= CANADA i WwW DEPARTMENT OF MINES 19724 oe CODERRE, Minister A. P. LOW, Deputy Minister GEOLOGICAL SURVEY . W. BROCE, Director ! ee GUIDE BOOK No.5 - EXCURSIONS in the | Viester Peninsula of Ontario and Manitoulin = OTTAWA ith GOVERNMENT PRINTING BUREAU | 1913 GUIDE BOOK No. 5 EXCURSIONS IN THE Western Peninsula of Ontario and Manitoulin Island (EXCURSIONS B 4, B 7, B 9 AND C 5.) ISSUED BY THE GEOLOGICAL SURVEY OTTAWA GOVERNMENT PRINTING BUREAU y 1913 Ni 35066-—1 \ uw GUIDE BOOK No. 5. Excursions in the Western Peninsula of Ontario and Manitoulin Island. CONTENTS. PAGE. Excursion B4—Silurian section at the Forks of Credit river, by William A. Parks. 5 Excursion B7—Ordovician section on Credit River near Streetsviile, by W. A. Parks. 15 Excursion B9—Algonquin beach, Glacial phenomena and Lowville limestone in Lake Simcoe district, Ontario, by W. A. JOMMstonn ces occ ot ee eee on 23 Excursion C5—Geology of selected areas on Lakes Huron and Erie in the Province of Ontario, by W. A. Parks, C. R. Stauffer, M. Y. Williams and T. Tee AWW rally tate Mitesh, ire in ware cies ie ara o7 ister llwistraviOnSts-lcc-en ana oe ees a ee 108 35066—14 5 EXCURSION B 4. SILURIAN SECTION AT THE FORKS OF CREDIT RIVER, ONTARIO. BY WILLIAM A. PARKS. CONTENTS. | PAGE. HINGROUINGHTONM ce irae cha: are aleve ue, Myon ee 6 PAT OPAe Ogu G Ox nares te asise msc SOAS cael en eae a cee oe 6 MO GCUMOISE WE AC we ain lo ee tence ee ye 6 Lorraine and Richmond at Streetsville........ o] Gar Cucccriontr ws es ee 8 GreditsRorks Section)... 3.62 sacs ak 12 Ball Baan tet ces tit a) era et cots es vy Sete 13 6 INTRODUCTION. The remarks contained in the introduction to the guide book for Excursion B3 are equally applicable to the section at Credit Forks. In fact the sections at Hamilton and at the Forks of the Credit are both essential to an understanding of the formations exposed along the face of the Niagara cuesta. For the correlation of these sections and for the necessary general information the reader is referred to the guide book for Excursion B3. ANNOTATED GUIDE. IRoguUOIS BEACH. Miles and Kilometres. Toronto On leaving the city, the Oly i001 Alt. 254 ft. railway traverses a flat area o. km. 77.2m. covered with post-glacial sands showing evidence of wind action. At Lambton, the shore of the post-glacial Lake Iroquois is 6.7m. Lambton visible to the north, where LOU7 kam, Alt. 399 ft. excavations have been made I21.3m.in the characteristic gravel bars of the ancient beach. On crossing the Humber river, good expo- sures of the Lorraine shales may be seen in the scarped banks of the stream. The Humbervale quarry near here has yielded many excellent examples of the large trilobite, Isotelus maximus, Locke. Further expo- sures of the Lorraine shales occur in the valley of Mimico river a short distance beyond the Humber. At this point the railway 14.4m. Cooksville approaches so close to the 23 km. ANNE, QO Mi Iroquois beach that expo- 118.8 m. sures of the gravel bars may be seen from the train. Just beyond Cooksville, the beach is ascended and a more rolling aspect is presented by the surface of the country owing to less modifi- cation of the glacial accumulations by post- glacial agencies. Guide Books Nos. 6 and 7 are published by the Bureau of Mines, Toronto, Ontario. The contents of these are as follows: GUIDE BOOK No. 6. Toronto and vicinity. by A. P. Coleman. Moraines north of Toronto, by F. B. Taylor. Muskoka Lakes, by G. G. S. Lindsey. Clay deposits and works near Toronto, by M. B. Baker. The Madoe area, by Cyril W. Knight. GUIDE BOOK No. 7. Preface, by W. G. M. The Sudbury area, by A. P. Coleman. The Cobalt area, by Willet G. Miller. The Poreupine area, by A. G. Burrows. Timagami, by Willet G. Miller. WA rasa > bop iecitew Depred ae or SS een pene 7 —smetneengl 5 i s ‘ et a e ~e a, 4 anSmadawy { f Ss BMSWNG) Sas | e ae nv B4andBé. True North Legend Niagara Lockport Cataract Silurian Cataract (basal) Richmond Queenston Fichmond and Lorraine Ordovician Norval 5 Route map between Streetsville and Credit Forks Miles 1 Q 2 + 6 Kilometres Lo 2 + G a y ae Bret e a ae eed le Oe ee ee ee en i ok i LORRAINE AND RICHMOND FORMATIONS AT STREETSVILLE. Miles and Kilometres. In the valley of the Credit 20.8 m.. Streetsville river at Streetsville, Lorraine B3n3 kal: Alt. 500 ft. shales are overlain by fossil- 152m. iferous strata of the Rich- mond formation. To the west of Streetsville this marine type of Rich- mond, in its turn, is covered by the red unfos- siliferous shales of the Queenston member of Niagara cuesta at the Forks of the Credit. the Richmond. While this member is entirely without organic remains in the southern part of the province, it reveals a distinct Richmond fauna at points farther north. Beyond Streetsville the ascent is gradual but continu- ous. Little of interest is to be observed until 8 See the vicinity of Cheltenham is reached when the Niagara cuesta comes into view. At Inglewood the red Rich- 41.3m. Inglewood mond shales are exposed in 66 km. Alt. 896 ft. undulating hills which are 272.4 m. surmounted by the _ sharp escarpment of the Niagara cuesta, topped by the heavy beds of the Lockport dolomite. On crossing the high 45.5m. Forks of Credit bridge over the Belfontain 72.8 Ki.
  • ...Dept. Mines, Can., Mines Branch, The Building and Ornamental Stones of Canada, pp. 146-164. Soe Miller Ws Ge ao5. Bur, Mines) Ont., Rép, 19004 Pe. U, Pp. 39, 58, 95, 126. 4. Schuchert, Charles... Forthcoming article on the Catar- act formation in Bull. Geol. Soc. Am., Vol. 24. 15 EXCURSION B 7. ORDOVICIAN SECTION ON CREDIT RIVER NEAR STREETSVILLE, ONTARIO. CONTENTS. PAGE. Introductione ss .65 eo enh a Zot ter eer is 16 PATNI PAC CeO UICle yas ence rie Mie nies tik eee } fd 16 huchiondrand Wworraine formations. 5.20044. 17, | OTIS ae GVOV YG Ie Meee ccdea lass anlar pene a AND ae ane eed te eg 17 POR AVN CR ee oir eae ees Sink erste ete eel ity ane 19 DX 16 INTRODUCTION. The upper Ordovician strata of North America occur in formations of so variable a character in different locali- ties that their exact correlation is a matter of difficulty. The practice is now becoming general to embrace the whole series in the term Cincinnatian and to recognize the following formations: Richmond, Lorraine, Eden, Utica, Collingwood. The Richmond is a widespread and highly fossiliferous formation, which has been divided into several members in the Cincinnati area. The Lorraine formation is less well defined, particularly in the Streetsville section, but it seems advisable to retain the name rather than to add to the large number of loca! formational names. The Richmond, as exposed in Ontario, consists of a series of marine limestones and shales, and a great thickness of red shales with some green bands and an occasional bed of limestone. The marine type is best exposed in the Manitoulin islands, whence it may be traced with gradualiy diminishing thickness to the vicinity of Streetsville. The red Richmond shales (Queenston formation) are of great thickness at Niagara and Grimsby, where they are unfos- siliferous and rest directly on the Lorraine. Northward, the formation diminishes in thickness, overlies the marine type and carries fossils characteristic of the Richmond at Collingwood on Georgian bay. ANNOTATED GUIDE. Miles and Kilometres. Om. Toronto.—Alt. 254 ft. (77.4 m.) o km. Dats GP ane Streetsville Junction.—Alt. 549 ft. (107 34.7 km. m._ A general account of the country along the line of the rai way between Toronto and Streetsville is given in he guide to Excursion B4. 