Science, Faculty of
Earth, Ocean and Atmospheric Sciences, Department of
DSpace
UBCV
Sanschagrin, Roland, Rev
Master of Arts - MA
University of British Columbia
The purpose of this paper is to give a brief description of the stratigraphy of the Lower and Middle Ordovician formations of the St. Lawrence Lowlands together with a short summary of the historical geology of the time. The basis for the paper is the literature on the subject, as the author's personal investigation has been restricted to one summer's work in a small section of the Lowlands. For the purpose of this description, the limits of the area are first defined and the region is then subdivided into three parts. There follows a description of the Beekmantown formation in which the problem of the Potsdam and Nepean sandstones is discussed. Afterwards, the historical geology of the epoch is given in resume. The Chazy formations are in turn examined, and the historical geology of the period is supplied. The more complex problem of the Black River, Trenton, and Utica stratigraphy is then analyzed. Changes in facies and thicknesses of contemporaneous formations in different parts of the Lowlands are studied with particular reference to the work of Raymond, Kay, Okulitch, Clark, and Wilson. An attempt to correlate these formations is made, but, owing to the complexity of the problem and the small amount of information available on many areas, the picture is left incomplete. The historical geology of this third marine invasion covering the St. Lawrence Lowlands from Black River to Utica time, is reviewed. The bibliography does not pretend to be exhaustive. It contains works on the stratigraphy of the Lower and Middle Ordovician Period and some works dealing with the palaeontology have also been included as a useful complement to the stratigraphy.
LOWER AND MIDDLE ORDOVTCIAN OF THE ST. LAWRENCE LOWLANDS STRATIGRAPHY AND HISTORICAL GEOLOGY i ~ e T 3 / > 7 Hrt Fir Sty Lb by top. h REV. ROLAND SANSCHAGRIN O.M.I., B.A., Lc. Sc. App. A THESIS SUBMITTED IN PARTIAL FULFILMENT OF THE REQUIREMENTS FOR THE DEGREE OF MASTER OF ARTS i n the Department of GEOLOGY and GEOGRAPHY We accept t h i s thesis as conforming to the standard required from candidates f o r the degree of MASTER OF ARTS Members of the Department of GEOLOGY and GEOGRAPHY THE UNIVERSITY OF BRITISH COLUMBIA A p r i l , 1951 I Abstract The purpose of t h i s paper i s to give a b r i e f description of the stratigraphy of the Lower and Middle Ordovician formations of the St. Lawrence Lowlands together with a short summary of the h i s t o r i c a l geology of the time. The basis f o r the paper i s the l i t e r a t u r e on the subject, as the author's personal inves t i g a t i o n has been r e s t r i c t e d to one summer's work i n a small section of the Lowlands. For the purpose of t h i s description, the l i m i t s of the area are f i r s t defined and the region i s then subdivided into three parts. There follows a description of the Beekmantown f o r -mation i n which the problem of the Potsdam and Nepean sand-stones i s discussed. Afterwards, the h i s t o r i c a l geology of the epoch i s given i n resume. The Chazy formations are i n turn examined, and the h i s t o r i c a l geology of the period i s supplied. The more complex problem of the Black River, Trenton, and U t i c a stratigraphy i s then analyzed. Changes i n f a c i e s and thicknesses of contemporaneous formations i n d i f f e r e n t parts of the Lowlands are studied with p a r t i c u l a r reference to the work of Raymond, Kay, Okulitch, Clark, and Wilson. An attempt to correlate these formations i s made, but, owing to the complexity of the problem and the small amount of i n -formation available on many areas, the picture i s l e f t incom-plete. The h i s t o r i c a l geology of t h i s t h i r d marine invasion covering the St. Lawrence Lowlands from Black River to U t i c a time, i s reviewed. I I The bibliography does not pretend to be exhaus-t i v e . I t contains works on the stratigraphy of the Lower and Middle Ordovician Period and some works dealing with the palaeontology have also been included as a useful complement to the stratigraphy. Aoknowle dgements The present investigation of l i t e r a t u r e has been accomplished under the supervision of Dr. V.J. Okulitch. To him I wish to extend my appreciation and thanks fo r his di r e c t i o n , advice, and generous contribution of many p u b l i -cations used i n t h i s study. To Dr. T.H. Clark, under whom I worked one summer and who so kindly sent me his l a t e s t publications and some recent references, I am greatly indebted. I also express my thanks to the Geological Survey of Canada and the Bureau of Mines of Quebec f o r having graciously sent me t h e i r publications on the area. TABLE OF CONTENTS Page Introduction Abstract I Acknowledgments II Extent of the St. Lawrence Lowlands 1 Beekmantown Formations 5 Extent and Description of Beekmantown . . . . . . . 6 H i s t o r i c a l Geology: Beekmantown-Ghazy 11 Ghazy Formations 13 H i s t o r i c a l Geology of Chazy Time . . . . . . . . . . 16 Black River and Trenton Group . . . . . 17 Black River Formations 19 Pamelia . 22 Lowville-Leray . . . . . . . . 24 Trenton Formations 27 Rockland 29 H u l l ?1 Sherman F a l l 32 Cobourg 34 The Ottawa Formation . 38 Utioa Formations 41 H i s t o r i c a l Geology: Black River-Trentoh . . . . . . 47 Plates and Figures 51 Bibliography 57 FIGURES AND SYNOPTIC TABLES F i g . l - - - - - - The St. Lawrence Lowlands, 2a Synoptic Table 1 - Lower and Middle Ordovician of Ontario 51 Synoptic Table 2 - Lower and Middle Ordovician East of Oka A n t i c l i n e . 52 F i g . 2 - - - - - - Palaeozoic Formations of Ontario Peninsula . . . . . . . . . 53 F i g . 3 - - •- - - - Ottawa Basin, St. Lawrence Lowlands 54 F i g . 4 - - - - - - Montreal-Quebec Basin .'. . . . . . 55 F i g . 5 - - - - - - Eastern'Part - St. Lawrence Lowlands 56 1. Extent of the St. Lawrence Lowlands The physiographic province c a l l e d the St. Lawrence Lowlands Is a p l a i n - l i k e area, floored by f l a t l y i n g sediments, bordering the Canadian Shield on the South. It extends north-easterly from Lake Huron and the head of Lake Erie to A n t i c o s t i and the Mingan Islands. From the analysis of the sediments, we acknowledge with J.F* Galey (1947, p. 164) that "the seas i n which several groups of Palaeozoic rocks were deposited d i d not at a l l time extend continuously over the entire region of the St. Lawrence Low-lands. During the various advances and retreats of these seas, parts of the region were eithe r flooded or emerged before others. The r e s u l t i s that the stratigraphic sequence i s not everywhere the same. The following table shows the r e l a t i o n of the Ordovician formations west and east of the Frontenac Axis, the narrow neck of Preeambrian highland crossing the St. Lawrence River between Kingston and Brock-v i l l e , Ontario, and connecting the elevated Adirondacks with the Preeambrian Shield of Canada. WEST of the Frontenac Axis EAST of the Frontenac Axis QU1ENST0N - red shale QUEENSTON - red shale , heavy dol. MEAFORD - shale, limestone RUSSELL - n tt DUNDAS - shale, limey bands CARLSBAD - shale, d o l . bands BLUE MOUNTAIN - grey shale BILLINGS - black shale COLLINGWOOD, - shale, lim*y bands EASTVTEW - limestone, shale WEST OF THE FRONTENAC AXIS EAST of the Frontenac Axis COBOURG -• Limestone TRENTON - limestone LERAY - limestone OTTAWA - limestone, sand, shale, dolomite LOWVLXLE - limestone at the base PAMELIA - limestone, sand-stone , shale ST. MARTIN - limestone, shale ROCECLIFFE - shale, sandstone OXFORD - dolomite MARCH -. dolomite, sandstone NEPEAN - sandstone Because we are dealing here with various sedi-mentary f a c i e s , we have to keep i n mind that rocks of the same age are not necessarily present i n a l l parts of the Lowlands, and that even contemporaneous sediments d i f f e r i n l i t h o l o g y i from place to place. In the same formation, sediments are changing l a t e r a l l y and v e r t i c a l l y . For the purpose of analyzing the Ordovician formations, the St. Lawrence Lowlands are here divided into three parts: 1 - The Western part composed of the Ontario Peninsula and Manitoulin Island 2 - The Central part, or the Ottawa-St. Lawrence region, composed of two basins; Eastern Ontario and Western Quebec. j> - The Eastern part composed of A n t i c o s t i Island, the Mingan Islands, and the adjacent coast of Quebec F i g . 1 3. The westerly part Includes Manitoulin Island and the part of Southwestern Ontario that fronts on Lakes E r i e and Ontario and l$£s west of the Frontenac Axis. The region west of the Frontenac Axis i s underlain by marine sediments of Ordovician, S i l u r i a n , and Devonian ages. I t i s divided into two parts by the Niagara Escarpment extending westward from Niagara River to Hamilton, and from there, northwestward, forming Bruce Peninsula and c o n t r o l l i n g the longer dimension of Manitoulin Island. Resting on the uneven Precambrian f l o o r , the Ordovician sediments underlie the entire region. They outcrop, however, only between the Escarpment and the Frontenac Axis, being covered progressive-l y to the west by the younger S i l u r i a n and Devonian rocks. A band of Ordovician also outcrops on the northern edge of Manitoulin Island. These rocks, of a maximum known thickness of 1,654 feet, have been divided into about twenty formations. The central part of the St. Lawrence Lowlands extends eastward from the Frontenac Axis. I t covers the area between Ottawa and the St. Lawrence River and straddles the l a t t e r to Quebec City below which i t extends f o r approxi-mately sixt y miles i n a discontinuous narrow band along the north shore. The northern boundary i s delimited by the c r y s t a l l i n e Precambrian rocks of the Canadian Shield. To the southeast, i t i s separated from the Appalachian region by the "Logan's Line," a thrust f a u l t zone extending from 4. the Hudson River and Lake Champlain northeastward i n a more or l e s s gentle eurving arc to Quebec C i t y . From there i t follows the St. Lawrence River into the Gulf. As i n the Ontario Peninsula, unfolded Palaeo-zoic strata underlie t h i s section. Only the Cambrian and the Ordovician systems are represented here. These are i n -truded l o c a l l y by the igneous rock of the Monteregian H i l l s . Fragments of Upper S i l u r i a n and Devonian have, however, been found on Ste.-Helene Island i n Montreal i n a l o c a l breccia. This i s the only evidence of sediments younger than Ordo-v i c i a n i n the central part of the Lowlands. This central part contained, during Ordovician times, two d i s t i n c t basins separated by the Oka or the Beauharnois a n t i c l i n e . Thus, today, we have two separate subdivisions: F i r s t , a wide area occypying the region between the St. Lawrence and the Ottawa Rivers west of the Lake of the Two Mountains; second, a large t r i a n g u l a r area straddling the St. Lawrence eastward from Montreal, narrowing wedge-like to a point northwest of Quebec C i t y . In general, we f i n d the same succession of strata i n these two basins, but, because the present Oka a n t i c l i n e acted as a b a r r i e r , there i s a considerable d i f f e r -ence i n the d e t a i l s of sedimentary strata and i n t h e i r t h i c k -nesses. In Eastern Ontario, the maximum thickness of the Ordovician strata i s 2200' to 2600*, while i n Quebec, i t 5. reaches 8550 s i n thickness. The t h i r d d i v i s i o n , separated from the central section by a gap of approximately 360 miles i s the combin-ation of A n t i c o s t i Island, the Mingan Islands, and a short narrow s t r i p on the north shore mainland. Ordovician and S i l u r i a n sediments are encountered i n t h i s Eastern part. Here a minimum of 13551 of Ordovician s t r a t a i s present. Thus divided into three d i f f e r e n t areas, i t w i l l be easier to describe and compare s t r a t i g r a p h i c a l l y the numerous formations of the Ordovician period and to i n f e r i n part the geological history of the period. BEEKMANTOWN FORMATIONS Central Part Eastern Part W. of Oka A n t i . Oxford, 240-320* March, 25- 301 Nepean ? 0-500' E. of Oka A n t i . Beauharnois, 1060' Theresa, 100' Romaine - 260' According to S i r William Logan i n h i s "Geology of Canada" (1863, p. 110), "the name of Calciferous sandrock was given by the New York geologists to the formation which immediately succeeds the Potsdam sandstone. Calpareous sandstone beds mark the passage between the two; but the ch a r a c t e r i s t i c portion of the formation, at lea s t i n Canada, i s a granular magnesium limestone or dolomite, which, from i t s rough weathered surfaces and i t s s l i g h t effervescence with acids, may have suggested the name of the Galciferous sandroek. In 1899, Clarke and Schuchert, working i n New York State, used for the f i r s t time the name Beekmantown. Ten or twenty years l a t e r , that name was generally accepted and has been used since as the lowest sub-epoch of the Ordovician period. Extent and Description of Beekmantown So f a r as we know, the Beekmantown dolomites are missing from the Ontario Peninsula where the oldest rocks are of Black River age, rest i n g upon the uneven Preoambrian surface. No Beekmantown or Chazy beds have been found i n outcrop from t h i s area. In ea r l y Ordovician time, there has been no sea i n -vasion west of the Frontenac Axis, and no subareal deposits have gathered i n that basin. I t i s probable that the low l y i n g old gneisses of the Canadian Shield were very slowly eroded down. They may have furnished the impurities found i n the Beekmantown and Chazy Dolomites and limestones east of the Axis. Beekmantown formation i s very well represented i n the central part of the Lowlands, covering what i s now Eastern Ontario and Western Quebec. In Eastern Ontario, Miss Wilson (1946,a) gives us t h i s picture i n the Ottawa basin 7. l y i n g between the Frontenac Axis and the Oka A n t i c l i n e ; FORMATION Disconformity 240* Pure Dolomite OXFORD l a s t sandstone bed 30 1 sandy dol., sandstone MARCH 1st dolomitic bed 1' to 500' pure sandstone NEPEAN Great unconformity uneven Precambrian f l o o r The picture gathered by Dresser and Denis (1944) fo r the Quebec Basin i s similar but with an increased thickness, FORMATION BEAUHARNOIS THERESA POTSDAM Unconformity 1,000* of pure dolomite l a s t bed of sandy dolomite 100' of sandy dolomite, sandstone 1st bed of sandy dolomite 1* to 1,696* of pure sandstone Great unconformity uneven Precambrian f l o o r The f i r s t problem encountered i s where to put the lower l i m i t of the Ordovician. Miss Wilson (1946,a) i s i n c l i n e d to Include i n the Beekmantown a l l the formations from the Precambrian f l o o r up, while other geologists exclude 8. from the Ordovician the Potsdam sandstone. The Potsdam i s placed by them i n the Upper Cambrian. Emmons (I838) and, more e x p l i c i t l y , Cushing, (1908) put the lower l i m i t of the Beekman-town to the f i r s t bed of sandy dolomitic limestone, s t a r t i n g the