
The Master-general
Board of Ordnance.
Lieut.-Col. Colby, by order
of his Excellency the
Lord Lieutenant of Ire-
land.
and
Henry Still, Esq.
III. Donations to the Cabinet of Minerals.
SPECIMENS.
Agate Nodules from the Magnesian Limestone, Mendip
Hills.
Copper Slags from Swansea.
Specimens from the Mountain Limestone in the neigh-
bourhood of Tenby.
Bones of the Elephant, Rhinoceros, and Ox, from the
gravel, Brockhall Lawford.
Fossils from the Cliffs at Hastings and St. Leonards, and
a Tree from the Submarine Forest near St. Leonards.
Specimens of Endogenites erosa from St. Leonards.
Specimens from the Submarine Forest near Hastings.
Specimens of Wood perforated by a Pholas.
Specimen of Thorit.
. Three Fishes from the Magnesian Limestone, Thickley.
Specimens of Cyrtoceratitis costatus from Gerolstein.
. A series of specimens from the North Shore of the
River St. Lawrence.
Specimens of Lead Ore, from Gador, South of Spain.
Specimen of Fossil Wood perforated by Teredina per-
sonata.
Specimens from Vesuvius, Calabria, Sicily and Mount
St. Gothard, &c.
A Specimen of Marble perforated by Lithodomi obtained
from a Ship sunk in the Leghorn Roads in the year
1750.
A specimen of rock salt from Huamanga between Huan-
cavelica and Cusco.
A collection of specimens made in the crater of Vesu-
vius,
. Chromate of Lead from Siberia.
. Specimens from Malta.
A specimen of the Hastings sandstone.
DONORS.
The Rev. Prof. Buckland,
D.D. F.G.S,
eeeeeeeeoeneee eres eoseeee
The Rev. T. Salway.
The Rev. Wm. Thornton.
Woodbine Parish, Jun. Esq.
F.G.S.
Wm. Henry Fitton, M.D.
VEG,
Robert Wrench, Esq.
Capt. Belcher, R.N. F.G.S
Prof. Esmark, For. Mem.
G.S.
Wm. P. Cumby, Esq.
M. J. W. Hoeninghaus.
Capt. Bayfield, R.N.
John Willimot, Esq. F.G.S.
Henry C. White, Esq.F.G.S.
Count Bylandt.
W. Richardson, Esq.F.G.S
J. M. Maclean, Esq.
John Auldjo, Esq. F.G.S.
Mons. Donati.
J. W. Collings, Esq.
Charles, Babbage, Esq.
22
1833.
Dee. 18.
1834.
Jan. 8
22
Feb. 5.
26
Mar. 12
95
April 9.
List of Donations.
SPECIMENS.
Specimens of Asbestus.
Specimens from the Azores.
Specimens in illustration of Capt. Burnes’s Memoir on
the Geology of the Banks of the Indus, the Indian
Caucasus, and the Plains of Tartary to the Shores of
the Caspian.
Specimens from Jersey.
. Specimens from the Old Red Sandstone of South Wales.
. Casts of perforations by T'eredina personata from the
Plastic Clay, Hengisbury, Hants.
Suite of rocks and fossils to illustrate Mr. Murchison’s
paper on “ Herefordshire, Shropshire, and parts of
Wales.”
Specimens from Australia.
Casts of the Bones of the Megatherium from Buenos Ayres,
brought home by Woodbine Parish, Jun. Esq. F.G.S.
Casts of the Inferior and Maxillary Bones of the Mas-
todon and Tetracaulodon.
Specimens from the Coal-Field of Wyre Forest.
. Fossils from the Plastic Clay near Reading.
Specimens from the Islot of Alcatraz on the West Coast
of Africa, and from Gibraltar and Keith’s Reef between
Sicily and the coast of Africa.
Fossil Plants, Insects and Fishes from Aix in Provence.
Specimens of Lignite from Leira.
2. Specimens from France.
Corals from Aymestry.
. Cast of an Ophiura ; from the Lias, banks of the Severn.
Specimens of plants from the Greensand Formation of
Niedershona near Freyberg.
An Hippurite from Sicily.
Additional specimens from the Eifel.
Specimens of the Southstone Roche near Tenbury, Wor-
cestershire.
Specimens from the Mountain Limestone and Greensand
of England.
Fossil Fishes from Monte Bolca.
Specimens from Port Macquarie.
Selenite from the London Clay near Herne Bay.
. Portions of Septaria from the London Clay at Brixton,
and Fossil Wood perforated by Teredina personata.
. Native Iron from the Mass in the British Museum from
Otumpa in the Chaco, South America.
. Specimens from the Tertiary Formations of Murcia.
. Specimens of Pentamerus oblongus.
DONORS.
Richard Knight, Esq.F.G.S:
The Rev. J. H. Simpson.
Capt. Alexander Burnes.
Ashurst Magendie, Esq.
F.G.S.
Roderick I. Murchison, Esq.
F.G.S.
The Rev. Prof. Buckland,
D.D. F.G.S.
R.1I. Murchison, Esq.F.G.S.
Capt. H. Smyth, 39th Regt.
The Royal College of Sur-
geons.
The American Philosophi-
cal Society.
The Rev. Thos. England,
F.G.S.
John Rofe, Jun. Esq.
Capt. Belcher, R.N. F.G.S.
Geo. Bentham, Esq. F.G.S.
Richard Hollier,Esq.F.G.S.
R. I. Murchison, Esq.
V.P.G.S.
The Rev. T. T. Lewis.
Mathew Wright,Esq.F.G.S.
M. Felipe Bauza, Jun.
M. le Comte Duchatel.
LeonardHorner,Esq.F.G.S.
R. I. Murchison, Esq.
V.P.G.S.
eoeereereeeeoere esses eoese
Capt. H. Smyth, 39th Regt.
W. Richardson, Esq. F.G.S.
The Rev. Prof. Buckland,
D.D. F.G.S.
Woodbine Parish, Jun. Esq.
F.G.S.
Chas. Silvertop, Esq. F.G.S.
Mr. Rees.
1834.
April 25. Fossils of the Grauwacke Series of Shropshire.
May
July
Aug.
Nov.
21.
3.
List of Donations.
SPECIMENS.
Fossils from the Grauwacke of the neighbourhood of
Llandovery.
A large specimen of the polished Limestone found near
Gwinfe in Caermarthenshire.
. Cast of a Palatal Bone from the Chalk.
Specimens of Rowley Rag, unaltered, decomposed and
fused.
. Lava from Graham’s Island.
. Specimens of Greenstone, Porphyry and Sienite from the
Border Counties of England and Wales.
. Specimens from the Hastings sand.
Specimens from Spain.
Slickensides, from Cornwall.
. Fish from the Magnesian Limestone.
. Specimens from the Mines of Konigsberg, Norway.
A specimen of artificial cupriferous Iron Pyrites.
Fish from Monte Bolca.
Carbonate of Strontia with calcareous Spar and Brown
Iron Ore, Forest of Dean.
Minerals from the Trap of Scotland.
Corals from the Shale beds of the Mountain Limestone,
County of Fermanagh.
Casts of the Remains of Felis spelea and Gulo speleus
from Gailenreuth.
Magnetic Iron Ore from Sierra Leone.
Specimens from Tampico.
Specimens taken from the crater of the Water Volcano
near Guatemala.
A Fossil Crab from India (Gonoplax Latreillii),
7. Fossils from the neighbourhood of St. Ives.
20. Specimens from the London Clay at Hornsey.
14.
12.
13.
Specimens from the Channel Islands.
Cast of a claw-bone of a Crocodile, and of an Iguanodon
from Tilgate Forest.
. Cast of a Palatal Tooth from the Chalk of Dorsetshire.
Specimens from the Loam of Muswell Hill; and addi-
tional specimens from a well at Hornsey.
Remains of Anthracothertum Velaunum, Myoxus and Cro-
codile from Puy en Velay.
23
DONORS.
W. Williams, Esq.
Prof. Miller, F.G.S.
The Rev. T. T. Lewis.
Nathaniel Wetherell, Esq.
F.G.S.
John Corrie, M.D. F.G.S.
Capt. Stewart.
R. I. Murchison,
V.P.G.S.
Baden Powell, Esq. F.G.S.
Capt. Cook, R.N. F.G.S.
R. Taylor, Esq. F.G.S. of
Perran, Arworthal.
J. W. Colling, Esq.
H.C. Strom, Esq. Engineer
of Mines.
Esq.
ae L. Pratt Esq. F. G. S.
Capt. Yorke, R.N.
G. B. Greenough, Esq.
Pres.G.S.
Viscount Cole, M.P.F.G.S.
and Sir Philip Egerton,
Bart. F.G.S.
oe eee eee esos eeeeeeroeee
David Bastiat Esq. H.M.
G.S.
Thos. Weaver, Esq. F.G.S.
Col. Galindo.
The Right Hon. the Earl
of Cawdor, F.G.S.
J.R.Wright, Esq. F.G.S, and
H. Machlauchlan, Esq.
F.G.S.
N. T.Wetherell, Esq. F.G.S.
W.C. Trevelyan, Esq.F.G.S.