17 RICHMOND AND LORRAINE FORMATIONS. The Cincinnatian strata exposed in the vicinity of Streetsville consist of the upper red unfossiliferous shales of the Queenston division of the Richmond, the grey shales and limestones with intercalated coral reefs of the marine Richmond, and the lower arenaceous limestones and shales of the Lorraine formation. In the valley of the Credit river above the railway bridge, the sha'es and limestones of the marine R’chmond yield an abundant fauna. The lower part of the river valley shows the underlying Lorraine shales and arenaceous limestones of increasing thickness as the river is descended. Anticline in Richmond strata, Streetsville, Ontario. RICHMOND FORMATION. ___The red Richmond shales (Queenston) are not exposed in the valley, but they may be seen in the vicinity. The 35066—2 18 different beds of the marine Richmond and the Lorraine are not very persistent; in consequence, it is somewhat difficult to correlate the strata of different exposures. The most continuous layer is a heavy bed of limestone with numerous bryozoa which lies near the base of the Richmond. A cliff of about 25 feet (7-6 m.) of limestone and shale is presented by the scarped bank of the river near the bridge to the northward of Streetsville Junction. The lower portion only is actually exposed and shows the heavy bryozoan layer of about two feet in thickness. Beneath this are thin-bedded limestones and shales, which may belong to the Richmond or to the underlying Lorraine. This is one of the best localities for collecting the typical stromatoporoids and corals: Stromatocerium huronense Billings. Columnaria alveolata Goldfuss. Columnaria calicina (Nicholson). Streptelasma rusticum (Billings). Tetradium minus Safford. Just below this point an interesting minor anticline is shown: the heavy bryozoan layer forms the surface rock, but it is covered by three feet of boulder clay con- taining pebbles and also corals and stromatoporoids of the local formation. The northeast side shows glacial grooving and polishing, but the southwest side is much less affected by the passage of the glacier. The upper limestones, shales and coral reefs are ex- cellently exposed at several points on the west side of the river above the bridge. Besides the stromatoporoids and corals an abundant fauna is presented, of which the follow- ing are the more common species :— Callopora sp. Prasopora cf. hospital s (Nicholson). Rhombotrypa quadrata (Rominger). Catazyga headi (Billings). Hebertella occidentalis (Hall). Platystrophia biforata (Schlotheim). Platystrophia laticosta (Meek). Platystrophia clarksvillensis Foerste. 19 Rafinesquina cf. alternata (Emmons). Strophomena planumbona Hall, S. rugosa Blatinville. Zygospira modesta Hall. Cyclonema bilix Conrad. Lophosira bowdeni (Safford). Lophospira sp. nov. Oxydiscus sp. Schizolopha tropidophora (Meek). Schizolopha moorei Ulrich. Byssonychia grandis Ulrich. Byssonychia radiata (Hall). Byssonychia richmondensis Ulrich. Cymatonota typicalis Ulrich. Modiolopsis concentrica Hall and Whitfield. Modiolopsis cf. versaillensis Miller. Opisthoptera casei (Meek and Worthen). Pterinea demissa (Conrad). LORRAINE FORMATION. Below th: po:n first described the slant of the river bed causes an increasing thickness of the underlying Lor- raine to be revealed. Excellent exposures are presented near the bridge on the road between Streetsville and Streetsville Junction, and also immediately above the railway bridge. The section at the former point is as follows :— Richmond— 1. Corralline limestones and shales..... 18 ft. 5-4m. 2. Grey, thin-bedded limestone and shale .3 ft. -9 m. 3. Compact bryozoan limestone........1-6 ft. -35 m. Lorraine— 4. Grey shale and thin-bedded limestone 3 ft. -9m. Gee OAMGSEOMEN es ea et en aces 4 in. 10cm. Nos. 1 and 3 contain the typical gastropod, brachiopod and pelecypod fauna. No. 2 is characterized by the presence of Byssonychia richmondensis, Ulrich. No. 4 contains scarcely any organic remains. 35066—24 20 No. 5 is not richly fossiliferous, but it presents ex- amples of Rafinesquina alternata (Kmmons), Opisthoptera sp. and Modtolopsis concentrica, Hall and Whitfield. Near the railway bridge the cliff presents a face of about 31 feet (9-4 m.). The lower 17 feet (5-2 m.) consist of sandstones and shales with obscure and fragmentary fossils: these beds, in whole or in part, are to be referred Lorraine sandstone and shales, Credit river near Streetsville, Ontario. to the Lorraine. The upper 14 feet (4-2 m.) consist of limestone and shale with brachiopods and b: yozoa typical of the Richmond. The coral and stromatoporoid zone does not appear at this point, nor is it encountered farther down the river. On the east side of the stream, about a half-mile below the railway bridge, a cliff of 25 feet (7-6m.) in height presents exposures of Lorraine limes ones, sha'es and sandstones. Some interesting features of cross bedding 21 and ‘pillow structure’? in sandstone, with contempor- aneous erosion of the underlying beds, are to be seen at different horizons in the exposures. “Pillow’”’ sandstone with contemporaneous erosion in Lorraine beds, Streetsville, Ontario. BIBLIOGRAPHY. 1. Logan, Sir W E......Geol. Sur. Can., Rep. 1863, pp. 198-224. 2. Nicholson, H. A. ....Rep. Pal. Prov. Ontario, pp. 21-38, 1874. See also the literature cited for the Manitoulin islands, Excursion C-5. 23 EXCURSION B 9. ALGONQUIN BEACH, GLACIAL PHE- NOMENA AND LOWVILLE (OR- DOVICIAN) LIMESTONE IN LAKE SIMCOE DIS- TRICT, ONTARIO. BY W. A. JOHNSTON. CONTENTS. PAGE. EMEROGUICHO Merete ss rch ow apa Gn ee feet oun een 24 JENS OTOVO TEE NUSTGL- (OA UN UCL aeterae ay Race ttey eae Meet iene yee ted 28 Geology of the district about Orillia.............. Bit (GROTON: bh Sten ti gd oe een ng, 2 Cea a omen, Cot ae 31 Section of the Lowville formation...... Be Bibliography 24 INTRODUCTION. The excursion will proceed by Grand Trunk Railway from Toronto to the town of Orillia, which is situated near the narrows between Lakes Couchiching and Simcoe and distant from Toronto in a northerly direction about 85 miles (136.8 km.). En route, after reaching the Lake Simcoe basin, the Algonquin beach may be seen from the train at several points along the railway. After a closer inspection of the beach at the town of Orillia, a trip will be made by motor to the Longford quarries on Lake St. John about 8 miles (12.9 km.) in a northeasterly direction from Orillia, where a good section may be seen of the Lowville (Birdseye) limestone with basal series of shales, sandstone, etc., resting unconformably on the Pre-Cambrian crystalline rocks. Returning from Longford along the Monck road about 7 miles (11.3 km.) from Orillia, a section may be seen shewing a glacially transported, large boulder or mass of bedded Lowville limestone underlain by till. The Algonquin beach is well developed in the Lake Simcoe district, where it forms a record of the abandoned shoreline of the immense body of water which occupied the Huron and Michigan basins at the close of Glacial time. In this district, as well as in the northern portions of the Huron and Michigan basins, the beach has an upward tilt towards the northeast. Around the southern ends of Lakes Huron and Michigan, the beach becomes horizontal at an altitude of about 600 feet (182.9 m.) and maintains that height over a considerable area [1]. Hence it is supposed that the water of Lake Algonquin stood at this altitude viz. 600 feet (182.9 m.) above sea level. The lowest point reached by the beach in the Lake Simcoe district is in the valley of Holland river about 15 miles (24.1 km.), south of the extreme head of Lake Simcoe, where the beach has an altitude of 724 feet (220.6 m.), or only 6 feet above Lake Simcoe. It gradually rises to a point about 6 miles (9.6 km.) northwest of Orillia where it has an altitude of 883 feet (269.2 m.), the highest altitude attained by the beach on the west side of Lake Simcoe basin. About 20 miles (32.2 km.) east of Orillia, near the village of Kirkfield, where for a time the waters of Lake Algonquin discharged eastward into the valley now occu- ‘olequg ‘Avg Ajueys Ieou yoeoq uINbDuUOSTY JO YNIq pue d9v110} UMDI4S-IOpP[NOg ‘O° NOISUNOXG, 26 pied by the Trent chain of lakes and rivers, the beach has an altitude of 883 feet (269.2 m.) and 15 miles (24.2 km.) farther north rises to 925 feet (282.0 m.). Northward from the latter point, on account of the rough and com- paratively little drift-covered surface of the country, the beach is difficult to follow and although a strong beach, supposed to represent the Algonquin, has been found at a number of points as far northward as the town of North Bay, sufficient data have not been collected to enable definite correlations to be made. The maximum tilt rate of the beach in the Lake Simcoe “district is in a direction’ -N.