27

THE GEOLOGY OF THE DISTRICTS AROUND SETTLE AND HARROGATE. By P ER C Y FRY I-:EI\DALL, M.Sc ., F. G.S. f R ead J llly tst, 19/0. ) Some adva nce cop ies of this Pape r were printed and Iss ued to Memb ers, in connection wit h the Long E xc ursion, in July- August lase. T he Paper is now rcp rtnted with a, few slight alterations. COXTE:\TS. PA GE !.-[NTROU l ICT IOK • • 27 [I.-PRE-C A MUlH A N R OCKS • 30 III.-LOWER P ALA':0 7.0ICROCKS 3 1 I V.-CARBO:-;IF E ROl :S R OCKS- Basement Beds . 35 Limeston e . 36 Yoredale (Pendleside) Series . 37 Millstone G rit 4° Measu res 42 V .-PER~1IA;\I ROCKS 44 VI.-ICNEOlTS ROCKS. 49 VI I.-GLACIAL PH n :OMENA 5° V III .-TECTO NICS 53 IX.-REFERENCE S 5R

I.-I NT R OD{; CTIO~. H E principal districts to be visited," na mely, the western T dales ab out Sett le and th e mid dle region of Nidderdale, constitute two repr esentative portions of a west to east traverse of the Pennine Chain, which, both by its resembl an ces and contrasts, form s an interesting and useful com ple ment to the st udies made by th e members of th e Associat ion of the northern sections near Appleby, visited under Dr. Man 's guidance in 190 7, and of the southe rn terminati on visited in 19°3, when Dr. Wheelton H ind led an excursion to North Staffordshire, an d in 190 4, when Dr. Arno ld Be mros e conducted an excursion to North . The Pennine Chain consists essentially of a great fold of wide amplitude and generally 'low gradie nts extendi ng from th e T yne-Irthing depression, where it is abruptly tru ncated by faulting, to the Trent valley, where its greatly denuded arch falls away below an unconformable cover. Its western edge is cut off for long distan ces by a great system of dislocations, but on th e cast it dips gentl y beneath the unconformable cover of Magnesian . In the section entitled " Tectonics " som e more det ailed dis­ cussion of the structure ofthe Chain wi11 be attempted, bu t for th e present purpose it will suffice to point out that th e western fractured bo undary is interrup ted for a distan ce of over 30 miles, namely, from the neigh bourhood of Settle to the Saddleworth

'" Th is refers to the Lon g: E xcursion of I 9 1C'. 28 PERCY FRY KENDALL ON THE GEOLOGY OF

Valley, near Oldham, by a folded region consisting of a pair of great S.W. and N.E. folds-the Clitheroe and Rossendale anti­ clines-with the intervening syncline of the Burnley coalfield. The western area to be studied lies on the northern boundary of this folded region, and several days will be devoted to the examination of the faults by which it is limited. The Dales and Craven Highlands, near Settle, consist of a dissected plateau of nearly horizontal Carboniferous rocks that has been deeply trenched by streams such as the Twiss or Greta, Clapham, and Becks, the Ribble, Aire, and Wharfe. These streams have in several places cut through the Carboniferous strata and exposed in a series of small inliers the underlying Archreau and older Paleeozoic Rocks. The massive Great Scar Limestone forms an elevated plateau upon which are seated the great elongated piles of the Yoredales with, in each case, a capping of . These hills are the most mountain-like of the Pennine system, and the stately forms of Penyghent, Whernside, and form an imposing triad, whose geological structure is displayed in bold scars and slopes with the clearness of a diagram. To the southward the scenery abruptly changes at the line of the Craven Faults, and the knobbed and undulating country of the folded strata stretches away to the middle course of the Ribble, with the Yoredale and Millstone Grit escarpment of Pendle for a background. The day spent in Wharfedale will disclose another type of scenery characterised by a remarkable range of gigantic knolls of lying at the foot of another escarpment of Millstone Grit. The Harrogate country stands on the edge of the eastern slope of the just where the Carboniferous rocks descend below the Magnesian Limestone. The great line of folded country comes through here from the west. Harrogate itself is on the edge of a steep-pitched , faulted along its north-western flank, bringing up the Yoredale rocks from beneath the Millstone Grit. Between this place and the Magnesian Limestone outcrop the surface has been etched out of the eroded plain upon which the rocks were de­ posited. The Nidd Valley, in the region to be visited, presents two strongly contrasted aspects, the dividing line being defined by the Nidd Viaduct of the North Eastern Railway. The western portion is a broad valley with fairly steep sides, the normal aspect of a stream flowing through a Millstone Grit country, while on the east the valley has a gorge-like aspect whether the country con­ sists of Millstone Grit or of Magnesian Limestone, and this feature, as will be shown in a later chapter, is related to the glacial history of the district. THE DISTRICTS ABOUT SETTLE AND HARROGATE. 29

While all parts of the area to be covered by the excursion have received a full share of attention, the Western Dales and Highlands have, by their more varied structure and magnificent scenery, proved the most inspiring to geologists. A catalogue of the workers in this field would enumerate nearly all the great names of the first half-century of English geology, among which would be found those of William Smith, Adam Sedgwick (a Dalesman himself, with a type of physiognomy very characteristic of this region), Murchison, John Phillips, and many others. It is almost invidious to select from the names of contemporaries, but the brilliant researches of Prof. Hughes, Mr. Tiddeman, and Dr. Man have given to them, and to the place of their labours, a claim to grateful remembrance among geologists. Nor need the rising generation of geologists fear to find an exhausted field-problems grow out of problems, and the studies of the older Paleeozoic rocks, placed upon a sound basis by Prof. Hughes and Dr . Marr, are being continued in our own time by their disciples. John Phillips did not say the last word on the Marine Carboniferous, and Dr. Wheelton Hind, Mr. Cosmo Johns, and Dr. Wilmore have found more to do than the mere crossing of t's and dotting of i's. Mr. Tiddeman made this region the subject of a paper on Glacial phenomena that has served as a model and a basis for Glacial work all over the country; yet, even in the field that he worked, with results of inestimable value to all later students, much may still be done.

STRATIGRAPHICAL SEQUENCE IN THE SETTLE DISTRICT. Recent . Alluvium, Peat, Shell Marl, etc. . Plei f Boulder Clay, Sands, Gravels. { eistocene .) Cave Deposits. Penni i Upper Breccias and Sandstone. errman .. 'I Lower Breccia. . Millstone Grit. UPPER PRn1ARY.J Yoredale and Pendleside Series. 'l Carboniferous. Carboniferous Limestone. Basement Beds­ Homogenetic. Polygenetic. iGrits of the Rough Lands. Studfold Sandstone. Horton Flags. Austwick Grit. ~~ls:\~ira~e~'l~gnsd . 'lI Red Shale). LOWER PRIMARY, Graptolithic Mudstone (with Spen- gill Limestone and zone of Phacops elegalls). Conglomerate or Calcareous Grit. o d .. I Bala Shales (Ashgill Shales). r ovician . 1Coniston Limestone. 1Pre-. Ingletonian Series. 30 PERCY FRY KENDALL ON THE GEOLOGY OF

SEQUENCE IN THE HARROGATE DISTRICT. \ Recent • Alluvium, Peat, Shell Marl, etc. \ Tufa. QUATERNARY. PIeIS . t ocene 1 .I Boulder Clay, Sands and Gravels. ' upper :\larl. \ C pper Maguesian Limestone. '1' :\11ddle :\Iarl, Lower Magnesian Limestone. [p"mb" Lower Marl and Sandstone. r f (Plumpton Grit. "1 I) Shales. G~\ 1Cayton Gill Shell Bed. Millstone .I, Shales. UPPER -, Grit. 1 Follifoot Grit. PRDIARY. Shales. Carboniferous. +th (Kinderscout Grit 111 Grit. ] three beds. ( Shales. J Roadstone. Yoredale Rocks. < Shales. J Grit. ~ Shales.

II.-PRE-CAMBRIAN ROCKS. The oldest rocks of the Settle District are, by common consent, admitted to be the series of hard, gritty, conglomeratic and slaty rocks exposed in Kingsdale, Chapel-le-Dale, and Ribblesdale, forming a belt at least two miles wide in Chapel-le-Dale, and apparently dipping uniformly to the south-west at a very high angle. These were referred by Sedgwick to the Green Slates, and correlated by him and later writers with the Borrowdale Series. The dip of the beds in Chapel-le-Dale has an appearance of regularity, and in the absence of clear signs of repetition by fault­ ing or folding in any of the exposures seen crossing their outcrop they were estimated to be 10,000 feet thick. It has long been felt that the ascription of this series to the Borrowdale division could be only a temporary expedient, and geologists working in the district were fully prepared for the revision suggested by Mr. R. H. Rastall, who proposed in a recent paper (9)* to refer them to the Archaean system under the name of the Ingletonian Series. Petrologically these rocks are different from any rocks exposed elsewhere in the North of . The predominant materials are grits, for the most part of a green colour. They consist of angular grains of quartz and felspar, with some mica and occasional grains of quartzite. The colour is due to the presence of chlorite of secondary origin. Mr. Rastall lays stress upon the marked angularity of the quartz-grains and upon the freshness of See List of References on pages 58-60. THE DISTRICTS ABOUT SETTLE AND HARROGATE. 3 [ the felspar, which equals, in this respect, the felspar in the Torridonian arkoses, Slates form a less conspicuous element in the series. The most interesting members of the series are the beds of conglomerate, worked for road-metal under the commercial name of the" Ingleton Granite." A fairly good petrographical descrip­ tion of the rock was given by the late Thomas Tate (7), who recognised its main constituents and suggested that it might be a volcanic ash. Mr. RastaIl has amplified this, and has shown that the rock contains fragments of a great variety of metamorphic, igneous (both plutonic and volcanic), and sedimentary rocks. It shows in many places, as do the grits and slates, signs of severe pressure and shearing. The whole aspect of the rock is incom­ patible with any affinity with the Borrowdale series. On the other hand, it bears a strong resemblance to some of the Archsean detrital rocks, such as the Longmyndians and the sparagmites. The diversity of constituents is of great interest, as it may indicate the derivation of the materials from a large area of older igneous and metamorphic rocks, while the angularity of the fragments gives support to the view that the materials have not travelled very far. The nature of the junction between these rocks and the adjacent Ordovicians cannot be ascertained with certainty, and though there is no difference of strike it is probable that it is a faulted junction.

