RG 100(A) UPTON AREA, BAGOT, DRUMMOND, RICHELIEU, ST-HYACINTHE AND YAMASKA COUNTIES GOVERNMENT OF QUEBEC DEPARTMENT OF NATURAL RESOURCES

RENÉ LEVESQUE, Minister P.-E. AUGER, Deputy Minister

GEOLOGICAL EXPLORATION SERVICE

H.W. McGERRIGLE, chief

GEOLOGICAL REPORT 100

UPTON AREA

BAGOT, DRUMMOND, RICHELIEU ST-HYACINTHE AND YAMASKA COUNTIES

by T.H. CLARK

QUEBEC 1964

TABLE OF CONTENTS Page INTRODUCTION 1 General statement 1 Location 1 Transportation 2 Previous work 2 Method of work 2

GENERAL GEOLOGY 3

STRATIGRAPHY 5 Formations west of the Champlain fault 5 Bécancour River formation 5 Pontgravé River formation 6 Nicolet River formation 6 Yamaska River exposures 6 St-Germain complex 10 St-François River exposures 12 St-Germain river 16 Fields west and northwest of St-Germain 17 David river 18 Chibouet river 18 Road cuts along Sir Wilfrid Laurier boulevard 19 Formations east of the Champlain fault 19 Lévis limestone 19 Sillery sandstone 20

STRUCTURAL GEOLOGY 20 Chambly-Fortierville syncline 20 St-Hugues structure 21 Thickness of sedimentary section 21 The St-Barnabé fault 22 The St-Germain complex 22 Chibouet river 22 St-François river 23 St-Germain river 24 The Appalachian terrane and Champlain fault 24

ECONOMIC POSSIBILITIES 25 Oil and gas 25 Limestone 25 Miscellaneous 25

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APPENDIX A 26 APPENDIX B 34 BIBLIOGRAPHY 35 ALPHABETICAL INDEX 36

ILLUSTRATIONS

Map

No. 1411 - Upton area, geological map, also show- ing location of water wells. (In pocket)

Figures

1 - Generalized geological cross section of the Upton area 4 2 - Map of exposures on Yamaska river near St-Hugues 9 3 - Structure sections of St-Germain complex along St-François river 13

Plates

IA - St-François river above St-Joachim-de-Courval B - Bed of St-François river near St-Joachim-de-Courval, at low water IIA - Thin-bedded Utica slate in St-Germain complex. St-Frangois river, near St-Joachim-de-Courval B - Detail of A above C - Closely spaced tension cracks in slates, same locality as above IIIA - Felsenmeer developed on calcareous slates of St-Germain complex 3 miles northwest of St-Germain-de-Grantham B - Detail of A above Iv - Landslide near St-Louis-de-Bonsecours UPTON AREA

BAGOT, DRUPMAOND, RICHELIEU

ST-HYACINTHE, and YAMASKA COUNTIES

by

T.H. Clark

INTRODUCTION

General Statement

The Upton area is part of the St. Lawrence Lowlands, except for its southeastern corner which lies within the Appalachian geological.. province. The mapping (1944, revised to June 1, 1961) of the Upton area is part of a programme of investigation covering the whole of the St. Lawrence Lowlands, the purpose of which is to provide a better understanding of the distribution and kinds of rocks present, with particular reference to the search for oil, natural gas, limestone, and other useful products.

Outcrops are very few in this area. Nevertheless, strati- graphic boundaries, determined partly from outcrops within this area and partly by extensions of boundaries from the Yamaska area to the north and the St-Hyacinthe area to the south, can be confidently delineated, and will, it is hoped, provide those engaged in the search for natural resources with helpful guides.

Location. The Upton area is in the St. Lawrence Lowlands to the south of St. Lawrence river. It is bounded by latitudes 45°45' and 46°, and by longitudes 72°30' and 73°. It includes parts of Bagot, Drummond, Richelieu, St-Hyacinthe, and Yamaska counties.

Two large rivers cross the area. St-Frangois river cuts across its northeastern corner, and Yamaska river flows from south to north not far from its western border. Although these two rivers pass through Drummondville and St-Hyacinthe, respectively, before entering the area, they have within this area no towns of importance upon their banks. In fact, no large towns occur here at all. St-Germain - 2 -

(pop. 925)*, St-Guillaume d'Upton (pop. 802), St-David (pop. 800), Massueville (pop. 647), St-Jude (pop. 700), St-Hugues (pop. 487), and St-Bonaventure (pop. 383) are the largest villages. These and several smaller communities are concerned almost wholly with mixed agriculture and related affairs.

Transportation. A network of good, fair, and poor roads serves practically all of this area, and no spot is more than two miles from some sort of a road. Both main rivers are beset with rapids which make their use as highways impossible. The smaller streams, St- Germain, Chibouet, Salvail, David, and aux Vaches rivers, are all un- suitable as through-going routes even for small barges.

There are three railroads. The main line of the Canadian National Railways from Montreal to Halifax cuts across the southeast corner; a branch of the same line runs roughly parallel to and west of Yamaska river. A Canadian Pacific branch line runs from St-Guil- laume d'Upton in the centre of the area southwestward to St-Hugues and thence south to St-Hyacinthe. An abandoned track once connected St-Guillaume d'Upton with St-Germain and Drummondville.

