Field Notebook: Nova Scotia 1914

doc 108 1914 Nova Scotia

Paid laundry at home 5.06 $ .76 due me 1.24 CANADA POSTAGE 1 ONE CENT 1 CANADA POSTAGE 1 ONE CENT 1 CANADA POSTAGE 1 ONE CENT 1 CANADA POSTAGE 1 ONE CENT 1

doc. 108 3338 Charles Shuchert Yale University New Haven, Conn. 1914. 39057 Eastern Canada with McLean

Prof. E. Haycock Acadia College Wolfville, Nova Scotia. Meet K.A. Bell at Windsor May 26, 1914. both him to Tor Brook, Victoria and Dictyonema websteri locality Haycock. Lord Hain Held. and Chick. pms. See about slides of life restored for sad period.

[illegible]

New Haven, May 16-1914. Left New Haven with McLean at 5.00 P.M. for Boston. Got there at 9.40. Put up at the Adams House and then walked about the city for an hour. Boston, May 17-1914. Sunday: After lunch saw the Capitol, Bunker Hill Monument. Then to Harvard where we spent most of the afternoon seeing the Museum of Comparative Zoology. Then the Boston Society of Natural History and the Boston Library! Had dinner at the Adams House and then took the 7.30 at North Station for Boston. Had an after bath.

St John River Eastern about 75-feet vertical face. [illegible] Fault [illegible] Jurassican Bridge Fault R.R. Bridge [illegible] Oyler Cambrian limestone Bitinigrice limestone [D6086] [D6085] Section at the Suspension Bridge St. John, N.B. [looking west]cm

St. John, A.B. May 18. Monday Bot here at 12 noon paston time, Dining at the Royal Hotel. Spend the afternoon collecting grapholites at the Suspension Bridge. To the creek is a magnesian mill white limestone standing almost in end. This of Portugorrie age. Then a fault gone with the Johannian or Upper Cambrian strating against the Limestone but with a less steep dip. The thickness I did not make out but may be 500 feet or more. This is a series of light green thin folded sandstones and sandy shales with but a single layer holding payments of Linguhella. Then another fault gone followed by the Tetrapodites shales, with a thickness of probably at once than 35-feet. There are also standing at a high angle and much crumpled and altered so that the parts appear only in places. At the very base are some [illegible] [D6085]

[D6086] -> Etcheminian. The upper so far have gone of red shale and coarse red sandstone. Usually the red shales are very thin but at the top a layer goes to 5 feet thick. Also micaceous. Much of the material came from the trachyte and the red color seems due to oxidation. This Etcheminian maybe Lower Cambrian and may also be Parterqure. Hard to say which. For base see legend.

"Graptolites and Corynides. Almost at the "top of the exposure are for the layer 10" of Graptolites. These two groups may be 20- fut apart but hardly more. "The hackisporas (orthids) come from str" 15 fut below the upper Graptolite bed. They dr and occur in calcium nodules but are always changed to limy spote. St. John, Tuesday May 19-1914 At the Cambrian locality on Juley strat. Here at the base are a prupt cliffs of a greenist- White Trachyte) igneous material. All along this side of St. John this rock makes cliffs and to the south the land descents into the Cambrian valley and the rises into the Upper Cambrian overtones up. Above the Trachyte come in thin red dull greenist ory fine grains on calcium sandstone without fossil; 1 120 fut in thickness. This is the Etchomenian. (see page to left)

"sandstone This one is seen of wide distribution in north St. John. These shales and others with thin sandstones continues to the next strat cover south and then are off dark green shales to the bottom of the valley in which lies a stream. On the other side of the stream the land rises into the Upper Cambrian. If there is no repetition the Cambrian must be several thousand feet thick. This has not been my idea of the thickness.