IlL-LOWER P ALLEOZOIC ROCKS.

ORDOVICIAN. A series of rocks referable to the Coniston Limestone and Coniston Shale (Ashgill Shale) is brought in to the west of Chapel-le-Dale (Ingleton), most probably by minor dislocation, parallel to the most northerly of the Craven faults; a second small inlier of the limestone series is brought up by the same fault at Jenkin Beck, and another near the head of the lake at Clapham. Crummack Dale gives much better exposures, and near Horton, in Ribblesdale, the Coniston Limestone and Ashgill Shales come between the Ingletonian on the north and the Silurian rocks of the southern portion of the old floor, besides which small undulations expose these beds to the south. The relation of these rocks to the Ingletonian cannot be clearly seen.

SILURIAN. Rocks of Silurian age are exposed in Crummack Dale, Ribblesdale, and on the upthrow side of the Craven faults near 32 THE CEOLOCY OF SETTLE AND HARROGATE.

Malharn Tarn. The affinities of the series are clearly with the Lake District type rather than with that of North Wales, as might be expected when it is borne in mind that the Crummack Dale exposure is distant only some eight miles from Leek Fell, whence the great Silurian outcrop extends continuously through to the Lake District. The junction of the Silurian Rocks with the Ashgill Shales can be well seen at Crumrnack Beck head in a section interpreted by Professor Hughes as probably a double unconformity of Silurian upon , and Carboniferous lying in pronounced unconformity across the two. (See Plate IX.) The unconformity between the two older series, he points out, is but slight, and the rest always upon the same horizon of the Bala Series (Ashgill Shales), that shows little varia­ tion in thickness or lithological details. Near the lower end of Crummack Dale the basement bed of the Silurian is well seen in two exposures at Southwaite and Dam Bridge House respec tively. It is here a considerable bed of conglomerate, having a thickness at the former locality of 10 feet. The included pebbles, some of which are as much as 8 or 10 inches in diameter, are in all the exposures mainly constituted of fragments of the Ingletonian, a fact of ~reat significance. Harkness recorded also a pebble containing a fragment of Trinsic/etcs. Another good junction can be seen on Crag Hill, near Horton, in Ribblesdale. At this place the base of the Silurian is not conglomeratic, but consists of limestone, compared by Professor Hughes with the Hirnant Limestone of North Wales. The most complete succession of the Silurian rocks is seen in Ribblesdale, according to Professor Hughes, from whose memoir on Ingleborough (8) I have derived most of the facts relating to the older Palreozoic rocks that are given here. The oldest Silurian rocks are the Graptolithic Mudstones of Hughes, or Stockdale Shales of Aveline. They include a lime­ stone band, the Spengill Limestone, and succeed the conglom­ erate just mentioned. The fossils include many monoprionid graptolites. The Pale Slates.-These beds have yielded a very scanty fauna, including a graptolite referred by Miss Elles to Monograptus marri, Perner, They are correlated with the Tarannon Shales of North Wales. The A ustwick Flags.-These are flaggy beds of sandy mud­ stone with obscure cleavage, and have yielded a fair series of graptolites, of which M. uomeriuus is probably the most distinctive. TIle Austzvick Grits constitute a very important part of the series, and they serve as a link between the Crumrnack Dale outcrop and that in Ribblesdale by \vay of the great valley that lies along the foot of Moughton Scar. JI/:/~)'. PROC. GWL. Assoc., VOL. XXII. RI· PLATE IX. [Photo by (;od/ rey ------Leeds, - -- - -,

CRU MMACK BE CK !l EA D. I3ASE:YIENT SILURIA N (AT T HF. H AMM ER) RESTI NG UP ON T HE A SHGIL L S HALES: TH ETWOCOVEREDUNCONFOR:VIAB LY BY TIl E C AR BON IF EROUS LI :YIEST ONE . { To fa ce pag-c J~. I-re. 3'- :;'·;CTIO:" .\ l.O:"C TilE WE ST 5 11>E OF CI W)Dl. \ CK·D .I I.E.­ I ~'S IV Aft..r 1J1I.t;hlS. S~..ar Z; W Of'(,,:u.nnn cu.k

- _ Nor ocv ~1Cf! ~,

r-r­ H C' H H' ;.... i4 c,-.:

i ..~t..•.!JJ; h.,i DL\(K·D,\f.E.­ FIG..I.- SCCTIO:" AI.O:"C Til E L IST SlDE OF CI~l,;~ ., un :/, Afte,. /lllghrs. \l :/, s .0 \oJh (,I,.'f loR.. .- ,0 00 . •• ~v v 9 0 0 r. "0.0 . o ', :~., 0 ~. ~ ,,-"':', ", ...... ""-...... :.': .... S; \...... ' .. , .."., .....:::;;- .' \~".~~ ----;..,-~-~ 10 ~ ' ..-.:'" ...... <:'"

.Ilo.:~' '::::::"~ ~••' \:'"- .. • ..:..- \' I . - ..i o '-'1 c.J ,j o ~ 34 PERCY FRY KENDALL ON THE GEOLOGY OF

In Crummack they are the most conspicuous feature, forming a series of bold ridges transverse to the valley. The Carboniferous Limestone was laid down on a similarly ridged platform, and its beds can be seen to run out against the flanks of these inequalities of the old sea-floor. The ice of the Glacial period tore off masses of the grits and lifted them on to the limestone crest of Norber Brow, where they now stand 50 feet at least above the highest outcrop of the parent rock. The Austwick Grits are notable for the fine glaciated pavements and roches 11l0uto117zees that they exhibit. (See Plate X.) The .lI£oughton Whetstones.-These are soft, somewhat sandy beds, showing beautiful colouring in concentric layers of pale green and red. They yield graptolites, including M. ni!ssoni, and Professor Hughes explains their occurrence at Moughton by supposing a fault to bring them against the Austwick Grits. The palseontological evidence would assign them a position between these rocks and the Horton Flags. The Horton F!ags.-This formation is the most important of the Silurian rocks of this district. The rocks are described by Professor Hughes as sandy mud­ stones with interbedded grits passing down into more shaly beds in the Austwick Grits. The cleavage divides the beds into large slabs, much used for gate-posts and walling: they lie in a broad syncline that stretches across Crummack Dale, passes under the Carboniferous rocks of Moughton Fell, and reappears in Ribbles­ dale, where they are exposed in the magnificent unconformity at Arco Wood. (See Plate XI.) Fossils are nowhere very numerous, but both at Arco Wood and more particularly in the smaller quarries on Dry Rigg, to the south, graptolites (M. CO!OIZUS and M. roemeri) are to be found, especially in calcareous nodules. The Stud/old Sandsto1le.-The sandstones have no special features to distinguish them, except that in their upper part they present a coarse facies different from any of the other sandstones in the Silurian series of the district. Professor Hughes expresses a hope that the representat;,ive of the Winder Grit of the Sedbergh district with Acidaspis hughesii may be dis­ covered in finer grits a little higher in the series. Grits of the Rough Lands.-I am unable to discover any description or definition of these beds.

IV.-CARBONIFEROUS.

There is in this district a series of exposures almost without rival for the number and clearness of the sections, extending from the base nearly to the summit of the Carboniferous. A consider- PROC. GEOL. Assoc., VOL. XXII. PLATE X.

[Photo 0)/ God/rey Bingley, Leeds. VIEW LOOKING UP CRUMMACK. THE AUSTWICK GRITS ARE SURMOUNTED BY CARBONIFEROUS LIMESTONE. THE DISTRICTS ABOUT SETTLE AND HARROGATE. 35 able hiatus, however, is found in the Coal Measures, due to the fact that the only occurrence of rocks of this age is in the Little Ingleton Coalfield, about 16 square miles in area, a part of which is covered by red rocks, attributed, no doubt rightly, to the Permian, and much of the remainder is on low ground, heavily drift-covered and traversed by few streams. Very few collieries exist or have existed in this field, but borings have recently been put down, the details of which have not been disclosed; enough, however, is known to justify the expectation that the field will soon be opened up. So far it has not been possible to correlate the seams with those of the Great Burnley series.

BASEMENT BEDS.

The rocks that I here class with the Carboniferous Base­ ment Beds under the two denominations of Polygenetic * and Homogenetic are by many writers referred, respectively, to the Old Red Sandstone and the Basement Carboniferous, on the ground that "In the absence of fossils the exact date cannot be determined, but the rapid changes in their thickness, and especially the occurrence of another unconformity above them, marked by the existence of a conglomerate-rock with quartz-pebbles, whereas the conglomerates of the Old Red are polygenetic (composed of pebbles of Silurian grits, and more rarely limestones and volcanic rocks and Skiddaw Slate), suggest that some time elapsed between the formation of these rocks and the true basal Carboniferous deposits. Their lithological characters are certainly suggestive of Old Red Sandstone, and physically the base of the old Carboniferous plane is connected with the quartz-pebble-bearing conglomerate and not with that of the polygenetic conglomerate."] This description refers to the conglomerates at Ulleswater, but it is in principle applicable to the area about the Lune. Though there is clearly a difference of source and mode of origin separating the two conglomerates I -cannot discover good grounds for assigning one to the Old Red Sandstone period and the other to the Carboniferous, for the marine transgression that brought the Carboniferous sea over the -old post-Silurian land surface did not invade this district of until the Visean period, and terrestrial conditions may have prevailed there throughout the Tournaisian times, a period represented in the Bristol area by the deposition of more than 1,000 ft. of limestone. The two types of conglomerate I therefore provisionally in­ clude in the Carboniferous Basement series, using Dr. Marr's term Polygenetic for the red conglomerates with a mixed assem-

" Hughes (8) and Marr (4).