Theresa formation. Logan (1852,b; 1861; 1862), Owen (18^2), and B i l l i n g s (l8j?6) were the f i r s t to describe the few f o s s i l s found i n the Potsdam and to ascribe t h i s very pure sandstone to the Upper Cambrian. Everyone since has agreed with that conception. U l r i c h (1911) even recognizes the complete with-drawal of the sea from the St. Lawrence Lowlands a f t e r the deposition of the Potsdam sandstone. Here, there Is no e v i -dence of t i l t i n g as there i s farther to the east, i n what i s now the Appalachian Mountains. The passage beds of the Theresa sandstone at the base of the Ordovician are in v a r i a b l y com-posed of rounded, frosted, wind-blown sand grains, whereas the Potsdam i s predominantly composed of angular, bright, water-borne grains. Miss Wilson (194b,a) oonsiders the available fauna too small to permit d e f i n i t e c o r r e l a t i o n . Moreover, i n the Nepean sandstone, she found that L l n g u l e l l a acuminata occurs together with Ophileta compacta, Eooliomphalus g a l c i -ferous, and other Lower Ordovician forms. As the l i t h o l o g i c character of the Nepean-March-Oxford formations suggest a normal succession produced by an advancing shallow sea, and because she does not f i n d any evidence of a withdrawal of the sea i n the Ottawa region, Miss Wilson prefers to put the Nepean i n the lower Beekmantown rather than i n the Upper Cambrian. These two opinions, however, are not absolutely-contradictory. The Potsdam marine invasion may have been l i m i t e d to the area east of the Beauharnois a n t i c l i n e where the pure Potsdam sandstone was deposited. A f t e r recession, the new invasion may have deposited the Theresa and Beauharnois beds over the Potsdam, while to the west of the a n t i c l i n e , the sea may have deposited the normal sedimentary succession of the Nepean-March-Oxford's beds. This, however, does not seem to correlate as well the Beekmantown strata on the two sides of the Oka a n t i c l i n e , which, a f t e r a l l , was just a minor topographic feature. I t was surely not a r e a l b a r r i e r l i k e the Frontenac Axis which was prominent during the Palaeozoic era. Overlying the sandstone i n the central Lowlands i s a t r a n s i t i o n a l formation of alternating poorly consolidated dolomitic sandstone and sandy dolomite. I t i s 25' to 30V th i c k i n the Ottawa region, gradually thickening to 100' to the east of the Oka a n t i c l i n e . These t r a n s i t i o n a l beds have been named Theresa by Cushing (1908) from the type l o c a l i t y i n New York State. This name i s now generally accepted. Miss Wilson (1946,a) c a l l s them the March formation i n the Ottawa region even i f they have approximately the same c h a r a c t e r i s t i c s . Logan (1863) and E l l s (l895,a) have given 10. a de t a i l e d account of the Theresa extension i n the central basin of the Lowlands. Where not disturbed by f a u l t s , t h i s poorly consolidated d o l i m i t i c sandstone i s found more or l e s s i n a concentric zone within the basin next to the Kepean and Potsdam sandstones. The few f o s s i l s found i n these beds are d e f i n i t e l y of lower Ordovician age. Overlying the impure dolomite of the t r a n s i -t i o n a l beds i s a sequence of t h i n and t h i c k bedded, rusty, deep to l i g h t grey weathering, limy dolomite beds varying i n thickness from 240 feet i n the Ottawa basin to a mazimum of more than 1,060 feet to the northeast of Montreal. Subsidiary amounts of sandstone, shale, and limestone are present, as well as argillaceous i n c l u s i o n s , or t h i n shaly bands. Sand grains almost always rounded are common throughout the formation, becoming more so as the top i s approached. Many beds contain hard spherical masses from s i x inches to two feet i n diameter weathering concentrically. These have been considered to be concretions or cryptozoons. In general these beds are not f o s s i l i f e r o u s , containing a few Lower Ordovician algae, gastropods, brachiopods, t r i l o b i t e s , and ostracods. Raymond (1915,a) gave the name Beauharnois to t h i s phase of the Beekmantown beoause i t i s best developed along the a n t i -c l i n e of t h i s l o c a l i t y . Miss Wilson (1946,a) does not accept t h i s recognized name and c a l l s t h i s same formation Oxford i n the Ottawa Basin. These dolomitic beds follow approximately the same trend as the Potsdam and Theresa making a new con-11. centric band along the basin edge. The part of the Lowlands l y i n g i n the Gulf of St. Lawrence also has one formation of Beekmantown age, named Romaine by Twenhofel (1931) from Romaine Island where i t i s best exposed. It i s composed of two to twenty feet of poorly consolidated shaly sandstone overlying the Precambrian and f i l l i n g up i t s uneven f l o o r . About 250 feet of thick beeded cavernous dolomite with s i l i c i f i e d humps complete t h i s forma-t i o n . F o s s i l s are rare and almost always poorly preserved. On the basis of thirty-seven recognized species, Twenhofel (1931) suggests c o r r e l a t i o n with the Upper Beekmantown i n the Lake Ghamplain region. This would imply that the Mingan Islands region was not submerged u n t i l l a t e Beekmantown. Be-cause of the lack of outcrops between St. Maurice River and Mingan Islands, a distance of more than 400 miles, i t can be postulated that the shoreline of the Beekmantown sea was arcuate to such an extent that the deposits i n the intervening areas now l i e f a r to the east of the actual boundary of the Precambrian rocks. H i s t o r i a a l Geology: Beekmantown-Chazy The geological history of the Beekmantown time i n the St. Lawrence Lowlands seems to have followed approxi-mately t h i s sequence. The late Upper Cambrian sea completely withdrew from the Lowlands a f t e r having deposited the Potsdam sandstone i n the Montreal basin, and possibly the Nepean i n 12. the Ottawa basin. A f t e r a period of subareal erosion of the top beds of the sandstones, the new marine invasion marked the beginning of the Ordovician period. This submergence was f a r more widespread than the preceding Upper Cambrian one. Coming from the east, the invading sea reworked rapidly the free rounded windblown sand grains now found i n the Theresa and the March formations of the central area. The western boundary of the marine invasion seems to have been the Frontenac Axis because no Beekmantown beds have been found i n the Ontario Peninsula. Soon the water was clear nearly a l l over the r e l a t i v e l y shallow sea of the central area of the Lowlands on both sides of the Beauharnois a n t i c l i n e . West of the a n t i c l i n e , 2j>0 feet of calcium car-bonate was deposited i n early Beekmantown time over the pure sandstone of the Nepean formation and dolomitic beds of the March formation. On the evidence of f o s s i l s , reduced thickness, and l i t h o l o g y , we can assume that the sea slowly withdrew from the Ottawa basin at the beginning of middle Beekmantown stage. In the Montreal basin, however, the shallow sea continued i t s existence during t h i s entire Beekmantown time, and we now recognize there more than 1 ,000 feet of carbonate overlying the sandy dolomite and sandstone of the theresa. During the l a t e s t part of t h i s submergence, an arm of the sea Invaded the area now occupied by the Gulf of 13. St. Lawrence near the Mingan Islands and deposited 260 feet of limestone over the ten to twenty feet of reworked b a s i l beds. Only Upper Beekmantown f o s s i l s have been found there by Twen-hofel (1931)* The end of the Beekmantown period saw a complete withdrawal of the sea from the entire St. Lawrenoe Lowlands f o r , with the beginning of the Chazy stage, a t o t a l l y d i f f e r e n t type of sediments and a completely new fauna i s encountered. CHAZY FORMATIONS Central Part Eastern Part W. of Oka A n t i . E. of Oka A n t i . St. Martin 1551 Aylmer 300 1 Mingan 155 1 R o c k c l i f f e 20»-150» This group, f i r s t named by Emmons (1842) from the type l o c a l i t y i n New York State, i s widespread i n the central and eastern parts of the St. Lawrence Lowlands. I t i s missing e n t i r e l y west of the Frontenac Axis where Chazy time seems s t i l l to be a period of erosion of the Ontario Peninsula. In the Ottawa Val l e y , the Chazy i s represented by shale with sandstone lenses and limestone. Raymond (1912,a) c a l l e d t h i s formation Aylmer because of the obvious differences between these beds and those of the Chazy area. As these two d i v i s i o n s of the Aylmer are maintained throughout the Ottaxva basin, Miss Wilson (1946,a) has considered them as two formations: the R o c k c l i f f e lower shales and sandstones and the St. Martin upper limestone beds. 14.. The R o c k c l i f f e i s composed of f r i a b l e l i g h t olive-green shales with a few pockets of dark ir r i d e s c e n t shale. The sandstone usually i s present i n lenses. I t i s fine grained and grey i n colour i n the eastern and central part of the basin, changing to a deep red to the west. These lenses vary from small proportions to t h i n , widespread sheets and to masses twenty feet or more i n thickness and several square miles i n extent. Some rip p l e marks are present. The thickness v a r i e s from twenty feet at the c i t y of Ottawa to an average of 150 feet farther east. The St. Martin formation i s dominantly limestone, but at i t s western margin and at i t s base, shaly limestones, t h i n beds of dark shale, and even sandstone are intermingled with the limestone. Generally, the limestone i s thick bedded and contains impurities. The maximum thickness i s unknown, but 155 feet have been found i n cores from a well near Alex-andria, Ontario. The St. Martin has not been distinguished west of the c i t y of Ottawa, and, i f present, consists of a few feet of shale inseparable from the R o c k c l i f f e below. To the east, the St. Martin becomes thicker and the limestone members become more prominent. I t i s quite probable, according to Miss Wilson (1937) that the deposition of part of these two Chazy formations was contemporaneous, the Rockcl i f f e being more marginal than the St. Martin. East of the Oka A n t i c l i n e , the Chazy exposures 15. are mostly pure limestone. The beds are p r a c t i c a l l y horizontal and only the top portion of the formation i s exposed. The log of a well at Ste.-Therese, north of Montreal, shows that these represent only the uppermost f i f t y to si x t y feet of the group, and that the lower 230 feet are sandstone, shales, and impure limestones. The exposed pure limestones are l i g h t grey and c r y s t a l l i n e , l a r g e l y composed of c y s t i d and c r i n o i d gragments. Coarse cross-bedding and refif structures are widespread, and a large fauna represented by over f i f t y species belonging to several phyla has been co l l e c t e d from these beds; Camarotae-chia i s the t y p i c a l braohiopod. Logan (1863, pp. 125-133), Sowter (1888), and E l l s (1902,b) have recorded the d i s t r i b u t i o n of the Chazy formation throughout the whole area. When we compare the f o s s i l l i s t of the Chazy formations of the central Lowlands with the one of Lake Champlain section, i t can be seen that the Lowlands exposures represent only the upprG part of the t y p i c a l Chazy from New York. Chazy formation has also been described from the Mingan Islands, i n Eastern Quebec. There, twenty to t h i r t y feet of c l a s t i c s t rata composed of a basal conglomerate, sandstone and shale, are usually found re s t i n g conformably upon the Romaine formation. The larg e r part of the formation i s fine-grained limestone containing i n a few places an abundance of well preserved f o s s i l s . Of 111 species, f i f t y -16. three are unknown elsewhere and twenty-five are i d e n t i c a l with or closely r e l a t e d to those of the central Lowlands. The t o t a l restored thickness i s given by Twenhofel ( 1 9 3 1 ) as only 145 feet. H i s t o r i c a l Geology of Chazy Time With the retreat of the sea at the end of the Beekmantown there began a period of erosion which i s now represented by the disconformity between the Chazyan and Beekmantownian beds. There has been no movement or t i l t i n g during t h i s erosion period. The available exposures of the contact show Chazy sandstones l a y i n g conformably on the Beek-mantown dolomite. The sudden change i n the l i t h o l o g y of the sediments and the appearance of an e n t i r e l y new fauna, are the reasons f o r postulating complete emergence. These f e a t -ures were f u l l y analyzed by Miss Wilson (1937). The Beekmantown sea withdrew from the Ottawa basin during the middle of the epoch. I t l e f t the Montreal basin a f t e r depositing a thicker series of carbonates and f i n a l l y , the eastern A n t i o o s t i area near the end of the epoch. A long period of erosion, or, at l e a s t , of non-deposition took place. We know from the fauna that no beds representative of the Lower or the Middle Chazy cover the Lowlands of the St. Lawrence. These beds are well represented i n the Eastern part of the Appalachian trough where the complete section, lower, middle, and upper Chazy, was accumulated as we see It 17. at Chazy, New York. The new sea then must have come i n from the southeast, probably along the north flank of the Adirondack mass, from the present position of Lake Champlain, spreading northeastward as f a r as the St. Maurice River and northwest-, ward beyond Ottawa. There seems to have been plenty of detritus to be spread around, because sandstone and shale are general i n the lower beds. In the Ottawa basin where the Chazy limestone i s impure the water must have been muddy. Later i n the period, the Montreal basin, fa r t h e r out from the shore, enjoyed cle a r waters and accumulated pure limestones. Calcareous skeletons and plates of echinoderms of a l l kinds were spread widely i n that t h i c k l y inhabited sea, and re-c r y s t a l l i z e d upon b u r i a l by new sediments. Even corals b u i l t up t h e i r reefs. That same invasion extended also to the Mingan Islands. The great difference, however, i n the fauna seems to require two d i s t i n c t troughs with highlands between. The sea invading t h i s portion of the Lowlands may have been coming from the main Appalachian geosyncline. The Chazy epoch came to i t s end with a complete withdrawal of the sea from the Lowlands, probably i n the same d i r e c t i o n from which i t had come i n . Black River and Trenton Group The nomenclature f o r the Black River and Trenton Group has changed very much since the f i r s t attempt 18. at c l a s s i f i c a t i o n by Amos Eaton (1824). We are dealing here with a continuous series of limestone strata from the beginning of the Black River to the end of the Trenton period. Lithology by i t s e l f , i n most of the cases, i s not s u f f i c i e n t to d i s t i n -guish d i f f e r e n t fromations. Raymond (1912, a, page 347) has divided these beds into more than ten zones according to t h e i r c h a r a c t e r i s t i