"Then comes in a white coarse dear bedded sometime about 30-ft thick. This somewhat coarsely bedded. This coarser at the bottom and finer grained at the top and more even bedded. The upper surface appears to be uneven to the extent of 2 feet. This seems to be the structural line of the Acadian Cambria. On the latter refers, the green sandy shales said to be the Patterinus zone, about 65 ft. This is sandy shales once sandy than shales. In the Middle Cambrian fossil from fine shales and green fine grained sandstone with an abundance of print in my collection for here. Of these about 20 feet referred to others. All these give off the white quartzite become more and more fine grained to sands at the top, where the prints abound in grams. About 1/4 mile further east we are in the public park where the contact between the trachyte and the Etchemian can be clearly seen. The basal 8 feet of the Etchemian is an aulose dull red in color, any coarse in material with grains

Fault line State quarries Barry Hill, Cambria Public Park Richmond dyes from Sanda Drive. Coast Station area Tracy hills. Cliff cliff Eastward arm hills at millis. Eclerminis old formation. Quartz Ridges Old land surface ad when. greatly altered by faulting. This land surface may have been uneven causing the difference in the hills resting upon the Tracyte. The Eclerminis may be ancient folding of the joint in which quartzite of the sea. rising disturbed formation. May the Eclerminis be of entirely charac. ter, or at least of shale deposits?

"No specimens "Whirls 1 pebble of 2 or 3 inches across. These pebbles are not well rounded and are of hard material usually a red granite. Then there are pieces of red jasper in some, sometimes red shale pieces, quartzites and schists. The variety is considerable but rarely are any of the pieces well rounded. The whole matters down rather easily into a coarse sand. A little further south the white quartzite of Lulley strus is seen to come within 15 feet of the trachyte cutting out nearly at the Etchavernies. Portergrise. The dolomite is practically recrystallized. Below it is a thick zone of quartzite also much recrystallized. Both are cut by granites and other igneous rocks. Left at 12.40 for Truro then we arrived at 8.20. Staying at the Leasant Hotel.

[illegible]

Inuro, May 20 - Wednesday. Before breakfast visited Victoria Park. At 9.40 on way to Antjamil, where we arrived at 1 P.M. Had dinner at the Royal George and then by carriage to Arisaig. The team and man cost £5-00. Started at 2.30 and got to Mrs Johna. McDonald's at 5.30. Done 21 miles. Arisaig, May 21. Thursday. Spent the day with Mac Leane along the sea cliffs from Arisaig Brook to the end of Stonehouse cliffs. Much material has fallen down making it once easy to get the fossil and the horizons spotted. Fossils laurine are not abundant.

Beeby this shale, Sandy shale (sand variety) Aporhyolite Beeby Hill Lake and level small lenses / banded sandstone.

Arisaig May 22 - Friday. Started out east to see the basal Silurian beds. In Rory McDonalds brool one saw the Beckhill formation resting on the Arthosylite. Here it is a fine grained sometimes with several zones of arenaceous limestone and one of them have fossils in abundance but of few species. Stripes of the formation go on once into shales and others come into the Ross Brook shale. This fossiliferous zone is about 10 feet thick and forms the bulk of the Beckhill formation. The reason why it is sandy here is because it is adjacent to an island of opthylite that in long gone down into sand giving into the regolation muds. These beds stand vertical. We then went further east to Becks Hill Cove. Here on the eastern side of the cove the Beckhill shale formation again stands up and due to a erosion of the flood district. The formation is a fine sandy, arenaceous shale with very few fossils.

[illegible]

luses I tended sometimes. There are many of the in the lower 100 feet, very rare one of these in liming when it over the face of a single species of Deschland - Dolmanella and Leptaena shrubridalis. Japhrictis bilateralis comes in about 75 feet above the base [have known not seen). The entire Beechy Hill shale are marked by a delicate Bathrithus, are found float and of no value on prints. On the eastern side of Beechy Hill one one sees considerable of the Beechy Hill formation but no contact with the apotphylite is seen. Here again the upper part is more clearly. In all of these places the contact with the Ron Brook shale is decided and we can scale out the contact easily. Saw two four forms here, We then went to Rostno Brook where the Beechy Hill formation stands on and as always and in contact with the apotphylite. In the low

[illegible]

back of the bridge over the brook one sees the contact with the asphyxolite. The basal material appears to be either rolled down asphyxolite clay with quartz pebbles or it is the rounded soil and then a fine grains conglomerate, in any event the asphyxolite was weathered and was land on which the Silurian sea migrated. As all rotns brook are of the Beccary this formation is hard and sandy and makes cliff. The bridge stands on the uppermost beds of it and to the north the land at once descends into the lower ground of the Roro Brook dale. Billions give the thickness as 200 feet.

