62 BY THE DIRECTORS,

II. The most obvious deposits in the glacier-lake are the deltas of:glacier-fed streams.

12. Ennerdale Water is presumably dammed by the Drift, apparently aterminal moraine, deposited by a lobe of Irish Sea ice upon its re-advancc."

This story is continued south of the Ehen valley wherea series of gravel deltas have been mapped.

Near Standing Stones deltaic material of exclusively LakeDistrict origin was deposited in a lake at about 875 ft. O.D.

Near Cockhow at over 700 ft., and westward at lower levels,gravel deltas were thrown out from Irish Sea ice into lakes,the waters of which have escaped by a series of marginal anddirect overflows converging on Uldale (PI. 9B).*

EXCURSION TO THE WHITEHAVEN DISTRICT.

SATURDAY, JULY 26TH, TO FRIDAY, AUG. 1ST, 1924.

Directors: BERNARD SMITH, M.A., D.Se., E. E. L. DIXON,A.R.C.Se., B.Se., T. EASTWOOD, A.R.C.Se., C. EDMONDS,AND S. E. HOLLINGWORTH, B.A., B.Se.

REPORT BY THE DIRECTORS.

SATURDAY, JULY 26TH, 1924.

Leader: T. EASTWOOD.

THE party proceeded to Distington by bus to inspect the fractureddome of the Lower Carboniferous rocks forming the Barfs inlieron the north-west of the village. A large disused quarry in theFirst (or highest) Limestone was visited; the wavy character ofthe bedding was noticed, and a few fossils, together. with somebarytes, were collected. The cover on most of the quarry isBoulder Clay, but near the limekilns Hensingham Grit succeedsthe First Limestone.

By the courtesy of Mr. T. Fletcher, Barfs Silica Quarries atWest Gill End were next visited. The large quarry is inHensingham Grit of variable grain, and evidently at one timean arkose, though the felspar is now completely kaolinised.Baring operations in this quarry have revealed the finest glaciatedpavement so far discovered in West Cumberland (PI. 7B). Thestriee range N.N.E.-S.S.W., following the drumlin ridges seen tothe north, which contain Lake District and local rocks. To thesouth-west the Hensingham Grit is terminated by a down throwfault seen in a quarry, in which are exposed highly disturbed shales,sandstones, ganisters and occasional dark earthy limestonescarrying fossils, which indicate that the measures belong to the

• s..E. HOLLINGWORTH in Summary of Progress for 1923 (Me.... Geol. Surv.), PP' 76-77.

EXCURSION TO THE WHITEHAVEN DISTRICT. 63

Snebro Gill Beds. A cavern recently exposed by quarryingalong the fault face in the Hensingham Grit gave rise to con­siderable speculation as to its origin. The suggestion by Prof.Fearnsides that it is due to collapse over a solution chamberin the underlying First Limestone appears most feasible, * andaccounts for the lining of the cavern by silty clays washedin from the Boulder Clay.

The party then proceeded to Harrington for lunch beforecommencing the walk along the coast to Whitehaven. Southof the Harrington Ironworks, sandstones (including the" Harring­ton Marble ") and fireclays, amongst dark shales with ironstonesassociated with the Micklam Fireclay Seam, were seen on thebeach; while measures up to the Six Quarters Coal were pointedout in the cliffs. At Cat Gill the Upper Three Quarters Coalbetween the Micklam Fireclay Seam and the Six Quarters Coalwas examined. Returning to the beach the broken groundassociated with the John Pit and Jane Pit faults-here of greatlydiminished and trifling throw-was pointed out. Continuingsouthwards, lower measures were seen on the beach and the twosandstones, comprising the Four Foot Coal Rock, were seenaround Cunning Point. These vary laterally and vertically,in the space of a few feet, from coarse grits to fine sandstones,in both cases with a development of ganister at the top, which,under the action of the sea, weathers into rough surfaces.Casts of tree roots were pointed out in the most northerly exposure.South of Cunning Point the Micklam fault, with a downthrowof about 800 feet to the south-west, was crossed, and on thebeach the reefs of sandstones above the China and BannockBand coals were noted. Good sections in the Bannock BandRock were seen at Lowca Point, while the China Band and itssandstone are visible in the cliffs above the railway.

Traversing the village of Parton, built mainly on a shelf ofold beach, the party walked towards Whitehaven, along thedisused mineral line at the foot of the cliffs, a halt being made tocollect fossil plants from the light grey sandy shales below theCountess Sandstone. On the north side of Redness Point a fault,with a down throw of some 200 feet to the south-west, lets inWhitehaven Sandstone against measures high in the ProductiveSeries, represented by the Countess Sandstone, etc. The oldcliff quarry by William Pit furnishes a magnificent section ofthe Whitehaven Sandstone, while the apparently conformablejunction with the Productive Series is seen on the beach.