c fauna, and has given formational names to these zone s: Group Faunal Zone Formational Names Climacograptus t y p i c a l i s U t i c a Utiea Ogygites canadensis Collingwood Fu s i s p i r a and Hormotoma Upper Picton Rafinesquina deltoidea Lower Picton Prasopora Trenton Trenton Crinoids H u l l T r i p l e c i a extans Rockland Cryptolithus) Parastrophia) Glens frails Gonioceras anceps Leray Black River Tetradium cellulosum Onchometopus simplex Lowville Upper Pamelia Fauna variable Lower Pamelia Marshal Kay (1937) has reviewed the complete history of the c l a s s i f i c a t i o n of the Mohawkian series. The 19. Following table shows the present standard c l a s s i f i c a t i o n that has been developed i n Northwestern New York and Eastern Ontario. Gloucester Collingwood Cobourg TRENTON GROUP Sherman F a l l H u l l Rockland ( H i l l i e r ( (Hallows11 (Denmark ( (Shoreham (Napanee ( (Selby Ghaumont BLACK RIVER GROUP Lowville Pamelia BEEKMANTOWN As we deal with the entire St. Lawrence Lowlands, we w i l l use the term Leray instead of the more recent Chaumont, because i n Canada, no younger beds than Leray are known i n the Black River Group. As f a r as possible, we w i l l follow t h i s c l a s s i f i c a t i o n f o r the entire St. Lawrence Lowlands. Where that i s not possible, we w i l l r e f e r the l o c a l terminology to t h i s standard one. Black River Formations The series of strata l y i n g between the Beekman-town limestone below and the Trenton limestone above, has been 20. given the term Black River by Vanuxem (1842) of the New York Geological Survey. I t was f i r s t considered to be a lower part of the Trenton. For more than seventy years, i t has been i n -discriminately used by various authors, but i t i s now r e s t r i c t -ed i n Canada to the separate group of limestone beds between the Chazy and the Trenton. In the l a s t f i f t y years, the group has been d i f f e r e n t i a t e d into three main members, recognized i n the St. Lawrence Lowlands: 1 - The Pamelia dolomite (Cushing, 1908) below overlying the Chazy discomformably; 2 - The Lowville limestone (Clarke and Schu-chert, I899) replacing the descriptive term "Birdseye" (Eaton, 1824); 3 - The Leray limestone (Cushing, 1911) above replacing the r e s t r i c t e d term Black River given to those beds by Clarke and Schuchert (1899). Kay (1937) i n h i s "Stratigraphy of the Trenton Group" believed that the strata i d e n t i f i e d as Leray beds at places east and west of the Frontenac Axis, are not of Black River age but of Trenton, due to the close s i m i l a r i t y of t h e i r fauna to the overlying Lower Trenton beds. Therefore, accord-ing to Kay, what has been c a l l e d Leray i n Canada should be included i n the Rockland formation of the Lower Trenton Age. Okulitch (1939 ,13) disagrees with Kay about the Leray formation found at Coboconk. On a faunal basis, i t should be retained 21. i n the Black River Group. As the question of the Black River-Trenton boundary i s an unsettled one, because of the lack of a complete faunal l i s t from type l o c a l i t y and of no sudden break between the two, we w i l l follow the former d i v i s i o n , leaving the Leray i n the Upper Black River and the Rockland i n the Lower Trenton. The Black River Group, because of i n t r i n s i c d i f f i c u l t i e s , i s often treated as a unit without attempting to divide i t into i t s component formations. Miss Wilson (1946,a) even unites i t to the Trenton and c a l l s a l l these beds the Ottawa Formation. We w i l l f i r s t t r y to d i f f e r e n t i a t e these beds as much as possible, and, l a t e r , we w i l l give her description. Here are some other terms that may be met with i n the l i t e r a t u r e f o r t h i s group of rocks: 1 - Rideau, given by Ami (1902,a) to the lower beds of rather fine conglomerate re s t i n g d i r e c t l y on Preeam-brian i n the Kingston area. They are now considered part of the Pamelia. 2 - Coboconk, given by Johnston (1912) to the Leray beds i n Central Ontario west of the Frontenac Axis. Kay (1937) placed t h i s formation i n Lower Trenton. Okulitch (1939,b) replaced these beds i n the Upper Black River.. 3 - Watertown, given by Cushing (1911) f o r a seven-foot t i e r above the Leray. 4 - Glenburnie, given by Kay (1929) f o r a couple of feet of argillaceous limestone that l i e s between / 22. the Watertown and the Leray i n a section near Glenburnie, Frontenac County, Ontario. 5. Chaumont, proposed by Kay (1929) to include Watertown, Glenburnie and Leray. Pamelia Cushing (1910) describes t h i s formation from the type l o c a l i t y i n New York, as consisting of a sandy base over-l a i n by blue, black, and grey limestones and dolomites with shaly partings. He found that same succession extending across the St. Lawrence to Kingston. Ami (1902,a) had c a l l e d the lower beds Rideau, r e s t i n g d i r e c t l y on the Precambrian. These beds are now considered to be the basal beds of the Pamelia. The Pamelia formation may have been found 115 miles west of Kingston. Okulitch (1939,b) i n h i s description of the Coboconk seotion proposes a c o r r e l a t i o n of the 181 Shadow Lake and of the 4j?» G u l l River with the Pamelia beds of King-ston. Farther west, the Pamelia beds have been recognized l o c a l l y i n the Lake SImcoe d i s t r i c t where they seem only to f i l l i n parts of the i r r e g u l a r i t i e s of the Precambrian f l o o r . In the central part of the Lowlands, the Pamelia formation has been recognized on both sides of the Oka a n t i c l i n e . Raymond (1911,a) correlated c e r t a i n beds at Ottawa with the Pamelia i n New York and at Kingston. In the Ottawa Valley, i t i s approximately 70 feet thick. The lower part i s composed mainly of impure sandstone layers with con-2?. siderable shale and a few, t h i n , dark grey or black limestone bands. The upper part i s interbedded limestone, shale, and dolomite, with a white sandstone layer at the base. According to the f o s s i l content, these beds are more c l o s e l y a l l i e d to the Lowviile of the Black River than to the underlying Chazy. To the west, the Pamelia beds extend up the Ottawa River v a l l e y i n the Preeambrian Shield to Allumette Island, where they have been preserved from erosion by down-block f a u l t i n g . Sixty feet of Pamelia have been recognized by Kay (194-2) at Douglas on the Bonnechere River and twenty to t h i r t y feet at Allumette Rapids along the Ottawa close to Pembroke. From Ottawa, Ray-mond (1912,a) followed eastward the Pamelia to L'Orignal, Province of Quebec, where he saw the l a s t outcrop of i t . Fur-ther;- work by V.J. Okuliteh (1936,a) recognized some seven to ten feet of Pamelia beds at St. Vincent de Paul Quarry and at Pointe C l a i r e on Montreal Island. The formation seems to cut out completely to the east only at J o l i e t t e . I t i s also re-s t r i c t e d to the North Shore of the St. Lawrence. In Southern Quebec, from the St. Lawrence to the International boundary, the complete lack of Black River beds, together with the evidence of Lacolle Congolomerate, indicates the non-deposition or the non-preservation of these beds. As no evidence of erosion was ever noticed on the upper surface of the Pamelia, i t indicates that a complete section of the formation i s ex-posed. Several forms of Tetradium with Bathyuriscus acutus, and several zones of Ostracods characterize the Pamelia. 24 Low i l i e -Le ray The three d i s t i n c t formations of Lowville, Leray, and Watertown on the New York side of the St. Lawrence are not recognizable i n Ontario i n the v i c i n i t y of Kingston. The Watertown, the highest of these beds, i s unknown. No charac-t e r i s t i c cherty beds of the Leray are found. The s l i g h t physical differences between the lower and upper portion of the limestones made i t convenient f o r Kindle (1916) to treat the Lowville and Leray i n t h i s area as a single l i t h o l o g i e u n i t . In the Kingston area, overlying conformably the fine even bedded top strata of the Pamelia, i s a coarser-textured limestone. The bedding i s much less regular and the colour i s a darker grey. Gross-bedding and aggregations of f o s s i l fragments show current action i n some sections of the lower beds. The upper beds of the Lowville-Leray, show a somewhat rubbly character, breaking up under weathering into i r r e g u l a r shaped pieces a few inches i n diameter. This limestone i s i n places nodular. Rounded pebble-like limestone masses are i n -terspersed through some more shaly beds i n d i f f e r e n t places. The thickness of the Lowville-Leray limestones i n Kingston i s about 35 ' to 40'. The abundance of f o s s i l s , the colour, and the coarser texture distinguish these from the Lower Pamelia beds. Thirty-two feet of these beds are found at Coboconk, 115 miles northwest of Kingston. In the Lake Simcoe area, the Lowville-Leray limestones rest on the Precambrian. I t i s very well exposed along the Precambrian and Palaeozoic contact north 25. of there, where, due to g l a c i a l plucking, i t forms escarpments three to twenty feet high. Parks (1914) lias recognized t h i r t y feet of Lowvllle beds i n that area overlying the d e t r i t a l red and green s c h i s t s , sandstone, and limestones, f i l l i n g disoon-formably the i r r e g u l a r Preeambrian surface. Foerste (1912) has described the Lowville basal formation along the western shore, of Cloche Peninsula north of Manitoulin Island. These basal beds, exposed f o r several miles, consist of reddish clay shales whose thickness i s not known even approximately. South-ward i n Cloche Peninsula and at Swift Current, whitish lime-stones overlie the red clays. Where the limestone beds rest upon the Preeambrian, they frequently are reddish and i n c l u -sions of quartzite pebbles are numerous. The limestone beds become very fine grained towards the top and have the d i s t i n c -t i v e birdseye appearance. Foerste (1912) has correlated these beds with the Lowville and Leray formations on a l i t h o l o g i c a l and palaeontological basis. The thickness varies greatly. In places, basal beds reach more than 70 feet f i l l i n g up the cav-i t i e s i n the uneven Preeambrian f l o o r . The overlying limestones have been estimated to 50 feet. In the central part of the Lowlands, the Lowville and Leray formations have usually been treated separately. Here, the Lowville i s made up of t h i c k and t h i n beds of f i n e , dense, or o o l i t i c , dove-weathering limestone. Between the limestone beds are many dark shaly partings. The t y p i c a l fauna, Tetradium cellulosum and Bathyurisous extans i s general 2b. i n these beds and separates them from the overlying Leray beds. The presence of Phytopsis tubulosum gives the c h a r a c t e r i s t i c "Birdseye" e f f e c t to that formation. These beds have long been known by t h i s descriptive term given them by Eaton (1824). Near Ottawa, the Lowville formation i s only t h i r t y feet thick and o v e r l i e s the Pamelia beds nearly everywhere. Like the Pamelia i t thins out eastward. At Montreal, Raymond (1912,a) has recognized only seven feet of i t . Okulitch (1939,a) a f t e r more detailed work, has recognized sixteen feet of Lowville at Montreal and nine feet further east along the Ouareau River close to J o l i e t t e . Everywhere they have the same dove-weathering appearance. The Lowville-Leray boundary i n the central part of the Lowlands i s no more d e f i n i t e than i n the Ontario Peninsula. The overlying Leray formation i s made up of thick beds of dark, dense, l i g h t weathering limestones. They con-t a i n numerous f a i r l y well preserved f o s s i l s . In both the Montreal and New York areas, the d i s t i n c t i v e features of the Leray beds are the presence of nodules and plates of black chert and i r r e g u l a r l y horizontal brownish sandy layers i n the massive limestone beds. White sublithographic limestone beds are also present. These disk-shaped masses of chert and sandy layers are not present around Ottawa where only the massive fa c i e s i s recognized by the f o s s i l s content. Raymond (1913,d) reports a maximum thickness of 40 feet i n the v i c i n i t y of Ottawa. As we go westward, the formation becomes thicker. 27-I t follows approximately the same trend as the Pamelia and Lowville. In the Montreal area, the Leray i s only 21 feet at Pointe C l a i r e and 23 feet at St. Vincent de Paul. Further east, i n the Ouareau River section close to J o l i e t t e , the Leray i s made up of t h i n and t h i c k limestone beds of generally bluish-grey colour with occasional shaly partings. The cherty f a c i e s i s absent from that l o c a l i t y and a v a r i a t i o n i n the fauna has also been noticed. The Leray, there i s 28 feet t h i c k . The upper beds of the Leray formation may be present along the Ste.