Field Notebook: Newfoundland, Nova Scotia 1910

Schuchert, Charles

1910

Yale Peabody Museum of Natural History

Original Source

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paleontology stratigraphy fossils Cambrian Ordovician

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126 Pages

doc. 0097 Newfoundland 1910

Alice Schuebart 3937 Argent Ave, Howard Q. 119 E. Dermtl, Cincinnati. Phil Schuebart 860-816 W. Fifth St. Cin. Q. Iron Hut as above n 105 Academy Ave, Price Hill. Margaret Corcoran 14 Dale St. New Haven, Conn. Mrs Oade 472 Orange St.

doc. 0097 Nova Scotia + Newfoundland [3100] Nova Scotia [3482] 1 lot of Pennsylvania only B5151 Charles Schuchart Yale University New Haven, Conn. U.S.A. June 25-1910. + [7956] Williams, M.Y. coll Nova Scotia June30-July1 1910

27th Meetn J Customs at Bay J Islands - One Eastern. Bimbe Bay,

F. G. Cox, Flowers Cove, St. Barts with me from Bonne Bay Agre & Sons Limited. Birchy Cove, Bay of Islands. Lee Lettus. With him last time June 25-1910 the morning and later than July 7- Reid Newfoundland Co., St. Johns. Capt. Jas. G. Farguhar Maritime Transportation & Salvage Co. Ltd. Halifax N.S. Steamer Starlaw, Bay of Islands to Halifax Bruce from North Sydney 3 times a week to Port aux Basques, N.F. H. Mrs. Eastham, Collector of Customs Bay of Islands. Advised me about boat. Requested me to Jas. Barry. The owner of the Vertena that we saw there. Edwin G. Grant, Blanc Sablon with me Feb 5-1910 to be confirm me some assistance. Capt. H. G. Wakeham Gaspe Basin, Quebec Inspector of Fisheries.

Arisaig. With Charlie from Portjornied to Arisaig July 10- 1960. Eighteen miles drive to Arisaig. Ami and Russell then at Johnny Joe McDonalds. Left in stage to Portjornied, July 21.

Instructions from Halcott, March 18-1910 "In find in the collections of the Canadian Survey, some specimens of the heads of Olenellus-like trilobites from L'Anse au Loup, on the Straits of Belle Isle. They are in a limestone matrix and represent two species. The matrix is a rather hard gray limestone, which is not the limestone carrying the "carcs." Professor Hyatt collected a lot of the latter, but did not get any trilobites. "There is a very good deal from Anne Bay." Loran Cambrie begins on the west of Madore Bay and extends NE to Pointe Belle Isle. See Blanc Sutton section. All the beds at Fortune Bay appear to be phosphorous. Loran Cambrie probably 1100' thick is found near entrance to Long Arm of Canada Bay. Murray says the entire "Potsdam" is 12600' thick. Bedlamtown - Chaggy 4000' li (Jane Bay). From Cape Rosman for 100 miles to Hawkes Bay" Point Rich Limestone. St. John's Island. Maybe seen from Anchor Point to Hawkes Bay. Tale Point, Daniels Harbour, Portland Creek Steering Island and Cow Head. Bonne Bay.

Adnicie type localites. St. Barbe Bay. Port au Choix Point Riel Table Head Cow Head Bonne Bay. Important obs in L. Cambrie, East Line of Bonne Bay from Quebec North Bay to 6- 7 miles up.

3482 start 3100

Wednesday June 29-1910. Arondale, Hora Sertis. While waiting for a train at New Glasgow walked East of the town about 1/2 mile and in small stream we saw an outcrop of grey bidded coarse sandstone, above it dull shale. In the stream bed there is much black shale with an abundance of Spirorhis, Ostracoda and fish scales. There is also much evidence of plant re- main but little that is recognisable. Scoura by Stigmaria are small fern leaves and the leaf of Cordaites? Have taken some of these fossils. Did not see a trace of a strictly marine animal. The evidence is all in favor for continental deposits. Left New Glasgow at 12.40 and met Williams at Onegmick and together we then proceeded to Arondale to see the Siluria. At 2 P.M. we started East along the International Railway but seeing nothing more than drift shatter of are descended into the valley Barnes River and on the opposite side above of Fletchers Cliff (=150°) localities are saw a good exposure of the lower part of the Arisaig series. We found one Amphiothena Demispherica and fragment of which appeared to be either Stroph. Odonta or Orthothela. The horizon evidently is the Arisaig formation and apparently in the lower part of the upper Green Slate. Farther off on stream Towhful saw other outcrops of the Arisaig but he saw no fossils.

Thursday June 30-1910 Grondale, Nova Scotia. Started at six a dark threatening morning and by nine a slight rain set in. Rained up to 1 P.M. A few hundred feet east of Barnes River station on the I.C.R.R. can be seen an outcrop of the Medina agnacans limestone and in the stream red sandy shales. The former is schistose with the joints vertical. The shales dip at a high angle. Farther east and to the south of the railroad along a county road may be seen a far better exposure of the Medina in close association with the complementary red (arkose) "Cambro-Siluric". Here are collected Conularia, Struthiasma bilatusis (comm.), Meristina (large and very thick Shelled), Platyceras and a Pleurotomaria. Also Cornulites flexuosus. Contact with the lower rocks was not seen although we looked all around for it. In the afternoon went to Marshy Hope and in less than one-half mile east of the station to the north of the track again saw the "Medina". Here may also be seen two beds of white quartzite, one high up on hill in the woods, the other at the edge of the hill near the road across the railway. The only fossils seen were crinoid ellumens. So far all the Siluric we have seen along the I.C.R.R. is in the Lesicaig formation and the "Medina" more of which is older than Clinton.

Brick wall Silurian slates Junction of Rangipo Road and an old tram road. It is probable that the lower beds of the Siluric are on here. Siluric. Apparently Org platt. The section continues off partly undetermined. The hills a Ordovician formation may yet be present. Brick wall Silurian slates The Marlows a Brunian high-way. Shelf faults. 2 30 1 Rangipo River Ariroy McAlaways Old Bridges Dun. old removed. Baileys Creek Hue This fault trend off of the Siluric to this old boundary due to a fault Rangipo Stream Diorite

"Friday July 1st 1910 Crisaig. Left Orndale at 7.30 A.M. with Mr. Patterson's wagon for Baileys Brook to see the Lileric there. It rained a good deal during the night and all is wet this morning. The Lileric here makes a very hummocky and high hill terminated on the north by Vameys Brook. On the southern side of the line at about the centre of its length we saw the brick red sandy shales said to be of Devonian age. They stood nearly on edge with a slight dip to the south east. To the north of this outcrop for nearly a half mile we saw considerable loose material of the Lileric often split into forms. These blocks while loose are not far removed out of place and represent the main Paleozoic horizon of the Crisaig section. Higher up in the series Chonetes novacostatus had a breadth of nearly an inch, and still higher we saw the crassely plicat large spirifens. Nothing of the distant Lileric red hill were seen here. Going across the Lileric ridge to the north and down to Vameys Brook leaves across the Lileric limestone in place and here the dip was again nearly vertical but distinctly slanting to the North. The place is a little more south than the F on Vameys Brook of Fletcher's map. There must be many hundred feet of Lileric still above the outcrop before coming to the Devonian. At the junction of Vameys Brook limestone road and the main Baileys Brook - Cardrona road Devonian again crops out, nearly vertical until the dip slightly to the north."

Red Shale ? Old soil And waste pieces of the this mixed in. "Exposed from foraged prog" Period and "Carbonifera" Continental deposits. Sea level.

Saturday July 2-1910 Arisaig. The "Red Slatonic" at the top of the Moydart formation. Below are thin bedded sandy limestones of a greenish color for about one foot in total thickness that towards the top introduce very thin bands of the red shale. There are marine prints here chiefly ostraco- coda. Then about 4 inches of stratified red shales with thin papery limestones some of which have ostracoda. Then the heavy bedded indistinctly stratified red or maroon unprinciples sandy shales that is vertically cleaved. In the lower and upper portions there are many living small emersions arranged along the bedding planes. At the top the red beds are sharply differentiated from the higher green arenaceous shales that have an occasional very thin cross bedded sandstone or an arenaceous limestone with poor red indistinct pedestals. I cannot see no pieces of the red shale embedded in these greenish shales. While the contact between them is sharp there appears the due no overlap. The upper shale part of the Stonehouse formation has but few prints and upon unconformably rests the decidedly amygdala- doloidal trap. On the other side of the trap is the red sandy shale and conglomerate said to be Carboniferous. It is a very decided continental deposit with zones of once or more angular fragments of the Siluric shales at London hits intruded with brick red shales and thinner zones of conglomerate with smaller pebbles. The "Carboniferous" has zones of a finely crystalline intrusive. In the afternoon examined the geology to the east of

Why is not this red shale a sediment deposited in the bottoms of the Asphalte floor and upon which later Asphalte flowed? If this Basalt turns out to be like that of the Cauc, it is not pre-Lilunic in age. If it is Cauc, maye the question arise if it faulted against the Asphalte? In this event the Lilunic lies in a "graten".

"Arisaig light-house, here one sees considerable of a Phyllite exhibiting plainly flow structure that craters and. Associated is material that looks like brick-red shales but which Williams thinks is the same phyllite metamorphosed and squeezed until it breaks up in the crater into a shale. To the south occurs a thin zone of rather laid breccia. At the light house outside of the phyllite or to the north occurs a dark basalt. Between them occurs considerable thickness of tuff usually of a brick red color in parts of which are embedded fragments of a distinctly crystalline igneous rock. To me are these igneous rocks one of extrusive origin previous to the Siluric. They were formed out over the Cambro-Siluric land. Upon the hemmrod surface of these rocks was deposited the Siluric Sedimentaries beginning with the "Medina". We saw these in full force at Beechy Hill Cove followed by the fissile dark, almost black, loose slates of the Arisaig Formation. It was here that Trenchard collected his Medina fossils. The ones I got nine years ago was at Arisaig Point. The fossils came from very hard fine grained calcareous sandstone while Trenchard's were rather fine chalky ajillaceous limestones. Does this mean that the "Medina" at Arisaig Bay may have been tailed by the igneous masses? This once I believe that the fossils at Darlington are from the hard quartzite banks. Therefore not necessarily any taking.

Hpret. 2300 Devonic. Greeklime. Carboniferae conglomerate Carb. Basalt.

Sunday June 3-1910 Arisaig. Remained in the house during the morning finishing the Antiesti joba with Troughel. In the afternoon walked out 2½ miles to Mrs. Ares Brook to see the so-called Deronian of red shales and agylacens sandstones (Arie say they are tuff, stratal and volcanic ashes). Near the Shore Road side Williams found 3 fragments of fish remains. These deposits are evenly laid but at various levels occur brick red shales full of small more or less living nodules. These look more like continental deposits than the rest. Going down the brook to near the shore one comes upon a great mass of the dark basalt underlaid by the Carboniferous and conglomerate of continental origin. Both of these tub of against the Deronian in such a way that their great position must be due to a fault. the basalt at the top of the Stonehouse Lillenic cuts it off here as at the Deronic of Mrs. Ares Brook. There must be a fault here for in no other way can be explained the position of these Carboniferous basalts against the Lillenic. These basalts are clearly sheet flows for they are full of flow dikes near the base. There are at least two of these flows interwoven with the Carboniferous conglomerate of continental origin. Also basalt of the same character that bits up again the phylite at the base of the Lillenic section at Arisaig join.

Wednesday July 6, Newfoundland, Port au Basques is on mica schist. In the distance we see Table Mt, 1700', perfectly flat on top. The remnant of an old peneplain. It is a small remnant. Elsewhere there is no general level, known style lies on the sides. It looks like a plane against which the sea once worked leaving it now as a cliff, Table Mt. Apparently much of the country to the east of the railway is of this high peneplain country. One still sees the plain and the cliffs to the south of Codroy. To the north the Carib dy rises to a peneplained land but it is more dissected. The Anguilla Bays to the north of the railway are level topped and go to 1832-1762 feet. In the stream bed of the Great Codroy river we see the Carib, sandstones dipping a general N.E. W., striking at a low clip to the south. Further northeast near Mor- nis the valley is flat and filled with morainic material. It's an old wide valley. We are in the forest all the way to Gables and now a morainic country. Around Robinson there are extensive peat plains, Around Fishcels we see the Carib, shales and sand- stones. All dip about 45° Crossing Fischele from one sees what looks like a cliff 1 S.E. to N.W. Good Carr.

"reverses around here, then again out on peat plains. St. Georges is a considerable sized fishing village. Considerable "E" - "Ordovician" is exposed along the railway line reaching Birchy Cove. These we must see later. Along the eastern side of Georges Lake near its northern end one sees much red strata apparently standing on end. It appears to be Ordovician as the Cambrian mounds farther to the east. Around Birchy Cove on both sides of the Hummocks, the topography is rugged but none of the hills go over a certain general level. This ancient peneplain known is not so plain here as in southeastern Newfoundland. That this is the old "Cretaceous" peneplain accentuated is probable maybe seen from the fact that the higher hills attain to a level probably nearly 700 feet above the sea inspective of the hardness of their strata. Thus during a hard heavy red bed quartzite are no higher than others having red softing slates. The maroon softing slates are somewhat metamor- phosed and considerably squeezed but complete slate schistosity is not developed. Saw no fossils other than very faint traces of probable forerits. The heavy bedded quartz - conglomerate beneath is all torn apart and jointed with all the spaces filled by secondary vein quartz. In the slates one sees only little of the vein quartz.

The cleavage at the slate outcrop east of the town is N. 60 E. dip 34° N. A little further east the dip in 32° N. strikes N. 70 E. Still farther east strike N 35 E, dip 36 N. East of the saw mill the strike is N. 30 E, dip 58° N. The slates have polished surfaces and often the joints crumpling due to pressure. As yet one have seen no fossils in the strata of the Humber Arms. August 25-1910. Saw the limestone conglomerate in the hill east To the south west of Buckley Cross about 3 miles. For further remarks see the notes of this date.

Friday July 8 Rinchy Cote. As we could but sail Forenkfel and I spent the afternoon walking along the Reid Manor gauge railway to the east of Rinchy Cote. One mile east one comes upon a group of maroon roofing slate that may be several hundred feet thick. It is undulating by & quartzite and overlain by more quartzite - conglomerate. Further down into the Hunter river one meets with great masses of slate greenish to black. Then groups of sandstone occur along with arenaceous dolomite. In the Hunter valley we saw a pinnacle dolomite. All of these strata have been subjected to great pressure and all are metamorphosed more or less than the slates of the Hudson Valley. Cleavage is well developed and as a rule conforms with the bedding though in places the cleavage lines pass through the groups of lentic shales. In all of the harder beds one sees quartz veins of all signs and running in all directions. In the shales one sees little of these veins and as a rule only where the sandy beds are present. Just as one enters into the gorge of the Hunter river comes upon its very thick ancient delta. The top of which above the railroad is fully 100 feet high. In other words the Hunter arm in case probability runs 100 feet deeper than it is now. The sand and rounded boulders of the delta lie at a steep angle dipping into the Hunter Arm.