-217 —2 eae the rate increases from 2.3 feet (.7 m.) per mile in the southern portion to nearly 6 feet (1.8 m.) in the northern portion. Lakes Simcoe and Couchiching, and a number of smaller lakes to the east, occupy shallow basins which rarely exceed 100 fee: (30.5 m.) in depth, and evidently owe their present existence as lakes to the upward tilting of the land towards the north. Were the land depressed to the relative altitude which it had when the Algonquin beach was made the present outlet of Lake Couchiching, for example, would be about 175 feet (53.3 m.) lower. North and east of Lake Simcoe, the drift is relatively thin, but in the district to the west and southwest of the lake the drift becomes much thicker, and no exposures of solid rocks are known to occur. Well borings made in this district show the drift deposits to have a thickness of at least 375 feet (114.3 m.), and as the drift hills rise to an altitude of 200 to 300 feet (61 to 91 m.) above the valleys in which the borings were made it is possible that the drift has in places a much greater thickness. Numerous sections in the drift show two till sheets separated by stratified sands and gravels. The uppermost or last till sheet consists of two distinct portions, an upper part, often with a well bedded character and composed of a loose sandy till, and a lower portion consisting of a more compact, sandy clay till with little or no trace of stratification. Associated with the former and generally crowning the summits of hills and ridges are well stratified deposits of sands and gravels, which often bear a semblance to beach ridges. Their mode of origin is not clear, but they do not appear to be referable to wave built features. Over a considerable part of the district the till of the lower portion of the last till sheet merely forms a thin 27, veneer which conforms to the contour of the underlying stratified sands, gravels and clays. These interglacial or interstadial beds are of considerable thickness, and appear to have suffered erosion for a long period of time prior to the deposition of the last till sheet, during which time broad valleys were carved in the earlier deposits. The till of the lowei till sheet is generally only exposed in the beds of streams, where it is seen to be composed of hard, compact, sandy clay till, without stratification, containing numerous well polished and striated cobbles and boulders. This till withstands erosion remarkably well, and where trenched by streams is sometimes seen to stand up in vertical sections or to form rock-like ledges which cause rapids. Well borings in the district show the presence of a still lower till sheet, but this till is not known to be exposed in any sections. Extensive deposits of stratified sands, gravels and lake clays also occur in the district below the level of the Algonquin beach. So far as known, no fossils have been obtained in this district from the sands and gravels of the Algonquin beach or from the interglacial beds. Fresh water shells are, however, abundant in the sands and clays of the valley of Nottawasaga river, but at no great height above Georgian bay. On the northeastern side of Lake Simcoe an area of drumlins of the long nairow type is well developed. The drumlins are generally composed of a sandy unstratified till or boulder clay which appears to be almost entirely derived from the last till sheet. The longer axes of the drumlins coincide with the di ection of glaciation as shown by striae on adjacent rock surfaces. The general direction of glaciation throughout the district is towards the south- west, and, as a rule, wherever the surface of the rock has been protected from weathering, striae are abundant and well preserved. Over a considerable portion of the district around the west and south sides of Lake Simcoe, imperfect drumlin forms are developed, and in fact the greater part of the region appears to have been subjected to some degree of ice moulding beneath the overriding ice of the last sheet. Accordingly terminal moraines or ice marginal deposits are rarely well seen in the district. Some parts of the area, 28 notably the relatively high upland tract lying to the south of the town of Barrie, are gently undulating, nearly flat, till plains characterized by numerous small depressions. The most notable exception to the prevailing ‘“‘d:um- linized”’ and till plain surface is the range of hills which lies about midway between the towns of Barrie and Orillia and from 7 to 10 miles (11 to 16 km.) west of the ‘ake. These hills, the highest of which rises to an altitude of nearly 600 feet (182.9 m.) above Lake Simcoe, are com- posed, in greater part, of a loose sandy till partially strati- fied. They are, in part morainic in character and appear to have been formed during the retreat of the last ice sheet. The greater portion of the area of Lake Simcoe district is underlain by limestones of the Trenton, Black River and Lowville formations (Ordovician), the last of which rests unconformably on Pre-Cambrian crystalline :ocks. The limestones dip gently towards the southwest at a rate generally not exceeding 25 feet (7.6 m.) per mile, and have an estimated maximum thickness in the district of 550 feet (167.7 m.). Eastward from the lake, the limestones are often well exposed and form a rock divide between the waters of Lake Simco and Trent valley. The northern portion of the district, including the area surrounding the lower end of Lake Couchiching, is occupied by Pre-Cambrian rocks. Near the contact of the limestones with the Pre-Cambrian rocks, an escarp- ment is generally developed, and fronting the escarpment, and often at a considerable distance from it, are numerous outliers of limestone, showing that the limestone, at one time, extended far over the Pre-Cambrian rocks to the north. ANNOTATED GUIDE. Miles and Kilometres. Om. Toronto, (Union Station). Alt. 254.0 o km. feet (77.4 m.). 14.0 m. Thornhill.—Alt. 635 feet (193.5 m.). 225) kin. Leaving Toronto the railway passes north- ward over a series of drift hills and ridges locally known as Oak Ridges which are, in part, morainic in character, and extend for Miles and Kilometres. At 2 100s 66.3 km. 64.0 m. 103.0 km. 29 over 100 miles (161 km.) in a general east and west direction, roughly parallel to Lake Ontario and a few miles north of the lake. The drift in the hills, which rise to an altitude of 600 to 900 feet (182.9 m. to 274.3 m.) above Lake Ontario, is known to be of con- siderable thickness. At Thornhill, 14 miles (22.5 km.) north of Toronto, a well boring penetrated 640 feet (195.1 m.) of drift before reaching the Trenton limestone which was the first solid rock formation encountered. The boring continued through 585 feet (178.3 m.) of the Trenton, Black River and Lowville formations to the Pre-Cambrian. Chesley. Alt. 980 feet (298.7 m.). One mile south of Chesley station, the summit on the line of railway is passed at an altitude of 1,002 feet (305.4 m.). Going northward, the railway rapidly descends in'o a broad valley which extends, nearly at the level of Lake Simcoe (low water 718 feet, 218.9 m.), for some 20 miles (32.2 km.) southward from the head of the lake. This valley was occu- pied by a deep embayment of Lake Algonquin, the shoreline of which is well marked on both sides of the valley. Near the village of Sch mberg, at a point about 15 miles (24.1 km.) south of the extreme head of the lake, the Algonquin beach has an altitude of 724 feet (220.7 m.), only 6 feet (1.8 m.) above the level of Lake Simcoe. Bradford. Alt. 724 feet (220.7 m.) At the town of Bradford, a well boring penetrated 330 feet (100.6 m.) of drift deposits before reaching the Trenton limestone. The terrace and bluff of the Algonquin beach near the station, has an altitude of 749.0 feet (228.3 m.). At Lefroy 10 miles (16.1 km.) further north, the beach which may be seen on the west side of the railway near the station, rises to 774 feet (235.9 m.). Barrie. Alt. 726 feet (221.3 m.). The town of Barrie is situated at the head of Kempenfeldt bay, an arm of Lake Simcoe. Miles and Kilometres. 