1" Mart-, Pres. Add" Quart./ourn. Gcot. Soc., lxii, 19\J6 j p. lxxxii (footnote). 36 PERCY FRY KENDALL ON THE GEOLOGY OF

blage of pebbles, some of distant origin, and calling the grey conglomerate of simpler constitution, and probably marine origin, Homogenetic (not a strictly cognate term). The latter is quite clearly linked to the overlying Car­ boniferous Limestone stratigraphically, as it is by the occasional occurrence of Carboniferous fossils.

CARBOKIFEROUS LaIESTONE. In no department of geological research has more remarkable progress been made in Britain during the last ten years than in that of Carboniferous stratigraphy and palreontology. Thanks to the labours of Prof. Garwood and Dr. Vaughan, a satisfactory palseon­ tological index has been devised by which the Lower Carboniferous. rocks can now be correlated, and though minor modifications or supplements may from time to time be found necessary, their methods have been successfully applied in zoning the Lower Carboniferous to the whole of the South of England, to Wales, the Isle of Man, many districts of Ireland, to Derbyshire, and to the northern portion of the Pennine Chain. Mr. Cosmo Johns has been carrying on a similar work in the classic regions of John Phillip's pioneer labours. The fact that Mr. Johns has not been able to present his results to the Geological Society places me in the not un­ common but none the less unfortunate position of knowing their general tenor, but being debarred from making use of them. In the following remarks I shall endeavour to avoid the repetition of old errors if I am restricted by the exigencies of the case and occasion to a very imperfect statement. The floor of older rocks upon which the Carboniferous Lime­ stone reposes is an undulating plane with ridges rising to eleva­ tions of 100-15° feet above the intervening hollows. These ridges follow in a general way the strike of the harder members of the Silurian series, and Mr. Johns's work upon the zoning will, I believe, demonstrate that the lower layers of the limestone were accumulated around these prominences, that were, at a later stage, covered by higher beds. These features may, perhaps, represent the half-obliterated traces of the early Carboniferous landscape. The Carboniferous Limestone is lithoiogically a fairly uniform mass of white limestone, locally dolomitic, with some black limestones at the top. The bedding is in some parts regular and in layers a few feet thick; in other parts it forms massive beds several scores of feet in thickness, without a well-defined break in the bedding, but marked instead by platy jointing of great persistence. Such a form is to be seen at Malham Cove, in Trow Gill, and at Gordale. In the upper part great obscurely­ bedded or perhaps quaquaversally bedded bosses of highly PROC. GEOL. Assoc., VOL, XXII. Photo by Afr. W. H. Banks, Ridgehollrne, ]{blJrtoll.l PLATE XI.

ARCO \VOOD QUARRY. CARBONIFEROlJS LIMESTONE UNCONFORMABLE UPON HORTON FLAGS. [ To face jYlJ,'·C 36. THE DISTRICTS ABOUT SETTLE AND HARROGATE. 37 fossiliferous limestone, called by Mr. Tiddeman "reef-knolls," occur in some localities. On Inglehorough, where the clearest sections will be seen, the whole of the Lower Carboniferous rocks can be examined bed by bed. (See Plate XII.) T~e following table IS compiled from Prof. Hughes's memOIr :-

MILLSTONE GmT, '23 ft. "Shale. Main Limestone. Sandstone. Shale and Sandstone. YOREDALE Middle Limestone. ROCKS, 8~o ft. Shale and Sandstone (ISO ft.). - Simonside Limestone. Shale. Hardrow Sandstone. Hardrow Limestone. Hardrow Shale. CARBONIFERO\;S I Great Scar Limestone, including Black Shaly LI~lESTONE, 600 ft..( Limestone and Black Marble (at the top). Mr. Johns has shown that no representative of the Toumaisian occurs on Ingleborough, the lowest part of the Great Scar Lime­ stone belonging to the upper part of Dr. Vaughan's .<''eminula zone, C2SI • Above this the succession is normal, and the zones 1\ and ])2 are recognisable.

YOREDALE (PENDLESIDE) SERIES. The Yoredale Rocks, and their precise relations to the Bristol sequence and to the rocks between the Carboniferous Limestone and the Millstone Grit, in the southern part of the Pennine area, have long presented great difficulties. A change of type was long since noted by Mr. Tiddeman to occur at about the line of the Craven faults, and Dr. Wheelton Hind and Mr. J. A. Howe, after a lengthened and careful study of the sequence on Pendle and elsewhere, established a paleeontological succession that has been shown by further research to be recog­ nisable as far west as Galway; east to the Rhine; and south to the Lower Culm series of Cornwall and . To this they gave the name of the Pendleside Series-a prominent bed 01 limestone near the top having previously been named the Pendle­ side Limestone by Mr. Tiddeman,* The recent work of 1\1r. Cosmo Johns (I8)t tends to show that the Main Limestone of Wensleydale and Ingleborough con­ tains a fauna substantially identical with that of the Pendlesidc Limestone, thus bringing the two areas in harmony.

* "The Burnley Coalfield." Mem. Geol. SUt'll. t Dr. Hind strenuously disputes this conclusion (19). FI G. 5.-S ECTl O:-: ACROSS t x o r.rmo n o A:-:n Til E CI~A\'E:-:F ,Il :I.TS.-A. N . Dioerryh ous«. ~

T il " CR,\\ 'EN 3 ~ ~ .. .~=:-~ ::-: FAUL TS. "", • 3 ~~~~~ c =.s=,=--=t:k _I:~'~__ _ • 2 / / /

5. Coal Measure s, 2 Ca rboniferous Lim estone. 4. illillstone Grit. I. Ol der Primary. 3. Yorcdale Series- l. Thorough Gill Fell (2164) FI G. 6 -P o F. KO/lli/II. S.

A:~

B Ma/ham Tarn (124-0) Newton Moor He/lirie/d E ('1-50) o B - ==------= General Section across Craven Faults. A. Millstone Grit. D. Silurian Beds. B. raredele Beds. E. Alluvium . C. Carboniferous Limestone . PROC . GEOL . V OL . PLATE XII. Assoc., XX II. [Pl'« fJ by Cod/n y' JJ/J/R"/~}'. Leed s J

INGLEBOHO lJGH VIEWE DFHOMTHE PLA T EAU FOP-MED Dr T HE TOP OFTHF. GRE AT SCAR LIME STONE . f To/ ace t age 3H. THE GEOLOGY OF SETTLE AND HARROGATE. 39

The visit of the Association to Ingleborough will, it is to be hoped, add some further evidence in elucidation of this very interesting problem. It is particularly desirable that some attempt should be made to ascertain whether Dr. Hind's zones can be found in the Yoredale series; thus, the Black Marble series of Prof. Hughes's table should be searched for the great goniatite, Proiecanites cotnpressus, that occurs in a similar rock above the white limestones in the Isle of Man and elsewhere. It is probable that near the same horizon a foraminiferal limestone with Saccammina will be found. I have found bouldersof sucharock at Clapham and in Wharfedale, as well as near Semmerwater and in Wensleydale, and, in company with Mr. Johns, succeeded in locating the bed in Mill Gill to a position about 20 ft. below the top of the Great Scar Limestone. Reef Rnolls.-These remarkable dome-shaped hills of highly­ fossiliferous limestone were first described by Mr. Tiddernan (I I). He showed that they occur on the top of the Great Scar Limestone and that they are surrounded by shales, sometimes containing pebbles of limestone that he regards as a kind of talus-bank surrounding the knoll and contemporary with its formation. The bedding is generally very obscure, but in Mr. Tiddeman's opinion, has a quaquaversal arrangement, a view that is corroborated by the detailed observations of Mr. Dakyns (12). Mr. Tiddernan points out that the "Knoll­ reefs" are all on the downthrow side of the Craven Faults, and he regards them as heaps of shelly material that have accumulated by the growth of colonies of animals upon a slowly subsiding sea-floor adjacent to the moving fault. Dr. Marr, on the other hand, attributes the reefs to the breaking and" packing" of thin beds of limestone embedded in shale while undergoing a shearing movement beneath a great over-riding thrust-plane-the Southern Craven Fault. He regards the great abundance of fossils as illusory, and thinks that they are equally abundant in other places, but not so conspicuous, as the limestone is less crystalline when not in the knolls. The explanation of Mr. Tiddernan, though perhaps inapplicable to certain cases, commends itself to my judgment, saving the part that ascribes importance to the Craven Faults. Few workers in the district would refuse to admit the richness of the fauna of these masses, and the examination that I have made of their structure supports 1111. Tiddeman's interpretation. At my suggestion, Mr. Ernest Parsons made a minute examination of every exposure, large or small, of the knoll called Stebden, and his results, when plotted upon a large scale map, were strongly confirmatory of the opinion that the structure was quaquaversal. In the Mill Gill section in Wensleydale, small irregular knolls 3 or 4 feet in height of unbedded fossiliferous limestone can be seen to rest upon the even-bedded layers of 40 PERCY FRY KENDALL ON THE GEOLOGY OF

Great Scar Limestone, and to be surrounded by the Yoredale Shales with Posidonomya becheri. Cracoe knoll-the most westerly of the remarkable series of knolls in the Grassington district-seems to be more open to question than any of its neighbours-its structure is peculiar, for it shows a well-marked and steady dip towards the Yoredale Shales on the south; its fossil contents too are different, con­ sisting largely of corals.