Saturday July 9. Birdy Cove etc. As one pans Coors of [illegible] one again sees an elevated delta deposit, It is about 70 feet above the present level of the Humber Bay. In fact at every gully mouth one sees these elevated flats. To me it is evident that the oceanic level has recently been depressed from 75 to 100 feet and the rivers have since cut through their deltas to the present oceanic level. Otherwise one sees no raised beaches nor incised sea cliffs within the Bay of Islands. As the wind was almost dead on coming down Humber Arm my tacks had little made and as there would be no advantage in going out into [the] Gulf because the wind would die down during the night Kennedy concluded to anchor for the night inside of Birdy Island in front of Humber Arm. We went ashore at Birdy Island at 3.30 P.M. and walked all along the eastern and northern side to the northwestern point that ends in three manner islands. The strata of Birdy Island are well exposed all along the shore and consist in the main of greenish grey and almost black shales that only occasionally have thin bands of sandstone or argillaceous limestone. In addition there is a thin zone of quartzite and a much thicker one of conglomerate almost made of of small (quartz) well rounded pebbles and much mica. The former is in thinner beds but the latter is very loosely bedded. In addition there is a brick red slate mud like the one seen east of Birdy Cove. These slats are closely associated with.

"the quartzite and conglomerate as at Birdy Cove and in all probability are the same beds. The question to be asked are they on the same beds?" All of the strata of Birdy Island except the quartzite and conglomerate are extremely crumpled and mashed into one another and some of the thin sandstones are so broken up and the pieces separated from one another as to make it impossible to trace their fold. The shales were much squeezed and locally overthrust into one another. Then a decided cleavage is developed. What ever fossils are present are now not in sight due to the mashing and cleavage. If there were an abundance of them limestone tends on chances for fossils would be better. Nor has a single fossil been found in Birdy Island. The leary hidden conglomerate has a dip of 30°S, and a strike N.70°W. The quartzite has a strike of N.20 W. and a dip of 40° E. The dip may rise to 60° W. The cleaved shales standing vertical and parallel to the bedding planes had a strike of N.70 E. and a dip of 80°W. The direction of pressure to produce the cleavage came from N.20 W. The folds are more or less closed but not completely or as we see at least two folds on the northern main land opposite Birdy Island. On the tip of Birdy Island along the road crossing the island we saw a large erratic of red granite. Blomidon Mt (2120') to the east of the Ordovician is em-

"sensibly higher and flatter, it is without the forest crown of lower lands than the adjacent lower very rugged hills of the green mountains. On the Olmidan range we saw the good Cirque and many small patches of ice, dominating hanging glaciers. We saw some of these rocks, but slowly may guess it as diorite, serpentine etc. It has copper. A good deal of broody island has recently been under the sea as at certain places we saw head material above the Ordovician slate cliffs."

Monday July 11 At sea. As one gets out of the Hunter and past the North Arm of the Bay of Solimio are on a rough topography, nowhere are there wide or long beaches, all are small with steep cliffs back of them. The rocks ore are all green and the mountains rise to at least 400 feet, here and then they are pieces of an ancient trail at elevations of about 25 feet, the same that are seen in the upper end of the Hunter in front of all the streams. These pieces of the ancient trail are made up of the residual material that has come down from the adjacent high lands. The land all ends in sea cliffs like this: A flat peninsula at the sky line does not exist, while the green masses hold fairly true to a fairly uniform level still the sky line is very irregular. The land is indentified by pinks and open on the left side leading landward into narrow canyons. 30' sea cliff 2100 400 over 700 over marked sea cliff at about 400 Entrance area cliff 75' sea cliff Have 3 photos of this place To run over the place is known as Thoral Point. This refers to the lower elevated track = Beverly Head These beaches show more all along in front of Beverly Head north to Chimney Cove. At the next head south, Cape Surjoy, one does

All joints between // // sent to Balcott Sep. 1910. north-east of Plane Station From the top of the hill & looking across the straits of Belle Isle we see Newfoundland. The sky line is practically a flat line. From N.E. to S.W. it looks like this: N.E. (Butter are seen on the land side and some 700' high.) 2 sea level Pirate the Doctor's Villa house at St. Joseph's Bay Land smilling over to Ferrolle ferry mean 500' high S.W. The top of the 1st terrace is at the top of the basal 18 foot cliff. The width of it is about 40-50 feet. The 2nd terrace is 28'6" above the first terrace. Its width is about 40-50 feet.

and are the beaches hardly seen. They are carried away by the sea. By the time one gets opposite to Torrs River South of Bonnie Bay one were 6 to 7 miles off the land and could not see its detail. [Saw it on the return trip]. July 13-1910 Blancation, Labrador. We started in to study the here north part of JST Bros Fishery Establishment in charge of Mr Edwin B. Grant. A red granite a grains sticks out all around the fishery village for there is the rock along the shore is seen then bedded red to pink almost whole decidedly gran bedded androsic conglomerate. The contact with the granite can not be seen here but there can not be more than 5 to 70 feet to granite seen in the sea reef just beyond. The lowest beds are many on the somewhat irregular granite surface. The general dip of the granite surface in towards the south to the extent of about 30 feet in 3/4 mile. At the fishery establishment the granite is about 20 feet above the sea while 3/4 mile south it is thought will be one 10 feet beneath the surface of the sea. The androsic conglomerate consists of white quartz pebbles well rounded of 1 to pellets of one inch but mainly 1/4 to 3/8 inch and a red feldspar less rounded and of about equal size There are some minute platy mica that in local dipping or rather mixed of 4 inches and somewhat as the quartz. Thickness about 18 feet above water, down 5 to 70 feet below water to granite are the added). Then 13'6" ft / similar conglomerates. Again similar conglomerates seen for 15 feet that are somewhat

marks the top of the 3 terrace. Terrace rock covered sloping seaward and from 100 to 150 feet wide to next terrace. Base of 5th terrace at the top of these 23 feet. This the best marked terraces going below, it has a width of about 250 to 300 feet. The sixth terrace begins at the top of the Andraezathine reef and is estimated here to have a width of 1000 feet. In this 1000 feet the strata are concealed and are estimated to a thick- ess of 450 feet. The terrace is backed by a 13 foot cliff. The cliff having the Andraezathine at other places, is made up of two cliffs separated by a terrace about 20 feet wide. This terrace comes down at the top of the heavily bedded conglomerate.

leaving bedded and tending the less red, more pinkish but as as cross bedded as those below. The next 19 1/2 feet are the same as those just below, at 60 feet above base "Berlithus with scattered to bedding come in the next feet, The red and pinkish calcareous conglomerate between the 3d and 4 terraces has a thickness of 25 feet. Its heavy bedded, cross bedded and thin in for less of felspars here than below. The grains are also smaller. I came character of conglomerate for 25 feet to top of next terrace. At about 130' above base as a rule Over the top Berlithus are common. And on the Tododome I, lireous Here the tubs are about 4 inches long and 3/8 inch wide at top. The slope of the 5th terrace is about 17 feet to the steep rise of the first peal cliff. It then continues for 67'6" to the top of the peak cliff to the last erasure gained and locally conglomeratic pinkish, heavy bedded sandstone. The upper 2 feet has rounded pebbles of Trachyte calcite up to 6 inches long and more depressed. Then 7'6" of then bedded pinkish felsin gained sandstone. This gives us here 219 feet of conglomerate up to the Archaeocystatherina reef. Logan has 231 feet. The Archaeocystatherina reef has a greater visible thickness of 12' 4" and a thinwork of 11 feet. It is a true coral like reef with sandstone intervals of limestone and four caves or even shaly. Then there is 12' 10" of other irregular beds that join place to place fairly on the reef character. This is to the top of the creek in edge of hill at this place. We have them for all we see 25 feet of this coral reef here. At the bottom the reef is wavy. At about one hundred feet above base Above the Archaeocystatherina reef in the 6th terrace and thus slope cross about 100 feet of sterile the character of which is not seen.

Above the 73' foot cliff comes the 7th terrace. It is 23'-foot wide and covers 6 feet of strata. Back of this terrace is a cliff 23' feet high. Above is the 8th terrace with no cliff back of it. This terrace has a slope of 300 feet in width and covers about 20 feet of strata. The 8th terrace has many green cratics. It is 321 feet above the sea. Its slope covers about 20 feet of strata giving the highest altitude at Ozone Lakin as 346. "Sediments here have occur at various levels up to the Archaeogathinae. At one place I saw some that were at least 8 inches long and about 1/4 inch throughout. These looked once like the Potsdam A. linearis. He made the limestone series 132 feet thick. Lyman gives it as 173 feet. The seaward side of the headlands show less of the terraces only the major ones stand out clearly. This may be due to the once active wave action here originally or due to the present sea erosion. "If the prevailing dip is "60 feet to the mile" and the width of the Cambrian here is 10 miles we should have a thickness of 600 feet which is much more than his measured section."

"[Illegible] a cliff 13 [illegible] high in which are seen a few thin bedded and laminated li. Tunbridge saw no fossils here. "The 7th terrace consists of feet of beds. Then follows a cliff 23 feet high that has local exposures of Tunbridge sandstone and sandy li. The 8th terrace consists [illegible] 15 feet of strata. No fossils seen here. The dip and strike of the basal strata near the sea level has a strike of N. 10 E and a dip of 8 E, In the strata just below this terrace the strike is N. 20 E, dip 8 E. "We walked north-west across the hills to L'Ance St. Claire and from the southern side we see that the strata along the northern side of the bay undulate like this: [Diagram] White conglomerate Red conglomerates L'Ance St. Claire N.W. The undulations in the strata appear not only towards the Straits of Belle Isle but also directly the other way, i.e. to the N.E. The latter are more decided than the former and both undulations can be made out at L'Ance St. Claire Bay, "The prevailing dip [illegible] towards the Straits of Belle Isle. Logan gives it at 65 feet to the mile. "The feldspar is particularly abundant in the lower red and arkosic conglomerates. In the higher conglomerates the feldspars are practically absent. "From this we draw the conclusion that the old shore line was not far away and that the Cambrian sea broke down the Red granite and the lighter [illegible] gneiss as the material for the basal strata,

"Higher a later decomposition was more perfect as the feldspars are practically absent and the shore was somewhat further away. When the Creceryathinae appeared the shore was not very far away for in these beds there are grains with considerable sand. In the help of however the material is mainly a limestone but locally seems to be somewhat magnesian. "The size of grain of the conglomerate and sandstone is about the same throughout. Cross bedding occurs at all levels. The marked difference however is that the basal beds have much red feld- spar and dark mica (fertilite). For this reason these lower beds are red in the cliffs. Higher up the feldspar is absent or practically so and therefore the heavily bedded conglomerate just beneath the Creceryathinae are light pink to whitish. In those upper sandstones the conglomerate grains are more local, the pebbles are fairly well rounded and average a 1/4 inch in diameter. "In the river valley back of Blanc D'Avon are exposed masses of granite on both sides of the river. The altitude above the sea is the same as the mass upon which the JST Bros Establishment is built. I judge these are about 30 feet above sea level. The masses higher up the streams are the base upon which the Cambrian was laid but all of the latter has been eroded off here. A little distance beyond the Cambrian is exposed and it is the auric red conglomerate with an abundance of feld- spar,

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"Thursday July 14-1910. Blane Lahn. "Spent the morning collecting some Archaegathinae from the hill northwest of Blane Lahn. "In the afternoon walked across country following the telegraph line to Bradne Bay. At the southeastern end of the bay much of the basal conglomerate is exposed along the beach but none was seen in contact with the granite. These basal conglomerates are often very coarse grained, the quartz pebbles often 1/4 and some up to 1 inch across. Some are well rounded but most of them are subangular, i.e. the edges are rounded. Much feldspar is present and often pieces of to 3/8 inch across. "These basal conglomerates are not only considerably cross bedded but have decided dips in several directions in a short space. Evidently it is the material first deposited filling in the holes between the granite hummocks. It is probable that the granite had a level top with depressions eroded somewhere into which the autroic material was first unloaded. "Saw Scolithus in some of the basal beds and crushed grains and crushed grains and crushed grains further back in the bay. Instead are in eroded out for 1000 feet and now filled with hard sand. "Further north (1 1/2 miles) is a northeasterly trending range of ancient mountains. These still stand at least 500 feet higher than the highest Cambic and it was this land against which the Cambic sea marked. "Some of the hills around Bradne rise to the Archaegathinae zone.

"Friday July 15-1910 Forteau, Labrador. A very light wind and a warm morning at Blanc Sallon. The flies and mosquitoes will be bad and we have from 12 to 15 miles ahead of us to Fortean. As we leave Mr. [illegible] house we see one boat starting to meet us at Forteau but it is probable that one will be there before the boat. We had an easy time across the bay north east of Blanc Sallon to L'Ense St Clair but the difficulty began after we left the latter place. At first we followed the same path but finding this too rough on the lead rocks we concluded to follow the telegraph line and path. This at times was also very rough but we finally got to Forteau at 3.30 P.M. As we proceeded towards Fortean the cloud cover of haze dissipated constantly to a low level and finally just before we began to turn into Fortean Bay it came to within 30 feet of the sea. In the back part of the bay to the south of the village it may be 250 feet above the sea. The very heavy bedded sandstone below the 7'6" of thin-bedded sandstone all the way from L'Ense St. Clair to back of Fortean Bay is white coarse grained sandstone almost a pure quartz. There is no feldspar present and the clay is argillite instead of shale. In other words the farther one gets away from the old shore the thinner is this sandstone eroded and the feldspar is absent. These argillite sand- stones are finally 20 to 30 feet thick. Below the argillite sandstone the other beds are the same as

at Blanc D'arm, i.e. red sandstones, craze and more often crampy. Ostlithus fring is seen at almost all levels. In the back part of Fortean Bay (probably 1/2 mile from the back shore) the red granite again appears at the surface. He estimate it to be 3 1/2 miles in a straight line from here to where we saw the coral reef within 30 feet of the sea. If we accept Zopans dip of 60 feet to the mile then where the granite comes to the surface in Fortean Bay the coral reef should be above the sea 25-7 feet which is probably so feet higher than the actual occurrence. A dip of 50 feet to the mile seems to be more correct. Further back in the bay to the north of the village the dip is certainly greater but it is possible that this is due to local flexure rather than a continued steepening of the dip to the north. The Archaeogatherine reef maintains its reef character seen at Blanc D'arm all the way to Fortean. It has the true coral reef structure only that the hemmolds are not so pronounced as in later Coral reefs. Between the lumps there may be a little calcareous shale and at various levels the sediment may again assume the regular stratified or bedded character. One can get better specimens of the layer form here than at Blanc D'arm. Then too one sees more often Putorisina criculate, among the corals. During the storms we had at Fortean before supper we star

on the hill side to the west of the village. He had a most awful Time among the sprawling arctic conifers, the mosquitoes and the Haemflex. He however learned that in the strata above the reef occur the trilobites and thicket brachiopods. Glenelles payments are common. Tomorrow we will make an effort to gather a lot of this material. Mr. Shaw directed us to Cape Jam, Mercer at Fort Jean who would direct us to some one to put us up at night. He had not the place to do this as he is in here only during the summer. However he took us to a Mrs. Flynn a very old lady who at times sports of the boarding preacher. On p. 287 of the Geol. of Canada Logan speaks of the Cambrian as being "divided into five or six tabular masses, separated from one another by narrow denuded portions of the grains, which in cvery case terminates in a deep bay" The separation into tabular masses is probably due to ancient rivers that flowed from Laurentia into the trunk streams now the Straits of Belle Isle. These valleys at Blanc Jardin and Forteau are wide (from 2 to 3 and mostly more than 5 miles) but the beaches are on the sides of the hills, while in the bottom of the valley there is often a few hundred feet sand that has accumulated in small dunes. When the sea was at the level of the upper beaches many of these tabular masses were islands. Forteau has the widest valley of these seen. L'Anse St. Claire the smallest. According to Woodley's map there appear to be ten of these tabular masses. Today we saw a large piece of conglomerate with quartz pebbles and of which offer an 1 or even 1 1/2 miles across. Logan speaks of some of its 3 inches. These are now more still rounded.