-Anne River near the V i l l a g e of St. Alban according to Okulitch (1939,d). The four or f i v e feet of l o c a l Leray beds are criss-crossed i n that area with numerous shaly and s i l i c e o u s stringers and i s greyish blue oh weather-ing. I t i s than apparent, that the Leray beds are generally thicker than the Pamelia and the Lowville i n the central part of the Lowlands. These three formations t h i n out from Ottawa eastward towards Montreal and Quebec. The Trenton Formations The Trenton formations succeed the Black River limestone i n a continuous series of limy beds. No r e a l break has ever been noticed i n the St. Lawrence Lowlands between these two groups. The separation of these continuous lime-stone beds have been based on f o s s i l s , and, as the change i n fauna i s also gradual, i t i s not always easy to put one's 28. finger on the boundary of the two groups. That i s why many arguments have come up between s p e c i a l i s t s about placing c e r t a i n beds i n the Black River or i n the Trenton. "Under such circumstances," says Okulitch (1939,b, p. 331) "our sub-di v i s i o n s of t h i s continuous record w i l l necessarily have to be, to some extent, a r b i t r a r y and depend on a s t a t i s t i c a l evaluation of large f o s s i l c o l l e c t i o n s rather than on one or two 'index' fossils.w The word Trenton was o r i g i n a l l y used to desig-nate rocks both older and younger than i s now the pract i c e . In the type l o c a l i t y i n New York, a complete section i s not present. The term as i t i s now employed i s generally used to designate a group of limestone and shale formations d i s t i n c t from the Black River by i t s faunal content. The stratigraphic development of the limestone and i t s fauna received l i t t l e s p e c i f i c attention u n t i l Raymond (-1912,a; 1914,a) succeeded i n subdividing the thick Trenton series of Ontario into a number of formations as follows: Gloucester shale - Climacograptus zone Cbllingwood shale - Ogygites canadensis zone Cobourg limestone - Hormotoma & Rafinesquina zone Trenton limestone ( r e s t r i c t e d ) - Prosopora zone H u l l limestone - Orinoid zone Rockland limestone - T r i p l e o i a extans zone 29. Later Kay (1929) substituted the name Sherman F a l l limestone f o r Raymond's r e s t r i c t e d Trenton limestone. This name does not seem yet to be of general use. The tv/o upper shaly formations, the Collingwood and the Gloucester, have been s h i f t e d around and f i n a l l y set aside under various formational names as belonging to the U t i c a . There i s much that can be said concerning the p o s s i b i l i t y that the lime-stones and shales are contemporaneous i n o r i g i n , even i f they are due to quite d i f f e r e n t environments of deposition. So the Utica shale f a c i e s w i l l be treated here as a stratigraphio unit d i s t i n c t from the Trenton limestone but belonging to the upper part of the Trenton age. This i s what i s usually done i n Canada. Rockland Formation The Rockland limestone comprises the lowest Trenton, heavy bedded, dove-grey, somewhat c r y s t a l l i n e lime-stones, interbedded i n some l o c a l i t i e s with shale layers four to ten inches thick. Towards the top, the beds generally become thinner and break into platy fragments. West of the Frontenao Axis i n the Ontario Peninsula, Kay (1937) has sepa-rated the Rockland into two members: the Selby below and the Napanee above. The lower limestone characterized by Doleroldes ottawanus Wilson i s the Selby member. I t "consists of dark-grey to black, medium- to fine-textured petroliferous lime-stone i n t h i n beds, weathering buff, and having a jointed, s p l i n t e r y fracture." (Kay, 1937, P. 252) In the type 30. section i n Ontario, only the upper four feet of the member i s encountered, but, i n general, i t averages ten to twelve feet. The Selby member Is exposed i n many l o c a l i t i e s i n southern Lennox and Addington County, Ontario. It thins out and d i s -appears to the west. I t i s absent i n the northwestern Prince Edward county, where the Hul l l i e s on the c r y s t a l l i n e rocks. The Napanee member (Napanee, Ont.) over l i e s the Selby limestone. It i s marked by prominent shaly partings i n i t s limestone beds and an abundance of Dalmanelia rogata (Sardeson) (name changed to Resserelia) and Sowerbyella curds-v i l i e n s i s (Foerste), species that are uncommon i n the Selby. The limestone i s grey-blue, medium-textured, rather heavy bedded and has an exposed thickness of 34 feet at the type l o c a l i t y . The Napanee crops out i n a l l areas having the Selby member and follows approximately the same trend. The equivalent of the Rockland formation has also been recognized on Great Cloche Island i n Manitoulin d i s t r i c t , Ontario, and l o c a l l y c a l l e d the Cloche Island lime-stone. At the type section, i n the b l u f f west of Swift Cur-rent at the eastern end of the i s l a n d , the formation consists of 55 feet of light-grey, rather heavy bedded limestone with argillaceous beds i n the lower part. Foerste (1912) has re-ferred to these beds as 'ILeray member of the Lowville" and "Black River limestones.". Kay (1937), a f t e r further detailed work, has correlated these beds with the Rockland. The Cloche Island formation extends westward over much of the southern 31. part of the Island and i s seen also on St. Joseph Island and i n Michigan. The beds generally dip to the south beneath te H u l l limestone at the Goat Island channel. East of the Frontenac Axis i n the type l o c a l i t y , at Rockland near Ottawa, these beds reach a thickness of 40 feet. The average thickness i n the Ottawa basin i s only 25 fe e t . Westward from Rockland, the formation "extends i n rather continuous outcrop to Renfrew County, and i t i s ex-posed i n large o u t l i e r s along the Bonnechere River and i n the v i c i n i t y of Pembroke and i n small areas as f a r up the r i v e r as Mattawa." (Kay, 1937, p. 251) A large c o l l e c t i o n of f o s s i l s has been gathered from Pauquette Rapids. H u l l Formation Overlying the Rockland formation i n most areas, i s the H u l l limestone that includes the " s t r a t a which at Ottawa, B e l l e v i l l e , and i n central Ontario carry the w e l l -known Crinoid fauna." (Raymond, 1914,a, p. 246,549). Parastrophina hemiplicata (Hall) abundant i n the basal H u l l beds and rare i n the top Rockland, marks the boundary between these two formations. Generally, the formation i s composed of brownish to grey, sugary, limestone with more frequent bluish-grey clay partings i n the upper beds where Dalmanella i s common. West of the Frontenao Axis, the Hull formation extends i n a belt south of that of the Rockland from the v i c i n i t y of Midland on Georgian Bay, through Lake Simcoe, 32-K i r k f i e l d , L a k e f i e l d , and B e l l e v i l l e , and the southern penin-sula of LennoJJ. and Addington county underlying the north-eastern part of Amherst Island continuing into New York State. This formation has been c a l l e d K I r k f i e l d by Johnston (1910). The thickness of the Hull ranges from 85 feet to 110 feet. In the Manitoulin Island area, the Cloche Island formation of Rockland age i s d i r e c t l y o v e r l a i n to the south by the Hl/11 limestone on Goat Island. These beds are only 40 feet t h i c k i n the area and are similar to beds of the same age elsewhere. The H u l l limestone i s s p e c i a l l y well represented i n the Ottawa basin where i t has i t s type l o c a l i t y . The l i t h o l o g y i s i n part d i f f e r e n t . The lower beds are t h i c k and t h i n bedded blue limestone with a considerable amount of chert. They are also noted for t h e i r Crinoid content. The upper beds are more massive, coarse-grained, blue-grey limestone with comparatively few f o s s i l s except Tetradium. These two phases together reach a thickness of 90 feet to 100 feet i n the region. Sherman F a l l Formation Overlying the H u l l limestones are the Prasopora beds c a l l e d Trenton (restricted) by Raymond (1914,a) and John-son (1912). Kay (1937) has c a l l e d these beds Sherman F a l l . The base of t h i s formation i s placed at the f i r s t bed con-t a i n i n g Prasopora o r i e n t a l i s U l r i c h , a bryozoan that r a r e l y , i f ever, i s found i n other formations. This formation i s 22. generally more shaly but the l i t i i o l o g y i s v a r i a b l e . At Trenton F a l l s , New York, we f i n d 200 feet of dark brownish weathering, calcareous shales with dark grey, dense limestone interbeds. Coarse textured beds are infrequent. In Ontario, west of the Frontenac Axis, i n t e r c a l a t e d beds of coarse limestone have large r i p p l e - l i k e marks. In general, they are composed of l i g h t e r coloured and more evenly bedded limestone. I t outcrops i n a band southwest of the Hull formation from Amherst Island, through Prince Edward County, along the north shore of Lake Ontario. Farther west and north up the Georgian Bay, i t i s f o r the most part obscured by g l a c i a l d r i f t . It i s approximately 200 feet thick. Kay (1927) has subdivided the Sherman F a l l formation into two members: the lower part, he c a l l e d Shoreham, and the upper part Denmark. He found the Shoreham lower beds i n Lennox and Addington County, Ontario, and equivalent beds northeastward to Q,uebeo C i t y . The remainder of the Sherman F a l l formation are the upper beds of Denmark member. These Prasopora beds have been recognized by Caley (1926)' on Mani-t o u l i n Island where t h e i r general f o s s i l content i s d i f f e r e n t compared with the.other Prasopora horizons of Ontario. There, they seem to be only f o r t y feet thick. They have only a l i m i t e d d i s t r i b u t i o n f o r a few miles around L i t t l e Current and at Sheguiandah where they are seen i n contact with the Preeam-brian quartzites. The beds consist c h i e f l y of impure, arenaceous to magnesian limestone varying from dark to l i g h t grey i n colour and weathering buff. These beds are from a few inches to 1§ feet thick, with many t h i n ribbons of grey or 34. greyish, arenaceous shale. In the Ottawa basin, the Sherman F a l l has about the same c h a r a c t e r i s t i c stratigraphy and fauna. As i n the Ontario Peninsula, Raymond (1913) has joined together the Prasopora zone with the Cystid zone, giv i n g approximately a thickness of 100 fe e t . These beds are exposed at three separate areas within the Renfrew Gbunty D i s t r i c t northwest of Ottawa, where they have been l e f t by erosion i n a s y n c l i n a l structure i n the Canadian Shield. Gobourg Formation Overlying the Prasopora beds i s a series of " l i g h t to dark grey, argillaceous limestones and limy clays that weather to a loose i r r e g u l a r , grey, or buff-coloured clay-lime rubble. There are occasional interbedded bands of c r y s t a l l i n e and c r i n o i d a l limestones from a f r a c t i o n to two feet or more thick." (Sproule, 1936, p. 97) These beds have been f i r s t named the Picton Formation by Raymond (1912) and then changed to Gobourg Formation by the author (1921) when i t was discovered that Gushing had used the name Picton f o r a granite i n 1910. Ruedemann (1914) has described the Cobourg as a contemporaneous limy phase of the lower and middle tJtica. Parks (1928) has advanced the view that the Upper Cobourg and the Collingwood are inseparable because of the extension of Raymond's index f o s s i l f o r the Collingwood, Ogygites l a t i -5 5 . marginatus (Hall) into the underlying tipper Cobourg beds. Kay (1932) proposed to include the Gloucester and Collingwood with the Cobourg i n the Trenton group so as not to divide these formations considered as the Lower, Middle, and Upper U t i c a . The l a t e s t f u l l study of the Cobourg formation by Sproule ( 1 9 2 6 , p. 95) recognized i t as ^a separate and f a i r l y w e l l-defined u n i t , " giving i n d e t a i l the c r i t e r i a to determine the lower and upper l i m i t . The Cobourg formation west of the Frontenac Axis extends as a band across the central part of Ontario from Manitoulin Island to Pieton on Lake Ontario, trending i n a northwest-southeast d i r e c t i o n and forming another band over-l y i n g the Sherman F a l l . The surface width of t h i s band varies from a few yards on Manitoulin Island to a maximum of nearly twenty miles i n the v i c i n i t y of Lake Simcoe. These beds, l i k e the underlying Trenton and Black River gently dip to the south-west at a rate of t h i r t y feet to the mile. The t o t a l thickness i n Central Ontario i s about 200 feet, but the exact thickness varies greatly according to the amount of erosion during the Cobourg-Collingwood i n t e r v a l . In one l o c a l i t y on Manitoulin Island, f o r example, only t h i r t y feet of the Cobourg i s l e f t . In another nearby, the Collingwood black shale rests d i r e c t l y on Preeambrian quartzite. Kay ( 1 9 5 7 ) , following Raymond ( 1 9 1 4 ,a), has separated the Cobourg into two members: the Hallowel member, replacing the Lower Picton or Rafinesquina deltoidea zone, and the H i l l i e r member, replacing the Upper Picton or 3b. Hormotoiria and F u s i s p i r a zone. These names come from the town-ship i n Prince Edward County, where they are well developed. The Cobourg limestone beds have been recognized i n the Ottawa basin. The lower beds are present i n sections near Ottawa but seem to be absent further up the Ottawa River. Both lower and upper beds are present near Cornwall. Their description i s approximately the same as i n the Ontario Penin-sula, but the thickness has not been mentioned. When we cross the Oka Axis west of the Ottawa basin, we r e a l i z e that the Trenton of Montreal and Quebec i s very d i f f e r e n t from the Trenton of Ontario. The c o r r e l a t i o n of these limestone beds between these two basins had to be made through the Champlain Valley and around the Adirondacks. I t i s , however, i n e s s e n t i a l agreement with the t y p i c a l Trenton at Trenton F a l l s . According to Raymond (1913,a), the lowest 100 feet of Trenton i n the Montreal-Quebec area are older than the lowest beds of Ontario. Their c h a r a c t e r i s t i c f o s s i l s Parastrophia and Cryptolithus are unknown at Ottawa and Central Ontario but are at the base of the type section i n New York. Raymond*s f i n a l c l a s s i f i c a t i o n (1921) of the Trenton group i n Quebec Province i s : Uti c a shale - Upper Cobourg and Collingwood of Ontario Trenton (re s t r i c t e d ) - Rafinesquina and Prasopora zones (Sherman F a l l , Kay) Glens F a l l s - Trinucleus beds Lorette formation - Parastrophia beds 37. More recently, an almost complete section of Trenton limestone was acknowledged on the Island of Montreal where the t o t a l thickness i s 80G f e e t . Four new formational names have been proposed by Clark (1944) f o r these beds i n the region: Terrebonne formation Tetreauville formation Montreal formation Rosemount member St-Michel member Mile End formation U n t i l further work and publication on the description of the r e l a t i v e l y unknown Trenton l i t h o l o g y and fauna of the Montreal-Quebec basin, we have to be content with a very incomplete picture. The d i s t r i b u t i o n of the Trenton limestone has been given i n d e t a i l by Logan (1863, pp. 142-163). I t i s to be noticed that northeast of the St. Maurice River, the Trenton limestone can be seen to rest d i r e c t l y upon the Preeambrian i n a number of places. Generally, no basal d e t r i t a l beds have been noticed and the Trenton l i e s unconformably on fresh c r y s t a l l i n e rocks. Only i n the Lorette gorge close to Quebec City, a few inches of detritus have been noticed. The northernmost exposure occurs at Murray Bay on the north shore, but there i s a good reason to believe that the Trenton sedi-ments l i e beneath the waters of the s t r a i t between the Mingan Islands and A n t i c o s t i . 