Arisaig, May 23. Saturday. Started out for the upper part of Beectini and the Devonian contact. The Devonian makes the high land due and to the south in the low land undulate by the London series, We then went down One Gras broch and where in the lowest fault in the Devonian. It is a series of red to maroon shales interbedded with thin zones of greenish sandstones. The shales never always have small nodular con- cretions some of which stand vertical to the bedding. These I interpret to be caliche deposits, the sweating dry of the water under a dry climate due to capillarity. Therefore continental deposits, probably on a delta. than the top of the level, within a 1000 feet of the road just in the red shale a fish bone and three hirabres. If those are fresh-water shells it's quite a find. This design is low down in the Devonian series and probably several hundred feet lower than the first bed locality beside the road. Towards the lower part of One Gras broch we came up on this trip sheet, above the even September,

"the One Museum" sketch difficult in this of the Grimshaw 205.8 & 230 degre Dovermier [illegible] [illegible] [illegible] - "Brimmer" Grimshawn engrawmt. 106 W. [illegible] - "Brimmer" line [illegible] 20' offset from the boundary on the Museum on the west side. Find a sketch for this Plan that aligns with the Grimshaw Library and the Dovermier Grimshawn engrawmt. fee Top Land, [illegible] Estimate at 40' in thickness [illegible] - "Brimmer" line [illegible] - "Brimmer" [illegible] - "Brimmer"

in the hood Lilurian section. Beneath the diabase lies the Brandon conglomerate, strongly dure at the stream level about 4 feet. This conglomerate is a dark of the Cardigan series and Cumbrian maroon with flat pebbles, large dimensions up to 3 inches here (but elsewhere of to 1 to 6 inches), fairly well rounded and lying are on their flat sides and flat onto the bedding. This into stream deposit into a track shingle. On this conglomerate lies the diabase which to one seems to be an extensive for it lies regularly upon the bedding of the conglomerate, has its cliff, and the basal beds are vesicular and quite so. The orifice are small from 1/4 to 3/8 inch on the average. About 20 feet higher is a another more decided vesicular zone. Further examination shows that it is un- mistakably a flow and not an intrusion. a sheet Beyond is a flow and like the previous one. Over the sea shore one sees the upper foot. Here it is and calcite a breccia fully vesicles filled with quartz Then comes a considerable thickness of Brandon

been into- radition? so we for the 'fall.' Convert Old unified road surface sea level [illegible] What did the Roost have back then? All air and water? #483? Or is there a natural speaking tone? Three teams sit and sing? Twin within- telling cosmic hum of staff. a comet sea level higher elevations and whole lots and more to the bottom. the distance [illegible] #300-8, 9, #300-12, 15, the same as before in the summer and land binder

conformata. The kettle just above the second trap is made of of the diabase coming down into material fall zone. Finally to the north we see a third flow. Once again the base is highly vesicular and lies fairly roof upon the Drakon conform- ata. All of this evidence goes to show that this country was deformed into mountains during the Devonian, that the topography was rough in the Drakon time and that active volcanoes were abundant during the early Drakon time. All previous workers assumed that the red beds on the sea shore beneath the diabase was the end of the Lilerian section. Making out the extrusive nature of the diabase and that the same flow lies upon the Lilurian, Devonian and Drakon I concluded it would worth while to see if the Lilurian ended as supposed. To my great surprise I saw the Lilurian dipping