MONDAY, JULY 28TH.

Leaders: T. EASTWOOD AND B. SMITH.

The party left the Grand Hotel and proceeded by way of thetown and Rosemary Lane to the high ground, capped by White­

• The close proximity of the First Limestone has now (March, 1925) been proved in an<excavationon the edge of the cavern.

BY THE DIRECTORS,

haven Sandstone, above Wellington Pit, where various topo­graphical and geological features of the neighbourhood werepointed out by Mr. Eastwood. The cliff footpath was thenfollowed to Saltom. Progress was sometimes difficult onaccount of numerous landslips of the Whitehaven Sandstone,which here dips seaward, and is undermined by crop workingsin the higher seams of the Productive Series. At Saltom thefaults cutting out the Whitehaven Sandstone were pointed out.The mineral railway was followed to Croft Pit, where the NewRed rocks make their appearance.

The Magnesian Limestone exposed in some old quarries westof Barrowmouth Farm, was next examined, and attention direc­ted by Dr. Smith to an included bed of limestone rubble witha band of extraneous fragments of rock. An outcrop of St.Bees Shales, with fine dustings of brockram, was then inspected,and the party thereafter descended, across land-slipped ground,to the beach, where the unconformity of the New Red Seriesupon the Whitehaven Sandstone is well exposed.*

The relationship of the several deposits and the possibilityof an unconformity between the St. Bees Shales and the Mag­nesian Limestone were here discussed. Fossils were collectedfrom the limestone which Dr. Trechman was inclined to correlatewith the Middle Magnesian Limestone of Durham.

Returning to the cliff road, after examining an adit mouthof the old gypsum mine and a dump of the mineral, the partywalked south-westward along a section of typical ripple-markedSt. Bees Sandstone with shaly intercalations. Dr. Smithpointed out a bed of sandstone that had been thrown into a seriesof loops formed pene-contemporaneously with its deposition.The immediately underlying shale was packed between the folds,whereas lower beds and those overlying the sandstone wereundisturbed. This was attributed to slipping on the inlandsea-floor whilst the beds were only partially rigid. t

Messrs. McKay's Sandstone Quarries were next inspected,and mention was made of the export of St. Bees Sandstone toAmerica in former days.

Turning inland, the members, after a short halt at Sandwith,proceeded to the lip of the St. Bees-Whitehaven Valley, wherethe Director expressed his tentative views as to its formation,i.e., as a modification, chiefly by glacial erosion of, or deposition in,two separate valleys, one draining north-by-west, the othersouth-westward. From this there was some dissent, an alter­native view that it had been excavated as a drainage channel,marginal to the Irish Sea Ice, commending itself to some membersof the party.

• B. SMITH, 1924, H On the West Cumberland Brockram and its Associated Rocks,"· Geol.Mag., pp. 289-308. '

t B. SMITH, 1916, "Ball or Pillowform Structures in Sandstones," Geol, Mag., pp. 146-56.

EXCURSION TO THE WHITEHAVEN DISTRICT. 65

The upper part of Ben How Wood was next visited. HereMagnesian Limestone * overlies the Brockram, which rests uponpurple-stained shales of the Productive Coal Measures. Thehorizon is roughly about 60 feet above the Bannock Band Coal,which was worked lower down the dingle during the great coalstrike of 192I.

At Seldom Seen, a few hundred yards farther north, outcropworkings of the same date in the Bannock Band Coal were noted,and attention directed to the mouth of an adit to the Main BandCoal. The Main Band Rock overlying the coal is well exposedat this point.

From Seldom Seen the party walked to Whitehaven Brick­works, and by permission of the management inspected thelarge quarries in which are exposed several seams of coal withthe associated fireclays, .mudstones and shales used in themanufacture of bricks. The director (Mr. Eastwood) pointedout that the seams in the brick pits are higher in the sequencethan the rocks traversed between Seldom Seen and the pit.The seams in the brick pits are now seldom worked in thecollieries, though some have been wrought in the early daysof mining. The coals of the brickworks are numbered frombelow upwards, but have not been named. Th e lowest,however, is probably the Preston Isle Yard Band, and thenext in succession the Upper Metal Band. A few lam ellibranchswere found in the dark shale roof of the latter seam and severalplants were obtained from the mudstones in the higher quarry.

TUESDAY, JULY 29TH.

Leader: E. E . L. DIXON.