38. Another important point to mention i s the ab-sence of lower Trenton beds south of Montreal. The only-positive evidence of any Trenton i n that area i s the presence of the Lacolle conglomerate (Clark and McGerrigle, p. 1936) near the town of that name. This formation contains fragments of Beekmantown, Chazy, and Lower and Middle Trenton (Lower Sherman F a l l ) limestone. It i s covered by the Stony Point shale which i s thought to be of Middle Sherman F a l l age. An u p l i f t must then have taken place a f t e r the Lower Sherman F a l l time had begun, and before the end of Middle Sherman F a l l . During t h i s i n t e r v a l , t h i s minor and l o c a l u p l i f t gave b i r t h to the Localle conglomerate and, probably, enabled erosion to destroy the uppermost beds of the time, the Lower Trenton and Black River, i n the region south of Montreal. The Ottawa Formation A f t e r a complete detailed study of the Ottawa basin of the St. Lawrence Lowlands, Miss Wilson (1946,a, p. 25) did not succeed i n disentangling the numerous members of the Black River-Trenton groups i n that area. "A detailed study of the entire succession of the beds within t h i s comparatively large region, and the examination of many wells, have shown that there was no break i n deposition; that a l l the rocks average 86 per cent or more of carbonates, except f o r a few basal layers; that the thickness of the several l i t h o l o g i c types has shown a v a r i a b i l i t y not due to the consecutive deposi t i o n of several i n d i v i d u a l members but to the variable duration 39. of l o c a l conditions during one deposition; that, although a few f o s s i l s have a li m i t e d range, there i s a dove-tailing of the range of many others, considered t y p i c a l of the several members, across the boundaries of both members and formations; and that other f o s s i l s recur higher up where conditions are si m i l a r . "For these reasons, and f o r the p r a c t i c a l use of geologists and d r i l l e r s , the formation i s here considered as one, and the seven members of the former two formations are regarded as zones of faunal associations, with very i n d e f i n i t e and variable boundaries, depending upon the coincidence of a few short range f o s s i l s and minor v a r i a t i o n s i n the limestone. The name 'Black River-Trenton' i s retained as a time term." The Ottawa limestones were deposited i n the Ottawa basin a f t e r the period of erosion following the St. Martin formation of Chazy age. In the centre of the basin, the beds rest upon the St. Martin, (upper part of Aylmer), west of Ottawa upon the Ro c k c l i f f e (lower part of Aylmer), fart h e r west upon the Oxford, and i t probably l i e s d i r e c t l y upon the Precambrian rocks i n the extremity of the Xong arm of Palaeozoic sediments and i n l i e r s extending northwest of the Ottawa River. This overlapping i s due to the greater extension of t h i s invading sea covering a la r g e r part of the Precambrian Shield. The upper l i m i t of the Ottawa formation Is the appearance of the overlying black limestone and shale of the Eastview formation, a new name given by Wilson to the 40. Collingwood. The Ottawa formation i s 690' to '/OO' where i t has been preserved from erosion. To the west and north of the Basin, the formation gradually thins out i n contact with the rocks of the Precambrian Shield. Being unable to recognize Raymond*s palaeont-o l o g i c a l zones i n the Ottawa basin, Miss Wilson (1946,a, p. 21) divided the Ottawa formation into three l i t h o l o g i c a l phases: "A lower phase, t y p i c a l of basal deposits, consisting of shale, some sandstone, impure limestone, and dolomite; a middle phase of pure, t h i c k bedded, c r y s t a l l i n e limestone; and an upper phase with small amounts of shale, and t h i n , rather impure limestone layers near the bottom gradually giving place upward to the thick beds of limestone, some pure and c r y s t a l l i n e , some less pure with shaly partings. It i s emphasized that these phases merge with one another both v e r t i c a l l y and l a t e r -a l l y , and tnat t h e i r l i m i t s i n one part of the area are not necessarily those i n another." Many of the f o s s i l s persist from one of Wilson's l i t h o l o g i c a l phases into the next and no f o s s i l i s given to be t y p i c a l of any of these three phases. She gives the r e l a t i o n of her new l i t h o l o g i c a l phases with Raymond's faunal zones i n these terms ( i b i d . , p. 24): "The lower phase of i n i t i a l deposits roughly corresponds to the Pamelia and the lower part of the Lowville; the middle l i t h o l o g i c a l phase, to the top of the Lowville and the whole of the Leray, Rockland, and H u l l members; and the upper phase to the Sherman F a l l and Cobourg 41. members." The Ottawa limestone occupies more than 400 square miles i n the central part of the Ottawa-St. Lawrence basin. Miss Wilson gives t h e i r d i s t r i b u t i o n i n d e t a i l . U t i c a Shale From the description of the preceding Trenton group, we may say with Dresser (1944, p. 286) that "Un general, the Trenton limestones become purer toward the base and more shaly toward the top. The shaliness i s made apparent by more frequent and thicker shaly partings between limestone layers i n the Upper Trenton, and also by a greater diffused a r g i l l a c e -ous content throughout the limestone. This argillaceous i n -crease eventually reached i t s l o g i c a l goal i n the deposition of pure shale of the so-called «UticaT formation. Beoause, on the whole, the U t i c a shales are thick e r i n the east than i n the west of Canada and of New York State, the source of the muds has been considered to be Appalachian, which at that time must have been r i s i n g to greater heights than previously, so as to shed an enormous amount of mud into the Appalachian geo-syncline." This mud would I f i r s t accumulate marginally to the r i s i n g o l d land, and allow limestone to accumulate i n the clear waters beyond. "As the mud deposit spread westward ( i b i d . , p. 267), i t covered more and more of the already; accumulated limestone, so that, i n any li m i t e d area, the shale o v e r l i e s the limestone. But, i n places, the shale o v e r l i e s Middle Trenton limestone and, In others, Upper Trenton lime-stone. Thus, i n consequence, the lower part of the U t i c a may 42. be of Middle Trenton age, the middle part of Upper Trenton age, and the upper part may be post-Tretnon. Because of these con-d i t i o n s , i t i s well to keep the two rock formations apart as d i s t i n c t l i t h o l o g i c a l u n i t s , but to r e a l i z e that the develop-ment of certain parts of each may have been contemporaneous." With t h i s picture i n mind, i t w i l l be easier to take up the U t i c a shale formation separately i n the d i f f e r e n t parts of the St. Lawrence Lowlands. Raymond (1913,a) recognized two d i v i s i o n s i n the U t i c a of Ontario and Quebec; the Collingwood and the Gloucester. West of the Frontenac Axis, the contact of the Collingwood with the underlying Cobourg i s apparently discon-formable on Manitoulin Island. This has been noticed by Caley (1936) at four d i f f e r e n t places. On the south shore of Georgian Bay the hiatus i s at a minimum and the diseonformity i s only suspected. The Collingwood was described by Raymond (1913,a) as fine grained dark limestone al t e r n a t i n g with dark, rusty-weathering shales l y i n g upon the uppermost Cobourg and underlying the t y p i c a l black shales of the Gloucester. These beds were supposed to be characterized by Ogygites iatimar-ginatus H a l l (0. canadensis Chapman).. Further studies by Parks (1928) and Caley (1936,a) have discovered Qgygites i n the Cobourg and other horizons. Sproule (1936, pp. 94-95) has concluded that "Ogygites latimarginatus then should no longer be regarded as the index f o s s i l of the Collingwood formation. The genus Triarthrus i s a more s a t i s f a c t o r y 43. marker of the base of the Collingwood than i s Okygites. According to Parks, Triarthrus may also be used, i n Canada at l e a s t , to define the top of the U t i c a shale s e r i e s . " The Collingwood i s believed to have a thickness of about f i f t y feet and to per s i s t from Collingwood and Georgian Bay to the shore of Lake Ontario near Bowmanville. The formation, however, i s r a r e l y exposed because of i t s non-resist a n t character. Sixteen feet of these beds have been found on the north side of Manitoulin Island. Here the f o r -mation i s e n t i r e l y shale except f o r a few, t h i n , s i l i c e o u s limestone beds at the base. These beds are overl a i n by approximately 95 feet of soft, t h i n l y bedded to f i s s i l e shales and clay-shales, green, brown, and dark grey i n colour: It i s the Sheguiandah formation, a l o c a l name f o r the Gloucester shale. The contact with the underlying Collingwood i s not exposed and has been f i x e d where the genus Triarthrus ceases to appear. The two formations cannot be separated accurately i n well borings. .These beds are divided into three d i f f e r e n t Palaeontological zones: The Graptolite zone making the 18 lower feet; The Lophospira abbreviata middle zone, only b feet thick; The Dalmanella fultonensis l o r r a i n e n s i s zone forming the upper 71 feet. To the west, the Collingwood formation of Georgian Bay i s overlain by 200 feet of blue, so f t , sparingly f o s s i l i f e r o u s shales of the Blue Mountain formation. These 44. beds become darker southeastward and take the general name of the Gloucester formation when they reach Lake Ontario. This formation i s also very sparingly exposed but o v e r l i e s everywhere the Collingwood shale of si m i l a r l i t h o l o g y . The thickness i s about f i f t y feet.along Lake Ontario from Bowman-v i l l e to Whitby where most of the outcrops are seen. Through-out the Ontario region, where younger sediments of post-Trenton age are preserved, they are of lower Cincinnatian and of c l a s t i c character. In Central Ontario, these are represented by the Lower Dundas arenaceous shales and on Manitoulin Island by the Weflwemikongsing shales. East of the Frontenac Axis, the Collingwood and Gloucester shales are also represented. Raymond (1911,a; 1913,a) was the f i r s t to apply these names to the Ottawa basin and to separate these limestones and shales on a Palae-ontological basis. His further studies (1921, 1922) and those of U l r i c h (1912), Ruedemann (1922), and Parks (1928)' have re-shuffled many times the boundaries and the age of these beds. Recently, Miss Wilson (1946,a,p. 28) "because of the v a r i -a b i l i t y of the boundaries and the several types of l i t h o l o g y embraced by the term 'Collingwood', and the i n c l u s i o n i n i t of the 15 feet or more of shale more cl o s e l y a l l i e d to the Gloucester above," dropped the recognized names to give a purely l i t h o l o g i c a l d i v i s i o n of these beds. She brought i n two new names: The Eastview lower limestones interbedded with shales and the B i l l i n g s upper pure black shale, and retained 45. the terms Collingwood and Gloucester as time terms. The thickness of these two formations i s about 300 feet at Ottawa, l a s t of the Oka Axis i n the Montreal-Quebec basin, the Trenton limestone i s everywhere flanked towards the southeast by the Uti c a dark shales. Dresser (1944, p. 266) gives t h i s b r i e f summary of the d i s t r i b u t i o n . "They occur along the southeastern shore of the Island of Montreal and thence are r e s t r i c t e d to the northern side of the r i v e r as f a r as Grondines, beyond which they occur on both sides but predominantly on the north side... Beyond Quebec City, they are seen i n the gorge below Montmorency F a l l s and on the west side of the Island of Orleans. Their l a s t outcrop toward the northeast i s at Murray Bay. From Montreal southeastward, these black shales enjoy a remarkable development. They out-crop over a wide area eastward through Delson as f a r as the Richelieu River. Thence the belt of outcrop turns southward and includes a s t r i p of country approximately two miles wide west of the Ri c h e l i e u and ten miles wide east of i t . This b e l t , which extends to the International boundary, i s bordered on the west by the Tracy Brook f a u l t and on the east by 'Logan's Line." These shales i n Quebec are not e a s i l y divided into formations because Ogygites canadensis and Triarthrus spinosus c h a r a c t e r i s t i c f o s s i l s of Collingwood and Gloucester are com-monly missing. The upper parts of these shaly beds, generally u n f o s s i l i f e r o u s , are not e a s i l y separated from the overlying Lorraine shales. On account of these d i f f i c u l t i e s , no general 46. attempt to resolve these shales into component formations has been made. Clark (1947) uses the name Lotbiniere shale f o r these beds on the south shore of the St. Lawrence and simply uses the general name U t i c a shale (1948) f o r the north shore i n the Portneuf area. In the Localle area, Clark (1934) also divided the same shales on a palaeontologieal basis into two formations; the Stony Creek below and the I b e r v i l l e above. He found the Stony Creek more clos e l y r e l a t e d to the Trenton while the I b e r v i l l e i s more closely related to the standard Ut i c a . I t has been the custom to consider the U t i c a shale as being about 300 feet t hick i n the Montreal-Quebec basin. However, spe c i a l conditions of accumulation i n the Lacolle area may have permitted a much greater thickness of 2 , 0 0 0 ' to 3,000'* Maddox (1921,a) l i s t s 400' to 200':. at T r o i s R i v i e r s and 200' on the Island of Orleans. According to Twen-hofel (1927, p. 12) "the s t r a t a of Mingan islands are sepa-rated from those of A n t i c o s t i by North channel, forming a geographical break of 19 miles i n which Logan considered that, i f the 'average dip of 90 feet to the mile' were maintained across the channel, 1,700 feet of strata might exi s t there. This thickness i s supposed to represent the Trenton to, and perhaps including, the Lorraine, neither of which has yet been d e f i n i t e l y recognized i n t h i s region." However, loose blocks of bituminous shale are found abundantly along the western half of the north shore of A n t i c o s t i Island. The fauna i s 47. s i m i l a r to that of the Collingwood formation of Ontario. No-where does t h i s Macasty shale occur " i n s i t u . " They are supposed to l i e beneath the channel and may very well belong to the Utica.. H i s t o r i c a l Geology: Black River-Trenton As we have seen, at the end of Chazy time, the sea withdrew probably i n the d i r e c t i o n whence i t came. Then, a f t e r what i s thought to have been a r e l a t i v e l y short period of emergence, on account of a s l i g h t unconformity between the Chazy and the Black River, the sea encroached again over the St. Lawrence Lowlands, but t h i s time, probably from the west. The fact that the various formations of the Black River group are thicker i n the west than i n the east where they usually t h i n out, indicate" an advancing sea from the west. The r e s u l t of t h i s new marine invasion during Black River and Trenton time i s one of the most widespread submergences of Palaeozoic time. The lower beds l a i d down by the Pamelia advancing sea are generally t h i n bedded u n f o s s i l i f e r o u s black shales marking the presence of a muddy environment where much organic aecay was going on. The sea was generally shallow and i n places l i k e the Montreal area, the presence of intraformational con-blomerates marked l o c a l rluctuations and o s c i l l a t i o n s of sea bottom. With the spreading of the invading sea, more or l e s s impure limestone began to precipitate i n the centre of the basins and a new fauna invaded the area. We even f i n d a pure dolomitic fac i e s i n the Pamelia beds. In places l i k e the Ottawa Valley, 48. we have dolomite alternating with f o s s i l i f e r o u s shaly beds ind i c a t i n g a succession of pure and stagnant sea conditions. Eventually, however, the land sank enough to allow the free c i r c u l a t i o n of sea water during Lowville time and pure lime-stone started to form containing an abundance of f o s s i l s . The thin-bedded nature of the s t r a t i f i c a t i o n and some l o c a l uncon-formities show that the sea was s t i l l unstable and f l u c t u a t i n g i n places. By Leray time, such fluctuations had completely ceased and thick, even-bedded pure limestones were formed containing an abundance of corals indicative of clear water conditions a l l over the Lowlands. The thickness of the f o r -mations deposited during Blaok River time i s 90 feet i n Central Ontario, 180 feet i n the Ottawa basin, and only 50 feet at Montreal. This shows that the Ottawa basin was much deeper than the others during that period. Between Leray and Trenton times there seems to have been l i t t l e , i f any, break. Locally an erosional surface may be seen, but the l i t h o l o g y of the adjacent formations i s much the same and the break, where present, i s not well marked and may be only l o c a l . During Trenton times, the sub-mergence was at i t s greatest i n the St. Lawrence Lowlands as i n the rest of North America, and the remnants of Trenton limestone here and there on the Preeambrian Shield from Lake Temiskaming to Lake St. John i n Eastern Quebec, i s a good in d i c a t i o n of t h i s f a c t . 