"South West into the land, and therefore that there must be more Diluvian. On going of the little Stonehouse Hrmt I soon saw that above the red diluvian lay considerable more marine beds. There are light green Flaggy sandstones nearly always derived from (light slip) and sandy greenish clays... Forams are scarce but teralbs turn up frequently and occasionally chintas on a section. Apparently these are the teralbe beds only which I get so many teralbs when collected here for the first time. Finally one could get no further outwards but the last dip seen was to the N. Br. and in conformity with the still lown beds. We then walked some hundreds of feet to One Aras Hrmt where the dips were like the last one seen. This seems to show that the Bridg Diluvian continues unbroken into the Devonian. It is quite certain that many hundred feet of green Flaggy sandstones are shown cannot be added to the diluvian section as determined by Forams-

[illegible]

"is in due between the red Storehouse and the" "red Devonian" of Peel. Probably as much as 1000 feet. If this observation is correct then the Silurian marine series has a thickness of not less than 4500 feet followed by about another 1000 feet of or more red Devonian beds. Over the Silurian and Devonian un- conformably lie the Zonne Brinksen series. It has been deformed since its deposition. The question will then be asked as to what is the age of the "Red Devonian". If it is unbroken with the Silurian it is either all Silurian, or to judge by the Garpe sequence it may go up into the Devonian quite high. At Arriway con- tinental conditions begin in late Storehouse time (may mean early Lelina time), while at Garpe it did not start until Middle Devonian time,

Arisaig May 24 Sunday. This morning to my surprise young Mr. MacDonald was ready to take me to Antigonish. Got loaded up and was off at 8.30 A.M. Got to Antigonish at 11.15 A.M. Mac Lean made out my expense for the entire trip at 61 dollars which I paid by the Canadian Government. This course does not include meals and hotel en route. I am allowed 33 dollars to get back to New Haven, The transportation charges of to Antigonish is $23.80 including my Pullman fare. Therefore Mac Lean will owe me in the fare when he gets back the $33. I laid out on the way back. Stopping at King George Hotel, After dinner walked around Antigonish

"and saw the Loron Gindon conglomerate. There it is like that seen out of Stonehenge Brook, a dark maroon pebble conglomerate, and piece with desert drifts pattern. This pattern is in all the pieces and in of the color of the firm finding matrix. The pebbles are full sign up to 8 inches or some one foot across. In other places the conglomerate takes on the color of the Triassic sandstone a light red and then the pebbles are in the main of the opolylite. I first saw the conglomerate where the Carway road crosses the International Railway. Probably 1000 feet or more down from greatly I came across a gypsum bed 50 foot or more foot thick. It was covered by either a red clay or a fine red conglomerate. I saw it across a small stream inside the railway and could not get near to it. As the Loron is conglomeratic in or many places and is always there, this evidence in- dicates that the country was mountainous filling in the valleys below. The climate was arid"

and fairly cool. The water must have been marine in account of the great amount of gypsum de- posited. Antigonish May 25 Monday. Fooled around the village all morning and at 1.04 P.M. off for Truro. Arrived dere at 5 P.M., Stopping again at the Leasment Hotel. Truro May 26 Tuesday. Left on Dominion Atlantic on the 6.40 a.m. 9.2. To Tr Windsor at 8.00. a.m. Met Belle at the station and we are off at 9 A.M. for Horton Bluff. Returned to Windsor at 5.10 P.M.

These very coarse granites have not only broken through the Silurian series but Bell says they also cut the Cictaury Devonian. They then belong to the great Devonian disturbance. These granites run in great upheavals all through eastern Nova Scotia and especially in the southern wider portion of Nova Scotia.