The members drove to Mockerkin Tarn, where they wereshown a typical esker-delta with feeding- esker-the earliestdeposits hereabouts of the Lake District ice-cap aft er its separa­tion by waning from the Irish Sea ice-sheet lying to the west.The positions of th e ice-contact slope and feeding-esker are shownon the map (Pi. 8). t It was pointed out that th e plateau­like, kettle-holed top is terraced, th e upper flat being separatedfrom a broad ledge below by a marked step. The level of thestanding water evidently changed while the delta was beingdeposited in it. Further, the upper and lower parts are connected with different parts of the feeding-esker, which areslightly out of alignment, suggesting a lateral shift of the mouthof the subglacial stream contemporaneous with the change oflevel. The time-relations of the two levels are, however, un-

'Since this date (i.e. in Jan. 1925) an appa rent passage from the Magnesian Limestone up­wards into St . Bees Shales with thin limest one bands has been noted in this locality (B.S.)

t It should be noted that work , lat er t han the map, while confirming the view that the gra vel ­ma ss as far west as Ullock is a delta , renders doubtf ul th e nature of th ose (also lettered D1 0 11the map) beyond that point.

PROC. GEOL. Assoc., VOL. XXXVI., Part 1. 1925. 5

66 BY THE DIRECTORS.

certain. From the fact that the upper terrace had not beeneroded by the subglacial stream (unlike the terraced delta atHunter How, seen later) it was concluded at the time of thevisit that it was the more recent, i .e., that the water-level rose .Later work, however, and a fuller consideration of the factthat the lower part of the feeding-esker is the more easterly,and therefore, apparently, the more recent, suggest that thelevel fell.

The nature of the standing water, whether sea or ice-dammedlake, is unknown at present. It is believed to have been alake, but not related to, or contemporaneous with, glacier-lakeEnnerdale.

As a result of the discussion on the ground of another feature,the fact emerges that probably here, as elsewhere , more than onesubglacial stream has contributed detritus. Foulknott Hillis a gravel-knoll rising from the lower part of the northern slopeof the main delta, in line with a spur of the latter. (On the mapit is shown as a tongue, lettered DI, south of the word' Black.')It may have been cut off from the spur by erosion, but suchan origin is not suggested by its form . The Director had re­garded it tentatively as a deposit of a subglacial stream inde­pendent of that responsible for the main delta, and, on theoccasion of the excursion, Mr. Trotter, in the light of observationsin the Brampton district, made the sam e suggestion. Theprobability has been increased by later work. It has beenfound that a string of elongated mounds of gravel leads eastwardfrom the knoll, along the south side of Black Beck, and isapparently a discontinuous feeding-esker, quite distinct- fromthat south of Mockerkin Tarn.

Th e party then turned south to visit an esker (crest markedby a line of dots on the map) north of Todhole Beck. Theesker proj ects south-westward as a spur from an outwash-deltabetween this beck and Snary Beck. It therefore has th e positionof a distributary of the delta, and appears to have been depositedas the retreat of the Lake District ice-cap was slowing up forthe stand at the line of the ice-contact slope of the delta.

Passing Lamplugh Cross, Ii miles south-west of LamplughChurch, where a brief stay was made for lunch, the party nextexamined the gravel-mass north of Stockhow Hall, on thenorthern flank of the Ennerdale valley. This mass has beenfigured by Prof. A. H. Green and referred by him to a periodof marine submergence.* As it is evident from recent literature,not altogether non-controversial, that the hypothesis of a marinesubmergence is far from dead, it may be well to give someof the reasons why it fails to account for the features of thisparticular mass. The western margin trends N.-5., and hasthe linear character of an ice-contact slope. It is in line with

• • Physical Geology,' ed, 3, 1882, p. 633, lig. 224.

PROC. G EOL. Assoc., V OL. XXXVI. P LATE 9.

Geo/. SlIrv . P hoto.

A .-THE 600 F OOT STRAND-L INE AND SOME OF THE DELTAS OF GLACIER­L AKE E NNERDALE. Vi ew S. of Kirkland.

Geo/. SIIrv. Photo.

B .-LoOKING UP N ANNYCATCIl BECK V ALLEY.A d irect overflow fro m Gla cier-Lake E nnerd al e .

[T o lace p. 67.