"Saturday July 16-1910 Forteau, Labrador. Long before we got up the wind howls and at 7 a rain sets in. Our hopes for the day are largely blasted. "At 9.30 we start for the high hill about one mile north and over of Forteau. The wind howl again here and it was cold and damp. Outside of Archaeogathiniae little was to be had. We got several good Archaeogathus profundus and many free finjn shaped corals. Also Rutrynia cingulata, Paterina labradorica, We tried to read other localities and after seeing two other outcrops gave it up trying to force our way through the dense canifer bush. "At 2.30 we returned to the village and up the other path back of Mrs Flinn's house where we had seen the Olenellus before. Here we got pieces of Olenellus thompsoni?, Ptychurus senectus, Ptychoparia mizon, Rutrynia cingulata, Whidien bella and possibly other species. This outcrop comes out of an artistic grey-blue limestone. These layers are above the Archaeogathiniae reef (a few A. profundus occur here also). Finally, "The top of the Archaeogathiniae reef seen this morning maybe 20 feet above the white heavy bedded sandstone so could account for are elsewhere below the lower part of the reef. The fact that the layers from which we got our fossil this morning are about 20 feet above the reef seen at Glene Durham may explain the large size of the Archaeogathus and the presence of the brachiopods. "The Olenellus layers are about 15 feet higher or 65 feet above the white sandstone.

"The modular coral heads stand above the stratified layers and is in these depressions that the trackilports and Galleries occur. Some of the ends broke from the reef and rolled into the depression. The modular coral heads are a[?] the a red fine grained impure limestone while the intermediati bedded limestone are grey, granular and sometimes tend to be locally dolomitic. The appearance is that of a true coral reef."

Monday July 18-1910 Forteau, Labrador. The all day rain of yesterday left the ground very wet this morning. Then for the day is dark mist no wind and some wet fog. We collected all day in the limestones around the route and station point out of Forteau Bay. Above the heavy bedded white sandstone there is about 5 to 6 feet of red sandstone followed by at least 30 feet of the coral reefs. The entire mass has coral reefs between which are either thin bedded crystalline limestones tending to be magnesian and of a grey color, or they may be nodular or even somewhat chalky. It is in these stratified intermediate beds that we get the bachi-forts and Dalterella. Very rarely one sees a piece of Olenellus. Above the coral reefs occurs a granular platy crystalline bedded limestone in which occurs very rarely a crural, Hyolithes americanus, Partymus sanctius The Olenellus beds back of Mrs Flynn's house is above all the strata seen today. Associated with the Dalterella, which by the way are at times our attendant, we see an occasional Stenothea a narrow very elongate form. At about the middle of the coral reef today (20 ft 30 feet above base) we get many Obolella chromatica (looks much like Q. Crassa), Partyma cingulata (central valve very thick shelled), and another form within the dorsal valve of the latter, or an Orbitus and the operculum of Hyolithes n Dalterella. Higher (about 15 feet) occur the Paterina Labradorica

and Orbitella with fibrous shells. Pentagria origulata appears to occur at about the middle of the reef and then upwards at nearly all levels. Archaeocathus gets larger in the upper part of the reef but is practically absent at 30 feet above the base. The cylindrical stemmed forms are also better developed and larger in the upper part of the reef. It is now evident that we are not going to get a huge fauna and nothing in the way of interesting trilobites. If so we have had too small imperfect leads of Orbenelles. (The next day we got about six more but no good large leads.) One is struck with the thick and calcareous nature of the shells of most brachiopods here in the Lower Cambrian. It is only the small Paterina labadoica and the much larger Paterina that have phosphatic shells. The phosphatic adaptation seems to be a latter phase than the calcareous secretion.

"Tuesday July 19-1910 Forteau, Labrador. "A bright sunny day and no wind. Mosquitoes and flies bad. "Collected all morning at the top of the Reef back of Mrs Flamin's house (hill northwest of Forteau Bays), in the Olenelles - Portyipas beds. Here have a large lot of this material. No fine Q. heads however. "In the afternoon examined the gulch opposite Forteau village on the east side of the bay and a little farther inland than the head of the bay. A small brook has cut its way through the Reef and to the sea which one followed, making a good part of it. "Here one sees the red sandstones well exposed and that towards the top consist of a series of thin beds (8-172 inches thick) separated by shaly sandstones of about the same thickness. These beds here take the place of the heavy bedded white sandstones. Just over these come in the coral reefs but these are rarely in the form of reefs here, rather than bedded regularly bedded and nodular bedded limestones. About 50 feet is here once more exposed. From the upper ten feet or thereabouts one gets many fine layers and fine Archaeocyathus. Toothed shell stone cuts ten inches long and not more than four inches wide. The top of known bed was broken off so that the cut was originally about 12 inches long. The corals in this layer do not enclose reefs and therefore the single corallites develop once. All of the large forms have conical outsides. The other fossils are scarce and only a few brachiopods were seen here. Does this evidence point to close proximity of the shore? Across Forteau Bay to the west the reefs are present and especially along the Straits at Forteau Point."

"From the evidence in the gulch it appears that as one gets back towards the old shale line the strata of the sandstone series are all red and here take on towards the top a clay character. The white bear hidden sandstones occur farther south and away from the old shale and gulch. Then too the Archaeogatherias are no longer here in such decided cups as farther south, though on both sides of Fortuna bay (in the back n north end) the cups are large and better developed in the gneiss so to be far above the sandstones. "To soon or we intend to walk to La Chaise Golf and have our boat meet us there. "None of the higher beds from 65 to 132 (n. Zephrin 143) but are present here at all. All are now worn through erosion. As one goes northward the limestone series becomes thinner though not worn out. About Blanc Darton these higher beds are present but all are covered with vegetation and all we could study there were the lower to foot. Of the higher beds Forrest Jell saw four limited exposures and at first he broke the lime-stone but saw no fossils.

"Wednesday July 20-1910. L'Cause au Loup. "A fine warm day and a slight breeze. "Walked from Fortran to L'Cause au Loup along the shore a distance of about 8 or 9 miles. "On the east side of Fortran Bay we again encounter the red sandstones at the top of which are seen a little of the white sandstone, initially less than 7 feet. None was seen yesterday in the gulch and today we first began to see it about 1/2 miles out from the head of the bay. Then for the red sandstones which free of feldspar are softer here and evidently have more made in them. "When we got to Mr. Davis' house north west of Point Armon lighthouse we came upon the coral reefs that are here more lovely bedded and less a reef than on the east side of Fortran Bay. Then for the limestone is not often red but usually a grey to light green nodular limestone. We measured at least 80 feet of it there. The Olenellus came in about 65 feet from the bottom. Just east of Davis' house around the bay on the way to Point Armon the reef limestone reaches the sea while Island 1/2 mile the louse is fully 40 feet above the bay. Strays at this place that Richardson got some of his fossils. "Point Armon projects further into the Straits of Belle Isle than any of the other headlands hereabouts and it is because of this that the light house is placed here and also the reason why the reef limestones dip into the sea to the west of the light. "To the east of the light house and the Marconi

station all the way to Johnson Cove (which is just inside the western horn of Anse au Loup Bay) are exposed the reef limestone and out at the sea end a little of the sandstone. These limestones preserve nothing higher than what we saw this morning, and the reef character is almost total. The corals are more scattered here and do not congregate into reefs. The red limestones are practically gone and all the beds are grey modular li., or blue-grey diverse hard somewhat impure (either sandy or muddy) li. Other than the coral fruits are scarce. We saw orbitas at three levels and they may occur at any horizon from above 20- feet of the base of the li. At the base of reef li. They are somewhat chalky, and more impure than higher. The sandstones just below are decidedly chalky all the way from Point Armone to Johnson Cove. Again we saw them or found down in Red Cliff. The sandstone series just above the granites is in Anse au Loup Bay again a strange inherent conglomerate. It's the loose nature that causes it to wear out easily making good contacts impossible. Here again as in all the bays seen, the granite appears to be put to the head of the bay and it terminates in a broad valley in which there may be more than one horn or arm. The hills here are about as high as at Fontaine. The east horn of Anse au Loup Bay is made up entirely of red sandstones and is called Red Cliff. Photographed.

"The tenaces are well marked about Johnson Core and I photographed them. We have now exhausted the possibilities of our making Cambria collections, Paris told me today that Richardson in 1876 was at his house four miles and one at Guse an Long making collection of fossils. He sent in five heavy cases of fossils. The great majority of his fossils came from near a Point Armon near Paris' house. Logan makes the statement that his Cambrian section was measured at once an Long. If this is so he could not have gotten 143 feet of limestones here as hardly more than 80 feet can be seen! It is some probable that his section was measured at Blaine Latham. - Right mac Olenellus beds but all are small and one large and fine. But some Stenotheca. Otherwise nothing but what we have in abundance. Chelus chromatica seems to always occur in the lower part of the reefs and the shell is often a yellow or red granular limestone. Patersonia labradorica and Rostropon circulara seem to occur throughout. This is certainly true for the latter thank the former is never at home in the upper part of the reef.

"Thursday July 21-1910. Onse au Loup. A dark, cold, windy day with small rain after 10 A.M. Started out for the fine exposure of the limestone to the west of Point Amour Light house, about 6 miles east of Onse au Loup. Collected all day in the Olenellus horizon and got from 15 to 20 fair to good leads. One fine one ground but not so large as the one in the Canadian Geological Survey. These fossils only probably several smaller fossils than any are found. There are at least four species of Olenellus present and probably three. Associated with these trilobites are six Stenothecæ: Hyolithellus onicans, Autorgina cingulata, Paterina (small), C. Labradorica, an Orthoid? (common), Ptychopnus senectus. Got 2 large bags full and returned to the Victoria at 4 P.M. Got to the cabin. Later, During a storm off Table Head, one open hand of Cambrian fossils was upset and some of the material got a little mixed. The Olenellus lot above described is intact. The lot we are somewhat in doubt about is the lower Olenellus lot from Johnson Cove (15 to 20 feet above base of limestone). Some of these may have gotten mixed with the above and it is possible that some of the higher Olenellus led back of Mrs. Flahins house got mixed with the Johnson Cove material. If there is a second lot of Johnson Cove material not done up in large, taped bags, then this lot is intact and is not mixed. In any case one can see differences in the fauna of the two horizons.

"Friday July 22 Anse au Loup. As the day is fine and the wind light we conclude to sail for Florian Cove. As that are only six mile of the Cambie to the east we have the kirtana sail close to the shore eastward. The east horn of Anse au Loup bay = Red Cliffs is all of the thin bedded red (orangeated) sandstone standing in red cliffs to a height of about 150 feet (both sides 200). In the back of Anse au Loup bay the hills on either side have at the top no lime- stone and some can be seen on the sea cliffs at Red Cliff. As we round these cliffs are get a view of Diable Bay where there is another fishing village. In the dally in the back of the bay one see the granita mountains that are not more than 4 miles from the head of the bay. Granite is also well exposed (maybe 20 to 30 feet high) about half way out to the east horn or Cape Diabie. It is therefore quite evident that no lime- stones are exposed or even present to the east of the west horn of Anse au Loup. The red sandstones in Red Cliffs are thinner bedded and differ from those seen farther north. They are the deposits not far from the old shore. The wind died down and as we drifted out northeast in the straits we got further away from Florian Cove. At about three P.M. a fresh wind blew up and dead against us for our destination or we flew back again to Anse au Loup, arriving there at 5P.M.

Saturday July 23 - Onse au Loup. A quiet foggy morning and some rain, be hoped In mind up to ten and then gave it up for the day. In the afternoon walked along the shore of the west side of the bay to see the red sandstones. They are here they fed did sandworms hiding and I look each walked. Both these occurs at many levels. Also there is small vertical lining possibly due to vertical graining, we have a specimen of it. We then tracked limestone at 10 and 15 feet above the base of the reef limestone for fossils rather than the crabs. We get them in the intermediate spaces where the limestone is thinner and more, and is cleaving and harder. To our sur- priese we get Olenellus and probably Drepanocis leaves. Between no are got 7 or 8, one can be indistinct. Associated were Lutetina concinula, Oithis ?, Paterinia labradensis (small) and one Hyolithellus aricanus. The trilobites seem to range throughout the 8's feet of Li. congrua. Near the top Olenellus is once common and apparently large. We now must have near 500 pounds of fossils and crust and have probably as good a collection as that brought out by Richardson and Yorgan. One is struck here throughout the Labrador county by the absence of accumulations of glacial material and sharp moraines. All of the granite boulders seen are those of the beds exposed in the valleys. There one sees scattered here and there over the hillsides. The glaciers have removed all

the old red grit. The newer boulders are those of the Cambrian sandstones that lie along the old elevatory tracks. No sand accompanies these old tracks excepting on the lower beaches in the valleys at the head of the daps. "Granite is exposed just back of this village and appears 30 feet above the sea. Farther back in the river valley 1/2 miles the granite is exposed in extensive hills attaining to an elevation of initially 75 to 100 feet. It is probable that no Cambrian logh exists in this valley. All of the Cambrian hills seem to face these old granite hills in crestas. how so t, Camday August 15-1910.

Monday July 25. Florida Core. Arrived here on the Home at 1 P.M. At 2 started north and examined the shore for about two miles to Savage Cove. In this distance saw about so far or less of strata. The dip while any drift is distinctly towards the Strait What we saw are then headed to Lear's headed my fine paired, dense, emphyseally splitting Lyst. Here did limits that rather to a gill or a Gelatinous grey. The strata are in low domes and are much jointed. Here and then we sees a sun-cracked bed and then goes of intraformational conglomerates. Fossils are exceedingly scarce excepting a small species of Lingula identified as L. acuminata. It may be this species but if or are smaller than the New York specimens. These are common and generally in fragments. No other fossils were seen, except an individual. The land is here very low, gently northwest rising to 75 feet in the interior. Apparently all is once or ten terraced and the low peninsula appears to have been made by the sea. We crossed an elevation of 30 feet and here we saw the same head wall that may be seen on the present beach. What we saw today is probably near the tip of Arizona and June 4. [See Scott of Canada, 1863] p. 289). Evidently these deposits are those of a very shallow sea. Low in the old limits, sun-cracked and intraformational conglomerates.