86.0 m. 138.5 km. 30 A broad flat-bottomed valley extends west- ward for a number of miles from the head of the bay, and is floored by a considerable thickness of sands and gravels derived from the Algonquin beach, which has an altitude, at the town of Barrie, of 785 feet (239.6 m.). The sides of the valley are composed of drift, and rise steeply to an altitude of over 200 feet (60.9 m.) above the valley bottom. The record of a well boring, made near the town of Barrie, shows the surface deposits to have a thickness of 335 feet (102.1 m.) below the level of Lake Simcoe at which point the Trenton limestone was struck. The boring continued through 200 feet (60.9 m.) of the limestones of the Trenton, Black River and Lowville formations to the Pre-Cambrian. The deep borings mentioned above as having been made in the drift deposits at Thornhill, Bradford and Barrie, together with several others made in the district, confirm the ex- istence of a deeply drift-filled pre-glacial valley connecting the basins occupied by Georgian bay and Lake Ontario, the probable existence of which was pointed out by J. W. Spencer. [4.] Between the towns of Barrie and Orillia, a distance of about 25 miles (40.3 km.), the Algonquin beach is well developed and can be followed with nearly perfect continuity all the way. Throughout the greater part of the distance, the railway follows along almost at the same altitude as the beah. At Hawkestone, about 14 mlies (22.5 km.) north of Barrie, the bluff and boulder-strewn terrace of the ancient shoreline may be seen a short distance west of the station at an altitude of 821 feet (250.2 m.). Orillia. Alt. 724 feet (320.7 m.). 31 GEOLOGY OF THE DISTRICT AROUND ORTPETA: GENERAL. The town of Orillia is situated near the narrows between Lakes Couchiching and Simcoe, and is built in part on a sandy terrace just below the Algonquin beach. In the town, along the Coldwater road, which is the main road leading westward, the cut bluff and boulder pavement of the beach may be well seen. A mile west of the town, a gravel pit shows a section across a great barrier beach having an altitude of 853 feet (260-0m.) or 135 feet (41-2 m.) above Lake Simcoe. North and east of Orillia the drift is relatively thin, but west and southwest it becomes quite thick. A well boring made in the town itself shows the surface deposits to have a thickness of 170 feet (51-8m.). A half-mile north of the station at Orillia, a cutting on the Canadian Pacific railway shows well stratified sand overlain by till, and a half-mile east of the station a cutting affords a section through a drumlin-like ridge composed of boulder clay. Northeast and east of Orillia an area of small drumlins and drumlin-like ridges is developed. The drumlins are generally long and narrow, and range in height from a maximum of 60 feet (18-2 m.) down to 10 feet (3 m.) or even less, and vary in length from two miles to one quarter mile or less. The longer axes of the drumlins are nearly parallel and coincide with the direction of glaciation, which was towards the southwest. The drumlins are generally composed of sandy boulder clay, showing little cr no stratification. Occasionally they are seen to be, in part, composed of coarse sand and gravel partially stratified, with numerous boulders and cobble stones. At the north end of one of these drumlins one mile (1-6km.) east of North Mara post office, along Monck road, a section shows a large boulder or mass of bedded Lowville limestone, which is underlain by drift and was evidently glacially transported or shoved so that it now rests at a steep angle on the northern slope of the drumlin. The section is exposed by the face of the lime- stone having been opened up as a quarry. No exposures of solid rocks are known to occur in the immediate vicinity of the town of Orillia, but a short *JOEYUOD VY} SYIvU JaAOYS Vy} JO aseq ay: 119 Aq wrepopun suojsaury a[]JAMo7T peppeq jo sseut paziodsuey) Ayers SUIMOYS U0IWIaS ‘0 'gq NOISUNOXY 33 distance to the north and northeast the limestones of the Black River and Lowville formations, which underlie the Trenton limestone and rest unconformably on the Pre- Cambrian rocks, are well exposed and overlap the Pre- Cambrian. The northern end of Lake Couchiching is occupied by the Pre-Cambrian rocks, and near the contact an escarpment is generally developed in the limestone, which affords numerous sections. SECTION OF THE LOWVILLE FORMATION. At the Longford quarries on the west side of Lake St. John, about 8 miles (12-9 km.) northeast of Orillia, a good section is exposed of Lowville (Birdseye) limestone with basal-series of shales and sandstone or arkose. The eastern and northern sides of the lake are occupied by Pre-Cambrian rocks, but along the western side a limestone escarpment is developed, in the face of which a number of quarries have been opened. The beds dip slightly to- wards the southwest, and at the north end of the lake over- lap the crystalline rocks. Near the contact the beds have a steep dip and appear to be faulted. The general section of the Lowville formation is as follows — 1. Basal series of sandstones, shales, etc.—The base of the series consists of a few feet of coarse, calcareous sandstone or arkose, which rest unconformably on the Pre-Cambrian crystalline rocks. These beds pass upward into red and green shales with intercalated lenses or thin beds of sandstone, and occasionally thin beds of fine- grained, dove-coloured limestone. The thickness of the series varies, and the beds are frequently absent on the sides and tops of ridges or domes of the crystalline rocks, where the limestones are seen to rest directly on the old floor. The sandstone and shales are best developed in basins between ridges of the crystalline rocks, where they occasionally have a maximum thickness of about 40 feet (12 m.). They are local in character and derivation, and evidently represent the old soil covering of the Pre-Cam- brian rocks somewhat sorted, rearranged and recemented, and it seems probable that they represent the initial near- shore deposit of the next succeeding formation. 35066—3 34 2. Lower Lowville (Beatricea beds).—The red and green shales pass upward into impure magnesian limestones, which on fresh fracture are greenish-grey in colour and weather yellowish brown. They are characterized by numbers of drusy cavities, occasional quartz grains and crystals of pyrite or limonite, and are generally barren of fossils. They are only a few feet in thickness and are followed by 6 to Io feet (1.8 to 3 m ) of fossiliferous blue- grey to dove-coloured limestone characterized by an abundance of a species of Beatricea. These beds somewhat resemble in physical character the typical fine-grained ‘“‘Birdseye’’ limestone, but are less compact in texture and weather to a shaly mass. These beds contain a con- siderable fauna, among which may be mentioned: Rajfin- esquina minnesotensis, Zygospira recurvirostris, Cyrtodonta huronensis, Lophospira bicincta, Isotelus gigas and Tetra- dium halysitoides. They are overlain by 7 to Io feet (2-1 to 3 m.) of unfossiliferous magnesian limestone very similar to the beds which immediately underlie them, 3. Upper Lowville (Birdseye) limestone.—The Beatricea beds are overlain by about 20 feet (6m.) of fine-grained, even-bedded,:dove-coloured limestone, char- acterized by such fossilsas Phytopsis tubulosum, Bathyurus extans, Leperditia fabulites, and in the upper portion by a great abundance of Tetradium cellulosum. The Lowville limestone, which is sometimes included in the Black River as a sub-formation, is well developed in south central Ontario, and is remarkable for its constant lithological and faunal character not only throughout this district, but a; far as Kentucky, Tennessee and Alabama on the south. BIBLIOGRAPHY. 1. Goldthwait, J. W.....An instrumental Survey of the Shore lines of the extinct Lakes Algonquin and Nipissing in South- western Ontario. Geol. Survey, Can., Memoir No. Io. 2. Logan, Sir Wm. E...Geology of Canada: Report of Progress of Canada. Geol. Survey to 1863, pp. 983. 35 3. Murray, Alexander. .Can. Geol. Survey, Summary Re- Aeespencer, |i. Wes: 2... Sa baylor, FB 35066—35 port for 1852-3. Deformation of the Algonquin beach and birth of Lake Huron: Am. Jour. Sci., 4th series, Vol. 41, I89QI, pp. 12-21. The limit of post-glacial sub- mergence in the highland east of Georgian bay.Am. Geologist, Vol. 14, 1894, pp. 272, 285. 37 EXCURSION C 5. GEOLOGY OF SELECTED AREAS ON LAKES ERIE AND HURON IN THE PROVINCE OF ONTARIO. BY WILLIAM A. PARKS. With Sections by C. R. Stauffer, A. F. Foerste, M. Y. Williams and T. L. Walker. CONTENTS. Seolorna sae aes oe Roi ree toate aA ae INMMNOCAted CUE s soho An une lous deste Se Walcer@mbarioey nee eee ne a ete rote. INiatoanauiia ll Seep pencen tens a thes ous ee ee Spam! Geology of the region about Port Colborne. By Gees Staticreece aise ae eee eee B Ceneraludescriptione: «7.00. eye tee ea Sectiousiofene Onondaga. as) ee ee shireshlocaneaquartyacie. rine eee: Canadian Portland Cement Company’s GPSS Ze & ce noc tem amie a er ee ae istion Onondacagiossils va set. se nee TEAC MEO Chretien ae ee Pare i sl cluto geo te eat Shore line phenomena and forests at Rondeau . Onondacayoigreleesisilandi)] 5s a Glaciationtor Releeislands 9-2 5..... 