Gideon Mantell, Esq. F.G.S.
The Rev. Prof. Buckland,
D.D. F.G.S.
N.T. Wetherell,Esq. F.G.S.
M. Bertrand de Doue,
For. Mem. G.S.
ro)
List of Donations.
SPECIMENS.
. Fossils from Bognor and the Chalk near Felpham.
Palatal Teeth of an Eagle Ray, (Myliobatis, Cuv.) from
Bermuda.
Specimens of recent Coral from the Straits of Sunda.
Specimens from the Big Bend on the Missouri.
Tertiary Shells from the United States.
Specimens from the Ancient Beach at Hope’s Nose near
Babbacombe and from the Watcomb Fault, Devon-
shire.
. Specimens from China.
Specimens of Granite traversed by veins, from Dartmoor.
Vegetable Remains from the Anthracite of North De-
von.
Specimens from Australia.
. Anthracite from the Lehigh Coal Mine, Pennsylvania.
Palatal Tooth of a Fish from the Chalk.
Fossils from the Greensand near Lyme.
Hippurite from Untersberg.
Cast of a Molar Tooth of Mastodon angustidens from
the Crag, Suffolk.
. Shells from the Loam and Gravel near Cropthorne, Wor-
cestershire.
2, Fossils from the neighbourhood of Ilfracombe.
Specimens from the Coal of the South of Ireland.
. Fossils from the Calcaire Grossiere of France.
Casts from Flambro’ Head of Spongeous Zoophites.
Shells and Bones of Mammalia from Stutton, Suffolk, and
a Specimen of the Calcareous Nodules accompanying
the Shells.
Specimens of Lias from Cloverly and of the New Red
Sandstone Series of Shropshire.
. Porcelain Jasper from the Junction of the Sandstone and
Trap Rock of Stirling Castle.
Flexible Magnesian Limestone from Sunderland, and
Fossils from the Lower Greensand, Kent.
A Specimenof Franklinite from New Jersey, and of Shelly
Ironstone from Lake Mollor between Hamburgh and
Lubeck.
Fossils from the Greensand, Blackdown.
. Casts of bones of the Megalonya laqueatus from Big-bone
Cave in Tennessee,
DONORS.
Woodbine Parish, Jun. Esq.
F.G.S.
LeonardS.Coxe,Esq.F.G.S.
Woodbine Parish, Jun. Esq.
F.G.S.
HenryD.Rogers,Esq.F.6.S.
e@eeerereeene ese eeoeeeesrenees
Robert A. Austen, Esq.
F.G.S.
John R. Reeves, Esq.
J. H. Deacon, Esq. F.G.S.
Henry T. De la Beche, Esq.
F.G.S.
A. Cunningham, Esq.
F. Lambert, Esq.
John Dickinson, Esq. F.G.S.
Viscount Cole, M.P. F.G.S.
and Sir Philip Egerton,
Bart. F.G.S.
R. I. Murchison,
V.P.G.S.
Hugh E. Strickland, Esq.
F.G.S.
Esq.
Col. Harding.
Thomas Weaver, Esq.F.G.S.
J. Prestwich, Jun. Esq.
F.G.S.
— Leigh, Esq.
Edward Charlesworth, Esq.
R. I. Murchison, Esq.
V.P.G.S.
Richard Knight, Esq. F.G.S.
John Willimott, Esq. F.G.S.
eoceesre ee eeeee
Viscount Cole, M.P. F.G.S.
and Sir Philip Egerton,
Bart. M.P. F.G.S.
Richard Harlan, M.D.
29.
14.
June 10.
1833.
Aug.
1834.
Feb. 5.
June 4.
Dec. 6.
List of Donations.
SPECIMENS.
: Specimens from the Silverdale Mines, Staffordshire.
Shells of existing species from the Newer Pliocene De-
posits in the Baltic.
Specimens from the Isle of Portland.
Specimens from Chili, Peru and the Island of Juan Fer-
nandez.
Specimens of British and Foreign Minerals.
Specimens from the Island of Ascension, the Mauritius,
&e.
Specimens from the Pennant Grit and Dolomitic Conglo-
merate near Bristol.
Silicified Wood from the Portland Stone at Chicksgrove,
Wilts.
A Stalactite from Ingleborough Cave, Yorkshire.
A specimen of Shale with impressions of Fern Leaves
from the Grit Formation near Wodwowitz, Prussia.
A Fish from the Purbeck beds, in the Vale of Wardour.
Minerals and Rock Specimens from Norway.
Casts of an Occipital Bone, and the anterior Cervical Ver-
tebre of the Ichthyosaurus lately found near Lyme
Regis.
Specimens from the Mountain Limestone near Frome.
Specimens of Fossils from the Coal Strata near Keighley,
in Yorkshire.
Specimens from the Diluvium at Lawfurd.
Specimens of Spirolinites in Chalk Flints from Stoke,
near Chichester.
A set of Teeth of the Gangetic Crocodile.
Specimens from the Arigna Mines.
Specimen of a Trilobite from Dudley.
IV. Miscellaneous.
MISCELLANEOUS,
Glass Models to promote the study of Crystallography.
A Medal of Berzelius in Selenium.
A Silver and a Bronze Medal of Count Casparus Stern-
berg. ‘
Specimens of Iron Tubes from a Steam Boiler, Cornwall.
Deposits on the vertical walls of the Boiler of a Steam-
boat.
25
DONORS.
Sir Philip Egerton, Bart.
M.P. F.G.S.
Charles Lyell, Esq. P.G.S.
W. H. Fitton, M.D. F.G.S.
H. Cuming, Esq.
T. H. Holdsworth, Esq.
F.G.S.
The Rev. W. P. Hennah.
George Cumberland, Esq.
Hon. Mem. G.S.
Miss Benett, of Norton
House.
Woodbine Parish, Jun. Esq.
F.G.S.
M. John
Prague.
Miss Benett.
M. H. C. Strom.
B. Batka, of
H. Warburton, Esq. M.P.
F.G.S.
Miss Benett.
The Rev. Theodore Dury.
The Rev. Wm. Thornton,
F.G.S.
The Marquis of Northamp-
ton, F.G.S.
N.T. Wetherell, Esq.F.G.S.
John Rofe, Jun. Esq. F.G.S.
— Rofe, Esq.
DONORS.
M. J. B. Batka.
Count Sternberg, For. Mem,
G.S.
JohnTaylor,Esq.Treas.G.S,
Charles Lyell, Esq. For. Sec.
G.S.
nani’ ian
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PLATES AND MAPS
IN ILLUSTRATION
OF
VOLUME IV.
SECOND SERIES,
OF
THE TRANSACTIONS
OF
THE GEOLOGICAL SOCIETY
OF LONDON.
LONDON:
PRINTED BY RICHARD TAYLOR, RED LION COURT, FLEET STREET.
SOLD AT THE APARTMENTS OF THE GEOLOGICAL SOCIETY,
SOMERSET HOUSE.
———=
1837.
EXPLANATION OF THE PLATES.
Pirates I., II. & III.
Illustrate Dr. Buckland and Mr. De la Beche’s paper on the Geology of the neighbour-
hood of Weymouth and the adjacent parts of the coast of Dorset.
Prate I.
Geological Map of the neighbourhood of Weymouth and the adjacent parts of the coast
of Dorset.
The reader is requested to take notice that the authors do not profess to mark the
exact limits of the lower Purbeck Beds in Portland, but merely to indicate their presence
as the uppermost formation in the north end of that island.
Pratt II.
Series of Sections.—Colours the same as in the Map.
Fig. 1. Section from the Great fault near Upway to the Bill of Portland*.
Fig. 2. Section from the Great fault near Moigne’s Down Farm to Ringstead Bay.
Fig. 3. Section from the Great fault near Poxwell to the signal station near Osmington
Mills.
Fig. 4. Section from the Great fault near Sutton to the Sea at Ham Cliff.
Fig. 5. Section from the Great fault near Sutton to Jordon Hill in Weymouth Bay.
Fig. 6. Section from Abbotsbury Common over Linton Hill.
Fig. 7. Section from Abbotsbury Castle to Abbotsbury Swanery, showing the continua-
tion of the Great fault.
Fig. 8. Coast section from Jordon Hill to near Boat Cove.
the Oxford Clay and other strata at the east end of this section arises from an inden-
tation of the coast: the strata have an E. and W. direction throughout, and dip
rapidly N., and have not the bend here represented, by throwing the curves of the
The apparent curvature in
coast into a straight line.
9. Coast section from near the termination of fig. 8 to Ringstead Bay. As the coast
ranges along the line of direction of the strata, its indentations give these strata a false
appearance of dipping in different directions: they form a small arch at Osmington
Mills.
* The Scale (in length) of fig. 1. is one inch to the mile; of fig. 2. to 10. inclusive, two inches to
the mile: figs. 11. to 13. inclusive are on a larger scale, and fig. 14. two inches to the mile.
Fig.
Fig
Fig
Fig.
EXPLANATION OF THE PLATES.
. 10. Coast section near White Nore.
. 11. Fault in the Cliffs, a little W. of White Nore.