Tuesday July 26. Flora Cove - Current Island. Rained again last night, dark day, before to the station. Left Flora Cove at 7.30 A.M. The dolomites are once thin folded as we go south to Bear Cove and Anchor Point. There is some infra-mamifical conglomerate, some craegry and riffles. Saw a few Lingula acuminate. At times the dolomites are small crushed with by-form like thing but no structure of any kind is preserved. Maybe fossils. The strike of the strata at Anchor Point is, S. 20-30° W. and the jointing nearly due east. In one place we saw a small local fault of 100 feet or so in length. We saw something of the strata along the low shore nearby to Anchor Point. After that it rained hard and we had to give up all work other than walking to Mr. Hat Taylor house opposite Current Island. Our work is beset with or many difficulties in the way of the weather, insects, sea-sickness etc that our papers is not satisfactory. The topography is here as at Flora Cove, no higher. Saw some large pieces of glacial striated dolomites. It is doubtable that this work was done before the elevated lands were made. About this known I am not certain.

Wednesday July 27. Current Island. The day started in fine but soon changed into a foggy day with a tendency to rain. Spent the morning on Current Island. Saw stratly 150 fut of Lorgans grve E or S. It is a series of thin and thick bedded grey to light blue dolomites that overlie to a light yellow or a gray light grey. Many of the beds are sirdiforms. The beds lined with small quartz crystals. Some erosion is seen in many layers and there is considerable pucciation. The evidence is all for very shallow water deposits. The dip of the strata varies between 10-12 degres N.45 to 60 W, No fossils of any kind other than facrils were seen. In one small core a considerable area was seen specially striated. Their direction are N. 75 W. Their present level was practically that of sea level. At none of the higher levels once seen other striations. There is at least one once eroded elevated track with a cliff back of it. Its now healing down but the appearance is very young in fact 100 years or even less would have broken it down to its present appearance. Taylor tells me that inland at least 20 miles are found bones of whales (a jaw and macthree) and many ovals of Ostrelos edulis. The bones are still solid while the shells are chalky. These must have sitten to their present place when the sea stood at a higher level and this could not have been so long ago. In the afternoon walked along the crack towards St. Barbe and saw the same kind of dolomites as this morning.

fossils, here as this morning the rocks are full of quartz and dolomite crystal gerdes. May have seen another 100 feet this afternoon. Quartz gerdes predominate. All of the dolomites seem to agree with Organs gone E (=5) and probably represent the Little Falls New York Organic. In this work gone C represents the base of the Organic here continuing into D(=4) and E. The thoryoffy for Drat. Taylor as house. Oreth, Ligden kilero making to. Ferrule Yon kets, y another Oeull. Bet am 100-150 fet. Orey Northland Smith-Leeumit ? Play's ? 1300 ?400 fot. 1610 Smith 1610 fot. Ferrule 1359 Current Dolomit

Thursday July 28. On the way to Port an Chroi South Summit (Days) St. John is 1610 ft high and in all Ordovician (Two cliffs are once seen in North Summit. The summit stands out as green lead lands totally facing the sea. St. Johns Island is a low island pretty not run to just lips. On the west side in a once marked terrace, Terrace. As we turn into Port an Chroi harbor we see long cliffs of limestone some of which look modules.

Friday July 29. Port au Choix. Rained all night and this morning. Packed all the Cambro 3100-4 = B3821 Upper Beedmantown. = Basal Chazy Port au Choix, eastern Newfoundland. July 29, 1910 Head of Old Port au Choix Bay northward B3822 one-half mile. Zone 8 of Logans Section. July 31, 1910. South west of Port au Choix village. B3823 Zone 8 with possibly some of zone 9 of Logan's sect. = Upper St. George Series Schuster and Tarentine Port au Choix Bay July 29-1910 From inner end of bay and on land side. From the iron 30 to 35 feet of zone 10 or K. 3100-4 306344-306348 In the cliffs near the north east end of the bay may be seen the contact between zones 9 (I) and 10 (K). The contact is a sharp one as the beds of 9 are not nodular until those of 10

Thursday July 28. On the way to Port au Choix

Friday July 29. Port au Choix. Rained all night and this morning. Packed all the Cambrio foss into me large box and a barrel. or Old Portau Choix. In the afternoon collected from the Lead of the bay Northward to Bustard Cove. In this distance of about 3 1/2 miles saw about 30 to 35 feet of the lower four of zone 10 or K, firstly are of I or zone 9 and some of zone 8 or St. From the Lead of Port au Choix bay out without for about 1/2 mile one sees along the shore and in the low cliffs just back of the shore about 30 to 35 feet of a light grey to dark grey or brown bluish some- what magnesian, once or less mottled silicestone or larry beds. x These li. are full of gastropods that may be seen best on weathered surfaces where the shells are slightly siliceous. It is next to impossible to get good material. He got or saw fragments of a large Postelus, Amphimorinpanensis, Wasmuo? large Bathyrnus fawl, Maclurea posilly atlantica, a smaller Maclurea, large Tarachrema, other gastropods, a large near Striphomena, Leptaena near incrassata a small Camarella or Anagyzza, Rhynchotremia (one), Streptel- asma frond loose, and maybe from the top of zone 9 or I) and Eurytomites. Also small Endrenus or Camescens. These beds look to me like the Oringon Chage, the lower beds just above the sandstone there. Well see the higher beds tomorrow in going around the north side of the bay and out south- ward toward Point Rich. In the cliffs near the northeast end of the bay maybe seen the contact between zones 9 (I) and 10 (K). The contact is a sharp one as the beds of 9 are not nodular while those of 10

are distinctly nodular. Otherwise there is no lithologic change between the two zones. As yet one can not say that there is here a time break. The beds of zone 9 or I are also of a light grey character but weather more decidedly yellow, and even reddish and not nodular, being bedded and much jointed. They are also more conspicuous. Fossils are scarce and those seen are obscure traces of Brachioceras apparently like the Atlantica of zone 10. In order of the beds there weather out their lumps from ½ to one inch across. These are often common, but normally all call them gerles. "Cole-ger" gerles as Logan states one did not see. It is notable that in Bussard Core one saw a little of zone 8 or H. These beds again resemble the basal beds of K a 10. Here we saw but could not get Eurypterus and Brachinae of Atlantic. The dip at the mouth of the Port an Chrisy Lagoon is N. S. W, dip 5° O. Farther northward, about half way to Buggars Cove N. S° W., dip 10°. At Buggars Cove N. 60° W., dip 45°. About halfway to Buggars Cove one sees two terraces [the higher about 15 feet above the sea] with glacial striations. The strike runs N. 80° E. and are parallel with the direction of the terraces. To see this evidence means that the terraces are older than the glacial period during which they were made. The next higher terrace at 25 feet above the sea preserves our glacial striations of our own section too. This surface was much weathered.

Saturday July 30. Port au Choix. A fine day of sunshine. Collected all day from the head of Port-au-Choix bay along the western side out around the northern head of the peninsula and then south along the outer sides of the penin- sula to the abandoned French fishing village Port au Choix. 2oc before in zone H in front of our anchorage. Logan gives the thickness as 340 fut. Fossils are few. The most striking one being a large species of Receptaculites, probably 6 to 8 inches across, or came from The Logwood trees to this lot may come from a shore break and belong in zone far. Zone 7 or 8. Logan gives as 130 fut. Fossils are fair, abundant but most too impossibly to get. Near the top are soft large depressed gastropods (Maclurea-like, Torch crema, etc), Murchisonia formsterna, Helixen, Leachi and twls of trilobites, ostracods, a small Rafinesquina near incrustata, and Orthus near subaequata. We also saw here but could not get a large Eopstonites, and Pilocrerus canadensis (mostly roundish day). Lorn down in 6 ocean the same series of fossils but only the Pilocrerus. Zone 7 or 8, has the same fauna as 8 but no Pilocrerus, Logan gives the thickness as 130 fut. We did not buy these fossils and got as we could not tell our position or the are none most of the fossils are set any from 8 in 7 or 8 according to Logan the fossils are about the same. Zone 6 or 5 (as he says) We saw at the northern end of the peninsula The beds are heavy bedded dolomites full of diagnostic clumps and quartz, dolomite and calcite spherids. Fossils are very scarce, we saw as few depressed Maclurea-like gastropods. Logan gives the thickness as 400 fut. This probably that these beds are the bunk of zone 6. The higher beds are than mistook as

and different from those of 8. fing in 7. Fossils are very scarce here and the few one get are, All of the strata of 6 to 9, both inclusive are once or less magnesian limestones and some are dolomites. They are all very much alike, leary bedded, dense, every bedded a little grey to dark colored limestones. In zone 6 there are some thin bedded strata. In it occurs much mud-cracked material. One shot was mud cracked and had two cells marked though ripples, In some of the cells coarser cracked to the material was seen. There is much evidence for very shallow seas. Even in this zone are seen fossils but far less than in zone 8. A pebble conglomerate was also seen in zone 8. In zone H or certain beds the fossils are rather out in relief in a semi-silicious condition. However they are are as a rule very firm. The surfaces of such limestones are covered with a net work of raised faccid like strings of ball signs. What these represent I can not say. On first picture one does not see them, they come out in weathering. In zone & the leary bedded dolomites are much domal sometimes only 6 inches high and then 2 feet across and then the domes may be 2 feet or more high and from 6 to 10 feet in diameter. Usually on these domes appear thin bedded material. The latter are very local. And if one fossils today come from 8. A few from 7 are mixed with them. If we get any from upper part of below they are just about like the others.

Near the mouth of Port au Choix harbor the strike is N. 60 E., dip 7 S.E. On the outer side of the peninsula it is N.60 E., dip 8 S.E. Glacial striae seen in the harbor N.70 E. Core 8 is certainly equivalent to Piloceras beds of the Fort Carson section.

Five day with a little rain in the afternoon. Sunday July 31-1910 Port au Choix. Collected one day in beds 10 and 11 of Logan's section from the French fishing village Port au Choix on the gulf side of the peninsula all the way to Point Riche lighthouse. Distance about 3 miles. On the southern side of the French fishing village one sees deep red dull dullomite almost without fossils. These are probably all of Logan's zone 9.=8 a H and 9 a I Further south appear beds of zone 10. These one then follows a long distance along the strike and one gets into zone 11 before one were aware of it. There is nothing to distinguish the two zones other than the fossils. Zone 10 and 11 consist of a series once a less heavy bedded, grey to light greenish, once a very thinly limestone that under the overweather head down into a sharp gravel. The higher beds of zone 11 head down into larger flats and overweather into well joint siltstone. In these higher beds that are crowded with Lepidodictias and some trilobites. The gastropods are here much rarer and one sees as a rule only small specimens. The grey bed of zone 11 is in the lower half and is decidedly local. For a long time one comes on these beds and because one saw no sponges thought one were still in zone 10. All of our Eucystomites and most of the siphuncles of Endoceras and probably the Orthoceras are from zone 11. In the grey bed occur the first decided devill pterinacyprae but these too are decidedly local and we did not

get and than for specimens although we saw more than are five. Of the Eospongia are our specimens, 12 inches in diameter. Of these one has pieces. Of the annulated cylindrical sponge one fit some nice material and one from was 18 inches long. All four entire and better trilobites are from zone 11 but we saw and probably have more material from zone 10. The gastropods are in greater abundance in zone 10 and the lower half of zone 11. Of Endornus we saw only siphonelos in zone 10 but in zone 11 there are far more abundant and often one a lens of the entire shell is present. Portals from Euryotmites came from the lower half of zone 11. The strike of the strata 2 miles east of Point Pich lighthouse is N. 25 W. Dip 48. At about 1/2 miles east of the lighthouse it is N. 50 E. Dip 10 D. Near the lighthouse there are minor more undulations. The prevailing dip is towards the land. On seeing the trails of zone 11 we provisionally correlate it with the Sponge zone of the Oregon Island Chage. This is done mainly on the basis of the sponges and the first abundance byssus. Some of the gastropods are probably also in common but not a single brachipod has been seen that occurs in both places. If this correlation turns out then zones 9 and 10 are about or Oregon between the Oregon and Romaine formations while in Newfoundland the section appears to be complete.

Monday August 1-1910 Port au Choix. A dark day until 3 P.M., then sunshine, dry wind. Collected here day from Point Riel light-house after one left off yesterday along the southern side of the peninsula to the head of the bay in the Port au Choix post-office at Langhamille. For nearly two miles from the light-house landward are collected in Gme 11, beginning at the top of the zone and continuing to a little below the orange layers. The latter are near the base, from 15 to 20 feet above the base. This gme is composed with fossils throughout, chiefly gastropods, and Deper- ditias. At about 15 feet above the orange beds are seen many Eurytomites. Endreous occur throughout the lower half and as a rule include most parts of the shell. A tip end is often crushed and was absent in life. In gme 11 probably 50 feet above the base one thought one daw four specimens of the sixthuncle of Pilcerus. One of these are kept. Later when one came upon the orange layers one concluded that they are not Pilcerus. This matter must be looked into. Stromatocranium occurs with and chiefly below the storms. Dependitii seem like common thing from all the beds down to the orange layers and some where seen here as once. The abundance of Ilcaenus heads and tails filling the living chambers for Endreous came in about 20 feet above the base of gme 11. The annulated opyge are usually found singly but once than once today one found them in pairs, of two and

three. It is remarkable how scarce the buchisprds are. All that we saw today are small Rafinesquina with a median keel. Torohyle or Jan has found all the entire trilobites, Bygga or saw one today. June 11 is essentially a heavy bedded finely laminated that slathers into a shaly gravel under the influence of the weather. June 10 is also heavily bedded and shatters into gravel on weathering but in some one presion. It is far less fossiliferous than June 11 but the species and especially the gastropods are apparently the same as those of the higher zone. Of Euryptomites it is impossible to get good material because the chambers are filled with coarse crystals of calcite and it is only the body chamber and 2 to 4 from first chambers that are filled with mud. Then too many of the shells were rotten before covered as the under side has broken down and flattened before fossilized. Nearby all the Endocrinatidae were also rotted before covered as the under side is nearly always gone. The chambers are nearly always filled with mud but the endocore is nearly always crystalline calcite except the outer part. The strike near the fifth range M-70 ft. Dip 12 deg. One and half miles farther inland strike N-40 ft. Dip 10 deg. Saw a piece of the Lower Cambrian conglomerate of Labrador as an erratic today. It may also have come from the eastward area there seems to be L. Cambrian.