THE MILLSTONE GRIT. By comparison with the remarkable results attained by workers like Prof. Garwood, Dr. Vaughan, Dr. Hind, and others, in their researches upon the Lower Carboniferous, and of Dr. Hind and his collaborators in the Coal Measures, the Millstone Grit may seem to have suffered undeserved neglect. This is not, however, the case. A great body of new and important facts has been steadily accumulating, until their presentation in a complete form can be attempted. Meanwhile the publication of results has not been quite suspended, as witness the wonderful list of fossils from the Eccup Shales, near Leeds, and occasional lists from other localities, as well as the many valuable contributions by Dr. Hind. The purely stratigraphical relations of the series have not been neglected, and there are now available nearly complete measured sections from top to bottom of the grits in several districts of Yorkshire. The Millstone Grit consists typically of a series of coarse, massive, felspathic and pebbly grits alternating with beds of shale. The petrological character of these rocks has been investigated by Sorby and others. They might be briefly described as arkoses, consisting of quartz and orthoclase. Mica occurs sparingly in the coarser beds, but in the finer flaggy portions like that underlying the Rough Rock there are layers in which mica is abundant. The pebbles consist of either quartz or felspar, but only in very rare cases, e.g., in some quarries near Knaresboro', can these two minerals be found in a single pebble. Sorby, how­ ever, found that a considerable suite of rocks was represented in the pebbles, and recently Mr. Gilligan has communicated to the Yorkshire Geological Society a preliminary account of a remarkable assemblage of igneous and metamorphic rocks obtained by him from a bed of grit in the neighbourhood of Silsden, in Airedale. The enormous volume of material repre­ sented by the grit-beds is evidence of its derivation from a wry large tract of crystalline rocks, and as Sorby's investigation of the current-bedding in an extensive area near Sheffield indicated a general movement from north-east to south-west, it seems reason­ able to look to Scandinavia to some prolongation of that great THE DISTRICTS ABOUT SETTLE AND HARROGATE. 41 crystalline mass as the source of the materials. The way in which the grit-beds increase in number in a north-easterly direction and dwindle by disappearance of bed after bed when traced from towards Staffordshire, may be regarded as corroboration. The shales are, as might be expected, more difficult of exami­ nation than the grits, and though it has long been known that marine fossils occur in some of them, no attempt at a genera! correlation has been until recently attempted. During the last ten years, however, a more systematic examination has been in progress, and it is becoming clear that nearly every bed of shale is in part, at least, of marine origin. The fauna is much richer than that found in the Marine bands of the Coal Measures, though of the same general type. In a shale near the middle of the Grit Series at Eccup, the last British trilobite (Brachy11letopus ouraliClls) was found. Another marine horizon of greater importance, however, because its lithological character permits it to be traced over wide areas, is that known as the Cayton Gill Beds, or the "Shell Bed" of the Geological Survey maps. This is a sandy lime­ stone, often crowded with brachiopod shells; and as it makes good road metal, quarries have been opened on almost all its outcrops. It has been traced from the Crimple Valley, near Harrogate, to Cayton Gill, near Ripley, and thence up Nidder­ dale, and across the moors towards Wharfedale, where its marked lithological characteristics are lost. Near Giggleswick shales with marine fossils, probably on the horizon of the shell­ bed, form wide outcrops. In many districts a bed of coal with its underclay or seat­ earth is found on the top of a grit-bed, and in some places each bed of grit is thus surmounted by coal. The genera! conditions of deposition seem to have been that a great lagoon-like expanse of shallow sea with a muddy floor extended over England down to about the latitude of Birming­ ham. The area was slowly and intermittently subsiding; meanwhile a great river, from an area of crystalline rocks, flowed in from the north-east, bringing mud, sand and pebbles. When subsidence was active the river debouched before reaching the British area and mud only was deposited here, but as deposition overtook the tendency to deepen, sand-banks grew out over the shallows, moving farther and farther to the south-west, until, in some cases, even the Midlands was reached. At the shoreward end of these great sandy flats swamp-vegetation crept out, and its decay produced the peaty accumulation that, by later changes, gave rise to a coal seam, while the root-penetrated subjacent material formed the seat-earth that is seen under each seam. It should be emphasised that the coal seams occur almost invariably on the top of the grit-beds and not beneath them. A 42 PERCY FRY KENDALL ON THE GEOLOGY OF subsidence ensuing upon the period of stability threw back the debouchure of the river towards its source, and again deposition of mud succeeded. It is a remarkable circumstance that, though much of the shale, perhaps most of it, lacks the physical characteristics of marine deposits as we know them in the Carboniferous series, no fresh-water molluscs have been recorded from the Millstone Grit series of Yorkshire. The remarkable freshness of the felspar in the grit suggests interesting questions regarding the climatic conditions under which a great mass of granite debris could be produced with so little sign of decomposition of the felspar. The only conditions under which such a product seems likely, are those which prevail within the Tropics, where the intense heating of the rock exposed to the sun and subsequent cooling disintegrates the rock mechanically without affecting the freshness of the felspar.

COAL MEASURES. No general discussion or description of the Coal Measures seems called for here, as only a few minutes will be devoted to the section in the Greta at Ingleton, and the visit on the con­ cluding day of the excursion to the Whitwood Collieries will be directed more to the examination of the general conditions of the working of a first-class colliery and the mode of occurrence of the seams than to the specific study of the geology of the Coal Measures, It may be well, nevertheless, to give a very brief summary of the chief facts, and of the deductions that I draw from them. The Coal Measures of the Yorkshire Coalfield belong to the Lower and Middle divisions, saving only for the possible occur­ rence of a few hundred feet of grey and red measures in the Pontefract and district characterised by the abundance of .Anthracomya phillipsii. These occur at a horizon about 750 yards above the Barnsley Bed. The red colour may not be original but due to percolation from the overlying Permian rocks. The Coal Measures consist essentially of a great shaly series rather more than 5,000 ft. in thickness. The shales are mainly of fresh-water origin, they contain plant remains almost through­ out, and fresh-water lamellibranchs are of frequent occurrence, but there occur also well-marked bands of shale of a different texture from that of those to which a fresh-water origin is ascribed, and these contain a scanty marine fauna, with Goniatites, Pterino­ pectens, and Lingulre as frequent components. Six of these bands are known to occur above the Barnsley Bed, and the numbers will probably be increased with further research. They THE DISTRICTS ABOUT SETTLE AND HARROGATE. 43 constitute very important indices by which the horizons of the measures encountered in deep borings can often be identified. Of the coal-seams themselves little need be said, except that every seam known to me in this field rests upon a seat-earth or old soil-sometimes argillaceous, as fire-clay, and sometimes a hard sandstone or gannister--containing invariably multitudes of roots and rootlets. This fact, in conjunction with other oft­ cited, yet often ignored, features of the seams themselves, such as their wide extent, general uniformity of thickness, freedom from ash, and absence of included remains of aquatic animals, convince me that the seams result from the growth-in-place of the vegetable matter forming the seams. One further fact, for which my authority is Mr. \Y. Hemingway, of Barnsley, tells very strongly in the same direction, namely, that the plants found in the shales differ widely from those found in the seams. The case of Cannel, by the completeness of its contrast to true coal, affords at once proof of its own origin by a process of drift, and confirmation of the correctness of the theory that explains the formation of true coal by growth-in-place. Cannel never rests upon a seat-earth of its own, though occasionally usurping that of a coal-seam that has been washed out; it is of limited extent, very variable thickness, contains a high percentage of ash, and almost, if not quite, invariably contains remains of fishes and other aquatic animals. More decisive evidence for the inapplicability of the drift theory to the one case and its applicability to the other I am unable to imagine. Beds of sandstone, for the most part local and impersistent, occur at various horizons, but a few beds of great thickness are found that extend over a hundred or more square miles, the most noteworthy being the Eiland Flags in the Lower Coal Measures. The Yorkshire Coalfield, like that of Durham, is remarkable for the frequence of "washes" in the seams, i.e., of areas from which the coal has been removed and beds of sandstone, shale, or conglomerate substituted. These washes are, in my experience, of two kinds-narrow sinuous belts that may, in a few cases, be traced from pit to pit over a considerable area, and that, when plotted on a map, have the form, as they are in fact, of silted-up channels of streams that meandered over the Coal Swamps and scoured out the peaty material. The other type takes the form of broad tracts extending over perhaps hundreds of acres, and as these affect some of the finest seams in the coalfield, they often cause most serious loss and disappointment to coal proprietors. The fact is becoming increasingly clear to me, year by year, that washes are intimately connected with tectonic movements taking place during Coal Measure times. The broad washes in a large number of cases can be seen to be bounded and strictly limited by faults. An example illustrating this will be a main object of the visit to the Whitwood Colliery. 44 PERCY FRY KENDALL ON THE GEOLOGY OF

The Haigh Moor Seam is " washed" in many pits within ten or Jifteen miles of Norrnanton, and the rock taking the place of the coal, or lying upon it, is gcnerally a conglomerate with pebbles of shale, coal, and ironstone. At Whitwood Colliery there is a large area affected by the wash, which extends up to, and with only a trivial and insignificant exception is sharply limited by, the Methley Fault-a great N.E. and S.W. fracture throwing down to the S.E.-on which side the wash occurs. A small fault is found in one district of the colliery that throws a coal-seam to the extent of sixty feet, and does not affect a seam above it. The Coal Measures of the Black Burton Coalfield are at present very imperfectly known, but they include three con­ siderable seams, one being a Cannel seam, and their total surviving thickness, taken from the "horizontal" sections of the Geological Survey, appears to be about 1,900 ft. It may be that their original development was upon the same scale as in the Burnley Coalfield, and that 6,000 ft. of Coal Measure strata preserved at Burnley were removed by pre-Permian denudation from this little field; but I am inclined to ascribe much more to original differences of deposition, for beds occur in the River Greta at Ingleton containing dolomitic limestones attributed by Mr. Tiddernan to the Coal Measures, in which opinion he was supported by the late Mr. Binney. No such limestones occur in the Burnley Basin, but they occur in the Upper (Ardwick) Measures of Manchester. These limestones should receive attention during the visit of the Association, as any fossils found in them might yield decisive evidence upon the question of their age.

V.-THE PERMIAN ROCKS.