6. 5- 38 Monroe and Onondaga formations at Amherst- DUT ce Salt well, salt plants and soda plants at Windsor Hamilton formations at Thedford............ Silurian-section ‘at Goderich) 901/23 ae Weathering at Flowerpot island.............. Geology of Clay Cliffs, Cape ee i: Manitoulin island. By A. F. Foerste.. os Cincinnatian section: .c.55:...7 ote Collingwood fermation=*..3...2-.4- 0s Eden clays and limestones............... Lorraine s1OnimatiOne. yn eee eee Richniond formationss-.. 44.0. sae eee Fossils from the Clay Cliffs............/. Lowville—Pre-Cambrian contact on Granite island. Mohawkian strata northeast of Manitoulin island. By Ay Fe Foersteé: 22. eum hess03 sone Glochéasland* = he eRe ae eee Goatisland2 4s Gece ee ee 2 ee Silurian of the Eastern Part of Manitoulin island. By M.-Y. Willams 5205.3 .2) eee Introduction: "2 524 hes ae: eee eee Siltintan:.section.'. <2 ees on. eas ee Fhe Killarney Passage s/s sae eee The Pre-Cambrian of Parry island and vicinity. By DL. L. Walker... 6023. eee Palzozoic section at Collingwood.........5......- Bibliography «i228. 20.4.4 oe eee ee 39 INTRODUCTION. PHYSICAL FEATURES. The portion of Southern Ontario which lies west of a line from Georgian bay to Toronto is known as the Western Peninsula. The whole of this region is embraced in the coastal plain of Paleozoic age which was laid down on the western flank of the continental Pre-Cambrian protaxis. The area is divided into two physiographic units by a more or less abrupt escarpment (Niagara cuesta), which extends from Queenston on the Niagara river to Hamilton at the head of Lake Ontario and thence into the Bruce peninsula between Lake Huron and Georgian bay. East of this escarpment lies the Paleozoic lowland of Eastern Ontario which therefore extends only a short distance into the Western Peninsula and appears as a narrow belt along its eastern side. The western and much greater portion of the peninsula constitutes an upland with an average elevation above the eastern lowland of about 300 feet (91.2 metres). The southern part of the western upland is remarkably flat as shown by the following elevations along the lines of the chief railways: Elevation at | Elevation Elevation Niagara Falls.) at Summit. at Windsor. | ] Feet. | Met. | Feet. | Met. | Feet. | Met. | Michigan Central Ry.— | | Niagara Falls to Wind-| sor, 225-75 miles..... 585 | 177°8| 815 | 247-8) 580 | 176-3 (361-2 km.) | | | Grand Trunk Railway— | | Niagara Falls to Wind-. | | sor, 229-35 miles....| 573 | 174:2| 1007 | 306-1) 579-4 176-1 (366-9 km.) | A little farther to the north, the maximum elevation on the line of the Grand Trunk railway from Toronto to 40 Sarnia is 1,248 feet (379.4 m.), while in the county of Grey near Collingwood a maximum elevation of 1,706 feet (518.6 m.) is reached in the Blue mountains. A heavy mantle of drift covers almost the whole of the area and, in places, attains a remarkable thickness. Post-glacial accumulations in the form of stratified sands and clays are widely distributed and the strand lines of post-glacial lakes are marked by beaches of gravel and sand. These glacial and post-glacial soils are of great fertility and, aided by the southerly latitude, render the Western Peninsula of Ontario one of the finest agricultural sections of Canada. Glacial striz with a general southwest trend are to be seen wherever the rock is sufficiently hard to retain them and the exposure to the weather has not been too long. The rock basin of Lake Ontario, at its deepest point, is 738 feet (224.4 m.) beneath the surface of the lake, and Lake Huron reaches a maximum depth of 750 feet (228.0 m.). On the other hand, Lake Erie is nowhere more than 210 feet (64.0 m.) deep, and its average depth is very much less. The deepest part of Lake Ontario is off its southern shore: this lineal depression is thought to represent the bed of a great pre-glacial river which entered the basin of Lake Ontario from the west and drained a wide area in that direction. The waters of the Lake Huron basin are believed to have entered the Ontario valley by a great river whose course was down the western side of Georgian bay, across the Province of Ontario to a point a little east of Toronto and thence southward to a junction with the river in the Ontario basin. It would appear, therefore, that in pre-glacial times, Lake Erie did not exist and that Lakes Huron and Ontario were either absent or of much restricted area. The enormous accumulations of drift which choked the above mentioned pre-glacial valleys are responsible, with ~ some later modifications, for the present distribution of land and water in this area. Significant of the recent origin of the present system of drainage, is the fact that the water of streams rising 25 miles (40.0 km.) north of Toronto follows a circuitous path of 700 miles (1126-5 km.) in order to gain access to Lake Ontario. The thousands of islands along the eastern side of Georgian bay likewise attest the recent invasion of the waters of Lake Huron into the Pre- Cambrian oldland of Central Ontario. 41 Grand Manitoulin island and a number of smaller islands in the northern part of Lake Huron are formed of the same series of Ordovician and Silurian rocks that appear in the Western Peninsula. These islands must therefore be included in a general sketch of the Palaozic formations of the region. The Palzeozoic—Pre-Cambrian contact extends across the Province of Ontario from near Kingston to the head of Georgian bay. Northward from this point it is hidden under the waters of Lake Huron except for its occasional appearance on some of the islands along the east side of Georgian bay and on the islands between Manitoulin and the north shore of Lake Huron. GEOLOGY. The formations exposed in this district are indicated in the following table — Genessee (Chemung.) Devonian... .} Hamilton. Onondaga. Oriskany. (Monroe. Salina. Guelph. Silurian... ..{ Niagara. | Clinton. Medina. Cataract. Richmond. Lorraine Eden. Witicar Ordovician. . | Collingwood. Trenton. Black River. | Lowville. _ The brow of the Niagara cuesta is marked throughout its whole extent by a heavy bedded dolomitic limestone— he Lockport dolomite. The more or less precipitous face 42 of the escarpment affords many excellent exposures of the formations beneath; in the Niagara gorge the section ex- tends down to the Richmond, and in Manitoulin island to the Collingwood. The lower Ordovician formations are best seen on the small islands north of Manitoulin. The western peninsula affords numerous exposures of the upper Silurian formations and the different members of the Devonian series, but none of these are to be seen in the Manitoulin islands. The following list indicates briefly the points at which the various formations may be most conveniently studied: Chemung... ..: 2.4... 3. -Kettle point: Hamiltons.....22... ...bhedford: Onondagas-« aaa. Port Colborne, Pelee island. Monroeisn Ji 25k ane Amherstburg. Miagaravcste Mae ea an Niagara, Manitowan- ing, Collingwood. Medina and Clinton. ... Niagara. Gataractike ete see Manitoulin island, Col- lingwood, Niag- alias Lorraine and Richmond. Clay cliff, Manitoulin island. Near Col- lingwood. Collingwood and Utica. .Craigleith. “Prentonuce. eee Shore near Colling- wood. Lowville, Black River and Trenton..... Islands north of Man- itoulin. The relationship of the Cataract, Medina and Clinton formations may be studied to better advantage at Hamilton and at the forks of the Credit. (See Excursions B 3 and B 4). An opportunity to examine the Guelph exposures is presented by Excursion A1I2. The crystalline Pre-Cambrian rocks of the contin- ental protaxis occupy the whole of the eastern shore of Georgian bay and extend along the north shore of Lake Huron. The subdivisions of the Pre-Cambrian recognized within the area covered by the excursion are, in descending order, as below :— 43 Huronian. Laurentian. Grenville. Exposures of the Huronian are to be seen along the north shore and on numerous islands westward from the vicinity of Killarney. Bell has mapped the rocks of this age in two series—a lower series, ‘‘sericite, chlorite, hornblende, and arkose-schists, clay slates, greywackes, quartzites bands and dolomites’’, and an upper series con- sisting of quartzites. The quartzites form prominent ridges