Tuesday August 2-1910 Port-au-Prince. First day warm and windy. Collected in the morning in zone 8 along the northern medium side of Port-au-Prince harbor. First of two large Pil occurs the only specimen of that seen presenting the entire shell. Also saw four specimens of the large annulated sponge or common in zone 11. Have now about all the fruits it is possible to get in zone 8. The fauna is a small one and very hard to get. In the afternoon collected in zone 10 in the bay leading into Bar-a-melle Cove at the Port-au-Prince post office, this the same place as yesterday's collection. Bactriopods are the chief fossils of this zone. Got a few small Eurytomites. Saw one large Stromatocranium probably 18 inches across, but a smaller specimen. These occur only near the top. The conchili near the base. Zone 9 is a distinctly more granular, heavy ledged, lighter colored dolomite than the limestones of zones 10 and 11. Further it does not check up into grain under the weather as do the last mentioned zones. By persistent collecting one could get together some 10 to 15 species and possibly from once but all are saw are those of the upper zone. The specimens are smaller and the free is pseudomorphous celestite. The dolomite is mottled and is not knotty. Zone 10 above is decidedly more fossiliferous a light blue-grey color and is not dolomite but a limestone that may be somewhat magnesian. Then for it is knotty. Nearly all the low spiny gastropods lie with their feet.

side downward and the antilices upward. Tarchomena and a large form with the tip gently curved have their antilici downward. These positions are undoubtedly due to the current action on the sea bottom. In zones 10 and 11 nearly all the fosils are gastropods. In fact gastropods dominated the life of zones 7-11. To feed these animals there must have been enough plant life more of which is now visible. Brachiopods are extraordinarily scarce, the commonest genus being Refinogonia and it is rare. Tripoli occurs not rare but it is not often that we pass an entire specimen and those occur nearly all in the top of zone 11. Large Asaphus are seen in fragments especially in zone 10 but also occur in 11. In the former zone we saw fragments indi- cating animals up to 12 inches long. Byzonia are practically absent and only one found in the top but did not see them in some abundance. Ostracoda and especially Lepiditris are very common in zones 10 and 11 and especially the latter. Crinoid stems occur only in the top of zone 11. They are very delicate stems almost thread like. As far as I can see all the zones from 7 to 11 are one continuous series of deposits. Zone 8 seems like Fort Carin and zone 11 (lower part) correlates best with the lower part of the Minjuan formation.

Wednesday August 3-1910. Port Saunders. Walked across the narrow neck of land that separates Potan Chix Bay from Bargamelle Cove and then along the shore to Port Saunders. The distance is about 8 miles. The boat left when we did, 7.30 but did not get to Port Saunders until 6:30 P.M. He began collecting along the eastern side of Bargamelle Cove and found here zone 10. He remained on these strata all the way until the outer foot of Port Saunders Bay where zone 9 appears. In 1918 I see the horizon is lower in the Bearmountain. The new feature from the faunal standpoint was the abundance of Dithmotocentrum though here zone 10. Also the north end of some [also cup in zone 11]. Sponge, Tornohed get a fine large Cytreacum with a large spindle. Nautiloids were seen often and Cameroceras more often especially there are well preserved endocones that do not taper rapidly. As a rule we see more end-cones than entire and septate cones. Gastroids were again plentiful but not thick from. But one very large Machlits. The dip of the strata is almost as that about Point Rick until one gets to the mouth of Port Saunders where the gentler dip or fan occurred. At the mouth of Port Saunders, I have in zone 10 the strike is N. 35 W., dip 18 to 27. Along the strike we also notice slight undulations. Just a little north of the mouth of P.S. Harbor there is much morainic material of granite and especially of a white sandstone (probably of zone 3) that lies on a base of polished and striated limestone of zone 10. In the harbor about 20 feet above the sea we saw a greenish mud with Ogyra arenaria. It is probably

an glacial day. Thursday August 4-1910 Table Head. The wind this morning is in the same direction and as the Wtena cannot make Table Head today we conclude to walk to the place. The men took us in the cory to the extreme western point of Barke's Harbor and from here we started at 8 am Table Head where we arrived at 7.45 P.M. I just about done up. In a straight line it is said to be 15 miles but as the path runs it is all of 20 miles. Where we started to walk at the outer end (western) of Barke's Harbor one sees a fine contact between 9 and 10. There is here no mistake in this identification and Logan is no own in stating: "In Harke's Bay there is firstly a transverse dislocation, again bringing the lower limestone, 4 to 9 forward to the coast, along which they run for about twenty-five miles to Table Point" (List of Can. 1863; 297). So we came 9 again east of Trappen Core, beyond which point no rock is seen other than glacial ground consisting of large rounded blocks of granite, white and pinkish fine grained sandstone with blocks of Ordovician limestones. East of Trappen Core we counted 6 little rocky beaches up to 20 feet above the present sea level. All other of about equal height and are of very recent origin as no vegetation has yet taken hold upon the loose rocks.

"Still far the west of Trappus Cove we came up m 2 and smelled elevate rocks on at 15' with a cliff 20' high back of it. At 40 far above the sea the land is level smelling the second beach. These beaches are in glacial material (to me looks like onoramic). This glacial material continues all the way to Whale Bay and in all this distance there are no Cidnoric outcrops. Also saw Orga arenaria in them. At four half miles east of Whale Bay from the opening to Large Pond) Onoritic rock exposures again occur. It is a decay bedded dove colored, mottled with white, onepression lines. two (granite or limestone) having some silicous footprints of which are hole out all their own good and accessible. These look more like those of 8 that of any other horizon. In the present we think the horizon are &. See the books, our course or one part of whale bay area we came upon another settlement and here again we saw nothing more than glacial (onoramic) material. One of the inhabitants told us that the same kind of material occurred all the way to sea Fontaine Point. We therefrom took the skater path cut through the woods, "The Government Road" and on five miles or more among the mosquitoes and over the stumps on a hot day, Tomahfel thinks honestly the saw entirely in this distance from Bruce Bay. We came out of the woods at Ballen and from here to Table Point we walked over "the barriers" and the coast is all glacial material to about five miles east of the Point. See Tomahfel reports give 9. At Whale Bay the strike is N170E, dip 4 S. Five mile east of Table Point the general strike goes pm

N.S. to N.10 E., dip 19 to 40 E. The dip is very irregular and maybe reversed in places (undulatory). At the place 5 miles North of Table Point Torch/Al can a few flat gastropods, partly a cephalopod with many short arculi. This is thought to indicate gone g. Mrs House said that in digging a potato cellar for their winter house laid in the marshes they dug through for two 3 clam shells (Oryza arenaria). Probably an old headless husk. I should judge the elevation to be about 50 above the sea. Sperm whale bones and teeth were dug up under their summer house which is about 15 feet above the sea. We are stopping at Thomas House.

Friday August 5-1910 Talle Head. A dark day with constant rain all afternoon. Spent the morning at Talle Head in Division N zone 2 where Toothfjel entered a cratoline like arch and found Entire specimen of Ampyxze and Blacrus. Trilites are not abund- ant but good. I collected in a dark nodular limestone outside zone O1. that had an abundance of trilites in fragments and an occasional Brachiopod, but Ampyxze Agnostus, Maenus, Rempleurides, Bathgurus, ostracode Cyclopina?, Orthocera? and an elongate Lingula. There are other species, but a large lot. In the afternoon returned to Talle Head and went east around it until we came upon the Lependitta bed making the upper part of zone 11. Collected a fair quantity of this material as it was better than that of Point Riel.

Saturday August 6-1910 Table Head. Walked along the path across Table Head to the Lepeditia bed and then along the shore to Table Head from where evidently Richardson began his Table Head section (See. Canada 1863, 1869). Cannot accept Richardson's definition [illegible] minus divisions. "0/1 of 8" (1869). Accept his measurements. 100 feet One or two heavy bedded, pure to dirty colored, more or less crassly crystalline dolomites, that in weathering have much quartz sands. There is [illegible] change into crystalline dolomite. Forms as scarce but are those are seen at Port-cum-Coig Bay. Richardson's thin bedded definition is seen only on weathered areas and is shallow stuff and not original bedding planes. The dip is ductile here the [illegible] of the section and about that seen far over in out. M 30 E. dip 23 W. Thickness according to P, 100 feet. "#2 or 8" 165 feet. Richardson's "concealed gneis" is more once a less exposed at low gratan and are see that the character of the beds is identical with that of #1. Towards the top the beds are well exposed and are once very bedded, even handed [illegible] and and crystalline limestone like, with occasional small masses of chert. Here one sees almost no fossils. Some little 1/2 cm-crassily was seen. "I guess 1 and 2" or 9 135 to 174.5 feet (latter Tomkfields estimate. All divisions are arbitrary throughout the Table Head section. Division K = 100 feet. Division K is grade of a series of one or less heavy bedded directly [illegible] limestones with Lepeditias, small ? Camarella stromatolites and the common breccia, interbedded with every bedded highly fracturing (vertical) yellowish weathering fine grained

dlimites that have no fruits. Out of the finely crushed we could get at least ten species of fruits but all are or porn as to be unidentifiable. Dis is here - 13 Wt (8.2) "L" zone 11. 104 feet. A series of leary boded finely light-blue magnesian lime- stones. Near the base reem abundantly large Hormotoma, and Ormoceras. We also saw the common Orachura, Lependitia, many small ziphurelas of Endoceras, and rarely a Euryst. Ormoceras and the large Hormotoma go throughout Richardson's lithic definition is all away. At the top I gone to saw one slab with several specimens of the cephalopod feeding candida-falli like the cone shaped Anthrophyus "M" zone 1 (base of 12). In the field regarded as L. Same character of beds as before. Fruits not here as abundant and certainly not in good as Point Rick. Saw but a single specimen of the annulated range, Mr Esphingia here. In this these beds look very different from those of Point Rick. "L." zone 2, 96 feet. Same beds as before. Light blue to grey and nothing 'did did' about them as is stated by Richardson. "L" zone 3, 60 feet. The Lependitia beds. A series of leary boded finely light blue to grey magnesian limestones that are then down in yellowish thin boded scaly pieces, even ornamenting into their slabs. See one (Mr) F fruits, collected yesterday.

"L" gme 4,6 fnt. There is no such gme as defined by Rielandson. Character the same as before. "M1" or gme 12. Thickness 350 feet. A great series of heavy bedded grey to dove to light blue nodly limestone with fossils throughout making gastriports. Near the base get Orthus tricernaria, Raf, ridguli. [illegible] Phylloceras little them in total 16 at Portage Chimp. As the limestone is very hard and does not shatter as the lower beds it is very difficult to get the material seen. Lepididita is also common in the lower part. At the top there is a layer of Eospirigia 8 feet thick and the specimens are common. Torinwelf collected several specimens of trachyports in these upper beds suggesting the Mijgan forms. Saw here also several large (8 to 10 inches across) Euryptmeters but could get none and then the observation was from. Also got several specimens of ? Sillimorites. Got several Cyrtoceras, one annulated Cyto-ceras and one annulated hautiloid. Endoceras occur throughout between room food. Readily all of some fossils out of M1 are from the top of this gme. From the base besides those mentioned Horonitoma, Amphibin, large Osaphus tail and Maclurea. The limestone smells of petroleum on heating point. To 4 M1 the strike N50 W. dip 30 W. This is north of Tablehead "M2" gme 12 said to be 308 feet thick for I do not see more than 75 feet between the sponge bed and the first appearance of the Haedlit nodular beds of M1. On unweathered exposures M2 appears as a heavy bedded dark grey to light blue modular limestone, but under the weather

"It appears as a very thin bedded (1/43") decidedly nodular limestone. Heavy throughout the bedding is irregular and locally very decidedly so. On flat exposures the beds are seen to seem in low domes but in section look cross bedded. Fossils chiefly trilobites occur at various levels but all are broken and are the same as those collected in M 2. Made no effort to get them today as it only again special petrifaction collection. Among good form incl nautiloid and the ventral valve of Camerota. Forrestell collected good material from the lower 30 feet of zone M 2. The great abundance of large depressed gastropods ceases on top M 1. Small specimens go on upward but the large Maclewares drop out. From our crowd today it is certain that the entire series of limestones so far seen are a conformable series. There is no marked or sudden change in the petrology and the fossils hold on from zone to zone especially above zone 8. The gastropods and the trilobites are the large dangers. Brachiopods are very scarce and byrgon almost absent. Cefalopods are rarely abundant but if we could get all the material seen then would be a few more forms than those we have.

Sunday August 7 - 1910 Table Head. Another dark day with light rain throughout the morning. Started out at 7:30 to finish the top of the Table Head section. Torahfel measured the thickness of M.2 making it not over 70 feet instead of 308 feet as given by Richardson. The strike of M.2 at Table Head Point is N.32 E., dip 34 S. "M.1" or 13 Thickness 81 Richardson, Torahfel made it 70 feet. Blackish-grey, nodular, petrofiticorous, thin bedded limestone with a little black shale in pockets between the nodular limestone. These are interbedded with some regularly bedded grey limestone. The nodular layers are full of broken trilobites in pockets. All of my M.1 fossils collected today and on Friday are from those layers. Also those collected in the afternoon at the isolated mass indicated in the sketch of the next page (Ampyx quite abundant here). "M.2" or 13. Thickness Richardson 17 4 feet, Torahfel made it 208 feet. Thin bedded (thicker than M.1, i.e. 2 to 4 or 5 inches), regularly layered grey to light grey creases or dark green M.1 limestones with a little dark fissile shale between the limestones (1/4 to 8 inches of shale bands). Fossils are far rarer here than in M.1. Some were collected today and none on Friday. Above these limestones fans gradually into the black bituminous shales of zone M.3. M.1 and M.2 have the same dip and strike as M.2. "M.3" or 13, Thickness 22' Richardson, Dark blue to black shale that hasaly gradually fans into the limestones of zone M.2. Near the top the shales have thin bands (1-2 inches) of sandstone that become more abundant and or gradually fans into the sandstones of zone O or 14.

Sketch of faulted zone near Table Head. Bull / Mt. Lawrence. Strike 107 E. dip 85 S. Table head 3,2 Ramsay hill 3,1-2 Sand line In this area the strata and dip in an arc of strike as if the two heads had slid upon one another. Strike 07 E. dip 85 S. Iron residues / cliff standing slope Gone 8 delomites bromfield al. town Path Potato lander Potter farm Patton hill fault--- strike fault plunging 06 E. Gone 8 dome-fly delonites. Strike strikes 01.60 E. dip 10-25. Steel between Table Head and Belle Burns Just west of Belle Burns the strata are arrange in a small synclinal axis pitching 20° in the direction of N.60 E., 1/6 of a mile further north the strike is N.60 E, dip 15 S; 3/16 N.32 E., dip 39 W.; 3/16 N.25 E., dip 44 W, 4/16 N.50 E., dip 49 W.; The latter strike holds for 1/8 mile, then changes to N.45 E. dip 48 W. 1/16 mile further changes to N.10 E., dip 48 W. The latter changes almost immediately to N.25 E., dip 28 W. and holds thus for 1/1 mile arriving to N.15 W, dip 23° W. Near 3 miles N.30 E., dip 20 W.