12. Theoretical diagram representing the manner in which different rocks may be seen
in contact, in consequence of various degrees of denudation, on the same fault. II-
lustrations of this may be found in Sutton Valley ;—where there is little or no denu-
dation, the Portland Stone and Chalk are in contact at the surface; where a denuda-
tion occurs to the depth of the curved line a a, the Portland Stone and Green Sand
are in contact, on opposites sides of the fault; at the depth dd, the Portland Sand
and green sand touch each other; and at the depth c c, the Kimmeridge clay touches
green sand.
@. 13. Fault in the cliff west of Bridport Harbour.
. 13 a. Eastern termination of the Bridport Harbour fault.
. 14. Section from the cliff west of Bridport Harbour to Askerswell.
Prare III.
. 1. Tabular and proportional view of the strata in the Weymouth district.
. Angular flints and plastic clay.
. Chalk.
. Chalk interspersed with grains of green earth (Craie chloritée).
. Indurated green sand, with quartz grains and quartzose sandstone.
. Greenish brown sands with indurated concretions.
> Light brown sands. Fox mould.
- Green sandy marl beds, with nodules similar to the cow-stone at Lyme Regis.
. Purbeck beds.
. Dirt bed, above the Portland beds, frequently contains rolled calcareous
pebbles, and fossil silicified trunks of large coniferous trees, and of Cyca-
deoidez.
k. Best beds of the Portland Stone.
7. Compact light-coloured limestone, with beds, seams, and nodules of chert.
m. Grey shelly beds, the base of the Portland Stone.
n. Green, brown, and grey sands and sandstones.
0. Brown and grey sandy marls, with indurated nodules.
p- Kimmeridge clay, contains an abundance of deltoid oysters.
qg. Clay ironstone in the lower part of the Kimmeridge clay.
r. Upper grit beds, containing deltoid oysters: these beds are most fully deve-
loped near Sandfoot Castle.
- Oolite differently developed in different places.
. Brown sands, containing indurated nodules of calcareous sandstone.
. (Grey clay.”
mos SL SS
x,
=< & ws w
. Larger deposit of calcareous grit, containing Gryphea dilatata.
ww. Oxford clay, grey marl, abounding in Gryphea dilatata.
- Rubbly and slaty Cornbrash limestones, alternating with clays and marls.
y. Slaty and shelly grey and brown limestones, containing Apiocrinites rotundus,
lignite, broken shells, &c.
8
EXPLANATION OF THE PLATES.
z. Grey marl, with marlstone in its lowest region.
aa. Coarse granular limestone, loaded with grains and veins of hydrate of iron.
6 b. Light brown and yellow calcareo-siliceous sands and sandstones, often highly
micaceous.
Fig. 2. Section showing details of the Oxford oolite near the east extremity of Weymouth
Bay.
Fig.3. Detailed section of the strata that occur in the Isle of Portland.
Note.—Since the paper was printed to which these sections refer, a notice has appeared in
the London and Edinburgh Philosophical Magazine, August 1, 1833, p.158, by Mr. R. Phillips,
containing a minute analysis of the water of two sulphureous springs of similar quality near Wey-
mouth, both of which issue from near the junction of the lower beds of the Oxford clay with the
cornbrash or upper beds of the Forest Marble Formation. One is situated at Nottington, about
three miles on the North of Weymouth, and was described by Dr. Pickford in a small treatise
printed at Weymouth in 1821. The other rises at Radipole, about one mile from Weymouth, and
was discovered but a short time ago. The most important of the ingredients of these mineral
waters is sulphuretted hydrogen, which is derived from the passage of the water through strata
that contain iron pyrites in a state of decomposition. Mr. Phillips remarks that “ the saline con-
tents of these waters are so small in quantity, that they must be considered as quite inert, and
therefore those who wish to avail themselves merely of the sulphuretted hydrogen, may take them
in larger quantity than if they were active in other respects.
Pruates 1V. & V.
Illustrate Professor Sedgwick’s paper introductory to the General Structure of the Cum-
brian Mountains, with a description of the great dislocations by which they have
been separated from the neighbouring carboniferous chains: p. 47.
Prate IV.
Map exhibiting the geological structure of the district, and the range of the band of lime-
stone and calcareous slate between the quartzose green slate and the greywacké slate.
Piate V.
Sections exhibiting some of the great dislocations produced by the elevation of the
northern carboniferous chain: p. 59.
Prate VI.
Illustrates Professor Sedgwick’s paper on a Series of longitudinal and transverse sections
through a portion of the carboniferous chain between Penigent and Kirkby
Stephen: p. 69.
EXPLANATION OF THE PLATES.
Puares VII. tro XXIII.
Illustrate Dr. Fitton’s paper **On some of the strata between the Chalk and the Oxford
‘‘ Oolite, in the South-east of England”: p. 103, to 378.
Prate VII.
Contains small portions of the Maps of Kent, Surrey, and Wiltshire, reduced to half
the scale of the Ordnance Survey.
Fig.1. Part of the Coast of Kent: p.105—119.
Fig.2. Part of Surrey: p.137—142.
Fig. 3. The Vale of Wardour, South Wiltshire: p. 245—254.
Prate VIII.
A Sketch of part of the Coast of Kent, from Hythe to Folkstone Hill; reduced from a
drawing by the Rev. J. D. Glennie: p. 108—127.
Puate IX.
Map of part of the South East of England, and of the opposite Coast of France, on the
same scale with Mr. Gardner’s reduced Geological Map of England; about 18
miles to an inch. ‘The space occupied by strata above the chalk is taken from Mr.
Greenough’s Map. ‘The divisions below the chalk are inserted from the information
stated in the present paper, and will be given on a larger scale in the new edition of
Mr. Greenough’s Geological Map. The continuous red lines, numbered 1. to 25.,
refer to the sections described in this paper, and represented in Plate X.a. The
dotted lines adjacent to Nos. 15. and 16. represent the course of Mr. Lonsdale’s
sections, (Geol. Trans. 2nd Series, vol. ili. pl. 32.) ; and those adjoining Nos. 18
and 21, are ¢ransverse sections in Oxfordshire and Bucks. The blue lines denote
some of the anticlinal lines; those in the vicinity of Bristol are from Messrs. Buck-
land and Conybeare’s map, (Geol. Trans. 2nd Series, vol. i. pl. 38.) ; the rest from
the statements of the present paper.
On the French coast, from Calais to Treport, the colours are inserted from the manuscript
notes of the author: In the Pays de Bray, and thence to the mouth of the Seine and
coast of Normandy, they are taken principally from M. Passy’s map of the Depart-
ment of the Lower Seine, with some additions by Mr. De la Beche: thence to
Cherbourg, from the maps annexed to the papers of M. Desnoyers and M. Con-
stant Prevost, in the Annales des Sciences Naturelles, tome iv. 1825; and. of the
former, in the Mémoires de la Société d@ Histoire Naturelle de Paris, tome ii. 1825.
The depths of water in the English Channel are taken from the Admiralty Chart. The
lines under the figures were intended to represent the form of the bottom; but the
depths are so enormously exaggerated, that without explanation they would convey
a very erroneous impression. Mr. De la Beche’s section of the channel between
Portland and Cape La Hogue *, on the true relative scale of depths and horizontal
distance, and more than five times as long as in this map, is scarcely different from
an uniform line ruled with a common pen.
* Sections and Views,” &e. 4to, 1830. Plate II. fig. 2.
>
2 ee ee eee
vv ee ee
ee
ee
EXPLANATION OF THE PLATES.
Puate X. a.
Contains a series of sections, at right angles to the range of the chalk, on the lines
marked in the map, Pl. [X., Nos. 1. to 25. The series begins on the coast north of
Folkstone, and follows the outcrop of the chalk, round the Weald denudation of Kent
and Surrey, &c.; thence along the coast, to Devonshire; and in the interior, from
the Blackdown Hills to Norfolk. These sections are all drawn to the scale of the
Ordnance maps, one inch toa mile. The heights are of necessity much exaggerated ;
but additional lines are given below Nos. 6. and 7. in the true proportion of height
and distance.
No.1. Section from Folkstone Hill to Copt Point, Kent: p. 104.—(See the Map, Pl. VII.
fig. 1.; and Sectional Sketch; Pl. X. b. fig. 1.).
No.2. Through Tilburstow Hill and Godstone, Surrey: p. 137.—(See the Map, Pl. VII.
fig. 2.)
No. 3. Through Nuffield and Merstham, Surrey: p.137—141.—(See the Map, Pl. VII.
fig, 2.)
No. 4. From Hindhead, Surrey, through Tucksbury Hill, near Farnham: p. 144—149.
No. 5. Section across the Wealds, from the South Downs at Duncton-Beacon, through
Floxham Park, Plaistow, and Aldfold, to the North Downs at Netley Heath;
‘principally from Mr. Martin’s MSS.: p. 155—160.
No.6. The Coast of Sussex and Kent, from Beachy Head to Folkstone Hill;—part of
which is given in greater detail in Pl. X. b. fig. 3. The lower line of this figure re-
presents the cliffs on the true relative scale of height and horizontal extent: p. 161
—164.