with a general east and west direction which constitute a striking physio- graphic feature of this part of the north shore. Near Killarney an altitude of 1385 feet (421 m.) is attained and even greater heights are reached a short distance inland. Both series of the Huronian are invaded by numerous masses of diabase, diorite and granite which afford inter- esting contact phenomena. The gneisses and gneissoid granites of the Laurentian form most of the shore of Georgian bay from Killarney to the Palzozoic contact at its southern end. The continuity of this series is interrupted, however, near Parry Sound by a band of Grenville rocks with which some interesting erup- tives are asssociated. ANNOTATED GUIDE. Lake Ontario—Alt. 244-99 ft.; 74-37 m. Lake Ontar 10 is 193 miles (310-8 km.) long, 53 miles (85-3 km.) wide and 7,450 square miles (19,310 sq. km.) in area. The mean elevation is 244-99 feet (74-37m.) and the maximum depth 738 feet (224-9 km.). The north shore of the lake, in the vicinity of Toronto, consists largely of sand, but bold cliffs of glacial material face the lake to the eastward of the city at Scarborough Heights, where one of the finest glacial sections in the world is presented. (See Guide Book to Excursion B-2). Toronto island has been formed by debris swept westward from these heights by a current which sets along the north shore. To the west of the city a few exposures of Lorraine shales occur at the water level. The red shales of the 44 Richmond formation underlie the sands and gravels around the western end of the lake and continue to the Niagara river and beyond into the State of New York. Exposures are not to be observed at the water level, but numerous outcrops occur a short distance inland. A few miles inland from the south shore of the lake the Niagara cuesta rises to a height of about 350 feet (106-7 m.) above the water. The strip of land between the cuesta and the lake, extending from the Niagara river to Hamilton is the finest fruit-growing district in Canada. Grapes and peaches of excellent quality are produced in abundance, as well as many other kinds of fruit. Sixty-six varieties of grapes are raised in the district. Port Dalhousie—Alt. 250 ft.; 76 m. Port Dalhousie was an im- portant ship-building centre before the advent of railways in Ontario. At the present time it is best known as the northern portal of the Welland Canal, which connects Lakes Erie and Ontario. Two canals have been con- structed along this route by the Canadian Government. The first canal, commonly referred to as the ‘‘old canal,” has a depth of Ito feet 3 inches (3-07 m.); it was begun in 1824 and completed in 1833. Construction work on the new canal began in 1872 and was completed in 1887. The total length is 26-75 miles (43 km.), and the total rise, or lockage, is 326-75 feet (99:6m.). There are 26 locks, each of which is 270 feet (82-3 m.) long, 45 feet (13-7 m.) wide and 14 feet (4-2 m.) deep. St. Catharines—Alt. 346 ft.; 105-18m. Leaving Port Dal- housie, the electric railway crosses the fruit lands to St. Catharines. The ascent is gradual over post-glacial accu- mulations, which may be seen to the west of the harbour at Port Dalhousie. About half-way, the line of the old canal is crossed. St. Catharines is noted for its paper and rubber manufactories, but more particularly as the centre of the fruit industry. A saline spring at St. Catharines contains per gallon of water the following solids: NBC) ecm nee ee 2200-9370 grains Caley cee. oh ee REO“ EO® MigGlos occ... alee A Ao eee OAS OS IG ees AAR ie aces, 19-6833 grains CaSO4 138-5538 WACO Rs ious 3-6470 1 5G GSS eee -0980 IM feel B22 Ie oe op i ea Ree -0496 Leaving St. Catharines, the railway begins the ascent ot the Niagara cuesta. No exposures of the Richmond or of the overlying Cataract sandstone, shale and limestone are to be seen, but at Merritton (Alt. 411 feet, 125-2 m.) the white and red mottled sandstone and shale of the Medina formation crops out on the west side of the track. Thorold—Alt. 595 ft.; 180-8 m. On approaching Thorold, the old canal may be seen to the west and the new canal to the east. The dolomitic limestone of the Niagara (Lock- port) formation is exposed above the new canal and may be seen in the distance. From this point a large amount of excellent building stone has been quarried. The metallurgical works of the Coniagas Reduction Com- pany in which a large amount of Cobalt ore is treated are situated near Thorold. Niagara Falls—Alt. 557 ft.; 169-3m. Between Thorold and Niarara Falls, the railway continues on the upland and, in places, is close enough to the brow to afford an outlook over the lowland to the north. The Pleistocene deposits are of post-glacial character, and the district is better adapted to general agriculture than to fruit raising. A full account of the geology of Niagara Falls and the sur- rounding country is given in the guide to Excursions A4 and Br; to these the reader is referred. From Thorold to Port Colborne 18-8 miles (29-1 km.) the country is flat or slightly sloping to Lake Erie. About 15 miles (24-1 km.) from Thorold a peat bog covering six or seven square miles is crossed. Beyond this is an exposure of unfossilife ous shaly 'mestone, which probably belongs to the Salina formation at the top of the Silurian. The Oriskany sandstone at the base of the Devonian is not exposed, but the Onondaga limestone is represented near Humberstone and continues to the shore of Lake Erie. Port Colborne—Alt. 583 ft., 177-74 m. *QUIOGIOD WOg Moe jatar Jo Ye] SurMmoys Jeo] 1esNs Jo doz oy} WOIy MoIA *$-S) NOISUNOXA 47 GEOLOGY OF THE REGION AROUND PORT COLBORNE. BY CLINTON R. STAUFFER. GENERAL DESCRIPTION. The region about Port Colborne is a nearly level till plain, which was modified by the marginal lakes of the retreating continental glacier. Much of the land to north and west is covered by a great peat bog, which has been utilized toa limited extent in the manufacture of briquettes for fuel. The higher land usually means bed-rock close to the top of the ground, and it is not uncommon to see its smoothed and striated surface in the gutters along the highways and railroad tracks. The Lake Erie beach, in the vicinity of Port Colborne, is chiefly sand, and the mounds adjacent to it are of the same material, which the wind has heaped into dunes. In most cases the dunes have been rendered stationary by the growth of vegetation, but to the west of the town some of them are in a semi-active state of migration. The points of land (see the accompanying map) projecting into the lake, however, are almost invariably outcrops of Onondaga limestone (Devonian). This rock rarely rises more than a foot or two above the water level, but forms an effective barrier against wave erosion, which elsewhere has been so destructive. Port Colborne lies within the Ontario gas belt, and several of the wells may be seen in and about the town. The gas is obtained from a stratum of white sandstone within the Medina (Silurian), which is here about 450 feet (137-2) m.) below the surface. The Medina, which is chiefly red shales and sandstones, was seen outcropping along the Niagara gorge, especially at the Whirlpool Rapids and northward. It also outcrops along the escarp- ment westward to Hamilton. The general dip of the bed rock of this region is to the south, but it is usually too variable in amount to *QUING]OD WOg Jo som Ysnf auNp pues AreuOT}e}s B ‘JeO] TeBNS ‘)) NOISUNOXY PSUR Eaten APE Lan v0 Edey ae es Dn Vie Cea rae aa tienes Al2andC5. Legend Devonian Onondaga limestone Devonian | trace of Oriskany sandstone Silurian +i. Hogans quarry The Canadian Portland +2. Cement Co's quarry +3. Sugar Loafiasand dune Geological Survey, Canada Port Colborne Miles (Eee eee ‘ Kilometres i ee 9.8.3. mn Deets SER 49 record. Here and there fairly well developed anticlines and synclines appear, while at other places the rock seems to lie nearly flat. The southern part of the Port Colborne region is underlain by the Onondaga limestone, while the Cobleskill dolomite (Silurian) and the Salina beds (Silurian) occur immediately under the surface deposits to the north. These latter form but meagre outcrops although they are reached by the drill in boring for gas. [6] Great heaps of the Silurian rocks, removed during the construction of the Welland canal, may be seen to the northward from the village of Humberstone. These formations include