As the tide covered these rocks in the morning one came back To them in the late afternoon and from the shales Torkhope For a bag full of rock with two species of graptolites (Diplograptus) that are exceedingly common but only poorly preserved, There is also present a small "Lingula" probably a Leptaerius or Paterula. The "Orthoceras" of Richardson was not seen and there is no probability of "Pardoxides n Olenellus" occurring here. It's possible that a Triarthrus may have been gotten by Richardson. From the limestones near the base of the shales Torkhope got other fossils as Ampeyx, the keeled Leptaena etc. The sandstone gone 11014 is as described by Richardson. In the afternoon examined the shore for 3 miles to the north or west of Belle Burns. Just beyond the settlement the top of zone 8 is still present and as the shore follows the strike of the strata one travels a long distance before the higher bands come in. In the 3 miles traveled one found through zones 9 and 10. The latter zone was identified by the presence of Stromatoceriun, large Brantili, Ceprenus and Amphion tails. At 3 miles south of Belle Burns the rock had the aspect of the Leperditia bed but as none of these Ostracoda were pre- sent one concluded that the horizon was still in zone 10. The rock exposures continued for another mile or 1/2 miles, beyond which no exposures could be seen all the way to Daniels Horton about 4 miles beyond one view a 7 miles from Belle Burns.

At 4 P.M. we returned north to see the shore just north of Belle Burns towards Table Head. I walked over the top along the path while Torrenchief followed the shore to take the dip and stroll of the rocks. We then proceeded to the gastrolite bed (gms N.3) at the southern base of Table Head, while I collected in the isolated area of them redder Hack modular limestone of N.1 standing nearly vertical and just back of the botanical gardens of the houses. In certain of these beds Amphyx and Agnostus were more common than I had seen them at Table Head. While collecting here William Lynd appeared and the schooner was seen beating about outside south of Table Head. After seeing Torrenchief and talking over this surprise we did not re-visit the area until Monday evening. We concluded that we had finished the Table Head region and would go on to Carr Head. Every thing was arranged to go aboard the Vistena and at 7.30 we pushed away from the shore in the day with Lynd and Bland at the oars. A high swell was on and to me it looked dangerous to go out and board the Vistena. We landed safely aboard the Vistena and at once went to bed. He rolled badly all the night and Torrenchief after 1 P.M. was a very sick man.

Monday August 8-1910 Corn Head. Arrived at Corn Head small boat dock at 9.15 A.M. Stepping on shore at the Post Master's Mr. John Payne, or John Paine. In the afternoon examined a part of the shore along the north side of Corn Cove. Here one sees the conglomerate zone No. 15 which Richardson says has a thickness of 700 feet. These conglomerates consist of limestone pieces, as a rule sharply angled from the smallest grain to blocks 15" x 15" x 7" that must weigh about 100 tons. It is a helter-skelter unassorted mass of light grey magnesian limestone with all the crevices between the layer pieces filled in by the deposition, in which it was laid. It is the material laid down at the base of cliff without any weathering; all the angular pieces laid down as they fell. When there is a tendency to assorting of the smaller pieces these are then somewhat rounded. All of the material seen looks like that I & seen at Ingle Bay but then maybe material of these the goes up to No. 1, as all of these horizons have magnesian limestone of a light grey to dark color No. 2. As yet we have seen no pieces suggesting zones No or the sandstones O. Every now and then one comes upon zones in the conglomerate series of lovely bedded stratums like, dense and brittle, easily fracturing, thin bedded limestone in which are only saw worm burrows always arranged in pairs. Have a specimen. These beds are also ripple marked. We also noticed minute faults in these beds with a throw of 3 to 4 feet pitching outward. Associated with these limestone also occurs dull flaky scales with very smooth surfaces, I saw no prints. In other places the bedded limestone have more less of assorted flats lying pebbles.

About half way down the Carr Cove one came up on a thickness of about 15 ft of Haed shales interbedded with sandstone and flint. Within a few feet along the strike a shale mill pass into sandstone while the chalk bands are more persistent. In the shales grapholites are abundant and are set too large keys free of Phyllograptus, Tetragraptus, Dictyonema and Bryograptus besides others that I do not get recognize. This find of Phyllograptus was a great surprise and is very puzzling as to their position in this conglomerate, from above zone N. Logan in Biology of 1 Canada a 1863:292 states that con- tact between the sandstone of zone N4 and the conglomerate zone is maybe seen 17 miles north of Portland Creek. As this point is written five miles of Carr Head one only see this contact. If there is no mistake here the Phyllograptus goes over face into the Norian series and not at all into the Camdic. At Portman Park Conglome is said to be associated with Phe- lrograptus which would indicate that there is no break in sedimentation between the sandstone and conglomerate. In Carr Cove the strike in E-W, dip 35-40 S. A little farther along out around it is N.60 W., dip 30 S. On the Phyllo- graptus beds it in E-NW, dip 45 S. Sorting across Carr Head should run to the Long Range. Out there one see to tower high above the low lying prealane. Harleys map give them as from 990' to 2125' while the prealane of Ordovician strata represents one or more raised beaches. These do not seem to rise higher than 75 to 125 feet. Do these mountains represent third land against which the Ordovician was crashed? (Late - no, the low land is entirely faulted down)

Tuesday August 9-1910 Cow Head. In the morning returned to the Phyllograpthus beds discovered yesterday. This is taken to be in the lower part of zone 15 on Cow Head peninsula, but is not necessarily at the base of the division. It appears higher than the upper contact of the North side of the peninsula, Richardson says it is in the lower part of zone 15. For more material and added it to the collection of yesterday. Proceeding one through the north end of Cow Cove and about 15 to 20 feet above the lowest Phyllograpthus one or came up on another graphite bed. These are marked as of today and "graphite zone 2. Still further on we came upon two other graphite zones that are about 20 to 30 feet above those of zone 2. These are all the same large Leiozula like Helomella that we collected in zone No. 1 and No. 2. These are common but are hard to get out of the flint graves. With them are associated Orbitulidae rather large for or low an horizon. At the highest level occur the elongate Phyllograpthus. These are all marked zone 3. The graphite zones are associated with much redder flint that must be flint of destruction and diagenetic change. There is a good deal of this flint and it is more persistent than the Rock shale and as a rule iron ore than the limestones. The hashicords occurs in the shale (limestone) and in the tops surfaces of the flint. In one place we came upon one that had been chopped out by Richardson nearly 50 years ago. The surfaces of these flint layers are often covered with small rounded pebbles = local thin sheets of conglomerates. In other places the limestones are persistent almost all

"thin bedded" crenul limestone, with almost no shale and without fossils other than the jointed room lumps that go vertical through the strata. Some of these crenul limestone are also conglomeratic but a close inspection shows them to be only foreign material but are intrusion of conglomerate (data conclude that this are true crop). In other places one comes upon limited patches of these thin bedded limestones that lie between the conglomerate masses. Either this material was deposited in holes between the piles of stone or from time to time the shale mass slipped down into clefts and crevices and or pushed into the mud and gauging out of sloped Lata concluded that they are fallen in large blocks, and the contortion were due to folding these beds under went before deposition in June 19 (1917 = ?, fault brecciation). In the afternoon started in along the north or east side of Carr Head peninsula and crawled all around it. Just a little distance along the shore from the village houses one sees large masses of thin bedded somewhat sandy limestones (sometimes about one inch in thickness) separated by themore and often lumps (in places a whole). Fossils are very scarce but we managed to collect a number of specimens of Lingula that may be accum. crata, L. marina? Dikellocephalus and Myloglyphea. These indicate Lanotgan or uppermost lower Cambic time (All other count to Daleett Cobs - 1917). There is so much of this upper Cambic material that one concludes at first it were deposited in place. Some of these exposures show faces at least 20 feet high and fully 100 feet long. The great mass if it seems to have the normal dips of the conglomerates but parts of it is badly folded and even crumpled. As one goes along towards the outer

far of the peninsula other good and even greater pieces are seen but in these are few of the Lingulas. All of these masses appear To be beds in place and some have one end cut off by a fault against which rests great masses of the heavy bedded conglomerate, Smaller masses are found in the conglomerate at all angles and are all of them are more or less bent, showing that these when Cambic strata were considerably folded before they stood in cliffs to be broken down and deposited in this sea of Ordovician time. They were the debris of a shallow sea as there is much ripple marking. As one goes out farther and especially around the south western point of the peninsula, one sees a great deal of other than bedded sandily limestones much like those of the Cambic but these are of sand size network and are not crumpled this we conclude that these are deposits in place and of the time of zone w. Nothing organic was seen in them. Associated here with these beds are hearin bedded granular probably old metric limestones also deposits of the time. Above these regularly deposited beds are very thin masses of conglomerate in which the flat limestone pieces are usually of small size and apparently partly of the after Cambic deposits. These pieces are nearly always angular and while the majority lie in the plane of the bedding [flat] still the mass is illy arranged. This zone of conglomerate may be 30 feet but thick. When one gets into Low Cove into higher beds away from of this the bedded conglomerate material is gone and we comes upon layer and irregular masses of grey limestone from the size of a pea to 150 true pieces. In these bunches one can

"I've studied great groups (Lamond), the Bay and slender Orthreus (Septem apart) and the Asephor tails. Above all this come in the gneissite beds. As the strata dip south westward naturally the ones one can find this afternoon just beyond the village houses are the oldest of any seen of gne W. As apparently none of this material is here of deep Cambric age it would seem that the sea of gne is time begun to form on the strata of this time and shortly after on those of the Phyllographus beds, and higher beds up to gne II. Nothing of gnes 12 and 13 was seen and certainly nothing of the sandstones of 14. As the Upper Cambric beds the strike is N. 70 E., dip 32 S. One foot mile beyond it is N. 80 W., dip 22 S. Near the lift house it is N. 35 E., dip 52 S. There are many faults usually small ones of a few feet, but several large ones were seen with a throw of at least 20 feet. The strike ranges from N. 55 E. to 75 E., and are usually vertical. These layer faults are probably not faults above but rather the edges of the great blocks of deep Cambric limestone. They look like faults but are in more probability not such. On the other hand the smaller faults are truly such for in several cases one could see the two edges of the faulted block. The thickness of the conglomerate must be more than 100 feet as given by Richardson. From Steaming Island to Car Cove it is more than 1 mile across the strike, with an average dip at 35 degrees the thickness will be nearer 1000 feet if not more. (cannot be much)

Wednesday August 10-1910 Cws Head. Spend the morning photographing the conglomerate around the eastern or northern side of Cws Head or Cwr Head Haven. Also Cow Cove shore. The great Mbl Cambria block out of which one picks the fossils yesterday is undulating and reclining by conglomerates in thick beds. To the right it appears the cut off by a fault but this may be only the end of the mass around which the conglomerate filled in. To the left it is clearly broken off with a very irregular edge into which the conglomerate and other smaller pieces of the Ml Cambria are details. This block is about 175 feet long and is about 20 feet thick. The of ended pieces in the foreground are also Cambrian and as the dip of these blocks is the opposite of the great mass are in fact other blocks underneath the great mass and in part the flexed or bent part of the great mass. It looks to one as if the Cambrian had been folded before it got into the conglomerate (Probably not if a fault breccia). In going eastward along the haven one sees several of these large Cambrian masses ranging from about 75 feet to 175 feet in length as spread. In character they are all thin bedded but the other detail is not exactly alike and each block has a somewhat different character. Then for some have Lingulae and trilobites, another only Lingula, while others seem to have no joints. All of the associated conglomerates of this shore appear to be made out of the same kind of rock as the Cambrian. In other words all the conglomerates here is in the main composed of the angular pieces of the Cambrian from the size of a sand grain upwards 175-feet long. One sees no foreign materials as granite, schists or sandstones. Of shelling siding there is almost none. Therefore no thrust movement. The great masses have about the same dip as the dip of deposition That in they lay fairly flat on the floor of the sea bottom at the time of fall in.

Climb of the Long Range Onts. From head of Can Core Hills, sorting eastward. Long Range Onts., On old periplain. Low fore-land apparently from 70 to at most 125 feet. Between 2 elevators brooks. Can Head Station. Can Core, Can Head Village Can Core.

Looked again at the Phyllogaptus lowest horizon strata, It is a a series of thin bedded dark limestones that have been changed more or less into flint interbedded with black lignite and sandy shales that cap the grit slits. Locally in the flint there are small rounded pebbles usually from 1/8 to 3/8 inch but in a few cases some coarse rounded dark limestone boulders up to 20 inches across. This mass of Phyllogaptus lies above a thick and once defined conglomerate, the horizon with the large blocks up to 700 tons. It is 15 to 20 feet thick or far as seen (the sea covers the outer part) and has a visible length of about +600 feet. Both ends are in the ocean but to the west its place is occupied by conglomerate, if a displaced mass it is the layer or far made out on Cow Head. In the Cow Cove conglomerate saw one poor Eurystomites about 7 inches in diameter. In the afternoon visited Steaming Island. Found it like con- glomerate like that of Cow Cove. Blocks space sizes up to 10 feet square, of angular magnesium limestone and some detritus, all of a grey color. In a few places saw faint outlines of gastropods in section none of which I could recognize. It now appears to me that none of this conglomerate from Steaming Island to Cow Cove has an age of younger than 6 . In other words the material is one of 4,5, 6 and possibly 7: Nothing higher. Picked up on Steaming Island a fossils that may be a sponge. The dip and strike of the Steaming Island conglomerate is that of the Cow Head rocks at about the little light house. There is nothing here to suggest an anticline. The structure is all monoclinel from here to Cow Cove,

"Further in listing from Steaming Island across to the eastern head of Cows Head Harbour, one sees the rocks striking up with the same landward dip. This is not in harmony with Logan descriptions of 1892, Hist. of Canada 1863, where he states there appears to be an anticlinal fold between Steaming Island and Cows Head. There is not the slightest evidence of glacial transportation. Frankel spent the day alone practicing east and most along the shore to near Parsons Pond (about 10 miles) to see once of the conglomerate of zone 15 and its contact with the sandstone of zone 14. Its outcrops read as follows:- "From Cows Head to the point in the east side of Yellow Bay the beach and cliff are formed of very fine sand chiefly quartz which is gradually building the cliff higher through hard by vegetation. Just south of the point mentioned above, on the reef at low tide are visible dark gray fine grained sandstone, separated by thin dark sandy shale partings. There is an estimated thickness of 200' with the top concealed. The attitude at top is N.75 E. dip 48 S and at the base N.65 E dip 48 S. A shade of green is in the color of the sandstone. No fossils observed. Below the sandstone in supposed con- formability is a zone of brittle, small checked, dolomitic siliceous limestone containing fragments of trilobites supposed to be Agathus. There is perhaps 50 feet of this. The color is a dark olive color and on breathing it becomes whitish gelatin. Below lies 50 to 75 feet of orange conglomerate, con- stituting of large and small blocks, some being made of