49. During the Trenton sea invasion, the natural b a r r i e r of the Frontenac Axis was under water and approximately 800 feet of limestones were deposited a l l over the St^ Lawrence Lowlands In the various basins. During t h i s time, the sea seemed to have been r e l a t i v e l y shallow, wel l - l i g h t e d , f i l l e d with food and inhabited by a great number of marine animals of a l l kinds. The abundance of f o s s i l s and the hydrocarbons throughout the formation i s proof of t h i s . As we go towards the top of the Trenton limestones, the formations become more and more impure and shaly everywhere i n the Lowlands. In the Manitoulin Island and Georgian Bay area, a l o c a l temporary warping at the end of Cobourg time has per-mitted the sea waters to recede, and a l o c a l well-marked uncon-formity shows a period of erosion or, at l e a s t , of non-deposition i n the area. The change of f a c i e s i n sedimentation of the Trenton sea from limestone to shaly limestone and pure shale i s also marked from east to west, respectively, where younger to older Trenton limestone i s overlaid by black U t i c a shale. As Appalachia was slowly r i s i n g , more and more muddy sediments covered the Lowlands extending progressively west-ward and o b l i t e r a t i n g almost a l l l i f e i n the Trenton sea. Pelagic forms of l i f e are generally found as f o s s i l s i n the U t i c a shale: Graptolites make up the bulk of the fauna. Black shale was deposited a l l over. Two hundred feet are found near Ottawa. Special conditions must have existed i n southern Quebec where the Stony Point and I b e r v i l l e shale 50. formations may possibly reach a thickness of 2,000* to 3,000*. These black shales seem to have extended northeastward to A n t i c o s t i Island where many boulders of Oollingwood age are found along the north shore of the i s l a n d . Nowhere, however, does t h i s shale outcrop i n A n t i c o s t i , but, nevertheless, i t s presence i n the i n t e r - i n s u l a r channel i s a l l but proved. This same s i t u a t i o n of a r i s i n g Appalachia and fast deposition of c l a s t i c sediments i n the Lowlands has continued during the succeeding Lorraine age where most of the sediments are grey shales and sandstones. With t h i s description of U t i c a shale and the h i s t o r i c a l geology of Black River-Trenton time, we have come to the end of what i s known as the Trenton group clo s i n g the Middle Ordovician Epoch. In conclusion, a synoptic table of the Lower and Middle Ordovician formations of the area i s provided, together with maps showing t h e i r d i s t r i b u t i o n i n the various parts of the St. Lawrence Lowlands. LOWER AND MIDDLE ORDOVICIAN OF ONTARIO GROUP MANITOULIN ISLAND WEST OF FRONTENAC AXES EAST OF FRONTENAC AXES Sheeuiandah sh. Blue Mountain sh. B i l l i n g s sh. 300' Collingwood sh. Collingwood sh. Eastview sh. 20' TRENTON (including U t i c a )Cobourg I s. Cobourg I s . Sherman F a l l s I s . Ottawa Is., sh. 700' Trenton I s. H u l l I s. Rockland I s . Leray I s. BLACK RIVER Lowville I s . Pamelia dol. CHAZY St. Martin I s . 155' Rockcl i f f e sh., ss. 165 ! BEEKMANTOWN Oxford d o l . 330' March ss., d o l. POTSDAM (TJ.C?) Nepean ss. 500' Synoptic Table 1 LOWER AND MIDDLE ORDOVICIAN EAST OF OKA ANTICLINE GROUP MONTREAL-QUEBEC BASIN ANTICOSTI & MINGAN ISLANDS TRENTON (including Utica) Gloucester sh. 200'-1500' Ma'casty sh. Collingwood sh. Cobourg Is. 800' below the Gulf of St. Lawrene# probably... 1700' Sherman F a l l Is. mm l a . Rockland I s. BLACK RIVER Leray I s. 50' Lowville I s . Pamelia d o l . CHAZY U. Chazy I s . 300' Mihgan I s . 143' Aylmer ss. BEEKMANTOWN Beauharnois d o l . 1060' Romaine d o l . 262' Theresa d o l . , ss. POTSDAM (U.C.?) Potsdam ss. 0-1696' Synoptic Table' 2 F i g . 2 F i g . 3 F i g . 4 F i g . 3 BIBLIOGRAPHY iAdams, F.D. (1912): The Monteregian H i l l s ; Geol. Surv. Canada, Guide Bk. 2, pp. 31-84. Ami. H.M. (1882) : a. Notes on an exposure of the Potsdam formation at Buckingham Basin, Lievre River, Quebec; Ottawa Field Nat. Club I, Trs. 2, p. 39. b. The Utica Slate; Ibid., pp. 61-66. c. Utica Slate Formation i n Canada (Abst.); Can. Nat. and Geol.; N.S. 10, p. 192. (1883) : Report on Geological and Mineralogical Branch of Ottawa Field Naturalist Club: Ottawa Field Nat. Club I, Trs. 4, pp. 64-66. (1884) : a. Notes on Ottawa Region; Ottawa Field Nat. Club II, Trs. 5, pp. 118-121. b. L i s t of Fossils from Ottawa and Vicinity; Ottawa Field Nat. Club II, Trs. 5, pp. 54-62. (1882): Additional Notes on Geology and Palaeontology of Ottawa and Vicinity; Ottawa Field Nat. Club II, Trs. 6, pp. 251-229. (1888) : a. On the Occurrence of 'phosphatic nodules' i n the Chazy Formation about Ottawa: Ottawa Nat. 2, pp. 45-46. b. Faulting i n the Vicinity of Ottawa; ibi d . , p. 48. c. Geology of the Government Experimental Farm; ibi d . , pp. 71-72. d. On the Sequence of the Geological Formations about Ottawa, with reference to the Natural Gas Question; i b i d . , pp. 93-96. e. On Utica Fossils from Rideau, Ottawa; Ottawa Nat. I, pp. 162-169. (1889) : Contributions to the Geology and Palaeontology of the Townships of Russell and Cambridge, in Russell, Ontario; Palaeontology; Ottawa Nat. 2, pp. 139-140. i i Ami. H.M. (1892) : a. Additional Notes on the Geology and Palaeont-ology of Ottawa and Its Environs; Ottawa Nat. 6, pp. 73-78. b. The Utica Terrane i n Canada; Can* Rec. Sci., 5, pp. 166-183 and 234-346. (1893) : Notes on Geology and Palaeontology of the Rockland Quarries and Vicinity i n the County of Russell, Ontario, Canada; Ottawa Nat. 7, pp. 138-147. (1894) : The Geology of Galetta, Ontario; Ottawa Nat. 8, p. 109. (1895) : Report of the Geological Branch, Ottawa Field Naturalist Club; Ottawa Nat. 9, PP. 167^169. (1896) : (With E l l s , R.W.) Fossil Organic Remains com-prised i n the Various Geological Formations and Outliers of the Ottawa Paleozoic Basin; Roy. Soc, Canada, Proc. and Trans., 2nd ser. 2, sec 4, pp. 151-158. (1899) : a. Report of the Geological Branch, Ottawa Field Naturalist Club; Ottawa Nat. 9, pp. 167-169. b. On Some Trenton (Ordovician) Fossils from the Light Grey Limestones of Cumberland County of Russell, Ontario; Ottawa Nat. 13, pp. 238-240. (1900) : Geology of Some Cities i n Eastern Canada (Ottawa); Roy. S o c , Canada, Proc and Trans., 2nd ser. 6, s e c 4, pp. 129-138. (1901) : a. Preliminary Lists of Organic Remains Occurring i n Various Geological Horizons Comprised i n the Map of Ottawa D i s t r i c t , Including Formations i n the Provinces of Quebec and Ontario, along the Ottawa River; Geol. Surv., Canada, Ann. Rept. 12, pp. 49-77. b. Lis t s of Fossils Obtained from the Several Formations along the Ottawa River Pertaining to the Report of Sheet No. 121 (Grenville), Quebec and Ontario; Geol. Surv., Canada, Ann. Rept. 12, pt. J, pp. 139-14-3. i i i . Ami, H.M. ' " . (1902) : a. Annual Report of the Geological Section of the Ottawa Field Naturalist Club; Ottawa Nat. 15, No. 11, pp. 254-262. b. Brief Description of the Map of the Ottawa District; Ottawa Nat. 16, pp. 187-189. 0. Ordovician Succession i n Eastern Ontario (Abst.), Science, Vol. 15, p. 82. (1903) : Ordovician Succession i n Eastern Ontario (Abst.), Geol. Soc. Amer., Bull . 13, pp. 517-518. (1904) : Preliminary Lists of Fossil Organic Remains from the Potsdam-Utioa and Pleistocene Forma-tions Comprised within the Perth sheet (No. 119) i n eastern Ontario; Geol. Surv., Canada, Ann. Rept. 14, pt. pp. 80-89. (1905) : On the Geology of Carp (Ontario) and Environs; Ottawa Nat. 19, pp. 92-93. Baker, M.B. ( 1 9 I 6 ) : The Geology of the Kingston and Vicinity; Ont. Dept. Mines, Ann. Rept. 25, Vol. 25, pt. 3, pp. 1-36. Bassler, R.S* (1915): Bibliographio Index of American Ordovician and Silurian Fossils; U.S. Nat. Mus., Bull. 92. (1922): The Stratigraphy of the Central Basin of Tennessee; Surv. of Term. Dept. of Ed., Div. of Geol., Bull. 38. Bather, F.A. (1912): The Trenton Crinoid, Ottawacrinus. W.Ri B i l l i n g s , and Note on Merocrinus (Walcott); Geol. Surv., Canada, Mus. Bul l . 1, No. 1, pp. 1-10. B e l l , R. (1867): Report on Manitoulin Island; Geol. Surv. Canada, Rep. Prog. 1863-66, pp. 165-179. (1870): Report on the Geology of the Grand Manitoulin, Gockburn, Drummond, and St. Joseph Islands;Geol. Surv. Canada, Rep. Prog. 1866-69, pp. 109-116. B e l l , R. (1888): (1893): (1898): (1907): Iv. The Petroleum Fields of Ontario; Roy. Soc. Canada Trans. Vol. 5, sec. 4, pp. 101-113. Honeycombed Limestone i n Lake Huron; Geol. Soc. Ann. Vol. 7, pp. 297-304. Report on the Geology of the French River Sheet; Geol. Surv. Canada, Ann. Rep. New Series, Vol. 9, Pt. 1. Manitoulin Island Sheet; Geol. Surv* Canada Bil l i n g s , (1854) (1856) (1857) E. (1859) (i860) (1861) On Some New Genera and Species of CystIdea from the Trenton Limestone; Can. Jour. 2, pp. 215-218, 250-253, 268-274. Fossils of the Potsdam Sandstone: Sea-weeds, Shells, and Footprints on the Rock at Beau-harnois; Can. Nat., Vol. 1, pp. 32-39. a. Fossils of the Potsdam Sandstone and Footprints on the Rook at Beauharnois; Can. Nat; Geol. 1, PP. 32-39. b. On the Grinoidea or Stone L i l i e s of the Trenton Limestone, with the Description of a New Species; ibid., pp. 48-57. a. Fossils of the Calciferous Sandrook (includes those of deposit of white limestone at Mingan supposed to belong to the formation); ibid., PP. 345-367. b. Fossils of the Chazy Limestone with Description of New Speoies; i b i d . , pp. 426-470. Additional Note on the Potsdam Fossils: Amer. Jour. S c i . (2) 30, pp. 242-243, 337-338. On the Track of an Animal Lately Found i n the Potsdam Formation; Amer. Jour. Sci., 2nd ser. 31, pp. 17-23. (1863): Description of a New Speoies of Harpes from the Trenton Limestone, Ottawa; Can. Nat. Geol. 8, pp. 36-38. v. Bi l l i n g s , W.R. ' (188).): Notes on Two Species and One Genus of Fossils from the Trenton Limestone, Ottawa; Ottawa Field Nat. Glub I, Trs. 2, pp. 24-35. (1883): Notes on and Description of Some Fossils from the Trenton Limestone; Ottawa Field Nat. Blub I, Trs. 4, pp. 49-52. (1885): a. Two New Species of Crinoids (Trenton, Ottawa); Ottawa Field Nat. Club II, Trs. 6, pp. 248-220. b. Additional Notes on the Geology and Palaeont-ology of Ottawa and Vicinity; Ottawa Field Nat. Club II, Trs. 6, pp. 251-259. (1887): A New Genus and Three New Species of Crinoids from Trenton Formation, with Notes on a Large Specimen of Dendrocrinus proboscidiatus; Ottawa Nat. 1, pp. 49-54. Caley, J.F. (1936): The Ordovician of Manitoulin Island, Ontario; Geol. Surv. Canada, Mem. 202 pp. 21-92. (1940) : Palaeozoic Geology of the Toronto-Hamilton Area, Ontario; Geol. Surv. Canada, Mem. 224. (1941) : Palaeozoic Geology of Brantford Area, Ontario; Geol. Surv. Canada, Mem. 226. (1942) : Palaeozoic Geology of the London Area, Ontario; Geol. Surv. Canada, Mem. 227. (1945): Palaeozoic Geology of Windsor-Sarnla Area, Ontario; Geol. Surv. Canada, Mem. 240. (1947): * The St. Lawrence Lowlands, Geology and Economic Minerals of Canada, 3rd. Ed., Geo. Surv. Canada, Eoon. Geol. Series 1, pp. 156MS8. Chapman, E.J. (1864): A Popular Exposition of the Minerals and Geol-ogy of Canada—Part V, Palaeozoic Rocks of Canada; Can. Jour. N.S. 8, pp. 185-210. Clark, T.H. (1919): A section in the Trenton Limestone at Martins-burg; N.Y. Bull . Mus. Comp. Zool. Harvard, Vol. 62, No. 1. v i . Clark, T.H. (1934): Struoture and Stratigraphy of Southern Quebec; Geol. Soo. Am., Bull., Vol. 45, No. 1, pp. 1-20. (1939) : a. Description of Log of a Deep Well near Montreal (Abst.); Roy. Soc. Can., Proc. Vol. ZXXIII, p. 198. b. The St. Lawrence Lowlands of Quebec; i n Geologie der Erde, Vol. 1, Geology of North America, pp. 579-588. o. l i e Jesus and Parts of the counties of Terre-bonne and Deux-Montagnes; Que. Bur. Mines, P.R. 132. (1940) : a. Montreal Area (Advance Report); Que. Bur. Mines, P.R. 147. b. Preliminary Report on the Montreal Area, Que. Bur. Mines, P.R. 147. (1941) : Preliminary Report on the Montreal Area; Que. Bur. Mines, P.R. 158. (1943) : Preliminary Report on the St. Jean and Beloeil map Area, Que. Bur. Mines, P.R. 177. (1944) : Structure and Stratigraphy i n the Vic i n i t y of Montreal; Roy. Soo. Canada Trans., Vol. 38, Sec. 4, pp. 23-33. (1947) : Summary Report on the Lowlands, South of the St. Lawrence, Que. Bur. Mines, P.R. 204. (1948) : Preliminary Report on the Portneuf Map Area; Portneuf and Lotbiniere Counties; Que. Bur. Mines, P.R. 225. (1950): Grondines Map Area, Ghamplain, Portneuf, Laviolette, Nioolet and Lotbiniere Counties; Que. Bur. Mines, P.R. 237, Pt. 1. Clark, T.H., McGerrigle, H.W. (1936): Lacolle Conglomerate, a New Ordovician Formation i n Southern Quebec; Geol. Soc. Am., Bull., Vol. 47, No* 5, pp. 665-b74. v i i . Clarke, <T.M., Schuohert, C. (I89?): The Nomenclature of the New York series of Geological Formations; Science, Vol. 10, pp. 874-878. (1903): Classification of New York Series of Geologic Formations; N.Y. St. Mus., Hdbk. 19, p. 28. Coleman (1936): Geology of the North Shore of Lake Ontario; Ont, Dept. Mines, Vol. 45, Pt. 7, pp. 37-74. Commissioner of Crown Lands of the Province of Quebec (1884) : Exploration i n Montmorency county, including island of Orleans, Occurrences of Bituminous Limestone and Antraxolite; Quebec Bur. Mines, C.C .Li reports 1883. (1885) : Reports on o i l and gas occurrences i n Valleys of St. Lawrence and St. Maurice Rivers; Que. Bur. Mines, C.C.L. reports 1884. Coryell. H.N. (19I0): A Study of the Collections from the Trenton and Black River Formation s of New York; Ind. Ac. of Sc. Pr*, pp. 249-268. Craig, W. (1889): Contributions to the Geology and Palaeontology of the Townships of Russell and Cambridge, i n Russell, Ontario; Physiography and General Geology; Ottawa Nat. 2, pp. 136-139. Cashing: H.P. (1907): (1908): (1910) : (1911) : Physical Oscillations during the Cambro-Silurian i n Northeastern New York; Sci., N.S., Vol. 22, p. 774. Lower Portion of the Paleozoic Section in North-western New York; Geol. Soc. Am., Bull., Vol. 19, PP. 155-176. Geology of the Thousand Islands region, N.Y. State Mus., Bu l l . 