EXCURSION TO THE WHITEHAVEN DISTRICT. 67

the similar margin of a belt of hummocky drift, extendingnorthward to the railway near Rowrah station, which appearsfrom its character and composition to be a recessional moraineof the Irish Sea ice-sheet. The Stockhow Hall gravels alsocontain, besides the ubiquitous Lake District slate-debris, muchWhitehaven Sandstone and other material from the west. Again,within the gravel-area there are two linear slopes, parallel to thewestern margin, which are not erosion-features, but appear tobe ice-contact slopes formed during halts in the westwardretreat of the ice, before the position along the western marginwas reached. One of these slopes is seen beyond the kettle-holein PI. gA. The southern part of the gravel-mass is a ridgerunning E.-W., its crest falling steadily eastward from the topof the supposed ice-contact slope at its western end. In linewith this ridge to both east and west are similar bold gravel­ridges and the series together constitute a discontinuous eskerextending with two gaps from Bankend on the east to Salter onthe west. * The southern part of the Stockhow Hall mass,therefore, is part of an esker at right angles, as would be expected,to the ice-contact slopes. Consequently we may conclude thatthe Stockhow Hall gravels have been deposited at a N.-S. ice­front that has retreated by stages westward. Doubtless theywere laid down in standing water, but as we shall see there isevidence that this was not the sea.

North-east of Stockhow Hall the party passed the dark bluffat S., PI. 9A, which marks the 60o-ft. strand-line of glacier­lake Ennerdale, and at Kirkland saw a network of channels (map)cut deep in Skiddaw Slates, with a delta where they debouch at600 ft. O.D. on the side of the Ennerdale valley (near' 600' in PI.gAl. The number and looping of these channels seem to requirefor explanation streams that have been limited in position by thepresence along their eastern side of anice-front varying somewhatin its stand. The delta has been thrown down in water fillingEnnerdale hereabouts to a height of 600 ft. Whether this waterwas sea or lake there is no means of telling from internal evidencebut the following facts learnt elsewhere show that it was anice-dammed lake. The water-level is the same as that of oneof the terraces of the delta next to be described; these terracescan be correlated with known movements of the Irish Sea ice­sheet whose front, as we have' just seen, lay at one timeimmediately to the west; and overflow-channels withinthe same range of heights have been found by Mr. Hollingworthdraining across the ridge of fells south of Ennerdale.

The terraced delta, north of Hunter How, was next visited.This was deposited by a powerful stream which has cut a deepchannel (beside I, Pit No. I" on the map) right across the Kelton

• The gravels at Stockhow Hall, Bankend and Salter are incorrectly shown on the map (PI. 8)as of the same age as those at the mouth of the Kirkland channels.

68 BY THE DIRECTORS.

Fell ridge of Skiddaw Slates from Leaps Beck to the side of theEnnerdale Valley. As the stream flowed uphill or almostcontoured the valley-side in different parts of its course, it musthave been subglacial and under considerable hydrostatic pres­sure. Its delta, which is kettle-holed, is terraced at the follow­ing levels, 700 + ft., 700 - ft. and 600 ft. The streams thatdeposited the lower terraces eroded the higher, whence it is evi­dent that the lower are the later and consequently that the'water-level was falling by stages.*

Tea at the Anglers Inn brought the excursion to a close.

WEDNESDAY, JULY 30.Leaders: T. EASTWOOD, C. EDMONDS and B. SMITH.

A char-a-banc was taken to Hensingham where the higherpart of the Lower Carboniferous and part of the Millstone GritSeries were examined. The first section visited was in SnebroGill-the type locality for the beds of that name. The floor ofthe higher part of the gill is a silicified limestone with spongespicules succeeded upwards by dark shales with thin lenticularlimestones often crowded with fossils. In the shaly crinoidallimestone near the water conduit Prof. Fearnsides detected afragment of a goniatite-the first to be found at this horizon.The top of the section in the gill, consisting of rough sandstonepassing into ganister, was examined, while the black shales withgoniatites associated with the Udale Coal seen at the head of the­little waterfall were searched for fossils.

The party then proceeded to Bedlam Gill and examined thelower part of the Snebro Gill Beds, consisting of dark sandy shaleswith thin sandstones and ironstones, close down to, but notactually in contact with, the Hensingham Grit. Several feetof this grit are exposed in the stream before the former is cutout by an east and west fault, throwing northward and bringingin the Udale Coal, which is here better exposed than in SnebroGill. Goniatite hunting again became the order of the day.

Overend Quarries were next visited, commencing in the largequarry nearest the village of Hensingham with its capping ofBoulder Clay and Hensingham Grit on the First Limestone. Thelength of the quarry is sufficient to demonstrate a slighttransgression of the base of the Hensingham Grit across the higherbeds of the limestone. Search was made for characteristic fossilsin the limestone, and casts of Lepidodendron were pointed outin the Hensingham Grit, but proved too large for collection.