No.7. Part of the South Coast of the Isle of Wight; from Afton-Down to Rocken-End,
and from Dunnose to Bembridge Down:—(See also the transverse Section Pl. X. b.
fig. 4.). In the lower line of this figure, the heights are in the true proportion to
the horizontal distances.—p. 182—202.
No.8. From Durlstone Head, through Swanage, to Ballard Down, Dorsetshire: p. 206
—215.
No. 9. From Broadbench, in Kimmeridge Bay, Isle of Purbeck, to the Chalk-hills: p. 206
—215.—(See Pl. X. b. figs. 5. and 6.).
No. 10. Section at Lulworth Cove, Dorsetshire: p. 215—216.—(See Pl. X. b. fig. 7.)
No. 10’. Section at Man of War Cove, west of Lulworth, Dorsetshire: p.215—217.—
(See Pl. X. b. fig. 8.)
No. 11. Coast near Bere, Devonshire: p. 234.—(See Pl. X. b. fig. 9.).
No. 12. Blackdown Hill, Devonshire: p. 238.
No. 13. Sections of the Vale of Wardour, in South Wiltshire: p. 245—255.—(See the
Map, PI. VII. fig. 3.).
— — on the anticlinal line, A. B.
—— on the transverse line, C. D.
—— on the transverse line, E. F.
—— on the transverse line, G, H.
No. 14. Vale of Warminster, South Wilts: p. 257.
EXPLANATION OF THE PLATES.
No. 15. Poulshot-Green to Etchilhampton Down, North Wilts; drawn by Mr. Lonsdale :
p: 261, 262.
No. 16. Sandridge Hill to Beacon-Down Hill, North Wilts ; Mr. Lonsdale: p. 262—-266.
(The dotted red lines adjacent to Nos. 15. and 16. in the map PI. IX. denote the
course of the Sections connected with Mr. Lonsdale’s Paper in the Geol. Trans.,
Qnd Series, Vol. iii.; Pl. 32, figs. 1, 4, and 6.]
No. 17. Swindon to Liddington Castle Hill, North Wilts: p. 264—266.
No. 18. Oxford, through Shotover Hill, and Great Hazeley, to the chalk range, south-
west of Stokenchurch Hill: p. 270—274.
The flap, No. 18/., gives the section, on a line nearly parallel to No. 18., along the
main road from Oxford to London, through Wheatley and Tetsworth: p.271—
279.—(See the transverse section Pl. X.b. fig. 10.)
No.19. From Blackthorn-Hill, in Oxfordshire, through Muswell-Hill, Brill, and Thame,
to the chalk near Bledlow ridge: p. 270—-279.
No.20. From the north-west of Whitchurch, through Aylesbury, Bucks, to Wendover
Hill, Berkshire: p. 270—284.—(See the transverse section, Pl. X. b. fig. 11.)
No. 21. Through Woburn, Hockliffe, and Dunstable, Bedfordshire: p.270—293.
The flap, No.21'., is the Section from Fenny Stratford, through Little Brick-Hill,
to Hockliffe: p. 270—293.
No. 22. From Caxton Gibbet, Huntingdonshire, through Cambridge, to Balsham:
p. 305—308.
No. 23. Haddenham, through Denny Abbey, to Bottisham, Cambridgeshire: p. 305.
No. 24. Through Upware on the Cam, to Swaffham Prior, Cambridgeshire: p. 305.
No. 25. Through Lynn, to Swaffham, West Norfolk; by Mr. C. B. Rose: p. 310—312.
No. 26. Hunstanton Cliff; Norfolk: p. 310—313. (See Plate X.b. fig. 12, a. b. and c.)
Prate X. b.*
This Plate contains miscellaneous Views and Sections, on different scales, illustrating the
country represented in some of the sections of Pl. X.a.
1. A sketch of part of the Coast near Folkstone, not visible in the direct line from the
sea: p.106—108. Reduced from a drawing by the Rev. C. D. Glennie.—(See
Plate X. a. No. 1.
Fig. 2. Section on the west of Pulborough, in Western Sussex, showing the subdivisions
of the Lower Greensand: Mr. Martin’s MSS.: p. 155.
fig. 3. Enlarged Section, on the same scale of height and distance, of part of the coast
near Hastings and St. Leonard’s, Sussex: p. 164.—(See Pl. X.a. No.6.).
Fig. 4. Transverse Section, from Brook Point to Shalcomb Down, Isle of Wight: p. 200.
—(See Pl. X.a. No. 7.)
Fig. 5. Enlarged Section at Emme?’s Hill, Isle of Purbeck: p. 211.—(See Pl. X.a. No. 8.)
Fig. 6. Ideal Section, from S¢. Alban’s Head to Worbarrow knob, in the Isle of Purbeck :
page 211, 212.—(See Pl. X.a. No. 9.)
yy
°
5°
* This Plate is subsidiary to Plate X. a. ; but is placed before it in binding, that both may fold
out and be consulted at the same time.
EXPLANATION OF THE PLATES.
Fig. 7. East side of Lulworth Cove, Dorsetshire: p.216.—(See Pl. X. a. No. 10.)
Fig. 8. Plan of Durdile, and Man-of-War Coves, and Section of the latter: p. 215—217.
(See Pl. X.a. No. 10/.)
Fig.9. Enlarged Section of part of the coast of Devonshire, from Seaton to Branscomb
Mouth: p.234.—(See Plate X. a. N.11.)
Fig. 10. Transverse Section through Garsington and Wheatley, in Oxfordshire: p. 273.
—(See Pl. X. a. No. 18’.)
Fig. 11. Transverse Section through Quainton and Whitchurch, Bucks: p. 271.—(See
Pl. X. a. No. 20.)
Fig.12. a.b.and c. Hunstanton Cliff; Norfolk.
Fig. 12. a. Map of part of the north-west Coast of Norfolk; from the Ordnance
Survey, and on the same scale,—one inch to the mile: p..310—313.
Fig. 12.6. Enlarged Section of Hunstanton Cliff; by Mr. Murchison: p. 310.—
(See Plate X. a. No. 26.)
Fig.12.c. View of Hunstanton Cliff; from the point « of the preceding figure;
from a sketch by the Rev. W. Whewell: p. 310.
Fig.13. Abstract Section, representing the whole series of strata illustrated in Plates
X.a. and X.b.: p. 318, &c.
Prates XI tro XXIII.
These Plates contain figures of the new and more remarkable fossils, obtained from the
tract described in Dr. Fitton’s paper. The details are explained in Mr. Sowerby’s
descriptive notes; Appendix A.—p. 335—348.
Pirate XI.f
FOSSILS OF THE UPPER GREEN-SAND AND GAULT.
CHALK MARL. Fig. 6. Pollicipes radiatus. (Low- | Fig. 14. Solarium conoideum.
Fig. 1. Tornatella elongata. er green-sand, p. 130.) 15. Pyrula Smithii.
6*, ———— rigidus. 16. Rostellaria elongata.
LIES EUS 2 SNL 7. Venus? tenera. 17, ————— buccinoides.
2. Lucina? globosa. 7*.Venericardia tenuicosta. 18, ————— marginata.
3. Avicula grypheoides. 8. Nucula bivirgata. 19, —————-- carinata.
9. Modiola bella. 20. Ammonites circularis.
GAULT. 10. Lima semisulcata, 21, —————- symmetricus.
4. Pentacrinites. 11. Auricula inflata. 22, ——- crenatus.
5. Pollicipes levis. 12. Natica canaliculata. 23, ———- cristatus.
5*, ——--_~ unguls. 13, Solarium ornatum.
Pirate XII.
FOSSILS OF THE GAULT (continued),
Fig. 1, 2. Hamites rotundus. | Fig. 3. Hamites attenuatus. | Fig.4. Hamites spiniger.
Prate XIII.
FOSSILS OF THE LOWER GREEN-SAND.
Fig. 1. Echinus? arenosus. Fig. 3. Trigonia spinosa (var.). Fig. 4. Diceras Lonsdalii.
2. Panopea rotundata.
+ In the following lists of names, the mew species are in Roman characters; those previously figured, in
Italics.
EXPLANATION OF THE PLATES.
Puate XIV.
FOSSILS OF THE LOWER GREEN-SAND, (continued).
Pholas giganteus.
. Modiola \ineata.
. Avicula pectinata.
. Ostrea retusa.
. Anomia radiata.
levigata.
Fig.
Dow Wt
Fig. 7. Anomia convexa.
8. Zerebratula Tamarindus.
oP quadrata.
10. —— Faba.
11. ——_-—— elegans.
12. ——— conyexa.
Puate XV.
Fig. 18. Yerebratula parvirostris.
14. prelonga.
15. Lingula truncata.
16. Pleurotomaria striata.
17. Ammonites furcatus.
FOSSILS OF THE LOWER GREEN-SAND, (continued).
Scaphites Hillsii; the detail of the figures is explained at p. 339.
Puate XV. a.
FOSSILS OF THE GREEN-SAND OF BLACKDOWN,
Siphonia pyriformis ; the figures are explained in detail at p. 340.
Puiate XVI.
FOSSILS OF THE GREEN-SAND OF BLACKDOWN, (continued).
Fig. 1. Pollicipes levis.
. Serpula filiformis.
Tuba.
Vermes.
. Panopea ovalis.