Horsten Bluff Tuesday May 26. Between Horsten and Amport. At the eastern end of the shore bluff east of the but more to west effect Horsten fault in rocks either limestone or sandstone, we see the following. The main rock are thick beds of arkose conglomerates. The material is coarse, the pebbles averaging about 1/8 to 3/8 inch with individual grind quartz pebbles up to 1 1/4 inches across. One half of the ar- kose is feldspar some fresh and other some a less carbonized. There is also much black muscovite The pieces ranged up to 3 1/2 inch across that in untransformed are still heals in laminae. Then in der much biotite but more muscovite. The whole material is a fagmental granite rock carried far from the source of supply, because none of the quartz pebbles are rounded; only the edges to the smallest extent are worn away. The bedding is torrential in heavy cross-bedding, and often deeply and sharply channelled into the red clays. Then there are local and quartz pebbles, also pebble each shales free of muscovite blades that have much fagmental plant material and spore cases of 1/8 inch in diameter. Then too there are in

[illegible]

the arkoses rounded flat masses of green shales pieces of some round hard torn off are rolled into the arkoses. All in all it gives one the idea of stream action rather than sea wave as- sorting. Rearly there are small accumulations of quartz pebbles in size from 1 to 2 1/2 inches. The red clays are brown or little in their colour, hare much muscovite and sand and have a hardy fracture. In places are very irregular deposits decoral deposition we also saw here and there rootlets more angular than vertical in position. are more local and The Haarl shales are crasser and are associated with the arkoses as if they formed in local pools during the intervals between the forests. The Haar shale in depth to plant material and muscovite. The arkoses have at times just masses of red shale including, masses torn up by the stream and cut into leaving beds 5 to 75 feet dry standing out off in each end by the arkoses. One sees no evidence of logs in the arkose but occasionally in the clay shales there are small pieces of Lepidodendron.

It may be seen from this statement that the auric strata seems one part bearing as the rest in this series. The auric horizon maybe 1000 feet thick, [illegible] Any prominent idea is that the median stratum is stronger than the eastern, therefore than may be thought less and the section completed auric strata formed on the median stratum. Through the auric stratum is seen pink. [illegible] [illegible] [illegible] [illegible] [illegible] [illegible]

In a blue and rose lagus are seen and rock like plants. and Chocacyllaria. associated on certain layas about 4 miles there are for Estheria. Saw no ostracoda but did see some cases. This locality is stiff to the east of the fault. It is here probably that the Levia were collected. A few hundred feet farther over and the strata stand on end. And rose red mud and shale. Revolution Horizon. It looks to me as if the Androsen should be at the base of the Horton but Bruce says the evidence seems to point that they are at the top. The critical Horton is probably 200 or more feet thick and consists of dark blue to almost black shales with more or less thick zones of fine grained sandstone. All are hindered due to the past deformation. The rest of the Horton or more than one-half

of the section consists in the main of dark blue to almost black shales with almost no sandstone zones, then here and there a thin one, with more and more of sandstone towards the top. These laminas are even dominant in this section and at times are adosio but always of fine grain. Most of the sandstones are riffled, and sunscructed One cretionary limestone layer, more or less with sepetaria was seen. The layer at the top may be said to be decidedly lumpy. The thickness rangful from about 2 to 5 inches. It formed while the beds were still soft. Ostracoda are very abundant along with fanoid scales in the shales near the base of the Lower part of the section. Otherwise ostracodan are absent. Plants are scarce throughout but at the top are more common. In one zone of sandstone about 6 inches thick and in the adjacent shales saw orany critical Lycopods. In size they ranged from 3 to 10 inches in diameter, and there is one to dry square foot

ground. A joint worn away by the sand- stone and the top rolled away in the mud into which some projected. There can be no doubt that the ashic shalm of continental origin, but a marine fossil is seen here and the Estheria and Levia must be fresh water origin. The great shale shalm series is probably almost continental origin although the iron bedding of the shales looks more like marine deposits. The Ostracoda here occur near the base and as Byrichia seems due maybe of brackish water origin. However, signs of the sea are land plants, gamid scales and moss, dipping of very shallow water and plan of very irregular pattern, semi-cracking and cutied prints. The dark color of these shales is probably due plant material, broken up fragments, spores and spore cases (the latter are common). At first one is disposed to regard them as marine because of their iron bedding.