The excursions are planned so as to afford opportunity to study, on a line very near that of their nearest approach, the two strongly contrasted types of Permian rocks that occur on opposite sides of the Pennine Chain. The western type occurs in Dumfries, the Vale of Eden, the seaward margin of the Lake District, the Isle of Man, the Ribble Valley near Clitheroe, the Ingleton Coalfield, Lancashire, Cheshire, Flintshire, and Shrop­ shire. It consists essentially of bright red, frequently very coarse, sandstone, with marls, and occasional irregular developments of conglomerate (Brockram), and only in a few sections, e.g., at Barrowforth near Whitehaven, on the River Bela near Kirkby Stephen (20 ft.), and in Hilton Beck (25 ft.), a Magnesian Limestone. The eastern type, extending in an uninterrupted outcrop from the mouth of the Tyne to the city of Nottingham, is constituted THE DI ST RI CTS ABOUT SETTLE AND HARROGATE. 4S substantially of Magnesian Lim eston e, with subo rdinate and in­ constant beds of marl and sand or sandstone. T he full sequence IS: 6. U pper Marls with Gypsum, Anhydrite, Rock-salt, and some Sa nds tone. 5. Upper l\la gnesian Lim estone. {. Middle l\larls with Gypsum. 3. Lower :\la gn esian Limestone. c. Lower Marls (l\ Iari slate in Durham). I. Yellow Sa nd, Sa ndstone, a nd, locall y, cong lomerate (POXOIl St one). Any mem ber of th is series may be abse nt except the lower division of th e Magnesian Limestone. The paleeontol ogical contrast is nearly as great as the litho­ logical. In the western area larnellibranchs and small gasterop ods are sometimes abundant in th e marls, e.g., at Manchester and Stockport, but no brachiopo ds, polyzoa, or cephalopods appear to have been recorded, an d few, if any, fishes. The eastern Permians, on th e other han d, yield, along with the same suite of lamellibranch and gastropod mollusca, nautili, brachiopods, referable to many genera (e.g., Productus, Strophalosia, Spinjera, and L ingula), an d sometimes in great abunda nce, as well as man y polyzoa and fishes. These mark ed differen ces in important particulars are constan t through a north and south range of 1 70 miles, whereas the two types are seldo m separa ted by a greater east and west interval than 30 miles, an d I agree with the op inion of Dr. T eall, and of Goodchild and E. Wilson, that the facts are best explained by supposing that the Pe nnine Chain constituted a barrier in Perm ian tim es, and that th e rocks were laid down in separate basins of de position, though some con­ nection doubtless existed at som e stage by which the faun a of the western area was introdu ced. It is not , however, easy to indicate its site. The rocksof theeastern area will be examined at , where fine sections, showing th e unconformable junction with the Millstone Grit, will be seen. In all the exposures at present visible the Lower Magnesian Lim estone, sometimes sandy or gravelly at th e base, will be seen, bu t no Lower Marls are exposed. I have, however, seen a patch of chocolate-coloured mari on the Grit near the bridge on th e road to Harrogate. The Magnesian Lim estone about Knaresborough is generally un fossiliferous, but it presents many interesting problems in physical geology. The rock is generally very porous, and beside s simple pores it is rendered caverno us by ramifying hol es about an inch in diameter. These are often lined with crystals of dolomite. The general explanation of the open texture of the limestone is that the conversion into Magnesian Limeston e took place subse­ qu entl y to consolidation, and as the replacement of heavy calcium by the light er magnesium prod uced a substance, Dolomite, of 46 PERCY FRY KENDALL ON THE GEOLOGY OF higher specific gravity than th e original Calcite or Aragonite, some shrinkage must have taken place. There remains, however, th e difficulty of explaining th e formation of the larger hollows. Mr. Ernest Guy, acting upon a suggestion of mine, has shown th at, whereas in deep borings th ere are inclusion s of Gyps um, Anh ydrite, an d, more rarely, Barytes, in th e Magnesian Lim e­ stone, but no hollows; in surface exposures there are hollows, hu t very rarely traces of such an infilling. This raises a strong pre­ sumption that the hollows are produced by meteoric waters dis­ solving out th e nodul es of Gypsum and Anhydrite, leaving a space into which a lining of do lomitic crystals may be introdu ced. The lime stone in th e quarries at Knaresborough is traversed by the curious zigzag "suture planes " such as occur very abun­ dantly in the chalk of Flarnborough Head and elsewhere. They contain, as is usual, a film of marl representing the insoluble residue of limestone th at has been removed by solution. The Dropping Well at Knaresborough may, perhaps, be visited. It is a spri ng esca ping from the Magn esian Lim estone, the waters of which are practically a saturated solution of calc ium sulphate with som e calci um carbonate and magnesium sulphate . Some uncertainty exists as to whether th e Magnesian Limestone is the real source of the spring or whe ther it actu ally rises from th e Carboniferous rocks. It may, however, be pointed out that the H arrogate springs do not conta in a high percentage of calcium sulphate. The Magnesian Limeston e rests in marked un conformit y up on the various members of th e Carboniferous ser ies, passing from the Upper Coal Measures, near Newa rk, to Millstone Grit (Leeds to near Catte rick), Yoredale Ro cks and Carbo niferous Lim estone (T ees-Swale anticline), an d again on to Coal Measures through County Durham and across the T yne to T ynernouth. The maximum amoun t of pre-Permian denudation is probabl y little, if at all, sho rt of 8,000 feet. The western type of Permia ns will be examined at Westhouse and Mason Gill on the Ingleton Coa lfield. The sec tions near here were excellently described by Binney in 1855 and 1857 (2 0 and 21), but th ough cite d in th e Geological Survey on the district, littl e or no significance was attached to his most remarkable observati ons. Two principal sections will he examined; th e first is near Winking Bank House, Westhouse, and the second in Mason Gill. In the first, red sandstones with gravelly or conglomeratic layers are expo sed in a stream-course. The pebbles here consist mainly of fragments of Spirorbis limestone, upon which Binney remarked that th ough such limestones occur in th e neighbour ing coalfield, th e particular type represent ed in th e pebbles is not now to be met with in the Black Burton coalfield. A peculiar THE DISTRICTS ABOUT SE TTLE AND HARROGAT E . 47

flinty chert found by him was not known to him except from Ard wick near Manchester. I have confirmed th ese observations of Binn ey's in respect of both rocks. T he Spirorbis limestone occurs in blocks up to the size of a man 's head. T he Mason GIll section gives a splendid exposure of br ight sands tone with irregular layers of gravel or conglomerate. The stones range up to a foot in length , are very imperfectly rounded, and some ha ve th e ap pearance of being " stream laid " (i.e., have one end up-tilted ) in a direction from N.E. or N. to S.W. or S. Spirorbis limeston e no longer predo minates ; ind eed, I cannot be certain of its occurrence at all, but th e Mo untain Lim estone is abundantly represent ed by pe bbles and boulders very generally showing signs of dolornitisation subseque ntly to deposition. Millstone Grit is not uncomm on, and quartz pebbles, doubtless derived from th e same formation : the most remarkable rocks, however, are the fragme nts of " slates, Silurians, and Old Red Sand­ stones " (Binney). It is remarkable that no inferences respecting the physical conditions attending the deposition of the Permian rocks were based upon this observation, to me the most astoni sh­ ing in the whole range of th e Geology of Yorkshire. If the Permian strata contain fragments derived from the floor of older Palzeozoic, it is dear that not only must the base of the Carbon­ iferous series have been uplifted, but (a), the uplift must have bee n by movement of the Craven faults; (b), the whole Carbon­ iferous series-Coal Measures, Millstone Grit, Yoredales, and Ca rboniferous Limestone-must have been trenched th rough to th e very base, and the un derlying platform of early Palseozoic rocks itself subjected to erosion. The first of th ese dedu ctions is quite in agreement with my observations upon the Brockrams of th e Vale of Eden. T he constituents of thos e conglome rates in proximity to the Cro ss Fell inlier show that the Pe nnine faults moved by two stages­ th e first, in pre-Permian times, exposed the whole of the Carbo n­ iferous series except the basal conglomerate to denuda tion during th e deposition of the Lower Brockram, while a furth er movement dur illK the Permian period exposed even this basem ent bed and most pro babl y th e underlying Ordovician rocks to stream action when the Upper Brockram was forming, and that, despit e the fact that a thousand feet of sandstone had meanwhile accumulated against the fault scarp. The Ingleton evidence precisely accords with that of the Vale of Eden. The older conglomerate of Winking Bank Hall contains no tra ce of th e pre-Carboniferous rocks, hut on the other hand con tains much Coal Measure debris, while th e Mason Gill beds, higher in the Permian seq uence, contain no Spirorbis limestone, but a bundan t fragments of slate and ot her pre­ Carboniferous rocks. The throw of the fault movemen ts thus indi cated cannot be measured with exactitude, as we can (arm 48 PERCY FRY KENDALL ON THE GEOLOGY OF no precise estimate of the thickness of the Upper Carboniferous. The Carboniferous Limestone and Yoredales I have shown to have an aggregate thickness of 1,450 ft. The thickness of the Millstone Grit cannot be ascertained, nor can that of the Coal Measures. In the Pendle Range the Millstone Grit attains a thickness of 4,600 ft., while the surviving Coal Measures, the series being incomplete and lacking the portion with Spirorbis limestone, is about 8,000 ft. I do not consider that these enormous thicknesses were maintained into the Craven Highlands, and in this opinion I am confirmed by measurements taken from the Index to the Geological Survey Map of the district, which assigns 2,700 ft. to the Millstone Grit and 1,950 ft. to the scanty remnant of the Coal Measures still remaining in the Black Burton Coalfield.* Putting all these together it will be seen that the whole thick­ ness of Carboniferous rocks stripped off so as to expose the Lower Palseozoic floor cannot well have been less than 5,000 ft. An interesting question emerges from the consideration of the altitude at which the Permian rocks occur. The highest part of the outcrop is now about 700 ft. O.D., and the breccias at this altitude contain large blocks of pre-Carboniferous rocks that would demand a powerful current and consequent steep gradient for their transport. Now, the highest part of the old floor in Chapel-le-Dale is only 800 ft., therefore, if the blocks came from that area the later readjustments of the Craven faults cannot have produced a net down throw amounting to so much as 100 ft. J\1y observations are not sufficiently advanced to enable me to say whether the slate, etc., came from Chapel-Ie-Dale, but in view of these implications respecting the fault I think it much more probable that it was derived from the area between the Dent and Barbon faults to the N. \V., where in the absence of allY cover of Carboniferons rocks it is allowable to assume a much greater displacement of the faults. Whichever explanation may be adopted the conclusion will still be maintainable that these Permian breccias were laid down as gravel fans by torrential streams emerging from a deeply trenched plateau terminating in a fault scarp several thousands of feet in altitude. The sandstones that are interbedded with the breccias are interesting; they include very perfectly rounded grains, often very large, and in these may be recognised the characteristics of wind actions. Exactly similar grains constitute the Penrith Sandstone of the vale of Eden, and the Collyhurst sandstone of Lancashire