A small quarry to the east, providing a section in part of theSecond Limestone and the shales and sandstones intervening

• For a fuller discussion of these deltas and their relations to a re-advance of the Irish Seac Into Ennerdale, where its drift still dams the lake, see E. E. L. Dixon • The Retreat of theLuke District Ice-Cap in the Ennsrdale Area,' Summary of Progress for Ig21, Mem. Geol, Suru••Iga2. App, I ••

EXCURSION TO THE WHITEHAVEN DISTRICT. 69

between it and the First Limestone, was then visited, anddiscussions on certain questions of nomenclature arose .Small irregular bodies of heematite occurring in this quarryfurnish the only iron ore seen at the surface in the HensinghamInlier.

The party then returned to the char-a-banc and journeyed toBigrigg, where the "Coal Fault" was crossed and the mainoutcrops of the Carboniferous Limestone Series and MillstoneGrit, overlain in part by New Red rocks, were reached.

After attention had been drawn by Dr. Smith to the lieof the rocks, and the chief faults, the leadership devolved, withsome exceptions, upon Mr. Edmonds.

The section exposed in the Bigrigg Railway cutting wasexamined in detail.

Thanks are due to Messrs. D. Gill and C. Davidson for per­mission to visit this and other sections seen later. The lowestbed seen is a brown micaceous fissile sandstone containingimpressions of Carboniferous Limestone brachiopods. Thisbed lies between the Hensingham Grit below and No. z Sandstone.above (in the Snebro Gill Beds).

This sandstone is poorly exposed, and two faults seen east ofthe bridge introduce complications in the succession.

West of the bridge the" Barren Shales " appear, dipping tothe N.W., and are separated by a thin sandstone from theBlack Shales of the Millstone Grit, which contain goniatites anda rich lamellibranchiate fauna. This fauna persists upwards intothe light coloured paper shale above, and then gives place to{?) Carbonicola in reddish coloured shales with small ironstonenodules.

A coarse felspathic grit, provisionally named NO.4, succeedsthe foregoing shales ; it is very like the first (No. I) or HensinghamGrit. Some poorly exposed reddish sandy shales complete the'Section seen in the cutting.

The First Limestone appearing in the northern portion ofthe Orepit Houses Opencast, which has been work ed for hserna­tite, was next visited, special attention being directed to the.abundant occurrence of barytes. Potholes in this limestone havebeen partially filled with a rubble of grit, material from the oreylimestone and glacial drift, capped by fine laminated clays.The Langhorn section, south of the Bigrigg Fault, shows theOrebank Sandstone, here over 60 ft. thick, overlain by I4 ft. ofthe Second Limestone, on which lies the "Little Shale" and" Whirlstone," which form the floor of the First Limestone quarrybeyond.

Barytes i s abundant in thin" strings," and fluor-spar occursrarely.

The fauna of the First Limestone is characterized by thecorals Lonsdaleia florijormis laticlavia S. Smith, Dibunophy lum

70 BY THE DIRECTORS.

muirheadi Thom., and the brachiopods Productus latissimusJ. Sow. and P. giganteus Mart.

The sand dykes in the Limestone are apparently composedof somewhat similar material to that of the Hensingham Grit,and are very finely exposed in this quarry.

In the railway cutting, about fifty yards to the west, thebrockram is seen overstepping limestone which has yieldedtypical First Limestone fossils. Pebbles of the LatterbarrowSandstone and of the lavas and andesites of the Borrowdale­Volcanic Series rival broken masses of Carboniferous Limestonefor ubiquity. An old quarry a few yards from Orebank Housewas next visited. Here brockram overlying Hensingham Gritis let down in a trough between two faults. A thin bed of shalelies on the grit and underlies the brockram. In the latter" gravel are" was seen occurring along or near the faults andabove the shale. It was noted that the lumps of "are" consistedof portions of brockram which had been converted-bothcalcareous matrix and included larger fragments of limestone­to a hsematite in which unaltered fragments of sandstone, etc.,are embedded. It therefore appears to be clear that the" gravelore" was formed in situ and post-dated the faulting.* Similaroccurrences of " gravel are" in brockram were examined aboutISO yards farther north. The overstep of the brockram fromHensingham Grit on to the First Limestone was then demonstrated.

Thereafter the uppermost beds of the Fourth Limestone,with the exception of the Chert Bed, which is here denuded, wereexamined in Clint's Middle Quarry.

In the Junceum Beds the bands of Lithostrotion [uncewm(Flem.), which give the bed its name, stand out prominentlyon the weathered surface: two or three bands can be tracedthe full length of the quarry face.