"difficult strata. Below lies more limestone like the preceding holding many flat and lim spired gastropods, a celliform, and fragments of Bathymus. This zone is considered to be about so feet thick. Below lies more conglomerate roughly like the preceding, estimated at 50 to 70 feet thickness. Then more limestone like that previously described from which was obtained Refresquira, Bathymus, and a large lim spired gastropod. Below to the sandstones of Division 14 the wells are almost wholly conglomerate. "The frequency of stratified material, like those of Car Head containing Phyllopterus and Diellrochilus are here not marked, nor are true or false zones of coal being seen during the day. "The attitude of the conglomerates varies little, the general strike being between N. 60 E and N. 70 E and steepening from a dip of 45 S to 64 S at the point whereof the sandstones of div. 14. On the reef at a distance not greater than 100 feet from the conglomerates, sandstones identically similar to those of Table Head appear in just as precise striking N. 65 E, dip 65 S, almost the same attitude of the succeeding conglomerate, in which Hocks of a character similar to the sandstone and interstratified shells were observed, "No evidence, either internal in the sandstones, or the conglomerates, or on the contact between them, exists for the hypothesis of the coal reaching their present position by thrust faulting. This point is about 1/2 miles from the

"S. N. of Shallow Bay. About 1 mile east from the contact the sandstone has a strike of N. 65 E., dip 74 S. and there is a gradual steepening with proper earthward. 1/2 miles north of the centre the sandstones have the attitude N. 86 E. dip 80 S. About one mile south of Parsons Pond the sandstone becomes nearly vertical and in one place dips between 85 and 90 N. with a strike of N. 65 E. "Note: The fossils found today, with the exception of one cephalopod obtained from a flood in the emyl, are obtained from rock in which they were primarily deposited, this rock being deposited as a sediment in the conglomerate division, unless it be assumed that it be a flood fully 2000 feet long by 50 feet thick" "At the last appearance of the sandstones today, pale was becoming a more pronounced feature, so it is judged that zone Ch.3 was being approached." The conglomerate thickness changes somewhat from place to place as Torndofel saw pieces of 14 included and almost nothing of the thickbedded Cambria. Part of the emyl oras made up of material like that of Bow Core, i.e., 7 pieces of 4-6. It is now evident that the emyl. Division N - is a marine deposit in place and directly overlying the sandstone division 14. In all probability there is a time break between them, during which time all the strata previously to 15 once elevated above the sea. As the Ordovician landfall in here not over 5 to 7 miles wide in front of the left Long Range the question arises did these

Cambria and Ordovician strata formerly extend over the top of these mountains. The thickness of these deposits up to the crags, is at least 3730-5067 fathoms and the mountains are now a little more than 2000 feet high. It is probable that the mountains did not come into existence until after the Ordovician strata were deposited and before the Anticosti local beds were laid down. The igneous masses so well seen in the Bay of Islands and southward are of still later origin and are the probable cause for the meta- morphism seen in the strata of the southern half of the island. They are older than the Carboniferous as these strata are unaffected. The period of great deformation is as yet uncertain to me. The foreplain of the Low Range is a decided one and in places is deeply clef by the rivers. Today there is almost no erosion because as yet one have not seen a muddy river, All of the strata is held by the vegetation and the streams have no pedestals. Bridges exist here that in Ohio and Indiana would not stand six months. The foreplain therefore appears to be certainly as old as the Cretaceous and may be older.

Thursday August 11-1910 Sally Cove. As the wind is in the wrong direction and the Verena cannot sail we propose to crawl to Bonne Bay in two days. At 8 A.M. are landed on the sand spit that separates Cow Head Martin from Cow Cove. All the way from Cow Cove Pauls Inlet the land is very low and is made up of glacial material that has apparently been washed by the sea, granite boulders prevail. Pauls Inlet is a very low tidal estuary that runs back to the foot of the Long Range Mts. Small brooks are said to terminate in it. About 1/2 mile west or south of Pauls Inlet we came upon the first conglomerate (Dir. N) exposures. Here may be seen a very crumbling limestone mass (1/4 mile long) of much folded thin bedded grey limestone that looks like Upper Cambrian material. In a few places lying over the edges of this thin bedded material is lime- stone conglomerate but none of the pieces are large (usually a few inches). As this mass was much folded we concluded it was a foreign block in the conglomerate. About one mile east of Martin Point once conglomerate is ex- pounded and from here all the way to Sally Cove (4 miles east or north of Green Point) in the conglomerate exposures seem three lines between the thin and thick beds of conglomerate series of their bedded grey to dark bluish limestone interbedded with shale that is once a less dark but not bituminous. These limestones are nearly more than one inch thick while the shale may be an inch or less or even two inches thick. These thin bedded limestones

are not crumpled and as they may be traced in the extreme for 1/4 mile along one of the points must the interbedded deposits in the conglomerate series. I saw no fossils being found in these thin bedded limestone or in the shale. On the north side of Martin Point we saw a fine exposure of the conglomerate series. In the conglomerates, the limestone joints are thickened beds, never in large masses as in Cow Head Head, and the beds of conglomerates are regularly bedded. Between them are the thin bedded limestones and shales. The grain are very about 20 feet thick. There are also thinner shales. These are indigenous deposits and are not transported rock of foreign material. No fossils were seen though there should have been some from the character of the beds. East of Martin Point the strike is N.70 E., dip 50 N. At Martin's Point appears mostly N.40 E., dip 30 S. There thus appears to be an arc here. Today we saw nothing in the way of large masses of limestone in the Crag, as at Cow Cove. The pieces are all small and the bedding of the Crag, in our district and especially so at Martin's Point. We stayed one night at Sally Cove, which is 4 miles north of Green Point, at Morris. A school teacher her g by name of Miss Carson of Harve de Grace, E. O'Hdl.

Friday August 12-1910 Bonne Bay. Left Dalys Cove at 6.30 A.M. for Bonne Bay. A dark day with rain on and off. At Green Point we saw a large and fine exposure of the conglomerate series striking parallel with the shore and the strata standing nearly vertical. About 400 feet of thickness are shown. Near there are then hidden grey to dark coloured limestones interbedded with more or less cherted shales. Interbedded occasionally are thin beds (6-12 feet) of typical conglomerate in all of the pieces are small although they may be nearly one-ton feet long and 3 to 4 inches thick. Andward gradually the limestones become less dominant and the shales are almost without limestone. In these upper beds there is an ocean sand then large (?) conglomerate. About 100 to 150 feet above the base are some considerable Dictyomena and the numerous Necr Oenocephalus. No other fossils were seen. The beds are considerably faulted, usually the throw is small but in one case it may have been as much as 150 feet. The strike is N.80 E., dips 74 S. There can be no doubt that these rocks belong to group 15 because of the presence of the characteristic conglomerate of the group. We take it that this over is in this division (?) the upper part) where the conglomerate gives way to regular bedded material as is the case to the east of Cove Head seen by Torinholde on Wednesday Aug 10, at Shallow Bay. There can be no doubt that Div. 15 changes much along the strike or that in one place conglomerate predominates and in others, and especially towards the top of this division, bedded clayey sediments that cannot be interpreted as falling in masses.

In the dark shales of the upper part of the Green Point section there are occasional thin limestones and once nearly a thin conglomerate zone. Usually these limestones are gray and sometimes text decidedly while the shales are not grayer but are plaine. One of these limestones about one inch thick was clearly sun-cracked and on smell or with the edges of the prisms were elevated or that threated or edge had a thickness of 1/2 to 2 inches. This is a clear case of long sun drying. The other way beds did not appear on their edges for here and once their character to the graces of that sea. Further there was no evidence of sun cracking. The northeastern point of Lobster Cove shows in the lower part of the section here a series of dark to black then bedded to Jopery shales with some greenish sandstones like those seen by Towerkful in Hallings Bay. Higher the shales give gray to one and one of the greenish sandstone but from here we sees an occasional thin zone of the characteristic conglomerate. The dips here is from 40 to too degrees in the direction of about 10 degrees east of south. The strata are here more disturbed than farther northeast. Crumpling and crushing becomes once and once marked as we proceeds to Catt Point Lighth. Some metamorphic changes are also noticeable as the appearance of flint zones. Towards the Lighthouse point the greenish sandstones predominate again. No conglomerates are seen here. It is therefore apparent that the change from Dir 15 to 76 is a gradual one and

"This at North Point Left one is in the lower part of Dir. 16. In Division 16 Logan states "Greenish sandstone of chloritic aspect, made of apparently fine grains of quartz and feldspar, with a few scales of mica, mixed with greenish argillaceous matter? To me the chloritic character is not due to the changes these sandstones have undergone, but is derived from the land (probably Long Range) of that time. We have four samples of the rock and they should be examined for the chloritic character. In several places along Rocky (Roke) Mountain one sees the greenish sandstone of Dir. 16 but in striking across County from here to Morris Point [Reddy] starting the County is buried under the black soil and gravel. Arrived at Morris Point at 6 P.M., stopping at Mrs. Kennedy's. The scenery here is beautiful and very romantic. High hills and iron mountains in all sides.

Saturday August 13-1910 Bonne Bay. Crossed over from Morris' Point to Bonne Bay and as, it rained once a less stayed at the home of Ambrose Donnette where we are boarding until the boat comes. In the afternoon walked to the head of South Arm about 4 miles inland and south. About 1/2 of a mile south of Bonne Bay one sees the first of the sedimentary strata here very deary reddish fine grained conglomerate in which the pebbles [illegible] roughly exceed 1/8 inch. It has a greenish color and it looks as if to be in (?) horn fawn (?) Dirim 16. A little farther inland one sees the greenish fine grained micaceous sandstone just like those we saw yesterday near the Light House in Dir. 16. The dip here is S at an angle of about 65 degrees or more. Farther south appear the greenish sandstones interbedded with shale. At the first large brook (1 1/2 miles south) as far out as the shore and therefor cutting the sedimentaries appears a very greenish weathering intrusive rock (?) of which I have a sample. On the other side of the brook one sees more of the sand- stones and gradually these give over to sandy shales and finally to much crumpled and somewhat altered greenish shales. If the southward dip were maintained these shales should be on off of Dir. 16 and they may be. No fossils are seen. At the head of South Arm the shales seem to dip to the SE. Standing nearly vertical but this dip maybe only local or even deceptive. On the opposite side of the Arm just south of the prominent headland one notes the strata dipping S at an angle 65°

"visually" These sedimentaries are traced to a high mass of in- trusive marked on the map as [illegible] feet and 1270 ft. h't., it is of the same character as the high hill on the western side of the [clinite] arm. Between them lies the crumpled greenish slates and therefore these intrusives are younger than these sedimentaries and while at the time of their introduction deep seated. Across of the places where large forests came into the bay we see high accumulations of mira fars. These rise to 75 (and from to 100) feet indicating this must of a higher level formerly of the sea. Farther inland towards the high flat topped mountain [illegible] there appears to be another flat surface. If this is an elevatory level it indicates a former water level at least 300 ft and it may even be higher than this. Frank Jee spent the afternoon climbing the flat-topped mountain west of Bonne Bay. His notes are as follows:- "Crest of Derrid Point the mountain is shown on Norley's map as 2336 feet h't. and consists of chloritized dolomite. This dolomite has been subjected to much pressure and hardly a foot bricks square exists that does not show schist- sides with a few slabs developed in some places one inch thick. The metamorphism has developed round nodules of a light brown highly cleatable mineral that is also developed in veins up to three fourths inch thick. "The top of the mountain is extremely level gently rising inland where it met on the angular gravel and

boulder of divite, the result of the inoslation of the divite aftering scraped clean by glaciers, me could imagine himself in the Texas prairies. This level plain extends as far I can see. I sat on this plain isand for about 1 1/2 miles and found it extremely level. A crayon, run it out in the bouldus, can't be divine over this without meeting any distortion. No trees once seen on this plain but patches of grass, rock patch being a fox. On this upland plain are higher elevations, residuals on the old base level. Looking in all directions the level of the hill tips is the same level of this plain. This plan truncates all the rock systems, Pottsgrie, Cambria, Ordovicia, and Jgreus, having all kinds of structure, folds, faults, steeply dipping, oriental and massive orelly sandstones, shale, limestones, conglomerate, divites, and granites are rise to the level of this plain. Over the 20a and Bay are lower elevations. " About 800 or more feet below the old plain level is a system of broad flat floored valleys in some cases one half mile wide. This vally is cleared with angular gravel the result of breaking down by insolation of talus rocks and gravities. These valleys have lakes and the gradients of the brooks is by no means high. I descended the mountain from the plain at another point than where descended and then followed a brook to the Smith Gome about a 1 1/2 miles from Bonne Bay. After leaving the level of the valleys above described the brook became a river

"falls flowing in a narrow gorge until about 70 yards before reaching the Bay, the point of leaving the hills being a gulch cut in an old delta deposit, the level of which is about 60 feet above sea level. Several other deposits of similar character and elevation been seen at Horn's Point and at one near Brody Point. " In the above both the definite holds until about 250 yards from the Bay where appears about 70 foot of sandstones like those of division 16. These appear to have been cut thru by the divide. Below the sandstone lee green, red and black shales striking E-W and dipping 70 S. All have been subjected to metamor- phism. " The old base level is a plain case. It appears that this base level once developed and than the land was uplifted about 800 feet permitting during a shorter period of stability the development of the broad flat- floored valleys. This was followed by a second period of uplift to a delta level than the present in which the streams cut down below the present sea level forming the deep indentations of St. Bart's Bay, Bonne Bay, Bay of Islands, etc. Glaciation fell and accentuating and grounding the gorges and valleys. Following glaciation was a period of subsurgence followed by progressive but intermittent emergence during which the terraces were devoloped.

"The tintus of the mountains [illegible] color due to the oxidation of the iron of the clorite. This gives it its brown else seen in the sunlight." The highest plain is probably to be correlated with the pre-Cretaceous elevation and at the close of the Cretacic came down by then, or level. During the Tertiary was elevated on the elevated welling one sees from the cliff top. Just before the glacial period came another elevation (nearly 3000 feet) to an altitude at least 400 feet higher than at present. Then followed a long period of glacial scouring. The mountain range, to about 400 feet more than at present. Since then the sea has irregularly and gently withdrawn to its present level and is probably not yet through going down. Sunday August 14-1910 Bonne Bay, As our doctor is not athand we remained in the house. In the afternoon it rained hard.