dolomitic beds and shales of varying thicknesses. The Onondaga was formerly called the Corniferous limestone [5] because of the abundance of chert which it contains. While chert is a striking characteristic of this formation in Ontario near the eastern end of Lake Erie, it is rare or absent in the same beds which outcrop along the Detroit river and on the islands to the south. It is a most variable formation in its physical appearance. At the Port Colborne locality its upper portion is a dark bluish to brownish black limestone containing a great quantity of dark coloured chert. Just below this, and sometimes separated by a very sharp line, is a highly calcareous, semi-crystalline limestone filled with corals. This rock grades into beds of less purity, as the lower portion of the formation is approached, while the basal part is a conglomerate [9] (shown only in the bottom of the Welland canal) of Silurian pebbles mingled with sand and calcareous mud. The Onondaga limestone is abund- antly fossiliferous. Many of the fossils are silicified and stand out in relief with most of the structures preserved as the limestone weathers away under the thin coating of drift. Corals are most plentiful and these are often so numerous as to form true reefs. These coral beds may be traced westward from Fort Erie to Villa Nova—a distance of over 45 miles (72-44 km.) Many of the types described by E. Billings and James Hall, were obtained in the vicinity of Port Colborne. SECTIONS OF THE ONONDAGA. The Hogan Quarry. This quarry now abandoned but under the control of the Canadian Portland Cement 35066—4 50 Company, is located in the northwestern part of Port Colborne to the west of the interurban track (Port Col- borne division of the Niagara, St. Catharines and Toronto Railway) at the crossing of the Grand Trunk switch. Very little quarrying has been done, but quite a large surface has been stripped and this furnishes an ample opportunity for collecting. In general the rock is too hard for successful collecting from the unweathered portions. Corals and stromatoporoids are especially abundant and may be seen studding the exposed surface, while several species of gastropods and a half dozen brachiopods are not uncommon. Section of the Hogan Quarry. Thickness. feet. _metres. G:eSoilkandtanittss. sees cae ee eae I +305 5. Hard bluish limestone with rough black chert. Where weathered the chert stands out in relief. These beds are quite fossiliferous and afford good collecting. The top surface is well glaciated at the west end of the quarry. 4. Dark bluish limestone containing an abundance of - silicified compound corals which afford good collecting in the central portion of the quarry..... I- 3. Blue limestone with very little chert. The lower half is filled with corals chiefly of the small branching type. Among these Cladopora labiosa (Bil- lings) is abundant. In the cracks and crevices of the eastern portion of the quarry some small but very good spec- imensimay be found:. 4.) eee B “O15 2. Blue limestone with some black chert and often with shaly bedding planes. Sometimes the bedding planes are very rough and uneven, chiefly because of the presence of large corals. Crinoid stems of large size are conspicuous but the heads are rare. These beds are shown chiefly in the water hole... 5-83 1-78 _ on $s wn OO “458 On 5I Thickness. feet. metres. 1. Rather compact blue limestone, with little or no chert, and fossils less abundant. This portion extends to the water level in the lowest hole..... 5 1-52 The fossils found in this quarry are given in the first column on page 53. The Canadian Portland Cement Company’s Quarry. One mile westward from the last place discussed, on the Grand Trunk railroad, is one of the Canadian Portland Cement Company’s plants. In the manufacture of their product they use the Onondaga limestone and a post-glacial clay, both obtained nearby. This cement plant has a capacity of 3,500 barrels per day—over one and a quarter million barrels annually. The quarry is located a short distance to the west of the buildings, on a small low anticline, the axis of which runs a little to the north of east. In the quarry proper the beds dip off rather sharply to the north-northwest bringing in the higher beds in that portion of the pit. The best co!lecting is in the weathered portion of these upper beds, although much depends on the most recent stripping. The more massive beds of the interior and eastern side of the quarry, however, are not lacking in interest, for it is in them that the great masses of coral may be found. The surface of the extreme eastern side is well glaciated. Section of the Canadian Portland Cement Company's Quarry. Thickness. feet. metres. GmSoileandidiiiiterss mn Ao eae, Gee Ane GS. 3 “O15 5. Dark bluish limestone containing much black chert. Weathered | surfaces rough and uneven. These layers are sometimes separated from the under- lying beds by several inches of shale.. 4-5 1-372 . Somewhat massive, sub-crystalline, blue limestone with a small amount of chert, and corals rather abundant.... 3:5 1-067 35066 —4% Hiss 52 Thickness. feet. metres. 3. An impure blue limestone with little or no chert and a great many corals scat- tered through it. Bedding planes rough and irregular, often shaly and containing much carbonaceous matter. 2-6 -714 2. A rather massive, sub-crystalline, bluish gray limestone with partings of a greenish shale. This shale is found chiefly in the middle and lower part, and is said by Mr. Pettingill, chief chemist at the cement plant, to have a composition analogous to that of glauconite. The bedding of this mass is often rough and irregu'ar. Corals are abundant and well preserved, but almost impossible to collect. At the east side of the quarry these layers come to the top and show several sets of glacial striae on the exposed surface, the most prominent of which run S. 40° W._ These beds vary considerably in thickness, but the full amount here given is exposed along the east side of the quarry. This massive portion of the Onondaga is quite persistent and may be traced eastward into New York state..........053..4:4-. 18353 a5po4s I. Massive grey | mestone, passing down- wards into a slaty grey to brown impure limestone. These beds are streaked with semi-crystalline bands in which fossils are more abundant. They extend to the bottom of the water hole at the west side of the Quarry cues coe ee eee IO 3°05 The fossils found. at this locality are given in the second column of the accompanying table. The large mound, three-quarters o! a mile to the south of the cement plant is Sugar Loaf—a sand dune which is covered with vegetation and therefore stationary. Other dunes a short distance to the west are in a partial state of active migration. ONONDAGA CANADIAM PORTLAND CEMENT COMPANY’S oo) FOSSILS FROM HOGAN’S QUARR Y QUARRY NEAR PORT COLBORNE. AND THE Hogan Quarry. | | | | | | Canadian Portland Ce- ment Co’s Quarry. Sponges Hindia fibrosa (Roemer)............ Hydrozoa ... ty io>) 4 Clathrodictyon cellulosum Nicholson | x Stromatoporella granulatum Nichol- Xie Xeno x SO La Geeee Stromatoporella (?) tuberculata Nic-| holson..... Syringostroma nodulata Nicholson. ..| X X Corals Alveolites confertus Nicholson....... Alveolites distans Nicholson......... Alveolites ramulosus Nicholson......| Aulopora cornuta Billings..........| Aulopora tubiformis(?) Goldfuss.... .| x KK XK Bothrophyllum decorticatum Bullings XK aX Bothrophyllum promissum Hall... . . | Chonostegites clappi Edwards and) Haime.... Cladopora cryptodens (Billings)..... | Xx Cladopora imbricata Rominger...... | Cladopora labiosa (Billings).........| Xe X Cladopora pinguis (?) Rominger..... Cladopora pulchra Rominger.. Cystiphyllum vesiculosum Goldfuss. . [Xo =X eX ux Eridophyllum verneuilianum Edwards| and Haime Favosites basalticus Goldfuss........ Keo XX Favosites canadensis Billings........ Kea Xa aX. Fav osites cervicornis Edwards and Favosites emmonsi Rominger........ Xenex Favosites epidermatus Rominger....| Favosites limitaris Rominger........ x *K KK Pad Favosites radiciformis Rominger..... Xx Favosites turbinatus Billings........X xX Favosites winchelli Rominger........ | ~*~ Pad I 2 3 a OG KK OK OK OK OK * xs x KK KK OK Ke KK KK o4 Canadian Hogan Portland Ce- Quarry. ment Co's Quarry. Heliophyllum corniculum (Lesueur).. Xx X Heliophyllum exiguum Bullings...... x Heliophyllum halli Edwards and EL GUNG rear Sat iN ee cdi coe eine XBOX EX x|X X Xx Michelinia convexa d’Orbigny....... x Michelinia favositoidea Billings...... x xXuuex Romingeria umbellifera (Ballings).... x Snathophyllum arundinaccuin (2z7/l- UNOS) eee aeaen soa eT aT x Snathophyllum simcoense (Billings).. Snathophyllum stramineum (Billings) Syringopora hisingeri Billings...... XI OXGHEX X Syringopora maclurei Billings....... Syringopora nobilis Billings......... X X Syringopora perelegans Bullings...... x Zaphrentis gigantea Leseuur........ IK XE EXC OX Xt ae Xcemee Zaphrentis prolifica Billings......... Pad ~ ~< << < x x x x x< x< x > x ~ XK x x «KK KK Bryozoa Coscinium striatum Hall and Simpson x Fenestella parallela Hall............ x Fenestellaspie a iicciauueranineteo tae Xie xXaex Fistulipora subcava (Hall).......... X Reteporidra perundata (Hall)....... x Unitrypa pernodosa (Hall).......... Xx Brachiopods Amphigenia elongata Vanuxem...... x Atrypa reticularis (Linne@us)........ Xx Xx =X Xx Camarotoechia billingsi Hall........ Xx Camarotoechia tethys (Billings)..... Xx Centronella glansfagea Hall......... x Chonetes mucronatus Hall.......... x x Cyrtina hamiltonensis Hall......... x Delthyris raricosta Conrad.......... x Eunella linckleni Hall.............. X Leptzna rhomboidalis (Wilckens).... Meristella doris Hall............... Meristella nasuta (Conrad).......... Xo exe OX x|x xX Metaplasia disparilis (Hall)......... Xx X Orthothetes pandora (Billings)...... X xix Parazyga hirsuta Hall.............. Pentamerella arata (Conrad)........ x 3 X| X Reticularia fimbriata (Conrad)...... x< x KK KKK KK a0) Canadian Hogan Portland Quarry. Cement Co’s Quarry. i ee Se ay eG Rhipidomella cleobis (?) Hall........ Rhipidomella livia (Billings)........ Xx Rhipidomella vanuxemi Hall........| X Schizophoria propinqua Hall........ Spirifer duodenarius (Hall)......... | x x x Spinifer varicosus Hall.............. | Stropheodonta demisssa (Conrad)...., x Xx Stropheodonta hemispherica Hall....| x 4 Stropheodonta inequistriata (Conrad) | Xx X Strophonella ampla Hall............ Xe x Xo KIX Trematospira gibbosa (?) Hall....... x KK KKK XK x ~x< Pelecypods Conocardium cuneus (Conrad) ....... x Xx GOSURO DOG She cease ees ot ene Diaphorostoma lineatum (Conrad)... XGEX XaueX: XEN Xx Diaphorostoma turbinatum (Hall)... x x Diaphorostoma turbinatum cochlea-| (Nin: JEG Swear aco ceicle ote OB ae Loxonema pexatum Hall........... Platyceras carinatum Hall..........! x| Platyceras conicum (?) Hall......... | Platyceras erectum (Hall).......... XX x Xx Platyceras rictum Hall............. x Paltyceras thetis Hall.............. Xx Strophostylus varians Hall.......... x Turbonopsis shumardi (de Verneutl).. x x x Kx Crinoids Megistocrinus:sprsacerec ae ten oner Trilobites ehacopsrenistatay Hall sass eee X Phacops rana (Green).............. x | Proetus rowi (Green)............... xX 56 ANNOTATED GUIDE. Lake Erie—Alt.: 571-57 ft.;174-2m. Lake Erie is 239 miles (384-6 km.) long and 59 miles (95 km.) wide; it covers an area of 10,000 square miles (25920 sq. km.); the mean elevation is 571-57 feet (174-2 m.) and the maxi- mum depth 210 feet (64 m.) Lake Erie is the youngest of the great lakes, and owes its existence entirely to glacial and post-glacial agencies. The north shore of Lake Erie is low and sandy with numerous bars and spits. Dunes form in many places, and shifting sands cause much trouble in the harbours and even to a considerable distance inland. There are few rock exposures on the water line, but near Port Col- borne and at the western end of the lake, the Onondaga limestones are encountered a short distance inland. Rondeau—At Rondeau the drifting sands have been piled up in long ridges parallel to the shore and now present a characteristic undulating contour. Behind the series of bars lies Rondeau harbour, and west of that an extensive peat bog which extends for several miles w th a width of from a quarter to a half mile. In depth, the peat varies from almost nothing to 30 feet (9-I m.) in accord with the ridge-like bottom. Rondeau point, as well as most of the points along the north shore, owes its exist- ence to a current which sets eastward along the coast. Rondeau Provincial park occupies the peninsula of Point aux Pins and contains 1,950 acres (589 hectares) of wooded land which is probably the best example of the original forest to be found in the Western Peninsula. The ridge-like arrangement of the sand is well shown and is more pronounced on the lake side than on the harbour side. The tops of the ridges are about 12 feet (3:6 m.) above the water, while the depressions are about three feet (-9 m ) above that level. Towards the west, the elevation is so much less that the depressions graduaily become marshes and finally disappear beneath the lake. The soil is all fine, white, water-washed sand, and would support little vegetation if any except for the excellent sub-irrigation. Three distinct types of forest growth are presented as below :— 1. White pine belt along the lake front. a 2. Hardwood growth on the ridges. 3. Hardwood growth in the depressions. The most important trees are the following :-— On the ridges— White pine, Pinus strobus, L. Bur oak, Quercus macrocarpa, Michx. Chestnut oak, Quercus prinus, L. White oak, Quercus alba, L. Hard maple, Acer saccarinum. Beech, Fagus ferruginea, Ait. Tulip tree, Lyriodendron tulipifera, L. Basswood, Tilia americana, L. In the depressions— Red oak, Quercus rubra, L. Black oak, Quercus coccinea tinctoria, Gray. Scarlet oak, Quercus coccinea, Wang. Swamp white oak, Quercus bicolor, Willd. Black ash, Fraxinus sambucifolia, Lam. White elm, Ulmus americana, L. Silver maple, Acer dasycarpus, Ehrh. Red maple, Acer rubrum, L. Bitternut hickory, Carya amara, Nutt. In addition to the above there occur in less abundance black walnut, butternut, shellbark and mockernut hick- ories, yel!ow birch, sycamore, red elm, white ash, black cherry, white birch, aspen, large toothed aspen poplar, balsam poplar, hop hornbeam, blue beech and sassafras. m= ee Lae Sketch Map of Pelee Island. oY) Pelee Island—Thin and thick bedded dolomitic limestones of the Onondaga formation are exposed at many points on the island. Characteristic fossils may be collected in abundance at most of the Ridges of Onondaga limestone formed by glaciers and subsequently weathered. Pelee island, Ontario. outcrops. The more common species as occurring at a quarry on the west side of the island and at one near the north end are given below :— 60 West North Quarry. | Quarry. Rhizopoda— Calcisphera robusta, Williamson............... x x Hydrozoa— Clathrodictyon laxum, Nicholson... Bits rote atc X x Stromatoporella granulata, Nicholson. . Stromatoporella tuberculata, Nicholson and Murie Anthozoa— Acervularia rugosa (E. and H.)............... Cystiphyllum vesiculosum, Goldfuss............ Eridophyllum verneuilianum, F.and H......... Pavosites emmons,-Romingeia. 2.91.25 Favosites pleurodictoides, Nicholson............ Favosites radiciformis, Rominger............... Favosites turbinatus, Billings.................. Heliophyllum corniculum (Lesueur)............ Heliophyllum halli, E. and H.................. Syringopora hisingeri, Billings................. Syringopora tabulata, E. and H............... Zaphrentis gigantea, Leswueur.................. Zaphrentis prolifica, Billings................... Bryozoa— Coscinium striatum, Hall and Simpson......... Cystodictya gilberti (Meek)................... Xx FKenestella)parallelat Halls... ..090 seh ede alee x Benestellais pian ara vay oe nies ace are ee x Monotrypellatenuis, Hal) .2 2 ee ee x Brachiopoda— Atrypa reticularis (Linneus) Camarotoechia billingsi, Hall.................. Camarotoechiacarolina,pHalle. s.r Chonetes hemisphercus, Hall.................. Xx Chonetesimucronatussiaal 1s. oe ee x Cyrtina hamiltonensis, Hall................... Xx Bunellaglinek|cenisee alla ne ee eee Leptzna rhomboidalis (Wilckens).............. INucleospira concinnawhalia. x ~ KX x KK x mM KK KK KK KK KK OK x x ~*~ xX 61 | West North | Quarry. | Quarry. | | Stropheodonta demissa (Conrad)...............) Xx x Stropheodonta hemispherica, Hall..............| x x Stropheodonta perplana, (Conrad).............. X x Pelecypoda— Aviculopecten princeps (Conrad)...............| x Conocardium cuneus (Conrad)........... | x akacy Clasgelliptica,w Gla reese ee e|| Xx x Gastropoda— | latyceradsicaninatum a ieeeenie ns Sanne