In the shale at the base of this limestone Saccammina CarteriBrady, occurs in great abundance, and is the index fossil ofthe limestone bed below, to which it gives its name.

In the main quarry next visited the Junceum Beds form thetopmost tier, Cyathophyllum regium Phill., Clisiophyllum d.keyserlingi McCoy, Aulophyllum jungites (Flem.) mut. cumbrienseS. Smith and Michelinia tenuisepta (Phill.) are particular andspecial representatives of an abundant coral fauna.

Next below, Saccammina Limestone, yielding abundantspecimens of the index fossil, rests on a thin sandstone with plantimpressions, below which is a silicious shale that infills cavitiesor "potholes" in the bed below.

The "potholes" at the top of the limestone bed of thatname are well displayed near the base of the working face ofthe quarry; they consist of quasi-cylindrical cavities in the

"For further details see B. Smith, 'Haematites of West Cumberland, Lancashire and th~

Lake District,' (Mem. Geol. Surv.), ed. 2, 1924, pp. 41-42.

EXCURSION TO THE WHITEHAVEN DISTRICT. 71

limestone, ranging in depth from 4 to 6 feet and with an averagediameter of from 18 ins. to 2 ft. (PI. 6).

The presence of plant impressions in the sandstone, andof a thin coal seam at this horizon elsewhere, is significant.

Below the "Potholes Limestone" occur beds lithologicallysimilar to the Spotted Limestones of other areas. These grad­ually pass downward into pseudo-breccias, which give their pecu­liar character to the" Rough Beds." At the base of the" RoughBeds" the Girvanella Band, which forms the usual line of demar­cation between DI and Dz, is present. Chonetes d. comoides, also,is fairly abundant here. Below are the White Beds with" erosionchannels." With the latter are associated contemporaneouslimestone-breccias and algal limestones.

THURSDAY, JULY 31ST.

Leader: S. E. HOLLINGWORTH.

On the way to Ennerdale, the party alighted from the char­a-banes near High Waterside farm to inspect an excavationin laminated clay laid down in glacier-lake Ennerdale bywater from the Irish Sea ice when the lake stood at 400 ft. O.D.

The Director gave a brief account of De Geer's method ofmeasuring the" varves" or seasonal layers of sediment, and itsuse in correlating the stages of ice retreat in different areas.

The char-a-bancs took the party to How Hall, whence thelakeside road was followed to Bowness Point. Here, after ack­nowledging the thoroughness of Dr. Rastall's work on the Enner­dale Granophyre, the Director pointed out the principal featuresof the glaciation of Ennerdale. The trough, 150 feet deepbetween Bowness Knott and Anglers Crag, the dam of Irish Seadrift at the foot of the lake which has been notched to thedepth of a few feet only by the outflow from Ennerdale water,and roche moutonnee surfaces of hardened slate on BownessPoint, indicating a north-westerly movement of the ice fromEnnerdale were noted. The corrie-scarred character of thenorth-facing slopes of the valley, and the resulting developmentof the asymmetric north to south section, emphasized elsewhereby Professor Marr, also received attention.

The great width of the belt of unfolded Skiddaw Slate, westof the Ennerdale Granophyre, the fact that much of it is un­altered, and even the innermost portions but slightly metamor­phosed, were held to indicate that the granophyre, clearly ofpre-folding age, had itself, as distinct from its hardening effect,protected the slate from the folding affecting the slate fartherwest. Attention was drawn to the sealing up of cleavage planeson Bowness Knott, and the suggestion was made that this wasthe effect of the intrusion of the granophyre on a cleavage whichwas earlier than the main folding.

72 BY THE DlRECTOI'~.

Before leaving Bowness Point a group of south-west trendingfelsitic dykes, here a few feet wide, and traceable up the slopesof Bowness Knott, were examined. These contain scatteredpink porphyritic felspar in stout prisms, often rounded, averaging3 mm. in length, with occasional specks of a dark green chloriticmineral in a felsitic ground. They are believed to be off-shootsfrom the granophyre.

At the foot of Bowness Knott a fallen block of hardenedslate traversed by an apatite-rich pegmatite vein , which wasitself cut by a 2 inch basic dyk e, was seen. Apatite crystals 1"long , extend characteristically transverse to the vein .

During the ascent of Bowness Knott over steep coarse screeof hardened slate, a group of small doleritic dykes and a greyflow-banded spherulitic acid dyke were examined.