:~ The thickness of the Carboniferous and the consequent throw of the outer Craven fault is the subject of an interesting and valuable discussion by Dr. Strahan in the Guide to the Geological Model of Ingleborough and District (Mem. Geot. Surv.) tglO. Dr. Strahan assigns the following thicknesses to the respective members of the Carboniferous Series: Great Scar Limestone, about 600 ft., Yoredale Series, 918 to 950 ft.. Millstone Grit proved to 600 ft. Coal Measures proved to 1,978 ft., and the total displacement effected by the Craven disturbance is estimated at 5,375 ft. THE DISTRICTS ABOUT SETTLE AND HARROGATE. 49 and Cheshire. The abundance of felspathic grains and their large size, no less than the magnitude of the deposit, suggests the probability of their derivation from the arkoses of the Millstone Grit of the Pennine Chain, just as the almost entire absence of such materials in the Permians of the eastern type would lead one to conclude that the prevalent winds must have been easterly. Signs of dune-bedding have not been sought in the western area at present, whereas Professor Lebour expresses the opinion that the Yellow Sands of Northumberland and Durham show the characteristics of wind-accumulation. I am disposed to regard the marly and calcareous beds in the upper part of the Western Perrnians as the equivalent of the whole of the eastern series. The picture that I should draw of Permian times in the Pennine area would depict a country of high, barren, stony waste, with crumbling mounds of shale, sandstone scars, and terraces of limestone. This stony waste would be terminated by the great fault-scarp fretted along its margin by deep rocky khors or wadies down which, from time to time, torrential rains, such as those that visit at infrequent intervals the similar regions to-day, would send torrents of water sweeping the sun­ splintered rock fragments from their floors out into the low grounds. To the westward would stretch the tawny sands of a wide desert expanse unbroken save perhaps by the hills of the Silurian tract about the Lune, the Lake Country, and in the dim distance the mountainous group of the Isle of Man. To the south-east the PendIe Range must, if Mr. Tiddeman's interpre­ tation of the structure of Ribblesdale be accepted, have stood up as a great escarpment of greater steepness and altitude than at present. These conditions passed away with the movements that brought the shallow over-salted waters of the sea along both flanks of the Pennines.

vr.-IGNEOUS ROCKS.

The only representatives of Igneous Rocks in the districts to be examined are three dykes intrusive in the older Palseozoic strata in the neighbourhood of Ingleton. They have been described as Lamprophyres, and as they belong to a series that is in places intrusive in the Silurian and is uncomfonnably overlain by the Carboniferous, the inference seems just that they belong to the period of volcanic activity that extended through Old Red Sandstone times. Dr. Marr and Mr. Harker consider them to be connected with the intrusion of the Shap Granite, and their direction at Ingleton, N.W. and S.E., is consistent with this view. PROC. GEOL. Assoc., VOL. XXII, PART I, IgIL) 4 50 PERCY FRY KENDALL ON THE GEOLOGY OF

VI I.-GLAC IAL PHENO MENA.

T he excursions will range over a long strip of count ry and enter several distinct areas of glaciation, so that a general account combining these into a coherent whole is beyon d the scope of the present undertaking,but a short preliminary notice,stating in rather absolute terms the conclusion s reached upon a review of all the available data, may help to an understanding of the local details. At the climax of the Ice Age th e H owgill Fells and other adjacent hills seem to have formed a radi ant-point from which ice travelled, southw ard, eastward, and, to some extent, northward. In a westerly direction it was obstructed by a flow from the Lak e District, with which it became confluent, while on the north a great stream flowing up the Vale of Eden drew it round towards the east. The researches of Mr. Tiddeman, embodied in a paper (23), for which British geologists should be ever grateful, have shown the general directio n of the ice in a southerly direc­ tion, while the late J. G. Goodchild's pap er on the country to the north (24) closely followed Mr. T idd eman's in time, as it did in spirit. All the Western dales that will be visited, viz., Chapel-le-Dale, Clapdale, Crummack, Ribblesdale, Aireda le (Malha rn distric t), and Wharfedale, seem to have been glaciate d by ice genera ted within the main watershed extend ing from Whernside by Bleamoor, and Dodd Fe ll to the Stake. Some ice no doubt overflowed from the northern side of this crest, but if it augmented, it did not divert , the flow of the native ice, and, so far as can be ascertained, it brought in no distinctive bould ers, if any at all. The ice-flow in each of the principal valleys followed the general slope 0 1 the valley axis, but on the intervening watersheds the ice-streams were confluent, and hence such minor valleys as Crummac k and Clapdale were overflowed from their head s, so that it would seem justifi able to speak of an ice-sheet, rath er than of glaciers, . in describing the distri ct. The signs of glacier­ dammed lakes such as might be expected in a country subjected to glaciation of this type arc not wanting, but no comprehensive study of them has yet been made. The Ingleton valley presents no special featur es of interest, but Kingsdale, the valiey that enters from the north , shows some fine morainic featur es near Braida Garth, and the broad flat floor in its lower course and narrow, ravine-like outlet into the Greta present appearances suggesting a lake produced, either by obstru ction by a drift-dam, or else by glacial-erosion of th e basin -the former seems the more probable. The phenom ena may wei! be investigated during the excursion. Crummack is interesting THE DISTRICTS ABOUT SETTLE AND HARROGATE. 51 for the fine moutonnee crags alluded to earlier, and for the uplifte d boulders on Norber. Clapdale presents one notable feature in the enormous mass of drift that lies across a lateral recess between Rayside Plantation and Clapham Scars, enclosing a hollow some 50 feet deep against the limestone crags. In the upper part of Ribblesdale the valley is cumbered with Drift mounds, drumlins, and eskers in tumultuous confusion, and occasional roches moutonnees are to be seen, but my uns ystematic obser vations do not enable me to offer any details. The Malham country is chiefly notable for the great range of gravelly morain e-heaps lying upon the Silurian rocks near the T arn, that seems to owe its existence to a drift-dam . Wharfedale exhibits one notable glacial feature in the presence below Kilns ey of erratics of Silurian rocks. Mr. Dakyns has shown that , though there is no visible outcrop of pre-Carboniferous rocks in Wharfedale, the ascertained direc­ tion of the ice-flows forbids the supposition that they came from any extraneous source, and he concludes that there is an outcrop of Silurian rock beneath the Alluvium at the foot of Kilnsey Crag. This ....conclusion agrees with Mr. Cosmo Johns's observations upon the Carboniferous rocks of the distri ct, for he found the Seminula-beds, the lowest zone of the Carboniferous recognis­ able in Yorkshire, in the Crag itself. The H arrogate district belongs to a distinct system of glacia­ tion in Which, nevertheless, traces of the influence of the ice from the great breeding ground on the Western fells are man ifest. It would appear that at the period of maximum extension of th e ice all the Pennine valleys from the Tees to the Wharfe were brimming with great glaciers streaming in an easterly direction into the , but at a later stage the local ice in all the valleys south of Uredale shrank back towards theirsource, leaving their lower ends ice-free. The first phase, that must have been separated from the last by a very long interval of time, is indicated by a sparse scattering of drift over th e hills even on or near the watersh eds. The later phase is shown by beautiful moraines of recession, such as those at Glasshouses and Gouthwaite in the Nidd Valley, near Pateley Bridge, as well as by a wonderful "aligned sequence " of lake-channels and a related lateral moraine extending for over forty miles, from the Ure, near Jervaulx, to the neighbourhood of Bolton Percy, where the lateral morain e merges into a gigantic terminal moraine, sweeping in a semicircle of nearly twenty miles, measured along the are, to Stamford Bridge, completely spanning the Vale of York. The evidence of these features shows that, long after the 52 PERCY FRY KENDALL ON THE GEOLOGY OF

recession of the other Pennine glaciers, a great stream of ice descended U redale, and, at the particular stage selected for description, it became confluent with a yet more gigantic glacier descending the Vale of York, that, fed by ice that had crossed Stainmore Pass from the Vale of Eden, and augmented on the one hand by a Swale-dale glacier, and on the other side by ice pressing in from Durham and the , was powerful enough to bend the glacier of the Ure through an angle of seventy degrees and drive it across the spurs of the Pennines. The Ure glacier at Jervaulx was at least 700 ft. thick, and it obstructed the drainage of every eastward flowing stream through the line, producing a chain of lakes draining by trenches cut through the spurs, from lake to lake, with augmenting magnitude proportionate to the increasing volume of water, until Lake of Carvill Lewis was reached. Two channels will be examined during the excursion. The first, Cayton Gill, is a great gorge, quite streamless in its upper part, that runs a course of about two miles down to the old Lake Nidderdale at Ripley, where a great delta and lake-bottom flat marks its discharge. This lake received the drainage of Upper Nidderdale as well as of a glacier lake in the Washburn, the overflow channel from which forms a fine streamless gorge at John O'Gaunt's Castle, and becomes the valley of the Oak Beck, near Harrogate. The Washburn Lake was held up by the ice-barrier of the Wharfe glacier. The outfall of the Nidderdale Lake was driven on to the gently sloping plateau flanking the Nidd Valley, quite near to where a sharp descent took place, on to the floor of the valley, and along this margin a great winding gorge was cut from the position of the Nidd Viaduct on the North-Eastern Railway to a point where the Knaresboro- road crosses the river at Grimbald's Bridge. The pre-Glacial valley of the Nidd was obstructed by the lateral moraine of the great glacier at Nidd Hall to such a height that on the withdrawal of the ice the river was permanently retained in its new channel, and the continuation of the old valley was left untenanted save by an insignificant parish beck.

THE VICTORIA CAVE.