. Mya leviuscula.
. Amphidesma tenuistriatum.
MIO COR ot
Fig. 8. Corbula truncata.
9. Mactra? angulata.
10. Petricola nuciformis.
11, ———— canaliculata.
12. Psammobia? gracilis.
138. Lucina orbicularis.
Pisum.
Pirate XVII.
Fig. 15. Astarte concinna.
16. formosa.
Uf multistriata.
18. impolita.
19. Cyprina cuneata.
FOSSILS OF THE GREEN-SAND OF BLACKDOWN, (continued).
Fig. 1. Cyprina rostrata.
. Cytherea subrotunda +.
. Venus? truncata.
submersa.
sublzevis.
immersa.
. Cucullea formosa.
NOOB Owe
Fig. 8. Arca rotundata.
9. Nucula lineata.
apiculata.
; obtusa.
12. Trigonia quadrata.
13. Modiola reversa.
14. Mytilus tridens.
Pirate XVIII.
Fig. 15. Mytilus prelongus.
ineequivalvis.
17. Perna rostrata.
18. Avicula anomala.
19. Pecten Millerii.
, - compositus.
21. Lima subovalis.
FOSSILS OF THE GREEN-SAND OF BLACKDOWN, (continued).
. Pecten Stutchburiensis.
. Terebratula dilatata.
megatrema.
. Dentalium medium.
. Litorina pungens.
. Natica canaliculata.
granosa.
? carinata.
. Tornatella affinis.
CONaonpwNhe
Fig. 10. Vermetus concavus.
11. Scalaria pulchra.
12. Litorina gracilis.
13. Phasianella pusilla.
14. ——————_ formosa.
15. striata.
16. Fusus rigidus.
17. quadratus.
18. —— rusticus.
Puate XIX.
FOSSILS OF THE WEALDEN,.
Fig. 19. Fusus clathratus.
20. Pyrula depressa.
21. Brightii.
22. Rostellaria retusa.
23. —————- macrostoma.
24, ———_——- Parkinsonii.
25. Nassa lineata.
26. costellata.
27. Ammonites triserialis.
External forms of Endogenites erosa: the details are explained at p. 173—175.
+ In the Table at p. 355, Cytherea subrotunda is erroneously referred to Plate XXII. fig. 2.
EXPLANATION OF THE PLATES.
Pirate XX.
FOSSILS OF THE WEALDEN (continued).
Illustrates the internal structure of Endogenites erosa ; the details are given at pp. 175, 176.
Puate X XI.
FOSSILS OF THE WEALDEN (continued),
Fig. 1. Cypris Valdensis. Fig. 7. Cyclas parva. Fig. 13. Cyclas major.
Zz. —— tuberculata. 8. subquadrata. 14, Unio Mantellii.
3. spinigera. 9. —— elongata. 15. subtruncatus,
4. granulosa. 10. —— media. 16. Gualterii.
5. Corbula alata. 11. -—— , (var.) ; Wie Martinii.
6. Psammobia tellinoides. 12. —— angulata. 18. Mytilus Lyellii.
Pirate XXII.
FOSSILS OF THE WEALDEN AND PORTLAND-STONE.
Fig. 6. Paludina Sussexiensis. Fig. 11. An unknown body from
VEREPEM, 7. Neritina Fittonii. Quainton; (p. 349.)
Fig. 1. Exogyra Bulla. 8. Tornatella Popii.
2. Ostrea distorta. 9. A Conefrom the Isle of Pur- EE TE ANDES TONES
3. Bulla Mantelliana. beck; (p. 349.) 12. Lucina Portlandica.
4. Melanopsis? tricarinata, 10. A Cone from Sussex; (p. 13. Cytherea rugosa.
5. — attenuata. 349.) 14. Trigonia incurva.
Prate XXIII.
FOSSILS OF THE PORTLAND-STONE, KIMMERIDGE-CLAY, AND OXFORD-OOLITE.
PORTLAND-STONE (continued). Fig. 6. Terebra Portlandica. Fig. 10. Exogyra Virgula.
Fig. 1. Ostrea falcata. 11. Trigonellites latus.
2. Nerita angulata. KIMMERIDGE & WEYMOUTH STRATA.
3. Natica elegans. 7. Serpula variabilis. cca peas aes
4. Buccinum naticoide. triserrata. 12. Nerinea Goodhallii.
5. ————— angulatum. 9. Panopea depressa.
Pirate XXIV.
I}lustrates Mr. Bell’s Memoir “On a new fossil species of Chelydra”: p. 379—381.
Piate X XV.
Illustrates Professor Sedgwick’s memoir ‘‘ On the new red sandstone series, in the basin
‘‘ of the Eden and north-western coasts of Cumberland”: p. 383—407.
Fig. 1. Section on the coast of Cumberland, between Parton and St. Bee’s Head: p. 391
—393.
Fig. 2. Section from the mountains east of Mollerstang, to the overlying conglomerates
in the valley of the Eden above Kirkby Stephen; showing the great fault and the
breaks in the carboniferous series; p. 383—390.
Fig. 3. Section from the greywacké mountains of Westmorland, through Orton Scar and
Burrels, to the Eden; p. 386.
Fig. 4. Section exposed in Ben How quarry, between St. Bees and Whitehaven: p. 388.
Fig. 5. Section from the mountains of Copeland Forest, through Cold Fell, to the sea
north of the river Calder: p. 389—391.
EXPLANATION OF THE PLATES.
Fig.6. Section from Corney Fell to the sea-coast west of Bootle: p. 389—399.
Fig. 7. Section from the Mountain Limestone Hills at Low Furnace, to Salt-Coats oppo-
site the Island of Barrow: p. 389.
Puates XXVI. tro XXVIII.
Illustrate Col. Sykes’s memoirs “On a portion of the Dukhun in the East Indies”:
p. 409—432.
Puate XXVI.
Map of the Dukhun.
Puate X XVII.
Panoramic Sketches.
No. 1. is a distant view of the mountains, on which are situated the celebrated /ill
Sorts of Jewdun, &c. It is taken from the hill N. of the town of Goreh: p. 432.
No. 2. A view of the hills, to the North and East, as seen from Lakungaon in
the flat broad valley of Jooneir (Sewneir).
No. 2*. is a continuation of the view No. 2. from the North round to the West.
No. 3. A sketch of the Azlls to the North and East, as seen from the summit of the
armoury, in the fort of Ahmednuggur.
No. 4. A sketch of the northern flank of the Plateau on which the city of Ahmed-
nuggur stands ; as seen from Wamooree, in the plain of the Godavery river.
Prate XXVIII.
Fig. 1. Elevation and declination of the country above the Ghats, between 73° 35! and
74° 49' East Longitude, and 18° 50! and 19° 10! 3" North Latitude: p. 411—418,
432.
Fig. 2+. Elevation and declination of the country above the Ghats, between 17° 35! and
74° 49' Kast Longitude, and 18° 28! and 18° 50! North Latitude: p. 424—432.
These Sections are fully explained at p. 432.
Prate XXIX.
Illustrates Mr. Horner’s paper “On the Environs of Bonn”; p. 433—481.
The principal division of the plate is a Map of the Environs of Bonn; described at
p- 434.
Beneath is a panoramic view of the Hills on the East of the Rhine, as seen from
the Coblentz Gate of Bonn.
The remaining division of the Plate represents the vertebra of a Fish, probably,
of the genus Zamna, found in the loess near Basle; the smaller figures are of
the natural size; pp. 476, 480.
+ In the engraving of fig. 2., the names Moteh and Mota are confounded. Mota is the name of the
River, Moteh that of the Town.
+
ad
Geel. Trane, Lerten, Voi tv. Plate 1
POARTLAN D
laridsfoot Castle
ROAD
Bottom of Kimmeridge Clay
tland Nore
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LPAIR I
of , ‘ f fr Suse Castle
AB line cf Section Prats 2. ID © ik, S 1; a ‘S| Jef It ik Te, 5 [.K.Line of Section. Place 2.
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Green Sand. Purbeck Stone Portland Stone Pavrtllaned Sand & Sandstone KinmerifgeClay xt Colite b: Catrarenus (eit Oxford Clay Cornbrash &Forest Marble Inferior Oolite Blocks of Silicasus Ficlding Stone
BILL of LORTLAND
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General Section of the Strata in the Weymouth District,
Angalar Fhiuts and Plastic Clay.
Green Sand.
Purbeck Beds.
Portland. Stone.
Portland Sand.
Kinmeridge Clay.
Upper Calcareons Grit.
Oxford Oolite.
Lower Calcareous Grit.
Forest Marble.
Tnferior Oolite.
~.
WT de la Beche. del
Fig.1.
20.
100.
4°.
70.
80.
300
4oo.
zZ.
aa,
300.
bb.
Geol Trans. 2° Series Vol .N PLB.
Fig. 2.
Section between Ringstead Bay & Osmmington Mills.
Kimmeridge Clay.
Bed of Cay Ironstone.
Upper alcareous Grit.
Bubbly Linestone.
Oolite.
Gray Marl.
Grit Beds, marl partings. .
Light brown sand |
with concretions
Oxford Oolite.
Gray Marl.