Aft er lunch at the top, the contact of the granophyre with thehighly silicious slate was seen ; and the relations of th e grano­phyre to the large mass of basic rock, a coarse dolerite, studiedin a series of good exposures. These showed the basic rockto be completely enclosed in , and veined in all directions by thegranophyre, here often a pink felsitic type. Good specimens ofintermediate types of hybrid character , with hornblende needlesup to one inch in length, were obtained, indicating that theacid magma had incorporated much basic material prior toreaching its final position. It was agreed that the doleritic rockwas an earlier intrusion, probably belonging to the same period ofigneous activity as the granophyre. Before leaving the summitthe position of a large strip of similar dolerite, a mile long and250 feet thick, was pointed out on the crags south of the lake.

The moraine-covered ground east of Bowness Knott wascrossed on the way to the flow-banded spherulitic rhyolitedyke, which runs through normal pink granophyre diagonallyup the southern slopes of Great Borne. Many beautiful speci­mens were examined, showing coloured and concentricallyringed spherulites up to 1.5 em. diam., as single individuals,in strings along lines of flow. and as masses on intersurfaces of flow.

After tea at the Anglers' Hotel the party went by char-a-bancto near Cockhow on the Enncrdale Bridge-Calderbridge Road,where a series of overflow channels from glacier-lake Ennerdale,converging into a gorge 100 feet deep (PI. 9, B) east of FlatFell, was examined. They are transverse to the normaldrainage and are now mostly dry, and were admitted to be fineexamples of their kind.

FRIDAY, AUGUST 1ST.

Leader : B. SMITH.

The members left headquarters by motor at 9 a.m, for Bootle,via Calder Bridge, Gosforth and Muncaster. The famousviews of the valleys of Wastwater and Eskdale were obscured

EXCURSION TO THE WHITEHAVEN DISTRICT. 73

to some extent by mist and cloud, but the closer beauties ofMuncaster Fell, and the ancient harbour of Ravenglass, with itsranges of sand dunes, were admired.

On arrival at Bootle the party proceeded to Fellgreen,where the Director pointed out that a belt of Volcanic Rocks,little more than t of a mile in width, outcrop here between EskdaleGranite on the north and Skiddaw Slates on the south. Theslates appear to be faulted against the Volcanic Rocks, butboth the junctions and the whole of the volcanic strip are withinthe aureole of metamorphism of the granite.

Three parallel marginal channels cut by water flowing alongthe eastern margin of the Irish Sea Ice as it retreated westwardfrom the Fells are present here.* They have been cut in solidrock through an earlier-formed spread of gravel, probably laiddown as a marginal belt between the ice-front and the Fells.

Proceeding northward up the lowest or Bramire Channel,the junction of volcanic rocks with granite was crossed. Theparty then turned eastward and southward along the next higherchannel-s-Nettle Crags-after examining gravelly deposits nearthe heads of the channels. In some cases the rock-walledchannels are continued northward in drift for some distance. Across-cut between the Nettle Crags and Bramire channels andthe irregular descent and anastomosing nature of the lower partof the Nettle Crags channel were noted.

A section in Boulder Clay showing "interweaving" of drifts]was next examined, and the members proceeded to Cat Crags,from which vantage point a view of the southern end of theDamkirk Channel was obtained. The head of the channellies about t mile east of that of the Bramire Channel. Trendingsouthward for t mile the channel then turns south-westward.At Gibson's Spout the combined waters of Crookley and GrassgillBecks cascade into the Damkirk Channel, from a pre-glacialvalley, now being cleared of drift. At Cat Crags the streamleaves the channel by a late-glacial or post-glacial gorge. Thatpart of the channel now occupied by the beck is at a lower levelthan its continuation to the south.

Proceeding eastward the party crossed Damkirk Bottom andclimbed Damkirk Brow, from which the earlier-formed spreadof gravel was seen on Bootle Bank and Old Close. Two sharpridges of gravel lying south of the road (north and south Coppy­cow) were referred to deltaic deposits in a lake that was held up,before the channels were initiated, in the embayment formed bythe westward-protruding shoulder of Black Combe. Stillfarther east a fine series of moraines, running from north tosouth, and swinging south-westward, were inspected on Bootle

• For further details, see B. SMITH, 1912, The Glaciation of the Black Combe District, Qua,l.[our, Geot, Soc., vol. lxviii., pp. 402-48, pIs. xIi.-xliii.

t See G. W. L.<MPLUGH, 1903, "The Geology of the Isle of Man," M[1n. Geol . SUY"., p. 335.

74 BY THE DIRECTORS.

Fell. The party then turned northward across the Fell, takingadvantage of the comparatively dry terrace-like morainic ridges-accumulated as a series of steps between the retreating ice-frontand the hill-slope-to avoid the peaty flats as far as- possible.