142. Nomenclature of the lower Palaeozoic rocks of New York, Am. Jour. So., 4tn ser., Vol. 31> pp. 135-145. v i i i . Dawson, S i r J.W. (1861): Notes on the Geology of Murray Bay, Lower St. Lawrence; Gan. Nat., Vol. 6, pp. 128-150. (1865): On Certain Organic Remains i n the Laurentian Limestones of Canada; Can. Nat. Geol., N.S. 2, pp. 99-111, 127. Dresser, J.S., Denis, T.C. (1941): Geology of Quebec, Vol. 1, Bibliography and Index; Quebec Bur. of Mines. (1944): Geology of Quebec, Vol. 2, Quebec Bur. of Mines, Geological Report No. 20. (1949):, Geology of Quebec, Vol. 3» Quebec Bur. of Mines, Geological Report No. 20. Baton, R.W. (1824): A Geologioal and Agricultural Survey of the District adjoining the Erie Canal In the State of New York, 163 pp. Albany. E l l s , R.W. (1887) : Report on the Geology of a Portion of the Eastern Townships of Quebec; Geol. Surv. Can., Ann. Rept., 1886, Vol. II, Pt. J. (1888) : Second Report on the Geology of a portion of the Province of Quebec {Quebec City Sheet); Geol. Surv. Canada, Ann. Rept., Vol. 3, pp. 1-70 J. (1889) : Second Report on the Geology of a Portion of the Province of Quebec; Geol. Surv; Canada, Ann. Rept., 1887-88, Vol. I l l , Pt. K. (1894) : Report on Field Work in Ottawa, Pontlac and Carleton Counties, Quebec and Ontario; Geol. Surv. Canada, Ann. Rept. 7, pt. A, pp. 60-62. (1895) : a. The Potsdam and Galeiferous formations of Que-bec and Eastern Ontario; Roy. Sob. Canada, Proc. and Trans. 12, sec. 4, pp. 21-20. b. Report on Field Work in Ottawa and Argenteuil Counties. Quebec; Geol. Surv. Canada, Ann. Rept. 6 ( I 8 9 2 ) , pt. A, pp. 37-40. v i i i a. E l l s , R.W. (1896): a. Palaeozoic Outliers i n the Ottawa River Basin (followed by Ami's f o s s i l l i s t ) : Roy.Soc. Canada, Proc. and Trans., 2nd ser. 2, sec. 4, pp. 127-149. b. The Geology of the Ottawa and Parry Sound R a i l -way; Ottawa F i e l d Nat. 10, pp. 163-192. c. Summary Report on F i e l d Work i n Ottawa, Pontiac, and Carleton Counties, Quebec and Ontario; Geol. Surv. Canada, Ann. Rept. 7 (1894), pt. A, pp. 27-60. d. Report on a Portion of the Province of Quebec Comprised i n Southwest Sheet of "Eastern Town-ships;" Geol. Surv. Canada, Ann. Rept. f o r 1894, pt. J , Map—Montreal Sheet, Pub. No. 271. (1898): a, Report on F i e l d Work i n Eastern Ontario (Ren-frew, Addington, Frontenac, Lanark, and Carle-ton); Geol. Surv. Canada, Ann. Rept. 9 (1896), pt. A, pp. 23-54. b. Formations, Faults and Folds of the Ottawa Dis-t r i c t ; Ottawa Nat. 11, pp. 177-189. c. Report on F i e l d Work on the Perth and Ottawa C i t y Sheets, Eastern Ontario; Geol. Surv. Canada, Ann. Rept. 10 (1897), pt. A, pp. 57-62. (1899) : a. Report on F i e l d Work i n Southwestern Quebec and Adjacent Parts of Ontario; Geol. Surv. Canada, Ann. Rept. 11, pt. A., pp. 116-119. b. The Mineral Resources of the Ottawa D i s t r i c t ; Ottawa Nat. 12, pp. 14-21, 25-46. (1900) : a. Report on F i e l d Work i n the Ottawa Region, Quebec and Ontario; Geol. Surv. Canada, Ann. Rept. 12 (for 1899), pt. A, pp. 131-137; pt. G, pp. 10-13, 17-18. b. The Physical Features and Geology of the Palaeozoic Basin between the Lower Ottawa and St. Lawrence Rivers; Roy. Soc. Canada, Procl and Trans., 2nd ser. 6, sec. 4, pp. 99-120. c. Report on the Geology of the Three Rivers Map-Sheet; Geol. Surv. Canada, Ann. Rept. 1898, Vol. XI, Pt. J . v i i i b. E l l s , R.W. (1901) : a. Report on the geology of Argenteuil, Ottawa, and Part of Pontiac Counties, Province of Que-bec, and Portions of Carleton, R u s s e l l , and Prescott Counties; Geol. Surv. Canada, Ann. Rept. 12, pt. J (1899), Map No. 121, Pub. No. 750. b. Report on the Three Rivers map sheet, Geol. Surv. Canada, 11th Ann. Rept., pt. J . (1902) : a. Report on the Geology and Natural Resources of the Area included i n the map of the C i t y of Ottawa and V i c i n i t y ; Geol. Surv. Canada, Ann. Rept. 12, pt. G, pp. 1-51 (1899); Map, Ottawa Sheet, Pub. No. 714. b. Report on the Geology of Argenteuil, Ottawa, and Part of Pontiac Counties, Province of Que-bec (etc.); Geol. Surv. Canada, Ann. Rept., 1899, V o l . m, Pt. J . (1903) : Report on F i e l d Work i n the Ottawa Region, Quebec and Ontario; Geol. Surv. Canada, Ann. Rept. 12, pt. A (1900), pp. 129-139; ' Map No. 120, Pub. No. 903. (1904) : Report on the Geology of a Portion of Eastern Ontario; Geol. Surv. Canada, Ann. Rept. 14 (1901), pt. Aj pp. 1-79; Map No. 119, Pub. No. 789. (1907): Report on the Geology and Natural Resources of the Area Included i n the Northwest Quarter Sheet of the Ontario and Quebec Series Com-p r i s i n g Portions of the Counties of Pontiac, Carleton, and Renfrew; Geol. Surv. Canada, Pub. No. 977, PP. 1-71; Map No. 122, Pub. No. 660. Emmons, E. (I838): Report of the Second Geological D i s t r i c t of the State of New York; N.Y. Geol. Surv., Ann. Rept., V o l . 2, pp. 214-217. (1842): Geology of New York, Part I I ; Albany, N.Y., 437 pp. Fenton, C.ju. (1924):. Black River Brachiopods from M i s s i s s i p p i Valley; Iowa Acad. S c i . P r o c , 2 9 , pp. 6 7 - 7 7 . ix. Fenton, C.L. (1928): Forms of Strophomena from Black River and Rich-mond Formations; Am. Middland Nat. Vol. II, Nos. 5-4, pp. 144-159. Foerste; A.F. (1912) : Ordovician section in the Manitoulin area In Lake Huron, Ohio Nat., Vol. 12 No. 2, Dec. 1912, pp. 37-49. (1913) : The Mohawkian (Middle Ordovioian) strata north-east of Manitoulin Island, Geol. Surv. Canada, Guidebook 5, pp. 84-89. (1916): Upper Ordovician formations i n Ontario and Quebec, Geol. Surv. Canada, Mem. 8 3 . (1919) : Notes on Isotelus, Aoroliohas, Calvmene, and Encrinurus; Denison Univ. B u l l . 19, pp. 62-82. (1920) : The Generic Relations of the American Ordovician Lichadilae; Amer. Jour. Soi. 4, ser. 49, pp. 26-50. (1922): Distribution of the Ottawa Trenton Eohinoderm Faunas; Can. Nat. 3 6 , No. 5, pp. 84-86. (1924): Upper Ordovician Faunas of Ontario and Quebec; Geol. Surv. Canada, Mem. 138. (1933): Black River and other cephalopoda, Denison Univ. Bull., Lab. Nat. Hist., Vol. 27, p.1-146. Foord. A.H. (1882): On the Monticuliporidae of the Chazy, Black River, and Trenton Formations, with Descrip-tions of Ten New Species: Geol. Surv., Canada, Con. Micro-Pal., pp. l-2fa. Fraser, F.J. (1921): Heavy Minerals in the Basal Ordovician Sand stones of Ontario and Quebec; Geol. Surv. Canada, Sum. Rept. 1950, pt. D, pp. 28-60. X . F r i t z , M.A., Dyer, W.S., and Parks, W.A. (1923): The Stratigraphy and Palaeontology of Toronto and Vicinity; Ont. Dept. Mines, Ann. Rept. 32, Vol. 32, pt..7, pp. 1-134. Giroux, N.J". (1896) : Report of Field Work i n the St. Lawrence Valley, Ontario and Quebec; Geol. Surv. Canada, Ann. Rept. 8 (1895), pt. A., pp. 68-74. (1897) : Report of Field Work i n Eastern Ontario; Geol. Surv. Canada, Ann. Rept. 9 (1896}, pt. A. pp. 59-64. Goranson, R.W. (1926): Calumet Island, Pontiac County, Quebec; Geol. Surv. Canada, Sum. Rept. 1925, pt. C, pp. 107 and 115. Gordon, W.C. (1905): The Blaok.River Section near Bessemer (Mich.); Mich. Acad. Sc., Rept. 7, pp.-188-195. Goudge, M.F. (1933): Canadian Limestones for Building Purposes; Dept. of Mines, Canada, Mines Branch, No. 733, PP. 35-36, 72-74. (1935): Limestones of Canada, Pt. I l l , Quebec; Dept. of Mines, Canada, Mines Branch. No. 733, .pp. 13-19, 40-46, 56-68, 163-164. (1938): Limestones of Canada, Pt. IV, Ontario: Dept. of Mines, Canada, Mines Branch, No. 781, pp. 12-16, 44-58, 77-82,. 152-156, 180-183, 190-196. Grabau, A.W. (1909): Physical and Faunal Evolution of North America during Ordovicio, S i l u r i c , and Early Devonie Time; Jour. Geol., Vol. 17, pp. 209-252. Grant, Sir J. (1564): The Geology of the Ottawa Valley; Can. Nat. Geol., N.S. 1, pp. 419-426. Hall, J . (1851): Drummonds Island and North Shores of Lakes Huron and Michigan; Am. Acad. Proc.,.Vol. 2, pp. 253-2M. (1893): An Introduction to the Study of the Genera of Palaeozoic Brachiopoda; N.Y. Geo. Surv. Pal. Vol. 8, Pt. 1 and 2. Harkness, R.B. (192b): Natural Gas i n 1935; Ont. Dept. Mines; Ann. Rept. 42, pt. 2; Log of Wells, pp. 28-74. Harrington, B.J. (1896): The Composition of Limestones and Dolomites from a Number of Geological Horizons 1in Canada; Can. Rec. Sci. 6, pp. 27-22. Harvie, R. (1910): . On the Origin and Relations of the Palaeozoic Breccia of the Vicinity of Montreal; Roy. Soc. Can., Trans., Vol. I l l , Sec. IV, pp. .24^299. Hinde, G.J. (I889): On a New Genus of Siliceous Sponges from the Trenton Formation at Ottawa; Can. Reo. Sc i . 2, PP. 396-399. Hunter, A.F. (1904): Raised Shore Lines along the Blue Mountains; Geol. Surv. Canada, Sum. Rept., pp. 222-228. Ingall, E.D. (1926): Deep Borings in Ontario, Quebec, and Maritime Provinces; Geol. Surv. Canada, Sum. Rept. 1924, pt. C, p. 241. Johnston. W.A. (1910): Simcoe d i s t r i c t , .Ontario, Geol. Surv. Canada, Summ. Rept. for 1909, p. 158, (1911): , Simcoe d i s t r i c t , Ontario, Geol. Surv. Canada, Summ. Rept. for 1910 p. 189. x i i . Johnston, W.A, (1912): (1913): I1916): (193D: (1932) : (1933) : (1934) : (1937): Kay, 6.M. (1927): (1928) : (1929) : (1930) : (193D: (1933); (1933): Geology of Lake Simcoe area, Ontario, Geol. Surv. Canada, Summ. Rept. f o r 1911, pp. 253-261, Algonguin Beach, G l a c i a l Phenomena and Lowville Limestone i n Lake Simcoe D i s t r i c t , Ontario; Geol. Surv. Canada, Inter. Geol. Congr. 12 , Guide Bk. 5 , pp. 23-33. Sutton, Barrie, and Ottawa Areas, Ontario; Geol. Surv. Canada, Sum. Rept. 1915, p. 138 . Deep Borings i n Ontario, Quebec, and the Mari-time Provinces; Geol. Surv. Canada, Sum. Rept. 1930, pt. D, pp. 6 7 - 8 4 . Borings i n Ontario, Quebec, and the Maritime Provinces; Geol. Surv. Canada, Sum. Rept. 1931, pt. D, pp. 42-52. Borings i n Eastern Canada; Geol. Surv. Canada, Sum. Rept. 1932, pt. D, pp. 6 9 - 7 4 . Borings i n Eastern Canada; Geol. Surv. Canada, Sum. Rept. 1932, pt. D, pp. 69-71 (1933); Geol. Surv. Canada, Sum. Rept. 1933, pt. D, pp. 155-156. Stratigraphy of the Trenton Group; Geol. Soo., Amer. B u l l . 4 8 , pp. 233-302. Stratigraphy and Palaeontology of the Decorah formation; N.B. Iowa,GiS.A.Bull.38,No.l,p.225. Divisions of the Deoorah formation; Science, N.S., V o l . 67, p. 16. Stratigraphy of the Decorah formation, Jour. Geol., Vol. 37, p. 639-671. Ostrocoda of the Lower Mohawkian; Geo. Soo. Am. B u l l . 41, p. 202. Stratigraphy of the Ordovician Hounsfield meta-bentonite, Jour. Geol., V o l . 39, pp. 361-376. The Ordovician Trenton Group i n Northwestern New York; Stratigraphy of the lower and upper limestone formations, Am. Jour. S c i . , 5th ser., Vo l . 26, p. 1-15. Ordovician Stewartville-Dubuque problems, Jour. Geol., V o l . 43, p. 561-590. 2±ii. Kay, G.M. (1937) : Stratigraphy of the Trenton Group, Geol. Soc. Am., Bull., Vol, 48, p. 233-302. . (1938) : Structures northeast of Lake Ontario (Abst.), Geol. Soc. Am., Bull., Vol. 49, p. 1935. (1939) : Ottawa-Bonnechere graben (Abst.), Geol. Soc. Am., Bu l l . , Vol. 50, p. 1915. (1942): Ottawa-Bonnechere Graben and Lake Ontario Homo-ciine; Geo. Soc. Am. Bull., Vol. 53, . pp. 585-646. Keele, J. (1924): Clays of Eastern Ontario; Geol. Surv. Canada, Mem. 142, Chapter VII, pp. 50-70. Keele, J, Cole, L.H. (1922;: Structural Materials along the St. Lawrenoe River, 1 between Prescott, Ontario, and Laohine, Quebec; Dept. of Mines, Canada, Mines Branch, No. 549. Keele, J., Johnston, W.A. (1913): The Superficial Deposits near Ottawa; Geol. Surv. Canada, Inter. Geol. Gongr. XII, Guide Bk. 3, PP. 126-135. Kindle, E.M. (1914): A Comparison of the Cambrian and Ordovician Ripple-marks found at Ottawa; Jour. Geol. 22, PP. 703-713. ' (1916): The Ordovician Limestones of the Kingston Area, Ontario; Ont. Dept. Mines, Vol. 25, pt. 3, app. 1, pp. 37-44. (1919): The Climatic Interpretation of Two Early Ordovician Mudcraok Horizons; Can* Field Nat. 33, No. 5, p. 96. Kindle, E.M., Burling, L.D. (1915): Structural-Relations of the Preoambrian and Palaeozoic Rocks North of the Ottawa and St. Lawrenoe Valleys; Geol. Surv. Canada, Mus. Bull. 18. xiv. Lambe, L . M . (1897): Description of a New Genus of Polyzoa from the Trenton Limestone at Ottawa; Can. Rec. So i . 7, PP. 1-3. (1899): A Revision of the Genera and Species of the Canadian Palaeozoic Corals; Geol. Surv. Canada, Contr. Can. Pa l . 4, pt. 1. (1901): Ib id . pt. 2. Laverdiere, J.W. (1935): The Palaeozoic of the Deschambault Region, Pbrt-neuf County; Quebec Bureau Mines, Ann. Rept. 1934, Pt . D, pp. 45-62. (1937): Ste-Anhe River Map-Area, Portneuf County; Que-bec Bureau Mines, Ann. Rept. 1936, pt. D, pp. 29-51. Logan, S i r (1843): (1845): (1847): (1852): (1857): (1861): (I865): (1864): Wm. E . Preliminary Report, Geol. Surv. Canada, Rept. of Prog. 1842. Geol. Surv. Canada, Rept* of Prog. 1845, pp. 28-33. Geol. Surv. Canada, Rept. of Prog. 1845-46, PP. 6-9, 47-67, 119-122. a. Geol. Surv. Canada, Rept. of Prog. 1821-52, pp. 6-20. b. On the Footprints Occurring i n the Potsdam Sand-stone of Canada; London Quart. Jour. Geol. 8, pp. 199-213. Geol. Surv. Canada, Rept. of Prog* 1853-56, pp. 5-52. On the Track of an Animal Lately Found i n the Potsdam Formation: Can. Nat. 2, pp. 279-282; Amer. Jour. S c i . (2)2, pp. 17-23. Geology of Canada; Geol. Surv. Canada, Rept. of Prog, from i t s commencement to 1863. Atlas accompanying Geology of Canada, Maps 1 and 2; Plate 3. XV. Logan, S i r . Wk. E . ( I 8 8 9 ) : I b i d . , republished; New York State Mus., 42nd Rept., pp. 30-24. Longley, W.W. (1944): North Shore of the St. Lawrence, Mingan to Aquanish; Quebec Bur* Mines, P.R. 184. (1950): North Shore of the St. Lawrence from Mingan to Aguanish, Saguenay County; Quebec Bur. Mines, Geol. Rep. 42 pt. 1. Low, A . P . (1892): Report on the Geology and Economic Minerals of the Southern Portions of Portneuf, Quebec, and Montmorency Counties, Quebec; Geol. Surv. Can., Ann. Rept., 1890-91, V o l . V, Pt . L . Maddox, D.C. (1930) : Deep Borings in Ontario, Quebec, and Maritime Provinces; Geol. Surv. Canada, Sum. Rept. 1928, pt. G, pp. 102-104. I b i d . , Sum. Rept. 1929, pt. G, pp. 41-42. (1931) : a. Thickness of Ordovician Deposits in Ontario and Quebec; Geol. Surv. Canada, Sum. Rept. 1930, pt. D, pp. 49-57. b. Logs of Wells Dr i l l ed for O i l and Gas in Que-bec; Geol. Surv. Canada, Sum. Rept. 1930, Pt . D, pp. 85-133. Maloolm, W (1913): O i l and Gas Fields of Ontario and Quebec; Surv. Canada, Mem. 8 1 . Geol. McGerrigle, H.W. (193b): Laohute Map-area, Pt . I I , The Lowland Area; Quebec Bureau of Mines, Ann. Rept., pt. C, pp. 41-62; Maps 408, East Half and West Half. M i l l e r , A.K. ( 1 9 4 3 ) : Ozarkian and Canadian Cephalopods—Pt. I I , Brevioones; Geol. Soc. Amer., Spec. Pap. 4 9 , p. 51. xv i . M i l l e r , A.K. (1944): I b i d . , pt. IIT, pp. 47, 79-80, 82, 95, 109, 116. M i l l e r , A . H . , French, G . A . , Wilson, M.E. (1921): Geophysical Survey of the Hull-Gloucester and Hazeldean Faults; Geol. Surv. Canada, Mem. 162, pp. 190-222. M i l l e r , W.G. (1902): The Limestones of Ontario; Ont. Dept. Mines, Ann. Rept. 1904, pt. 2. Montgomery, R. (1920): The Ceramic Industry of Ontario; Ont. Dept. Mines, Ann. Rept. 2 9 , pt. 4; Ordovician Shales, pp. 20-21. Murray, A. (1849): (1822): (1827): The Main Shores and Islands of Lake Huron: Geol. Surv. Canada, Rept. Prog..1847-48, pp. 7-46, 92-124. Report on the Geology of the Region, between the Ottawa, St . Lawrence, and Rideau Rivers; Geol. Surv. Canada, Rept. of Prog. 1831-22, pp. 27-91. On the Geology and Topography of the MUskoka, Petawawa, Bonneohere, and Madawaska Rivers; Geol. Surv. Canada, Rept. of Prog. 1822-56, pp. 94-98. Nicholson, H.A. (1875): Palaeontology of Ontario, pp. 7, 8, 10, 12-14, 16-19. Okulitch, V . J . (1922): a. Fauna of the Black River Group in the Vic in i ty of Montreal; Can. F ie ld Nat. 49, No. 6, pp. 96-107. b. Tetradidae, a revision of the Genus Tetradium; Roy. Soc. Canada Trans. , 2rd Ser . , 29, Sec. 4, pp. 49-107. v i i . Okulitch. V.J. (1926): a. The Black River Group near Montreal; Geol. Surv. Gan., Mem. 202, pp. 119-131. b. On the Genera H e l e o l i t e s , Tetradium, and Chaetetes: Am. Jour. S c i . , 5th ser., 32, pp. 361-380. o. Some Ghazyan Corals; Roy. Soc. Canada trans., 3rd ser., 30, sec. 4, pp. 59-73. (1937) : Notes on Fletoheria inoerta ( B i l l i n g s ) and F l e t c h e r i a s i n c l a i r i n.