Lower
Qlcareous Grit.
[__—
Fig.d.
Section of the Chffof Black Nore W. side of Portland.
laleareous Slate,
Dirthed Fossil Trees, Cycadeoidex.
Top lap.
q
Roach.
Good Stone.
Gompact & Chalhy limestone
with chert.
Portland Stone.
Tubbly beds with chert.
Sandy limestone with chert.
Shelly gray linestone.
Gray & Brown Sandy Mart
& Sandstones.
Dark Sandy Marl
with
Sandstone concretions
Portland Sand.
Fallen Masses of Kock.
-_—
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Fig . (p.3g) Geol. Trans. 2? Series Vol A PLS.
Leak of Derbyshire Derbyshire Coal
Fig. 2. /p.60)
Lancashire Coal Blackstone Edge Fork sit re Coal
Fig. 3. (pp. 60.62) Ingleborough
TIT raeerrry
Ganbrian Mountains Fig. 6. (p.62/ Goss Fell Chain
7) Fig.7. (pp. 61.63) < N.
Swaledale Head Brough Scar
Wi
Bar ae Sy tones
Wew Red agnesian Gal Millstone Limestone. Shale, Sear Old Red Grouwadee
Sandstone. Limestone. Measures. Grit. & Sandstone. Limestone. Sandstone.
Fig 1. GENERAL SECTION oF THE CARBONIFEROUS LIMESTONE SERIES &.MILLSTONE GRIT.
(See p.70)
Thin bands of Coal.
Coal seam of Turna Fellmuch worked.
\ Thin band of Coal worked to the north of the
line of Section. Numerous Clagstone quarries,
Longitudinal and
Our.
|
in
alee co
Trace of Goal at Rawthay Gill.
— \
Silicoous Flagstone used for rooting slate.
Barton Coal seam, much worked .
Fis epetem ie
PARSE SCONE
A thin Coal band.not now worked.
Trials for Gat.
Blask marble Group.
Carbonaceous shale, F:
lig. 2, LONGITUDINAL SECTION 7
SSE. aco
Moulton Fell
Baw Fell oor”
Risell Uiduale
ceeecond Millstone V5).
Swath Fell
Garsdale
Fig. 3. LONGITUDINAL SECTION FROM THE TOP OF PENIGENT 10 THE TOP OF STAGS FELL NEAR
"oC S'-
Ws tone Cam Doa
Penigent . yo" pimest uw.
nw
Fart of NYU &NN3.
Second Milletone Grit, V5) Shale, Grit & Coral,
and first Millstone V3) «
River Ribble
SERIES OF TRANSVERSE :
SWhy We Fig. 5. TRANSVERSE SECTION. Se p94)
Moughton Fell
Clapham Clapham Beck
Horton
Why N. : Eby 8.
Barki Cr r
my Ca sterton figh Pell Ww.
Fig. 7. TRANSVERSE SECTION | ‘00 p95!
Howgill Fells
Short Gill
VGITUDINAL. SECTION THROUGH THE CARBONIFEROUS CHAIN FROM PENIGENT TO THE PLAINS OF THE EDEN NEAR KIRKBY STEPHEN | (5 p00
WW. Whernside &.
Simon Fell 3 ee ‘ 5) ea Great Colm
Clas — as a eet wocot Secundt Millstone V9)
Groups ot ’ : ye i: pala Shale, Grit. foul IA\First Millatone Grit V3).
’ ap immeatone D* Piet wh Combe 2 — _—kittle Colon State Quarries Be
- Chapel le Dale - = § ibd
The line trom Whernside : A
to Great Colm deflects ni im ec ££ C*eh oe
. due west acroes Deepdale.
Fg. 2. CONTINUE D.
©
DS : Dolphin Sty
got! aciteeen. Wild Boar Fell coal pass
metal Send Sioa p
‘ weail
oat vet *
. oe
a net there Kirkby Stephen
River Eden
e s t ° n © a : : Greate S c @F Zameen ; one "Conglomerate of New Red Sandstone oo
OF ST. AGS FELL NEAR HAWES. (Se p91 Fig. 4. LONGITUDINAL SECTION FROM THE TOP OF WHERNSIDE TO THE TOP OF SHUNNER FELL AT SWALEDALE HEAD «©: Sepi92
NINE. oS = |
a> = WE. |
Stags Fell Whernside ie Cross Cotter Fell Shunner Fell |
Mosdale Mill. grit representing all i
Cha grome Ton i 13"
groups F to
inclusive.
hudtihy S84 813.
HUES OF TRANSIERSE SECTIONS CONNECTING THE LONGITUDINAL SECTIONS WITH THE GREYWACKE CHAINS OF WESTMORLAND. — os AS ag abs)?
rea .
Fig. 6. TRANSVERSE SECTION, (5ap95) : Trace or Second Miltstone Vs)
penraie: . pate
Sear Limestone \V.
ESE.
Wey : ;
Harter Fell Fig. 9, TRANSVERSE SECTION, | 5ep.97/ Wild Boer Fell
Millstone Grit ke V5 to V3.
Clouds
Ravenstonedale
reywacké
pik
;
2
es
Geol. Lrans. 2 Serves Vol. LV, Ft. VIL.
Mole F.
Uprcoldhame
FOLESTONE
PART OF THE COAST
OF
KENT.
Fig 2
Tothiunst
PART oF SURREY.
Gmpton
' . a Hut
d pr oe ‘
“tt Ebbeshorne
c
-
yA Wak
‘Alvediston
VALE oF WARDOUR,
WILTSHIRE,
: = : Kinuneridge Clay
Hastings Sand & inferior beds
ee Purbeck Strata Lines of Section
Portland
awe Anticlinal line
Fig 3.AB
+ dechcontbe
—)
CSS Lower Greensand
——— ee di
a
Lower Greensand
Fig.3
{ I | Stone t
Weald Clay
Fight 2.” a sand!
Scale
1 % 0 1 2 3
Miles *
o
<
]
Sheth of Tart of the Coast of Kint, fiom Hy the to hotkstone Milt Gaol Teac By Saree OEY Bt
r“Quarrver » Lolsferd: Hla + Sadtwood Castle ~ v feachboro Summer House * Gucarrves bi fiat v4 Meal Down J24 ject
Hythe wdourt £08) feet Seabrook
~ * Paracre Wood: ovKickmond Shaw ~>~+Dentons Pinel ~ Cherctor Church
Bocsags i
¥ £69 feee ‘Prospect Place te dir ce 2 ~ Artillery Barracks ; ~ Castle ~ Chapel
Sandgate
A range of Rocks, of the lower Greengandab low water mark
. 3 ; 5
; ~ Castle Hill . Cliff Oop abou 199 feet Spring breades cme ~ Sagar Tioef Fide ere area Lit MAT x Lower H23. thf Marielle DW. 251 fiat
: Folkestone Copt Point. Tower. 1427"
. 132 feetr — *Palkavtone Mild 257 fie
fea ciaz Upper Greensand I Lower Greensand Weald Clay Frnedl by Clhslimaandtel
Gale =
‘
Redivced from wv Steetch by the Rev *1D Glennae
- The Hughes are taken prom the mean bored of the Sea
Bo eae ag)
Me
ra
Nh
ae
i
Geol Thins 2% Serves Vol I PLE
; te ae —__——— - ———_——_—— SSS
f. '
i \
~ I MAP
A A atore econ | aaa of part of the
: oy aa. SOUTH EAST or ENGLAND,
; pera — and of the
EE (eet et OPPOSITE COAST ,
j K B y oF FRANCE,
a) Bett de.
a ae eee
Se ee
2 sR) frtind stone & sand.
DR Birvneridoe 8 Wesnoth bets,
ese | ston! Oolite & beds beneath. a
—_—$—<_ lines of Section. N°1 to 26.
Anticlinal Lines.
The Depths of the Sea. at low wirter;
are expressed in tithome,
—YouTH or
Mo TU Ty
Mes.
WN. Foreland
Ken
= Adenge Baer
Lew
De Brightovi
Bowing deat —
; we Wesrthing x
Sabra Bill
oNeufchatel
« Guillefontaine lite
an
Bayinenion:
sph
eek
ee
Bhi
i Ene hi tS. # Ov THE {scan ia) i OF << Lute’; | Ss ia daa sae (CAS Ss (day ay EX ._ pit. Fog
HASTING s
7 shale
Chanare iy direction wt E
nee One Enitogenites
; pep : ; , Warriors Gate
op ort - Catle Rock Rast
: S' Leonards
a : 2 — sina sor oo wa08 Fiices
Fotkstoane, from the Eas t pe Fig. 4 | Fig. 8
x a ; Downy, j
tf owe ata West of PULBOROUGH, Susy 60 piss. — Dar dia Cowie: |
wt a Fig. 2 Brook Point to Shalcomb Down. /
% Isle of Wight. p200. / 4
: rst a =
ne zs wn aie pe ~ o
at . Por, ms 2
- wobittig ee? si ;
—=2== = =
Fae = a ee eae. > i= wy T Mile
deat Section ss EAD. Li of Parte ch .per X
be \
2 ‘ : Fig 6 \ '
gt cel wil sills a / Man of War Cove ’
se! we poll ww |
t PY otto! : ( Tet Mage 202)
io SMbans Head
y PSE eS tte 1) Ose ea aI ONT, Tie EC VO) ae { =
a © Fig. 7 290 sous foot
(see text page 216)
4 a
See 4 N. S
a : =f Frente Carpmune Poot —— pa 20 TSA et #4 ~ indies
= —— ee J n
—
. Part of the N.W. of fo lle.