Attention was directed to an accumulation of boulders resemb­ling a " steinwald," said to be a characteristic marginal-pheno­menon in Lapland, and due to water washing away finer materialfrom boulder drift.

The valley of the Kinmont Beck, a normal pre-glacial valleyfrom which the drift-filling is being removed, was then followedwestward to Low Kinmont, where lunch was taken.

Low Kinmont stands at the mouth of the more easterly oftwo nearly parallel marginal channels, cut through gravels into abroad shelf of granite, that extends northward to Eskdale.

Near Middle Kinmont granite exposed in the eastern wallof the Kinmont channel was examined, and found to be rottenand overlain by a granitic sand. It was suggested that thesoft state of the granite allowed of the easy cutting of the broadvalley at this point. The cap of gravel, here largely of granitesand with huge boulders, was seen behind Middle Kinmont,from which point the members crossed the plateau to CorneyHall, in the Corney Channel, which is occupied in this part ofits course by the post-glacial River Annas. From CorneyHall a dry glacial cross-cut to the third, or Near Bank,Channel was followed westward. Here the outer wall of thechannel must have been formed by the ice itself. Farthernorth the Near Bank" in-and-out" channel was entered. Ithas a low corrom-delta in its centre, thrown down by a smallstream descending from the eastern wall. An inclusion of vol­canic rock was discovered in the granite by Prof. Fearnsides.Proceeding eastwards once more the party dropped into theCorney Channel near Gillfoot, where the River Annas, leavingthe Kinmont Channel by an old glacial E.-W. cross-cut, enters.the Corney Channel and turns abruptly southwards. It wasobvious that the valley above this point, drained by a smallmiss-fit beck, was quite as deep, broad and impressive as thelower part which now holds the pirate River Annas.

A little farther north-east the Kinmont Channel was againentered and the course of the River Annas and its point of entryinto the channel pointed out.

Turning northwestward-with a sideways glimpse towardsWelcome Nook (at the head of the Welcome Nook-KinmontChannelj-i-the head of the Corney Channel was crossed. Thishas the appearance of having been partially filled by Boulder Clayduring a temporary readvance of the ice-sheet.

EXCURSION TO THE WHITEHAVEN DISTRICT. 75

The Director gave it as his opinion that the channels weremade by the overflow of waters impounded in a glacial lake heldup in Lower Eskdale, and that two channels he had observedcutting across Muncaster Fell were connected with this lake.

From Lane End the party rode to the Eskdale Granite Quarriesof the Eskmeals Granite Co., which were examined for a shorttime-by the courtesy of the Manager, Mr. J. J. Preston.

Tea was taken at the Pennington Arms, Ravenglass, andheadquarters were reached at 6-45 p.m.

DESCRIPTION OF PLATES.

Plate 6.-Contemporaneous Potholes in surface of .. Potholes Bed,"Fourth Limestone, Clint's Quarry, Bigrigg.

The bed here is overlain by about 2 feet of brown freestone and shale,and the .. pots" are filled with tough speckled sandstone.

Plate 9, A.-The 600 foot Strand-Line and some of the Deltas ofGlacier-Lake Ennerdale, south of Kirkland. (GeoI. Surv. Photo 2766).

Looking north-east from near Stockhow Hall. The pool is a kettle­hole lying in a notch of the delta of the Irish Sea ice-sheet of which thewestern margin (ice-contact slope) runs north from Stockhow Hall(PI. 8). The notch lies between a subordinate, somewhat earlierice-contact slope (the dark slope beyond the pool, extending from theleft edge of the view to the row of three trees) and the front (the foreground)of the deposits laid down at the time of the main ice-contact slope.

The mound beyond the three trees is also deltaic gravel, but of in­definite form.

The 600-ft. strand -line is marked by a hedge (below the letter S.)at the foot of a dark bluff. Below the letter C. to the right of this hedgeis the dark-shadowed mouth of the deep channels cut in the hillsideS.E. of Kirkland, and the light-coloured field topped by a hedge (belowthe figure 600) is the top of the 600-ft. delta formed by the stream thathas cut the channels.

The distant fells are Kelton Fell Top (above S.), Knockmurton andBlake Fell (between C. and 600).

Plate 9, B.-View looking north up the Nannycatch Beck Valley. Thishas been cut entirely in. Skiddaw Slate by glacial waters escaping fromglacier-lake Ennerdale, the 700 + ft., 700- ft. and 600+ ft. outlets,of which converge towards its head from the N.E., N., and N.W.respectively.