Near Settle, on the east of the valley, at an altitude of 1,450 feet above the sea, and 900 feet above the River Ribble, is the famous Victoria Cave, which throws a wonderful light on some most important problems of the Ice Age. This cave was dis­ covered accidentally in the year 1837 ; its exploration, conducted in a somewhat amateurish fashion at first, was completed in a methodical manner upon a scientific plan by a committee of the British Association in the years 1869-78. This systematic THE DISTRICTS ABOUT SETTLE AND HARROGATE. 53 research proved the following succession of deposits In the cave:- 8. Talus, 1-2 ft. 7. Romano-Celtic Layer. 6. Talus, 0-5 ft. 5. Neolithic Layer. 4. Talus, 19 ft., maximum thickness. 3. Upper Cave Earth, with Mammalia of existing species. 2. Laminated Clay. 1. Lower Cave Earth, with Pleistocene Mammalia. Rock Floor of Carboniferous Limestone. Outside the mouth of the cave, which was almost completely closed by deposits, a bed of stiff boulder day containing great quantities of scratched boulders, comprising fully So per cent. of Silurian grits, was found to truncate the bed 2 at an angle of about 40°. The interpretation of this is clear-the first deposit of cave earth with mammalian bones took place before the advent of the Ribblesdale Glacier. When the ice arrived muddy water from its melting edge filtered into the cave and formed the book-leaf (Laminated) clay, exactly similar in appearance to the lake muds recognised elsewhere. Of approximately simultaneous date would be the deposit of boulder clay cutting across the lower cave earth. The upper cave earth is evidently of post-glacial date (so far as this part of Yorkshire is concerned), but the character of the fauna seems to indicate that it is still anterior to the Neolithic period. The great mass of talus covering the upper cave earth may, perhaps, be some measure of the time that elapsed before the deposition of the layer with relics of Neolithic man. The Neolithic layer yielded few, but those unmistakable, traces of man. The Romano-Celtic layer contained a remarkable number of relics of Roman civilisation.

VIII.-TECTONICS.

In the introduction I have alluded to the Pennine Chain as a great fold directed north and south. The eastern slope is very gentle, while on the west it is, through the greater part of its length, cut off abruptly by a system of faults. It is cut off similarly upon the north, along the Irthing­ Tyne depression, by faults throwing down to the north, while its southern extremity is concealed beneath discordant beds. The western faulted limb is interrupted south of the Craven country by a fracture zone and a series of folds of which the 54 PERCY FRY KENDALL ON THE GEOLOGY OF principal members are the Clitheroe and Rossendale , and the syncline of the Burnley coalfield. The faults will be further considered later. The folds are directed in a general S.W. and N.E. direction, and they gradually lose their definition as they proceed to the north-east, and appear to be represented in part by the small faulted anticline bringing up the Yoredale rocks at Harrogate, and perhaps, to some extent, by the fold that I have called in my report to the Royal Commission on Coal Supplies the Wbarfc-i-Market-Weighton anticline, whose southern limb forms the northern boundary of the Yorkshire Coalfield. Another interruption to the western fault-system occurs at Stainmore Pass, where a significant transverse fold occurs that can be traced through to Middleton Tyas, and is continued across the Cleveland country to the sea at Robin Hood's Bay.* It is with the country adjacent to the Craven faults that we are concerned, and to elucidate their structure and effects it is necessary to regard them as parts of a system consisting of two great groups enclosing within their sweep the whole area from the mouth of the Tyne by Brampton, Brough-under-Stainmore, and Ingleton to . Commencing near the mouth of the Tyne, a fault-the Tyne Bottom Dyke (the word "dyke" is used by the Northumbrian miner to designate a fault, and has no necessary relation to igneous rocks)-runs nearly due east and west with a throw diminishing from hundreds of feet at the coast until it dies out. It is, however, succeeded, after an interval that may be only a mile or two, by a second fault-the Stublick Dyke-that con­ tinues its direction with an increasing throw till it encounters the Pennine Faults near Brampton. Both these east and west faults throw down to the north, and some part of their movement was accomplished after the deposition of at least some of the Permian rocks. The Pennine Faults, that have been well described by Dr. Marr (4, 28, and 29), run in a general N.N.W. and S.S.E. direction, with a net down throw to the west. They die out by the process of bivirgation (Suess) on Stain more Pass. Near Kirkby Stephen there commences the series of faults constituting a line of comminuted fractures that are called col­ lectively the Dent Fault. Its direction is about 8.S.W., making an angle of about I 15 degrees with that of the Pennine Faults. Near Leek Fell it meets at an acute angle a great fault, the East Barbon Fault, that comes down in a north and south direction from the neighbourhood of 8edbergh and swings round to the south­ east to Leek and thence onward, is known as the Outer Craven Fault; a parallel fracture, the North Craven Fault, the position * I presume this to be the anticline referred to by Dr. Marr in (( Ge010gy in the Field," but I do not assign to it as he does the dominant role in separating the Coalfield of Durham from that of Yorkshire. THE DISTRICTS ABOUT SETT LE AND HARROGATE . 55 and relations of which are not at first clear, runs about half-a­ mile to the northward. Near Settle these two have diverged until they are nearly three miles apart, but they again converge until th ey arc lost among a series of fault s dying out on th e moors between Pateley Bridge and Rip on. About two miles north of Ri pon an oth er pair of fault s commences, dropping the Permian and later strata into a trough between th em, and th ese run directly across the Vale of York ; they breach th e Oolitic Escarpment to form the remarkable pass known to York shire geologists as th e Cox wold­ Gilling Gap , and with many bran ches in which the south fault dies out or loses its identity, pass out perhaps to the sea in Filey Bay. The whole series regarded as one system might be represented by a square-topped figure 3 written left-handed. The upper half would represent th e T yne-Bottom-Stublick-Pennine Faults, the middle would be a node at Stainmore, and the curved lower half would be the Dent-Crav en-Coxwold series. The block of country within the upper angle is relativ ely upthrown. The Dent Fault throws down the Carboniferous rocks on the east against Ordovician and Silurian rocks, while the Craven Faults throw down by successive steps to the south. These great fractures have had a remarkable effect in relieving the country within from disturbance, and especially is this to be seen when the area most effectively protected by the faults is contrasted with places adjacent to the nodes ; for example, the In gleton She et of the r-inch map shows scarc ely a fault of any magnitude within th e protected block, while the Kirkby Stephe n She et to the north, where the protecting Dent Fault dies out, shows a considerable faulting in its northern half. Similarly, as the Craven Faults fade out near Pateley Bridge the rocks are severely dislo cated. Similar features are noticeable in the areas of th e east. The relat ive ages of th e faults and the geological date of their several movements have been referred to by Dr. Marr, but some new light has been thrown upon the sub ject by recent investigations that seem worthy of notice here. The faults alon g the Tyne Valley have already been noticed. They are clearly, in part at least, post-Permian, and may have originated in any pre-Permian period. Na evidence is however available to determine thi s. The Pennine Faults-outer, middle, and inn er-may have originated simultaneously , but the fact is clear that the middle fault is the most important, and, as Dr. Marr has shown , a throw amounting to at least 20,000 ft. was accomplished before the deposition of the Carboniferous rocks. A further movement of the fault or a very acute fold, of which r have seen no evidence, must have ensued after the deposition 56 PERCY FRY KENDALL ON THE GEOLOGY OF of the Carboniferous rocks and before that of the Upper Brock­ rams, as I have endeavoured to show (22). Dr. Marr is unable to accept my inferences, and I must therefore state the facts a little more fully. The basal conglomerate of the Permian, the Lower Brockram, is in the neighbourhood of Appleby com­ posed exclusively of detritus of the Carboniferous limestone in blocks ranging in weight up to about 2 cwt. At the top of the Penrith Sandstone, that here cannot well be less than J ,000 ft. in thickness, there occur in Hilton Beck several beds of another conglomerate or breccia containing, besides Carboniferous Lime­ stone, large pebbles of vein quartz, of Basement Carboniferous conglomerate, and angular fragments of a hard quartzite, along with small pebbles of Borrowdale rhyolite. These materials are identical in character with the beds on Roman Fell, and as the outcrop of the breccia is less than I Yz miles from the Outer Pennine Fault, I see no reason to doubt that they came from that source. The only alternative seems to be to suppose that they were derived from the Howgill Anticline, the nearest part of which is 10 miles from Hilton Beck; but against this there are two facts to be taken into account-the large size and angularity of the stones, and the dissimilarity between the Basement Carboniferous beds at that place and the stones in the breccia. The last movement of the Pennine Faults must have been post-Triassic. The Middleton Tyas anticline seems to have had a history closely following that of the later movements of the Pennine Faults. Its first recognisable movement was in pre-Magnesian Limestone times, but the Cleveland fold-its eastward prolonga­ tion-stands upon a site that underwent great and prolonged depression during the Jurassic period, and the anticlinal folding was not operative until after the Kimeridge Clay was deposited. The Dent Fault, Craven Faults, and Howgill Fell anticline seem to me to constitute one connected series of phenomena whose histories can hardly be separated, and the key to their interpretation may be found in the Permian rocks of the Black Burton coalfield. I have explained in an earlier chapter that these rocks, like those of Hilton Beck, contain two types of conglomerate-an upper one, containing, inter alia, blocks of Spirorbis Limestone from the Upper Coal Measures, and a lower from which this rock appears to be absent, but instead there are fragments of slate. Now two facts lead me to the conclusion that the slate was derived, not from the direction of Chapelle-Dale, but from the district to the north-west-vif the slate had been derived from the former locality I should expect to find the much more durable Ingleton grits as well as slate, and the breccias with slate are now only 100 feet below the highest outcrop of the old rock: it THE DISTRICTS ABOUT SETTLE AND HARROGATE. 57 is inconceivable that the post-Permian movement did not exceed that amount. The slate, therefore, came from an uplifted portion of the Howgill anticline. Now, unless the Dent Fault was already in existence, bringing up the Silurian rocks, they would have been covered deeply by Carboniferous strata just as the old rocks are under Ingleborough. The same argument would establish the same date for the initiation of the East Barbon-Craven Faults. The Howgill anticline, by which Dr. Marr appears to designate the whole complex fold between Ravenstonedale and Kirkby Lonsdale (see "Geology in the Field," p. 626), is then roughly contemporaneous with the faults, and I regard the gentle un­ dulations of the Carboniferous rocks on the east of the Dent fault as the shallow syncline complementary to the anticline. In thus assigning a post-Carboniferous date to the Dent Faalt, I do not mean to imply that the first fracture took place after the deposition of the Carboniferous rocks; on the contrary, I think it highly probable that it had a long antecedent history, rivalling perhaps that of the Mid-Pennine Fault. It will be remembered that there occurs in Chapel-le-Dale and Ribblesdale the Ingletonian series of Mr. Rastall, which, on the gr.ound of its severely crushed and deformed condition, and its entire unlikeness, lithologically, to any of the rocks of the Lake District or the Cross Fell Inlier, was assigned to an age earlier than the Skiddaw Slate. These rocks have a persistent north­ west and south-east strike (the Charnian direction) and have an outcrop, measured along the strike, of between 7 and 8 miles, and on the dip in Chapel-le-Dale of 2t miles. Yet, though its most north-westerly appearance at Thornton Force is only 3 miles from the Dent fault at Leek Fell, this vast series, as well as the Con iston Limestone that accompanies it, fails to reappear. The singularity of this is greatly increased by the fact that the Dent Fault has a down throw to the east, and therefore might be expected to bring up on the west yet older rocks than those underlying the Carboniferous rocks in Chapel-le-dale. If this interpretation be correct, the resemblance to the Pen­ nine faults would extend to another stage. The Dent Fault has a down throw at present to the east, but if it juxtaposes Ingle­ tonian to Silurian, its later and lesser throw must be a partial reversal of an original gigantic downthrow to the west. This is exactly how the Pennine Faults have operated. Its pre­ Carboniferous movement resulted in a down throw to the west amounting to 20,000-30,000 feet where it attained its maximum; a later post-Carboniferous movement threw down to the east to an undiscovered amount. The further history of the Craven system of faults must be sought in the Jurassic country, and for the sake of completeness PROC. GEOL. Assoc., VOL. XXII, PART I, I9IL J 5 58 PERCY FRY KENDALL ON THE GEOLOGY OF it must be mentioned here, though the area lies outside the range of the present excursion. Allusion has been made to the Coxwold-Gilling gap, where the trough faults, that I regard as a prolongation of the Craven faults, run through the Corallian hills and en ter the . The memoir on the Jurassic R ocks of Yorkshire, the late C. Fox-Stran gways's masterly compendium of the subject, provides the data from which the following dedu ctions have bee n drawn : the Dogger, a sandy calcareous deposit atthe base of the Oolites, extends continuously along the H ambledon escarpment up to within about zt miles of the northern fault, attaining at this point its maximu m development; it then d windles rapi dly, and dies out about z miles from the fault," but reappears on the upthrow side of the southern fault. This would not be remarkable if it were an isolated fact, as it is a very variable formation, but we find that the Corn brash, one of the most tru stworthy of the Jurassic subdivisions, either thins out altog ether some 4 miles from the fault, not to reappear for many miles, or else it und er­ goes a complete change rend ering it unre cognisable. A third member of the Jurassic series, the , though well and characteristically developed across the hills from Scarborough to the Hambledon escarpment, dies out about Whitestone Cliff, z or 3 miles from the fault, and the Kellaw ays and Corallian come togeth er at the line of the faul t. Such coincidences as these can hardly be fortu itous, and I draw the deduction that the faults were moving during a large part of Jurassic times. The Kimeridge Clay is th e newest rock of the district traversed, and it too is faulted. T aking the scheme of fault s as a whole, I recognise move- ment s of its parts at the following periods :­ P RE-CARBONIFEROlJS t P ennine , Dent, Craven PRE-PERMIAN ... I Fau lt s. INTER-P ERMIA N Pennine- Cra ven. POST-PERMIAN Tyne-St ublick Dyke s. POST-TR IASSIC Penn ine Fau lt s. DOGGER Coxwold-Gilling. CORNBRASH ...... } OXFORD CLAY ... Coxwold-Gilli ng. POST-KIMERIDGE The blocks illustrating this paper are lent by the Yorkshire Geological Society, with the kind permission of Prof. McKenny Hughes.