--'sp.Roy. Can. Inst. Trans. 21, pt. 2, No. 46, pp. 313-316. (1938) : Some Black River Corals; Roy. Soc, Canada, Proc. and Trans., 3rd ser. 32, sec. 4, pp. 87-111. (1939) : a. The Black River Group i n the Region between Montreal and Quebec; Amer. Jour. S o l . , 237, pp. 81-93. b. The Ordovician Section at Coboconk, Ontario; Roy. Can. Inst. Trans., V o l . 22, Pt. 2, PP. 319-339. c. Evolutionary Trend of some Ordovician Corals; Roy. Soc. Canada Trans., 3rd ser., 33, sec. 4, pp. 67-81. (1942): New Pterygometopinae from the Ordovician of Ontario and Quebec; Roy. Soo. Canada, Proc. and Trans., 3rd ser. 36, sec. 4, pp. 99-106. Osborne, F.F., and Grimes-Graemer (1936): The Breccia on Ste-Helene Island, Montreal; Amer. Jour. S c i . , Vol. 32, pp. 43-54. Owen, R. (1852) Descriptions of the Impressions and Footprints of the Protiohnites from the Potsdam of Canada; London Quart. Jour. Geol. 8, pp. 214-225. Parks, W.A. (1910): Preliminary Report on the B u i l d i n g and Orna-mental Stones* of Ontario South of the Ottawa and French Rivers; Dept. of Mines, Canada, Mines Branch, Sum. Rept. 1910, pp. 110-114. X v i i i . Parks, W.A. (1912): (1913) : (1914) : (1928): Report on the Building and Ornamental Stones of Canada—Quebeo; Dept. of Mines, Canada, Mines Branch, No. 203, V o l . 1, pp. 121, 126-138. Ordovician Section on Credit River; Canada; Guide Bk. 5, pp. 15-23. Geol. Surv, Report on the Building and Ornamental Stones of Canada—Quebec; Dept. of Mines, Canada, Mines Branch, No. 279, V o l . 3, P. 121. Fauna and Stratigraphy of the Ordovician Black Shales and Related Rooks, i n Southern Ontario; Roy. Soc. Canada, Proc. and Trans. , 3rd ser. 22, sec. 4, pp. 39-92. Parks, Mm. A. (1930): (1931): Report on the O i l and Gas Resources of the Province of Quebec; Quebec Bur. Mines Ann. Rept. 1929, pt. Bi Natural Gas i n the St . Lawrence Valley, Quebec; Quebec Bur. Mines Ann. Rept. 1930,.pt. D. Parks, W.A.; Stauffer, C .R. ; Foerste, A . F . ; Williams, M.Y. ; and Walker, T . L . (1913): Geology of Selected Areas on Lakes Erie and Huron i n the Province of Ontario; Geol. Surv. Canada, Guide Bk. 5, pp. 37-104. Putnam, D.F . (1947): Manitoulin Island; Geographical Review V o l . 37, pp. 649ss. Raymond, P . E . (1905) : a. The Tri lobi tes of the Chazy limestone; Carnegie Mus. Ann. 3, pp. 328-386. b. The Fauna of the Chazy Limestone; Amer. Jour. S c i . 20, pp. 353-382. (1906) : The Chazy Formation and Its Fauna; Carnegie Mus. Ann. 3, pp. 498-598. (1908): The Gastropoda of the Chazy Formation; Carnegie Mus. Ann. 4, pts. 3 and 4, pp. r / l , 178, 186, 191, 193, 204. xix. Raymond, P.E. (1910) : a. Notes on Ordovician T r i l o b i t e s ~ I I , Asaphidae from the Beekmantown; Carnegie Mus. Ann. 7, pp. 35-4-5. b. Notes on Ordovician T r i l o b i t e s — I T , New and Old Species from the Chazy; Ibid., pp. 60-80. c. On Two New Trilobites (Bathyurus superbus and Isotelus arenicola) from the Chazy near Ottawa, Ontario; Ottawa Nat. 24, pp. 129-134. d. Preliminary Notes on the «Chazy* Formation i s the Vicinity of Ottawa, Ontario; Ibid., pp. 189-197. (1911) : a. Chazy Formation i n the Ottawa Valley (Abst.); Geol. Soc. Amer. Bull. 22, pp. 719-720. b. The Brachiopoda and Ostracoda of the Chazy; Carnegie Mus. Ann. 7, PP. 215-229. (1912) : a. Ordovician of Ottawa Valley; Geol. Surv. Canada, Sum. Rept. 1911, pp. 351-356. b. On Two New Palaeozoic Starfish (one of them found near Ottawa) and a New Crinoid; Ottawa Nat. 26, pp. 77-81. (1913) : a. Ordovician of Montreal and Ottawa; Geol. Surv. Canada, Inter. Geol. Gongr. XII, Guide Bk. 3, pp. 157-162. b. A Further Note on Cryptolithus versus Trinu-oleus; Ottawa Nat. 27, pp. 2b-30. e. Correlation of the Middle Ordovician Formations of Ontario and Quebec (Abst.); Geol. Soc. Amer. Bull . 24, p. 111. d. Quebec and vi c i n i t y , Geol. Surv. Canada, Guide Bk. 1, pp. 27-54. (1914) : a. The Trenton Group in Ontario and Quebeo; Geol. Surv. Canada, Sum. Rept. 1912, pp. 342-250. b. Table Middle Ordovician; Geol. Surv. Canada, Sum. Rept. 19.12, p. 248. XX. Raymond, P.E. (1914): e. A Beatrioea-like Organism from the Middle Ordovician; Geol. Surv. Canada, Mus. B u l l . 5. (1916): a. The Pelecypods of the Chazy Formation; Car-negie Mus. Ann. 10, pp. 325-242. b. A New Ceraurus from the Chazy; New York State Mus. B u l l . Ib9, pp. 121-126. (1921) : A Contribution to the Description of the Fauna of the Trenton Group; Geol. Surv. Canada, Mus. B u l l . 21, 1921. (1922) : Trenton of Central Tennessee and Kentucky; Geol. Soo. Am. B u l l . 22, PP. 571-585. (1925): Some T r i i o b i t e s of the Lower, Middle Ordo-v i c i a n of Eastern North-America; Mus. Comp. Zool. B u l l . V o l . 67, No. 1, pp. 1-180. Raymond, P.E., Narraway, J.E. (1908): Notes on Ordovician T r i i o b i t e s — I l l a e n i d a e from the Blaok River Limestone near Ottawa, Canada; Carnegie Mus. Ann. 4, pp. 242-255. (1910): Notes on Ordovician T r i i o b i t e s — I I I , Asaphidae from the Lowville and Blaok River; Carnegie Mus. Ann. 7, pp. 46-59. Raymond, P.E., Okulitch, V.J. (1959): Some Chazyan sponges; Mus. of Comp. Zoology, V o l . 86, No. 5, PP. 197-214. Reinecke. L. (1915) : Road Materials i n Ontario; Geol. Surv. Canada, Sum. Rept. 1914, pp. 88-90. (1916) : Road Materials i n Ontario and Quebec; Geol. Surv. Canada, Sum. Rept. 1915, pp. 147-155. (1917) : Road Material Surveys i n 1913; Geol. Surv. Canada, Mem. 99; Map. Pub. No. 1665, and Map 168A, Pub. No. 1655. xxi. Retty, J.A. (1932): Reconnaissance along the Coulonge and Black Rivers, Pontiac County, Quebec; Quebec Bur. Mines, 1932, pt. D, pp. 99-103. Richardson, J. (1857): Report...on the Island of Anticosti and the Mingan Islands; Geol. Surv. Canada, Rept. Prog., 1823-36, pp. 191-242. On the development of Tetradium oellulosum Hall Sp.; Amer. Geol. Vol. 22, pp. 16-22. Graptolite Facies of the Beekmantown Formation in Rensselaer County, N.Y.; N.Y. State Mus., Bull. 22, pp. 246-375. Cephalopoda of the Beekmantown and Chazy Formations of the Champlain Basin; N.Y. State Mus. Bull. 90, p. 389. Graptolites of New York, part 2; N.Y. State Museum, Mem. 11, pp. 1-52. Lower S l l u r i c Shales of the Mohawk Valley; N.Y. State Mus. Bull. 162. Age of the black shales of the Lake Champlain region, N.Y. State Mus. Bull. 227-228, p. 108-116. The Utica and Lorraine formations of New York, New York State.Mus., Bull . 258, 175 pages. Alternating oscillatory movement i n the Chazy and Levis troughs of the Appalachian geosyn-cline, Geol. Soc. Am., Bull., Vol. 40, p. 410ss Ruedemann, R., Chadwick, G.H. (1935): Ordovician blaok shales of New York; Science, Vol. 81, p. 400. Safford J.M. (l85o): Remarks on the Genus Tetradium, with notices of the Species found i n Middle Tennessee; Am. •Jour. Sci., series 2, Vol. 22, pp. 236-238. Ruedemann, R* (1898): (1902): (1906): (1908): (1914): (1921): (1925): (1929): x x i i . S a l t e r , J.W. (18.53): F o s s i l s from the Ottawa River; Can. Jour. 1, pp. 221-222. (1859): Figures and descriptions of Canadian organic remains (Ordovician): Decade 1, Geol. Surv. Canada. Schuchert, C. (1930): Orogenic Times of the Northern Appalachians; Geol. Soc. Am., B u l l . 41, pp. 701-724. Schuchert, G., Twenhofel, W.H. (1910): O r d o v i c i c - S i l u r i c Sections of the Mingan and An t i c o s t i Islands, Gulf of St. Lawrence; Geol. Soc. Am., B u l l . , V o l . 21, pp. 677-716. Selwyn, A.R.G. (18«2): On the Geology of the Ottawa Palaeozoic Basin; Ottawa F i e l d Nat. Club I , Trs. No. 3, pp.. 34-39. S i n c l a i r , G.E. (1942): The Chazy Conularida and t h e i r Cogeners; Ann. Carnegie Mus. 29, PP. 224-225. (1944) : Some Ordovician T r i l o b i t e s from Ontario; Roy. Can. Inst., Trans. 25, pt. 1, No. 43, pp. 15-20. (1945) : Some Ordovician L i n g u l i d Brachiopods: Roy. Soc. Canada, 3rd ser. 39, sec. 4, pp. 55-82. Sowter, T.W.E. (1888): Preliminary Notes on the Chazy Formation at Aylmer, P.Q.; Ottawa Nat. 2, pp. 11-15. Springer. F. (1911): - On a Trenton Eohinoderm Fauna; Geol. Surv. Canada, Mem. 15-?, pp. 10, 11, 25, and 57. Sproule, J.C. (1936): A Study of the Cobourg Formation; Geol. Surv. Canada, Mem. 202, pp. 93-118. x x i i i . S t a n f i e l d , J . (1912): Mineral Deposits of the Ottawa D i s t r i o t ; Geol. Surv. Canada, Guide Bk. 3, pp. 87-117. Stewart, B.B.H. (1920): The Stratigraphy and Palaeontology of Toronto and V i o i n i t y ; Ont. Dept. Mines; Ann. Rept. 29, V o l . 29, pt. 6, pp. 1-58. Stewart, J . (1987): The Development of the Mines of the Ottawa Reg-ion; - Ottawa F i e l d Nat. Club I I I , pp. 22-29. (1888): Notes on Geological work of the Summer 1887; Ottawa Nat. I, pp. 170-171. Twenhofel, W.H. (1927): Geology of A n t i c o s t i Island; Geol. Surv. Can. Mem. 134. (1931): Geology of Mingan Islands; Geo. Soo. Amer. B u l l . V o l . 42, pp. 573-588. (1938): Geology and Palaeontology of the Mingan Islands, Quebec; Geol. Soc. Am., Sp. Paper No. 11. U l r i c h , E.O. (1911) : Revision of the Palaeozoic Systems; Geol. Soc. Amer. B u l l . 22, pp. 648-652. (1913): Ordovician-Silurian Boundary; Twelfth Inter. Geol. Gongr., Gomptes Rendus, pp. 593-667. U l r i c h , E.O., Schuohert, C. (1902): Palaeozoic Seas and Barriers i n Eastern North America; N.Y.St. Mus., B u l l . 52, pp. 633-663. Valiquette, J.H. (1912) : Report on Montreal Quarries; Quebec Bur. Mines, Mining Oper. i n the Prov. of Que. during year 1911. Vanuxem, L. (1842): Geology of New York. Part I I I , Comprising the Survey of the Third Geological D i s t r i o t ; Albany, N.Y. xxiv Waddington, G.W. (1950): Limestone Deposits of the Mingah Islands area, Saguenay County; Quebec Bur. Mines, Geol. Rept. 42, pt. 2. Waleott, C D. (1879): The U t i c a Slate and Related Formations of the same Geological Horizon; Albany Inst. Trans., V o l . 10, pp. 1S17. Whiteaves, J.F. (1883): Note on the Occurrence of Siphonotreta seotica Davidson i n the U t i c a Formation, near Ottawa; Can. Nat. Geol., N.S. 10, pp. 396-597. (1897): Description of a New Genus and Species of Gystideans from the Trenton Limestone at Ottawa; Can. Rec. S c i . 7, pp. 287-292, 595. (1905) : Description of a New Speoies of Matheria from the Trenton Limestone at Ottawa; Ottawa Nat. 17, No. 2, pp. 52-54. (1906) : From the Trenton Limestone of Ontario and Quebec; i b i d . , pp. 516-323. (1908): Notes on the Pelecypoda or Bivalve Mpllusca of the Chazy Formation i n Canada, with Descriptions of one New Genus and four New Speoies from the Chazy Sandstone at Hog's Back near Ottawa; Ottawa Nat. 22, pp. 102-115. Williams, M.Y. (1916): Formations adjacent to the Niagara Escarpment of Southwestern Ontario; Geol. Surv. Canada, Sum* Rept. 1915, pp. 139-142. (1921): O i l p o s s i b i l i t i e s of Manitoulin Island, Ontario; Geol. Surv. Canada, Sum. Rept. 1920, pt. D, pp. 26-32. (1937): General Geology and Petroleum Resources of Manitoulin and Adjacent Islands, Ont.; Geol. Surv. Canada, P r e l . Rept. paper 37-25. XXV. Wilson, A.B. (1913): A New Brachiopoci from the Base of the Ut i c a ; Geol. Surv. Canada, Mus. B u l l . 1, pp. 81-86. (1915): A New Ordovician Pelecypod from the Ottawa D i s t r i c t ; Ottawa Nat. 29, pp. 85-86. (1921): The Range of Certain Lower Ordovician Faunas of the Ottawa Valley, with Descriptions of Some New Species; Geol. Surv. Canada, B u l l . 33, pp. 19 -27. (1932): a. Notes on the Pamelia Member of the Black River Formation of the Ottawa Valley; Amer. Jour. S c i . 24, pp. 135-146. b. Ordovician F o s s i l s from the Region of Cornwall; Roy. Soc. Canada, Trans. 3rd ser., sec. 4, Vol. 26, pp. 373-404, 6 p i s . (1936) : A Synopsis of the Ordovician of Ontario and Western Quebec and the Related Succession i n New York; Geol. Surv. Canada, Mem. 202, pp. 1-20. (1937) : Erosional Intervals Indicated by Contacts i n the V i c i n i t y of Ottawa, Ontario; Roy. Soc. Canada, Proc. and Trans., 3rd ser. 31, sec. 4, pp. 45-60. (1944) : Rafinesqulna and i t s Homomorphs Opikina and Qp l k l n e i l a from the Ottawa Limestone of the Ottawa-St. Lawrence Lowland; Roy. Soc. Canada, 3rd ser. 78, sec. 4, pp. 145-203. (1945) : Strophomena and i t s Homomorphs Trigrammaria and Microtrypa from the Ottawa Limestone of the Ottawa-St. Lawrence Lowland; Roy. Soc. Canada, 3rd series 39, sec. 4, pp. 121-150 (1946) : a. Geology of the Ottawa-St, Lawrence Lowland, Ontario and Quebec; Geol. Surv. Canada, Mem. 241. b. Ichinodermata of the Ottawa Formation of the Ottawa-St, Lawrence Lowland; Geol. Surv. Canada, B u l l . No. 4. X X VI. Wilson, A.E., Mather, K.F. (1916): Synopsis of the Common F o s s i l s of the Kingston Area; Ont. Dept. Mines Ann. Rept. 25, V o l . 25, pt. 3, pp. 45-66. Wilson,A.E.; Stewart, J.S.; and Galey, J.F. (1941): Sedimentary Basins of Ontario, possible Sources of O i l and Gas; Roy. Soc. Canada, Proc. and Trans., 3rd ser. 35, sec. 4, pp. 167-185. Wilson, A.W.G. (1901): Physical geology of central Ontario, Ganad. Inst., Tr., Vol. 7, p. 139-186. Wilson, M.B. (1914): Southeastern Portion of Buckingham Map-area, Quebec; Geol. Surv. Canada, Sum. Rept. 1913, pp. 196-207. (1921): The Relationships of the Palaezoio to the Pre-eambrian along the Southern Border of the Laurentian Highlands In Southeastern Ontario and the adjacent Portions of Quebec; Roy. Soc Canada, Proc. and Trans., 3rd ser. 14, s e c 4, pp. 15-24. (1924): Arnprior-Quyon and Maniwaki Areas, Ontario and Quebeo; Geol. Surv. Canada, Mem. 136, Map* Pub. NO. 1739. (1931) : a. Ripple-marks in the Lower Palaeozoics of Ottawa Valley; Can.Min. Jour. 52, No. 14, pp. 347-348. b. Ripple-marks near Perth* Lanark County, Ontario; Can. Field Nat. 35, No. 2, pp. 25-27. (1932) : The Mammillary Mounds of the Bonnechere Valley; Ottawa Nat* 46, pp. 32-33. Woodward. H. (1889): On the Discovery of Turrilepas in the Utioa Formation (Ordovician) of Ottawa, Canada; Geol. Mag. dec 3, Vol. 6, pp. 271-275. Wright, J.F. (1923): Brockville and Mallorytown Map-area; Geol. Surv. Canada, Mem. 134; Map, Pub. No. 1964.
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Geological Sciences
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Lower and middle Ordovician of the St. Lawrence lowlands stratigraphy and historical geology
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