"Monday August 15th 1910. Bonne Bay. As one Schooner has not yet arrived and as it threatens to rain I remained in the house all the morning writing letters to Rosie, Ellick and Botmel. Our boat came about 11 A.M. and we heard of it by noon. The men came to us on the afternoon ferry. We got to the Vertona about 2:30 P.M. and at once started out to study the section along Deer Brook Way which is the northern fork of East Arm not far away from the quiet Reddy Harbor. Just outside of Reddy Harbor and approaching Deer Brook Bay we went ashore to study the strata. There we see more or less clearly bedded magnesian li, and dolomite that are more or less crumbled and weather out irregular small mass gyosts. Near the top of the section, takes a loose piece, ore get what looks like Billingsella and so put down small gasteroids that maybe Ophelita. We may have seen 450 feet of strata and these four lots of fossils come out of the upper 75 feet. In the lower half of the 450 foot seem much of the material is still almost a whole but it is still magnesian. At about 150 feet above that base there are solitary gones (in we get what appears to be extraorda) and intraformational conglomerates. The pieces are flat and thin (yet if you did this) and lie flat on are piled "edgewise." The strike of these beds is N-S, to N. 10 W., dip 45 to 60. Near the middle of the 450 foot section there is some cleft besides that mentioned above. At the top of the section the beds are considerably disturbed and here the metamorphism.

is more marked than in the Upper beds but all show some alteration. Near the Lead of Aber Dyfrdwy we had the men over across from the Ordovician shore, theday across to the eastern side. The distance may have been 1300 feet and here we came at once upon the Lower Cambrian metamorphosed shale interbedded with thin bands of quartzite. This is Rickardson's C9 and is 68 feet thick. They strike N-5, dip 28 deg. At about the middle of this zone, but found as loose pieces along the shore, I got slate jaws of a thick but very short Sallterella. Below the shale comes zone C8 that at the top is a grey to light blue limestone composed of small comminuted fossil material. In the little while collected during a rain we got Ptychus, Paternula and Platyceras primacera. Drilling thrust our work by in tomorrow. The next day we collected again more. The common fossils are Ptychus, Sallterella and Deltellus. Deltellus are rare. Of Platyceras primacera we have at least four. There are probably a few more species not listed here. Most of this material came from the base of C8 but the Platyceras came from near the top. Zone C8 has a thickness of 13 feet and is almost as described by Rickardson.

Tuesday August 16 - 1940. Bonne Bay. Started on the east shore of East Arm before 7 A.M. to begin our days work other are left off yesterday. A little rain in the early morning and one at 5 P.M. He spent (from 8 to) all the morning cracking the limestone of zone C-8. See notes of yesterday. [Lotus connects to C-6 or zone 24]. After lunch are continued the section southeast along the east shore of East Arm. For at least one mile the dip of the strata is undulatory and mainly along the strike so that we remains in zones C-8 and C-9. In C-9 we found today a few heads of Olenellus, considerable of thorax and tail of a large Orsinacis, several specimens of a small Asclacrimus and a piece of a small cystid in which the plates are small and irregularly arranged. Saltarella like those of yesterday were found in the condition of iron pyrite. The shales of zone C-9 as one proceeds southeast become more and more metamorphosed and cleave readily at right angles to the bedding almost like slate. Otherwise one might get some puffs. Furthermore these slates have many crumptions that stand vertically. They are somewhat thin, from 1/2 to 3/4 inch thick and from 3/4 to 1 1/4 inches long. There is no organic center but seem to represent filling of some habitation. Jones C-4 to C-7 were passed over rather rapidly because of the shores turning and one going over the strike and not along the strike as here before. Then for all these zones are much compressed and cleaved and the.

"Limestones have less fossils than gme C8. These limestones and shales are just like those of gmes C8 and C9. "Gme C3 is markedly different from the liple beds being a white to pindle (this mainly due to weathering) fine grained quartzite with alterny shales. No fossils more observed. There is a little of ripple marking but little or no cross-bedding. "Gme C2 is practically like C3 and it is in the lower arenaceous limestones (? dolomites) that are got Glenelle, thompsoni, Orsmacis vartmontana and Bathgenstus holo. [illegible] (from J.T.). Most of the material is entire but most fractured and somewhat obscure due to the thin bedded shaly nature of the material and the weathering. "Along the northern part of East Arm one notes that the strata along the eastern shore have the strike of the shore and that the entire mountain side has the slope of the dip of the strata. If this general dip is maintained then it is evident that the Cambrian formerly crossed over the Long Range Mts of Laurentian rocks. In section they are as follows [see Logan, Geol. Canada 1863: 865]

"From Tower of the following. The attitude near the mouth of Deer Brook Bury is N.18 dr., dip 32 dr. About a mile southeast, N.50 dr., dip 18 S. Here there is a fine development of joints striking N.30 dr., and N.60 E, forming fine rhomboidal blocks, where the strata begin to stand in end just north of the second small brook going south from Deer Brook Bury. The strata have the attitude N.50 E., dip 80 dr., and following that the strike is anything but the dip is always southeast. Near the point where the first attitude was taken there is a system of parallel faults striking N.20 E., dip of fault planes 64E. The south side has been elevated totally a matter of 25 feet or less. Three fault planes were noted. "Associated with good Glenclues but a large design than one C.2 we got 3 good and many from Cyclacimidae. These are about twice as large as those collected yesterday in C.g.

"Wednesday August 17-1910 Bonne Bay. Started out at 7 A.M. with the crew and returned to the boat at 7 P.M. He examined the east coast from the point stopped with yesterday to the southeast bay of East Arm and then came over to the headland between the southeast bay and the southwest bay. Then examined the entire west coast of the East Arm to near the promontory that faces Reddys Point. He began collecting in the slate, with Olenellus stopped at yesterday. After working around here for nearly 2 hours we got only 2 good Olenellus (entire) and some imperfect ones. yesterday we called this zone C 2 but today we are not certain of this as Richardsons section today appears to be wrong. He will re-measure the section tomorrow and then definitely locate our zones. Going south from this locality (which is about 1/2 mile north of a little sour mill) one passed over the quartzites of zone C 1, but beyond this we did not find the limestones of zones B 7 and B 1 nor the Laurentian greises. The anticline noted in Berl. Canada 1863: 867 we also saw but the southeastly dip is practically continued to the head of East Arm where the quartzites of zones C 1,2 and 3 again appear along the shore. There is certainly something wrong in Richardson's section. Crossing over to the peninsular headland at the head of the East Arm, and from here to within one mile of the promontory facing Reddys Point the entire 9 miles.

of the western shore of East Arm is if once a less leary Ledded magnesian limestone and dolomites rather darker [in places a blue-black] than the lown limestones seen about Port au Choix and to the northward. Fossils are exceedingly rare due in part to the magnesian character of the beds but mainly to the somewhat metamorphosed and especially cleaved structure. In places these limestone are sharply folded and even cracked. North of the layn some miles of the western shore the dolomites are rather like No 8 at Port au Choix and here one sees the depressional Maje Torch phenomena like steel and another depressional geo hyford. This limestone we take to be No 8 and so far as I could judge is the highest zone of bould clay the entire western shore of the East Arm. All of the limestones seemingly are Zones 6, 7 and 8, but 5 may also be present in the Headland at the Land of the East Arm. It is possible that even No 4 is present but as to this we have no evidence one way or the other. Passing from south to north through the East Arm one notes the undulatory lay of the beds and as the shore is also more a low lying the strata one does not rapidly get into deeper beds passing to the north. In general the dips is southeasterly but locally it may be anything. I can or whales in these limestones. Therefore the great limestone series of the north is maintained to this place.

"Thursday August 18 1910, Bonne Bay. I collected all the morning in the Lower Cambrie limestone zone C 8 (equivalent C.G.) of the east shore of East Arm. Got many Ostrus Crenus and other fossils. Torahofel and the men returned to the little saw mill of the east shore where the apex of the Lown Cambrie occurs and he only make a section from this place to the top of the Lower Cambrie. He got a very good Olenellus Thompsoni. In the afternoon Torahofel and I started in at the former lot that faces Reddy's Harbour and crawled along the shore south into the main arm of Bonne Bay, beginning at the east shore where the dead land is highest we saw no fossils but ascended the horizon to be 7 or 8. Just where a little core appears (practically the promontory still and not very so far higher) we got a few peculiar opercula of Madlura. This lot, a fossil is marked, Lot no 4, fifty feet higher we got Agnosthis lateralis and Lepadidita. This lot is also marked 4. This horizon I believe to be in zone 8 because at Mirijan it is associated with Piloceras a fossil also found in Newfoundland in zone 8. Lot 3 came 28 paces higher. Lot 2 came 130 paces higher, it consists of gastropods that remined of Divisions 10 and 11. Lot 1 came 50 paces higher. Here we got Amphilin tall and Lepadidita in abundance. We take this horizon to be in 10 and most probably in 11. The prevailing dip of all these strata is about 60 degrees to the south west.

"As to this domain all the strata are magnesian limestones but Shiffa comes in a great thickness of dark blue slates that cleare easily across the bedding and one therefore sees not a trace of fossils. It may be a half mile across the strata and certainly it is three-eighths [illegible] mile. Near the top the slates are grey and here Torrishofel saw the beginning of a great mass of the limestone conglomerate of zone 15. How thick this zone is one could not determine, Shiffa came in the greenish micaceous sandstone of zones 16 that we also saw on the western side of the Orain Garm, a little south of Borne Bay village. So far we have noted many little faults but no great ones and certainly there is no evidence at all present to indicate or thorough faulting. There is no slickensiding except when we can see the faults in where a little marking has taken place. The Take Head limestone divisions 12, 13 and 14 - are here represented by the above mentioned thick shale series. Division 15 is probably also more a lens shale here, but some of the limestone conglomerates are present seen today, Lee Logans remarks in Berti Gana In 1863: 869 and 292. Logans C 10 to D 1 both inclusive Shale to represent the Upper Cambrie on the basis of the fossils or pet on Allen Bortch Bay, in that for Wind conglomerate and at Flowers Core, (see f. 867-8). There is a quartzite here as at Flowers Core (Division 3). Had Torrishofel made a section in the morning of the Lower Cambrie. It is as follows:-

"The section begins with the lowest observed strata on the left side of the East arm of Bonne Bay at a point just north of the main power saw mill. Ascent was made of the small brook in a distance of perhaps 1/4 mile but in this distance the series was determined as an ascending one. [For whatever reason I saw any Laurentian grains here as may seen by Richardson, on the fire side of the brook] Once more given if the grains lay about a than usual and we assume that it is close by but the joint is absent.]

"[illegible] disturbed but generally the strike is [illegible]. Thickness 200 feet. "June 10. Pinkish and yellow quartzites interstratified with a few thin sandy greenish slates. Much schistosity developed. Contains entire Clenellus thompsoni. Thickness 50 feet. "Junes 1 to 10 and a part of 11 appear to equal Richardsons Division A. "June 11. Pink and white quartzites in heary beds with strike N. 35 E., dip 50 de. Has a few green of sandy slates. Almostiddled in places, with quartz veins of the milky variety. Thickness 280 feet. "June 12. Gray sandy slates much cleared with some quartzite. Thickness 100 feet. "June 13. Some disturbance may effects the strata, the strike changing to N. 8 E., dip 33 de., and then follows an estimated thickness of 25 feet of pinkish quartzite(?). (14) Gray slate with rarely thin yellow quartzitic bands. Slate much marked and with a finely cleavage developed perpendicular to bedding or at a high angle. Thick. 200 feet + (15) A concealed June at base adding but also 25 feet more. (16) "June 14. Dark gray much nodular gajzed occuring mg. li., holding papemtag Clenellus, Strike N. 13 E., dip 46 de. Equals Richardsons B7. Thickness 30 feet. "Upper part of June 11 to 14 include equal Rich. Div. B. (17) "June 15. Gray glistening slate of dead shades. Almost a phyllite. In places micaceous. Contains thin yellow quartz- ites marquling the bedding and much cleaved at high angles Thickness 72 feet.

(18) " June 16. Dark gray nodular metamorphosed mg. li. Like preceding and holding fragmentary olenellus. Strike N. 20 E. dip 60 br. Thickness 38 feet. (19) " June 17. Dark gray much cleared slate with thin yellow quartzite. Thickness 72 feet. (20) " June 18. Nodular mg. li. Holding Haell chert and fragmentary olenellus rarely, Thickness 7 feet. (21) " June 19. Dark gray slate with nodular layers, thin layers of nodular lime shale, and beds of quartzite essen- tially thin but may go to 10 inches. General strike N. 30-E., dip 54 br. Thickness 60 feet (22) " June 20. Sandstone splitting into prismatic blocks. In old light blue to drab. Minor fine lamination. Thk'd. 4 feet. (23) " June 21. Nodular, much cleared, gray slate, somewhat sandy. Thin quartzite up to 6 inches are interstratified near the base with a fine blue-black shale. Thickness 68 feet. "June 15/21 equals Richardsons C1, C2 and C3, (24) " June 22. Nodular mg. li., clay limestone with chert nodules showing very small fragments of fossils. Once a shale thin limestone and has interstratified cross-bedded quartzite. Old? li. a bluish-gray. Much metamorphosed and cleared, Thickness 36 feet thinning southward to 27'6". Equals R.C. 4. (25) " June 23. Blue, black and gray slate with thin yellow quartzite that are cross bedded. Strike N. 34 E., dip. 30 br, Thickness 30 feet. Equals Richardsons C1, 5. "Has much peculiar tracings. (26) " June 24. Nodular limestone 8 feet thick increasing

northward to 20 feet, due perhaps to shelly limestone being more limy. Very frondiferous. Equals Richardsons C.6. [He eroded in error the joints as coming from June 22]. (21) June 25. Circular more a less limy gray slate inter- terstratified with some pure dark slate, the latter containing interbedded yellow cross-bedded quartzites up to 6 inches. Strike N.24 E., dip 32 W. Some of the shale beds changed to flint. Holds Olenellus, the small Aglacinidae, a sach cystid and the psritized Dalterello. Equals Rich- ardsons C.7. Thickness 70 feet. (22) June 26. Gray to dark circular limestone, Rich- ardsons C 8. Thickness 13 feet. (29) June 27. Bluish-black slate with Dalterella casts, Richardsons C.9. Thickness 68 feet. "The summit of this section is found at the northern of Deer Brook Bay." This gives the Lower Cambrian here a thickness of about 1728 feet against 375 feet at Labrador, Richardson made it 1711 feet. He are in agreement as to thickness but cannot agree to his definitions of the various zones given in his Divisions A and B. What the original total thickness of the Lower Cambrian was one cannot tell as in all places seen by us the section terminated in the sea but ac- cording to Logan upon the zone C 9

"The Ordovician succession here is practically like that to the north with one marked difference. That are dolomites and limestone in the north to O1,3 where shale followed by sandstone, while here at Bonne Bay the shale phase appeared earlier, firstly as early as the time of M or even L. The shale phase then con- tinued with sandstone and limestone conformable changes to the end of Ordovician deposition. The Long Range Mts take their highest elevation in the region of St Johns Bay and then this altitude of the old Laurentian mass is maintained to the south side of Newfoundland. This axis is of very ancient origin as it is notable that the Cambrian of the two sides is very different. To the north of St Johns Bay the axis may not have existed as here the Benjic crossed it. In Ordovician time these seas also crossed it in the north but to the south of middle Newfoundland there appears little or deposits of this time. The great diorite intrusions are post Ordovician and as none of it cuts the Carboniferous must be older than the latter. I do not as yet know its age closer than this.

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