IX.-REFERENCES. G ENERAL. MtmOlrs 01 tht Gt ological Suruey, 1872. U Geology of K irkby Lon sdale and Ken dal." 1872. U Geology of Ke ndal and Sedbergh.' • See Mr . Herries's account of the effects of the Peak fault upon th e deposition of the Dogger---" Geology in the Field," chap . xxv . THE DISTRICTS ABOUT SETTLE AND H ARROGAT E . 59

1872. " Geology of Appleby and Ull swat er." 1875 " Geology of the Burnley Coalfield. " 111 90. •. Geology of Ingleborough." 1892. .. The Ju rassic R ocks of Britain ," vol. i, Yorkshire. 1908. "Geology of Harr ogat e." Second edition.

I. 1853. PHILLIPS, J,-" The Ri vers, Mountains, and Sea-coasts of Yorks hire ." 2 . 1878. DAV1S, J. W ., an d LEES, F .A.-" An Account of th e Geology of West Yorksh ire." 3. 1907. K ENDALL, P . F.-The Chap ter on Geology in the Victorian H istory of Yorkshire. 4. I gIO. MARR, J . E.-" Geolog y in th e Fie ld," Jubilee uol, 01 Geol. Assoc., chapters xxv i, xxvii,

OLDER PAL-EOZO [C AND ARCH.£AN. 5· 1879. MARR, J. E.-" On some Sections in the Lower Palaeozoic Rocks of the Craven Distri ct ," Proe. Yorks.' Ceo!. & Polyt. Soc., vol. vii, p. 397. 6. 1888. MARK, J . E ., an d NICHOLSON, H . A.-" The St ockdale Sh ales." Qua,.t. J oltl"n. Geol. Soc., vol. xliv , p. 654. 7. 18gl. T ATE, T.-" On th e so-called l ngleton Granite." Prcc, Yorks c.«. & Pulyt. s«; vol. xi, p. 480. 8. Igol-8. HUGHES, T . McK .- ·'lngleborough." Proc, Yorks. Ceo!. Soc., vols. xiv, xv, xvi, 9· 1906. RASTALL, R. H.-" The Ingle tonian Ser ies of West York ­ shire" Pr oc. Y01'ks. Geol. Soc., vol. xvi, p. 87.

CARBONIFEROUS. 10. [886. T UTE. REV. J . S.-"On the Ca yton Gill Beds." Proe. Yorks. Geot. & P olyt. Soc., vol. ix, p. 265. II. 1891. T JDDEMAN ,R. H._" Ph ysical H istory of the Ca rboniferous Rocks in Upper Airedale." Proe. Yorks. Geol, & Polyt. Soc., vol. xi, p. 482. 12. 1899. DAKYNS, J. R.-" Th e Limestone-knolls below Skipton and Gra ssington in Craven." Quart , Journ. Geol. Soc., vol. lv, p.359· 13· 1899· MARR, J. E.-" On Limestone-knolls in the Craven District." Quart, J ourn . Geoi. Soc., vol. Iv., p. 327. 14· 19°1. HI ND, WHEELTON, and H OWE, J.A.-"On the Pendleside Group at PendIe Hill:' Quart . J ourn. CeDI. Soc., vol. lvii, P·347. IS· 1906. VAUGHAN, A.-" A No te on the Carboniferous Sequence near Pateley Bridge." Proc, Yorks. Ceo! Src., vol. xvi, p. 75. 16. Ig07· GARWOOD, E. J.-Ceo!. Mag., dec. 5, va!. iv, p. 70. 17· 1907. \VILMORE, A.- " The Structure of some Cra ven Limestones." Proe. Yorks. Geol. Soc., vol. xvi, p. I SR. 18. 1910. JOHNS, COSMO.-" The Lower Ca rboniferous Rocks of Mill Gil!. " Tlu Natu ralist, July. 1910. Ig. 1910• HIND, WHEELTON.- " The Correlation of the Yoredal e and Pendleside Series." The Naturalist, August, 1910.

PERMIAN. 20. 18S5. BINNEY, E.-" Observations on the Permi an Beds of the North­ West of England." MOil. LIt. & Phil. Soc. of MallehutlT, vol. xii, New Series. 60 THE GEOLOGY OF SETTLE AND HARROGATE.

21. 1857. BINNEY, E.-'· Additional Observations on the Permian Beds of the North-West of England." Op. cit., vol, xiii, New Series. 22. 190 2. KENDALL, P. F._H On the Brockrams of the Vale of Eden and the Evidence they afford of an Inter-Permian Movement of the Pennine Faults." Brit. Assoc. Report, p. 604.

GLACIAL. 23. TIDDEMA:-l, R. H._H On the Evidences for the Ice-sheet in North Lancashire and adjacent parts of Yorkshire and West­ moreland." Quart. yourn. Geoi. Soc., vel, xxviii, p. 471. GOODCHILD, J. G.-" The Glacial Phenomena of the Eden Valley and the Western part of Yorkshire-Dale District." Quart. yourn. Geol. Soc., vol, xxxi, p. 55. 1896. KENDALL, P. F.-" On some Post-Pliocene Changes of Physical Geography in Yorkshire." Brit. Assoc. Report, p. 801.

FAULTING AND FOLDING.

26. 1889. TIDDEMAN, R. H._H On Concurrent Faulting and Deposit in Carboniferous Times in Craven, Yorkshire." Brit. Assoc. Rep., p.600. 27. 1906. KENDALL, P. F.-" Problems in the Physical History of the Cleveland Area," Proc, Yorks. Geol. Soc., vo!' xvi, p. 127. 28. 1906. MARR, J. E.-Presidential Address. Quart. Yourn. Ceo!. Soc., vol.lxii. 29· 1907. MARR, J. E.-" The Geology of the Appleby District," Proc, Geol, Assoc., vo!' xx, P: I29.

CAVES AND UNDERGROUND DRAINAGE.

190 0.-190 4. "Report of Committee on the Underground Waters of North-," P1·OC. Yorks. Ceo!. Soc., vols, xiv-xv,