2 , FEE VES Ta ONE DO! BF CLIF F, Norfo && .-pan.
BERE HEAD, Devonshirey ps. “ x
a stall Siptiheices | Fiy 12 bs.
Fig, 12. ©.
and WHITCHURCH, Bucks. p27.
Whitchurch
Seale of Miles
TUE WEALDEN
e
10.
u
ABSTRACT SECTION ot the Sertes: of Strata
represented m this Plate.and in PlateX.a-
Superficial Greevel
Bagehot Sard
Londen Cay.
Vlastic Tay:
alk: =
Weald Gaye
Hastings Sant
Aster Oolite.
Qurend Gay
_ hae
Yowale of Keestwater
Ce a
- —
> test
Mindhead
V3. MER een, SULTON. plo : na) yw
°
: :
Wd HInnpnHeEAD fro TeceKsS BURY
A
| ; Aldershot = .
Nuttlotd ie | Merstham eine yw ~~» ~
x” ca | core, “2 a ee
Birewk i i] V = ‘s 4 "
} oe : ‘ eit
2 = naa Pi = Fersham Common
Parclight Down 1
woe o e ‘ NT 6.5 P t
Pevensey
gi
Z ‘ exh .
‘soaps en a ah PO by hE ¢ wher -s < aii we ov es
hy
= Se aa ee ae tere
ag
au as Oo. Ty aE Di hie I Pa O F W IDG A 47 R piss.
S* Gtherenes Dowe 830 18
SEhensifasce Deowes Shanklin Down Bee AT SwavnaGe BAK”
2 A space of about four miles emitted here ix eanpicd - - pte.
by @ eoncinuution of the sume Strats.
5 AWD Oo. Wr BAY, p87 14, SS
or at oo ot amt e -
om ° ~
Qa
Red Clitr
: V° ss. Through Powrsuor GREEN: Vorth Wilts.
1 ene Ee Py es. Or Ten oe D iO Ir oR Wilts. p.246-256 = p2ee.
( VOU. VALE OF WARMINS VELES..p 287, ton Mit
Vlate VU fig. 3. Brimtock Lown é 7. 2. MI TER, Welts. p27.
—_ ra
rs This Deverill ‘dl Fs i Warminster
ng brie farmin:
oo OP ee
\
sSivele wf Distewwrs. Otwe Trach te «4 Mile.
?
SO0Oa
TH DOWNS,
WES TBR N
Ss
U
AY
S fieuks fo the
OR RE
ALE £L S.-pis.
New thls pliscw the Carnal falls by
The spene here cosignal 0 the Waskd Cpr is rack anayrervtnd. in consnywerice the Oily of the Section te the Line of Dip Bleck saiey ters 0 fe
The Summit level of the Surrey & Sussex Coral wheat
ue
yo Cowntodd
2 wile distant ix HOS thet above the Seer act Love Wester
Aldfold
Spur Wo Phistow
Aahrin
ee
Pa
oe I
Dallinglurst
The eights, thom Qitk ond t0 the East ot Uvthe, which appear w have firmed the trast at some remote ported .are now sapsirated trom the Soa
bo the artensive Mint of Remagy Marshes. Denge Nes, the South eastern extremity of this low tracttt HW Miles sistant from Applatore
ol Ke ingto Warehor
r a i aay on m nasi
Panchey Down
WW, COAST near BERE, Devon. p.23#,
N° it. BLACKDPOWN, Devon.
s ap -258
_ Ye
Ww = =: a
Soe ex | WHEATLEY through TET § WOR T M pp2mes.
Shot
3097! _tarspath,
con Wheatley Silisacast
L) Y t
‘moe aan Oo rays 4 a 40
Se a
ce ges ~
Tr
= thei a tel
a SWINDON through LIDPDINGTO Pade’ 97/3
‘Svindon _ pp. 264. NW
Ontton Park
Through
Chilton
LOW G=-C REN
Long Crendon
DON and T H A M £E.-p.279.
iio Fowersey
OT —
Blackthorn Hill Easington
ition ‘ - “> = Thame
ti
PO BAL S H A MH. .p.30b.
Whitehnech
oy
20. FROM WHITCHURCH, through AYLESBURY, to WENDOVER-~HILE._p203.
Halsham eros Stone Pits
Sule Mandeville "eg
Nem
Fulbenurne
—t
Road w Newmarker . — -—
&d Mbilex roan Lesradirn
Aslesbury
or
ESE rs see
__ncalhe oa — 2M F EN: -SvRATEORD through HOCKLIFF Bedfordshire. p-20s
Bom Briobhiit , a = “
= eae cas 270.2
ZL. Brickhill Drertieg wo?
Mocktife )
5 . hi P on
¢ ~ ate . ——_ NE ar tem
ys ow — a
PS |
Walon
_p3o5-
Swattham Poor
pit
Fancy — qn
bee!
Beets ee
Fenny Stratford
Gingl 24008
= £26. HUNSTANTON CLIFF, Norfolk.
Pecan
SRST
nt
SNR we
x
‘ Spe
CHALK-MARL.
ge SUS
~ } ae 4 es 4 é 2
§ pfeve {9% Ceol. Trans, 22 Serves Vol VELL
UPPER GREENSAND.
LOWER GS.
JD.C. Sowerby fecit,
a ae
ne ed er ae
al. Trans. 20 Series Fol. LVLLXL.
0
G
AUL T_( continued.)
G
-
Geol. Trans, 22 Series Vol IV Pt. £1,
LOWER GREENSAND.
a)
2)
WIG? B9gN99 0 4o4
pi mE
iS rn, F
Ky \ SSH PE
{ Wik ANN “te Qe
iW ieee
TDC. Sowerby Lect.
LOWER. GREENS AND_(continued)
Geol Drans. 2] Series, Vol IV EL. ALV
=
SSS
SSS
NSS
Uy,
Geol. Trans. 20 Series, Vol LV PL AV.
LOWER GREENS AND_(continued.)
JD.C. Sowerby fecit
Geol. Trans. 2 Series Vol IVPULXV. a.
GREEN SAND (of Blackdown, Devonsh re.)
Geol. Trans, 2¢ Series, Vol IV PLA,
GREEN SAN D- (ol Blackdown.) continued
Ceol. Dpans. 27 Series Vol. IVIL. XVIT,
fot Blackdown) continued
REE NS AVD-
G
TD.C. Sowerby teert.
CLDrans Ze Series Vol LVPTAVIM.
Geo
REEN SAND (ot Blackdown) continued.
’
G
<="
=
JD.C Sowerby fecit.
WHALDEN,
LnAOGEHITES COSA.
Cool. Trans. 4
Bee
Sertes VoOLLV Plt. X1LX.~
2.
Feet
TC.
Of the natural size
JD.C.Sowerly fecit
magnets ed & times.
WHALDEN,
Lndogenttes CPrOStH.
these two Ligures are magnitied 4 times
Geol.Trans. 20 Series Vol lV. Pt, XX.
‘
magnitted 8 mes
PUNO
WEHEALDEN, (continued)
Geol. Trans. 22 Series, Vol. LV PL, XAG.
TD.C. Sowerby fect
Geol. Trans. 2© Series Vol LV. PLAZTL,
WEHEALDEWN- (continucd)
J.D.C.Sowerby fe
Geol Trans, 20 Series, Val. LV. PU. AXTIT.
PORTLAND _ (continued)
JD.C. Sowerby fe cit
anadosryatnpy Miphzey)
POVILDULY AZT 1) PDP MMIAT
77 WT DAG PQA boy2y Jvpos o
VE LOTATIY PUOE PULRL SUNY. 7 °°D
: a Mee “it vias wae
; OE eed
be
*
Geol Tron. 26 Sor VOL PL AE ‘
| ’ <
HGL SECTION on tip COAST oF CUMBERLAND BETWEEN PARTON uno S’ BEES HEAD, p. 391.39, ;
Fig 4p. 366.
Ben How Quarry, near 8! Bow.
: fa
Fig.? p. 383. 390. we fie Fig. 3.p. 586. il
i
Fig 5.p. 389. ID. ig Fort Fig. Cp. 569 5A
1 5
WwW.
soot
uf in
flows” LI ~
os 4 or | a
——a7= = : ( Z
Sa = — S =
sa -
’ |
/
Green Slate & Torplyay Upper Slate Group. Old red Sandstone Gurboniterons Limestone Garboniterons Limestone Coal Measures Lower New Red Magnestan Limestone. New Red Sundstone
(middle series) & conglomerate. ‘lower davaston) i upper division | Sarudstone. revting ane
Heisei
ITN Tah
Mr bt iti
} Fal de
{sith
IN iti ee
Ai yl Wey
Geol Trans. 2"4 Series, Vol IV. PL XVI.
oS me i
P
ae
4
4
<4) os
Begaghiua®, A ie |
: 7 Aseer
(| Amba. EX 5 “
herald Springs s |
+ F Copla, °
Sind duar °o Arrawud. B
null diet 0) VY Tapheir Ghar Springs BOORHANPOOR
fa = fxg | oF
2 OY Se ze
. U Wewul or Vera s OME ~ Nussleerabad
° D ° ° —| 21
fi Thamal Springs " warungaon
a hoolia
(| | ag Galna Jauamner
°
| Movtier Burygaon
| Bhund 2. |
Malligagf
Z epee “a Adyuntah o
> a —, c handore |
of 2 . Peegnidner
LA Wianeir Unkey |
Ral ae ad MA. P
& = Vinchoor oti Ellora . of
; °.