Grandon - Wolfville May 27 Wednesday. Left Grandon at 9 A.M. for Wolfville to see Prof. E. Hagerott and the Dictyonema web- steri locality at Reed Hill. This is Commencement day at Acadia here at Wolfville and Prof. Hagerott was at the train to ask one up to the exercises. Had to go and then upon the stage. It lasted from 10.30 to 1 P.M. About 75 women and men took their degrees and 3 honorary degrees were conferred upon their own gradu- duates. In the afternoon with an automobile we joined the county line about. First one went to Hagerott's fruit farm and then to Reed Hill. The Horton lies only in the lower ground going into the Gasperau and Cornwells Falls. It is the impression that it never was on the higher hills to the east but may

have gone over the Deluvian hill to the crest of the Basperan valley. The present general topography was established since the Triassic for these deposits lies in the vallies but formerly did not outtop the Basperane ridge. It is the general belief that there is no Triassic in the lower part of this valley. However Heyerall states that in oral digging Triassic was encountered in the upper Basperan valley. It is this Triassic deposit that has preserved the topography of the Permian times. At White Rock in the upper Basperan valley we came upon orthirich quartzites and limer slates. The dip of either is hard to make out. Everywhere where we saw the slates ochistrity is developed, in other words it is axial ochistrity. Finally we found the locality for Dictymena websteri at Rock Hill

Ree tells me it is the opinion of Fletcher and others that the Diluvian is conformable upon the Gold Slate series and that all were folded together. This hardly seems probable when we learn that the latter has a thickness of 36,070 feet, one-half of which is quartzite the other slate.

although we did not find this fossil, there is always a light cloud olive green to dull blue slate with flaky surfaces. Occasionally there are gosses of a coarse grained quartzite. This series of slates and quartzites may relate to the Amboy series, as ends have been found about Carncame with primary clasts overasserting the fossil evidence is in favor of Upper Amboy. Prof. Hagerall showed me a large amount of Oristany material he collected near a pasture just a short distance to the early Victorian Falls. The fossils still are good show an Oristany and harmonizing with the Gorge in their full aspect. There are several species of Spirifera, 2 or 3 of Strophomenata, Eatmia near E. medialis of the New Zealand, at least one species of Rhopidomella, ? Hipparion propinquus Leptrocelia Hlabellula (large) and possibly a Drejafanturi (small). Near me D. armenus.

Dietary, Thursday May 28. Left Bwlfrille at 9.30 and got to Middle- ton at 10.45. Staying at the American House. After dinner took the train back to Dietany 4 miles and then walked north-east to Tor Brook. The iron mines are around Tor Brook but they are all shut down now. On the clumps we saw con- siderable quantity fossils in the "shale". Spiriferas are very common, and the largest among them is S. arenaeus. The variety is also not large. The ore is a very fine grained flax- sand or like that of the Clinton. The iron runs 25 to 30%. The bed is said to range from 3 feet to 4'6". At his man slive grew much squeezed slate in which near to we see as a few more Spiriferas. These slates are like those of the Llynfiand. All of the tracks, beds are simple valves and some show washing together. Saw one species of a Trepro- tomita, please as if Stonal onustus. The strata lie in a syncline. Tor Brook is on the eastern limb ad Dietany in the western. The syncline may have a width 10 or miles.

For report on the Chictan-Totthork area see Fletcher, Summary Report C.G.S. fn 1904(295-6), 293-318. has also a map.