20 = Tealeh Aurungabad = = |
}° : oo DUKHUN Mees
~ s Zopayaor
id Lhooltambis er a he DD) Te Bes
8 fahatao
Toe by Li Col! W. H. Sykes
|
re : 6 Vewassa PSs LGaS. |
Hurreechundurgheun, ae - a |
- eo - - g. oSomace a
Malse Chit * g Sewgaon Seale #8 Miles to an lich
Naneh Ghat © |
ee es J, digg, Phonan Wareh. We ra ocleesgaon 0 72 4 36°°~«@f8
anes oon Alla. 4 Kuzjoon AI °
4 = ¢) £0
Ahopeh 6 Grup, Bo Fe eee heor
Ng B ee Nod ne ee . YeAHMBDNUGGUR anwor
19 ae i more SS li ° |
a ~ a S Anko alia in: 19|
hae ican er |
Kundalldie ~% ¥ meyvon °)Sambcheir |
Sy Log ae ¢ wa |
5 ‘Sew , ohiada |
J Teckonehn aya c
sa ve Bhoom
( |
' 2 oDhokeh
Sgagaon Pada |
& Purrunayo ofuugree
Kull eoWangee oKumlapoor |
Thermal Springs aes Rarhlonee
8 les 3 é soorne Oondaxgaon olyapoor
ForuVictod Wahbuleshyiiire é | -
onk cto £ Sour o Kurlumbh
- 2 BSC Gi “pu” |
Bhosah oWohol|
4 Main
| ae Ge, SHOLAPOOR
| uttao aS Lodiy Antalkcowteh
i R TUAMACOWTN
or \ Booshunghur sa Brum poor. B,.. eMindroop °
Koo: >
6 Hulsingeéo ; ‘
Kanapgor, Cherdee Manowr
a i md A bdulpoor
WP Z4JOL lee
= Yasgaon d Tutt } ‘ dimilla
: . Be 6 Tamba
7 r io) : A "
liv B A
ae) te eee
fh Bhorgaon vtheecanent tae (ES a Ookileé
°
2 ° |
Kolapoor a ya Ze: Kolutnoor Mungolee loomgee
OD fagul S i °
f RS 5 B ecedree ‘Begehwarree s
cS) A de ae alk,
een Wepance meas Beelgel oumulgee =
Y Jao , ~ °
Dowleshwuro “Yoodul Muchutw ‘ar
faput
Malwant Southern linit | Yardwa ~4 KP aus
oft Trap in iojtaka Dudhee 5 ce BAGULKOT
7 Bu ° Gokauk
>
16 2 ba < iw Toragul , PAZ LOOT" _ | al i 1G
, & Munolee, B adam te
Reduced trom a Map by Cap? a ee et Samuduttee ° Safihal
°
Sopp Dep © Survevor Gen Lof SB oor Jim MEP OOT? “Sangolee on; pee ama yeas
. Miers ZA
India excepting places tn the SS Beamguah rere ae
Ros ° ~
Koran, which are inserted SI Wi Nundigurh Bs ok al
~ ¥ ° 5 a
tiem Arrowsmith Map. = Eiupheeree' D HARWAR BEACH |
° |
° 5
The Country described vs the ele auuel Hulliyal hoya
Ql? portion of the Map. = Misrikota a at
Boni: oSUu77Us
‘onignitel 2 Liichmeshwur
} Sawapo°
15 v 15
7\3 7\4 75
WAH. Sylees Feeit.
#
a\ i
;
: 7
a
f
a :
{NENG ROMY Duras
‘ am ss aye, hy
= me ’
sheng od”
cc
- Oe nl
~~ te a Pt > ues = ll =
& é : al oat
Yosh. here ee a Re roa SEY ws tt a on wa a ta
yw h * % . - a 4d sal © vere navy +
i PRPS * . ds r -
ns bs We tenth: heth ye
si a Pb err ae gate
fy RR Yar ’ : a
- me
a
sd / aR
taka
a —b ~~ — on
PANORAMIC SIKETCIRUES. Geol. Trans.2™ Sep VOLIV-PL.AXVH.
RANGE OF HILLS N AND W. OF JOONUR FROM THE SUMMIT OF A HILL N. oF THE TOWN OF GOREH.
i
2
iS
&
” Samanmnyamne Gh tae
AL\
Hill Fort of Hurreectuimndurghur
N T0 E. RANGE oF HILLS AS SEEN FROM LAKUNGAOWN IN THE VALLEY OF JOONUR.
HILLS TO THE NE. AND E. AS SEEN FROM THE ARMOURY IV THE FORT OF AHMEDNUGGTUR.
>
§
&
Sulahut
Pdihans Tomb
NORTHERN FLANK OF THE PLATEAU ON WHICH ,THE CITY OF AHMEDNCUGGUR STANDS AS SEEN FROM WAMOOREE.
4 Dongurgunge
‘
Thre Z/ Sas
Shetchad by LS Fidler
INATION of tur COUNTRY ABOVE tk GHATS, BETWEEN 73. 35.4ND 74£49. EAST LONGITUDE, ANp THE PARALLELS OF 18°50. AND 1990.31. NORTHMATITUDE: SHEWING THE GEOLOGICAL STRUCTUR E, OFTHE’ SAME.
sg 3
‘ i
¢ ; ) i 3
= i: ; 3 i
: : | ; 2 H a uns ¥ s s i
: ee ty : fa ¥ i er me : A i Se oye i
3 : = ‘ d . . *
: . isce | i3 i ot ane aa ] a) eg 2 i i { fred i
Level whe Coreh River
— SS = : = Level of the Sea
CLINATION oF tu COUNTRY ABOVE tr GHATS, BETWEEN 73°35.4ND TH49 EAST LONGITUDE, ANDTHE PARALLELS OF 18°28. 4xD 18°50. NORTH LATITUDE: §HEWYN G
1 me: GEOLOGICAL STRUCTURE or me SAME.
ss 8 3 S . ‘
RS i gE. ; i ; i = : ;
ae itchy = 4 : i 4 i
3 hs ene 3 a ka = = . 4
ali Tt, 4 y , ‘ a lie :
SRS fy af ary z ws < £ 5 es = a
¥ a3t i ison 3 3 ae ‘ é t
a! add Hil i s $ s g # i a
d
'
a Wee ers
Camper NO Fort W.
Level ofthe Inderane« ud Powna Ri
Level of the Sea-
The strata of the darker hue are Basalt of various kindle; those colored grey-green are vurietice of Anwodaloid, quarts, zeolite, red evllulan &eke The lanes following the rusnbers subjoined. to the names of Places,denote the mode in hich the heighte huore. be obtained,
signifies Barometric mearurenvent. Wauleulation trom the temperature of boiling Weter:
teal. Trans 2° Series VOLT: Plate NATE,
Caudal
Endenih 0 .
ENVIRONS oF BONN
“Do Meckenheim
;
» |
* \vaale of English Mites
INDEX (Not a Section) OF THE MINERAL | STRUCTURE as seen fiom the top of the Coblent: gate Bonn.
5
the Siebengebirge
——— ee
as. a. & |
ee syRé ab p
Pee iii ig] 46) 4 - a i
hee ianh os Soe eae ae fy : i
S S45 ES aR es S | © 3 :
ae e€ aycanee § 4 7s a a8 4 adel 4 4 Vertebra: belonginy te the Shark Family
t S © e a _. » as de _ probably the Genus Lamna.
cre : as he oe -tivm the Loess near Basle.
wade > CD otanis sue CBM ceate a ) a
i
. i
a , wa ey ose eee
3 ba : Sy, — a -
oe . ¢ P S 8 v eS 7 ?
™ “ae, me rt ‘ . > ——
oe Ce lee NE wing he —_ 3
a ain! V> © LAP oe a —— ay lah beth ee ee ee x -
er : a ae b ~~ J sata eine : ht = genge i ="
a a * . 4 j > <= - —— . a —— a a “
-. & ? a pe * : i - FR, So, cep
}
C :
* —
Z : . 5
i ; ; a
: ;
;
-
Qs
'
3 f
poe
: A aah ag Mae : ely *
Fale itigs pes, din youn Megpslteeth. i
POL oon — as) ange ate AS RSD,
> ne A Say ta
ies
= oe
AN
Ay,
il
04
|
10004 55
|
|
ii
|
EN
|
Cl
|
|
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3 1853
AD
fete Sh ae aR TS
iil)
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+ = z > s :
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