If Helderbygan is present it must lie more eastward than the Christian. Dresenya Brook. Friday, May 29-1914. Drove from Middleton this morning to Dres- senya Brook which is east of Phinney Brook. Still are east of Tor Brook Mines, and the latter is about 2 miles west of Messenya Brook. Tor Brook Mines is two miles east of Tor Brook Mine we saw the iron mines yesterday. Messenya Brook is a small brook flowing north down the hill of Paleozoic strata facing northeastward and the Triassic valley. The southern margin of this open valley is made by North Mountain of Triassic sandstone and trap. At the extreme southern margin of the Triassic one soon comes in Messenya Brook upon vertical standing slate, and then a thick [illegible] of slate limestone more whole than limestone. There

At the top of the troitiforms Cristany Belle got a very large head of Phaeos one 2 inches across from side to side. In the Loom Cristany Stale Belle got several large Chipidomela Hata.

are also some sandstones and arenaceous limestones. The entire series is at least 300 feet thick, and containing the higher fossils occur in it almost throughout, but more commonly at the top beneath the dark slates. The specimens are all from due to the fact on whom all of these beds have under- gone. Partially the commonest fossil is Torpidus-leptus caesarius [see if near the European Chengian form] and the second Spirifer avarius. Dav or Rensselaria and Bell think he saw me Hipparynx jarginus. Spirifers are common. The Shifferdotes are present in at least two forms but saw no Leptaena schmidlii. A very large Hymenopterus is often seen in peg- matite. Dav or Leptoceroidis stellata. Conoid shells are not rare. The Heldbergian is a series of living sandstones, either little sandstones, arenaceous slates and micaceous slates. In the main the Held. is sandy. The thickness may be as much as 500 feet. The held is marked at the top

{ "text": "Cenozoic Era\nTertiary\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and A.\nPaleogene\nMiocene\nPliocene\nOligocene\n200-30 m.y.\nAbel et al.\nQalafah\nB. and [TRANSCRIPTION_TRUNCATED_DUE_TO_LOOP]

"with" ocm quarty ly a cell n date of diabases, and the sandy nature of the [illegible], distinguishes it at once from the green slates of the Silurian Belns. Of the Silurian slates at West 400 are exposed at the top of the hill where the horn has its origin. 50-75 fur About [illegible] the diabase sill seems a dimy sandstone abounding in Spirifus and other fossils some of which we familiar. Between the exposures seems to be Beech's. Possibly 300 further from some fossils are common though - only one of 50 to 100 far. Here the Spirifus are small associated with small Athyris on abundance of dents of, pupalana and [illegible] . This faunule is directly connected with the Beech's but the horizon may be in the upper New Scotland though I saw nothing to enable this correlation possible. Below this faunule and slaty the sandy nature of the bed continues to the base but the fossils if present are not

seen. slate The rhio green Lilerian Helms are like those seen at Beest Hill and else where to the north. Bill found one fossil that maybe a Chmets or an orthid. The strata throughout practically stand m end or at least at so degree. If there is a change in dip I did not notice it. The section is a descending one from Up. Criskey through to Bescroft at least and firstly into New Scotland. Then firstly a great time break (the contact seems to be a disemprontable one) with the Lileria slats at the base of the section. Fletcher measured the section as upwards of 1500 feet thick. Of this 1100 feet in Iron Diermian (top out seen), and on 400 feet in Lilerian (base nowhere near).

Middlem - Jarmouth. May 30 Saw Bull eastward at 9 A.M. I left Middleton at 11:24 for Jarmouth, St here at 4.45 P.M. On found steamer Prince George. Left Jarmouth in a rain with some wind at 6. P.M. Have room 74 all to myself, Left to Boston on a fine Sunday morning at 9 A.M. The steamer was ahead of sche- dule one-half hour. Left for N Haven at 10. A.M.

May 24. Mc Donald fn carriage Trenton $5.00 " 25 Antismond tr Tauro 2.55 2.55 " 25 " Royal Senje Party 2.75 " 26 Learner at Tauro 1.50 , 26 Tauro to Windsor 1.80 " 30 Middleton tr Boston 8.00 " 30 " " Jarmott Chan .60 " 30 Meal on steamer (dinner) .75 " 30 Berth " " 3.60 " 31 Breakfast " " .50 " 31 Bostm to Q. H. 3.25 " 31 Baggage Transfer 35c 35c .70 , 31 Drink in cars 1.00 $ 29.40

19.60

лпи ае 1397 1/2