Previous work. Very little has been published that relates to the rocks of this area, and only those publications by Foerste, Clark, and Belyea are of importance. Brief notes can be found in Logan (1863, p. 205), and in Ells (1896, p. 18J, 22J). Foerste (1916, pp. 50-52) gave a description of the exposures at St-Hugues, and his report of 1924 contains descriptions of many of the fossils found there. Parks (1931, pp. 89-92) recorded a series of observations along St-Frangois river, and though it is impossible to recbnstruct a section therefrom, these observations do show the complex structure of the outcrops forming the cliffs of that river. Snider and Farish (1935, pp. 97, 98) added nothing new. Clark (1947, pp. 15, 16), in a general review of the stratigraphic succession south of the St-Lawrence, established the St-Germain Complex as a structural rock unit. Belyea (1952, pp. 54-60) gave a detailed lithologic log of St-Gérard No. 1 well.

Method of work. The base map used in this work was the Upton map (Dept. National Defence, Canada 31 is , 1 mile to 1 inch). Enlargements to twice published scale were provided for field plotting. x Population data are taken from Canadian Railway Guide with Airlines, June, 1960.

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All rivers were traversed, the St-Frangois along both banks. Cross- country traverses were made by pace and compass in all areas where there was likelihood of finding outcrop. No air photographs were available.

Preliminary studies were made in parts of the seasons of 1942 and 1943, but mapping was systematically carried out during the season of 1944, with Jean Préfontaine as field assistant.

GENERAL GEOLOGY

The rocks of this area are all sedimentary and, with one or two possible exceptions in the southeast corner, are all of Ordo- vician age. By far the greatest part belongs to- the series elsewhere characteristic of the extensive syncline which dominates the struc- ture of the rocks exposed in the St: Lawrence lowland. In the south- east corner there are a few exposures of rocks characteristic of the folded Appalachian mountain belt.

Formations Exposed in the Upton Area

Formations of the St. Lawrence Lowlands Group Formations, with brief descriptions

0 Richmond Bécancour River formation, usually referred to as the red Queenston shale. Seen only at St-David. R Pontgravé River formation. Not seen D 0 Lorraine Nicolet River formation V St-Hilaire member (Pholadomorpha zone). Not seen. I Chambly member (Proetus zone). Not seen. C Breault member (Crvptolithus zone). Outcrops I along Yamaska river near St-Hugues, and along St-François river below'St-Joachim-de-Courval. A N St-Germain A complex of faulted and folded beds of Lorraine, Complex Utica, and possible Trenton ages. St-François river above and below St-Joachim-de-Courval; Chibouet, David, and St-Germain rivers.

Formations of the Appalachian Province

ORDOVICIAN Lévis limestone. Southeast corner of area

? CAMBRIAN Sillery sandstone. Southeast corner of area - 4 -

Riv. Yamaska 1 N.W. aJ

6

6

4

LEGEND

8 BÉCANCOUR RIVER 3 ST. GERMAIN COMPLEX

7 PONTGRAVÉ RIVER 2 SILLERY

6 NICOLET RIVER LEVIS

5 UTICA 0 5 10

Scale in miles 4 TRENTON

FIGURE 1

Generalized cross-section from the northwest corner to the southeast corner of the Upton area. Vertical exaggeration approximately 10

D.N.R.O. 1962 NO. 1429 - 5 -

As with most of the St. Lawrence Lowlands, the western part of this area is dominated by the Chambly-Fortierville syncline, the axis of which cuts across the northwestern corner. Straddling Yamaska river near St-Hugues is a structure, superimposed upon the main syncline, consisting of two anticlines and an intervening syn- cline, all developed in Lower Lorraine (Breault member) rocks. This folding cannot be. recognized further to the northeast, and is shown as a closed structure on the map.

The eastern half, more or less, of the area consists of Lorraine, Utica, and possible Trenton beds, highly contorted by both folding and faulting. In the extreme southeast corner there are some exposures of the Sillery sandstone and of a limestdne that is probably a correlative of the Lévis limestone.

The order in which the formations are listed in the pre- ceding table from the top downwards, is also the order in which they are found as one progresses from northwest to southeast across the area. The probable geological structure, much simplified, along the northwest-southeast diagonal of the map, is indicated above in Figure 1. It will be noticed that there is, in general, an increase in structural complexity toward the southeast.

STRATIGRAPHY

Formations West of the Champlain Fault.,

Bécancour River Formation

The red shales and sandstones of this formation are exposed only in the bed of David river at St-David. At about 1,000 feet above the bridge the exposures begin and extend 400 feet upstream. The sand- stones arti in lenticular beds 1 to 3 inches thick that strike N. 45° E. and dip 13° N.W. The beds are broken by strong joints that also strike N.45°E. but that dip 75° S.E. Some red detritus can be seen at the upper dam, about half a mile upstream. This probably came from exca- vations made when the dam was built, but no exposures exist there today.

The attitude of the rocks shows that the axis of the main syncline lies to the northwest, although. there are no exposures in that direction to locate its position. Places where red rock has been encountered in digging wells are marked on the 'well map' accompanying - 6 - this report, and serve, in the absence of controlling exposures, to help delimit the area of outcrop of the formation.

The one deep well (Canadian Seaboard St-Gérard No. 1) put down in this area with the express purpose of finding natural gas is of some help in this connection. This is in the parish of St-Gérard Magella, near the northern boundary of the area and about 3 miles northeast of St-David. After passing through 50 feet of overburden the well penetrated red shale for 1,140 feet, and grey shale designated Queenston (Que. Bur. Mines, 1932, p. 50) for a further 90 feet before passing into the grey shales of the Pontgravé River formation. Because the well was drilled almost on the axis of the main syncline, it is not surprising that a great thickness of the Bécancour River formation should have been encountered, or that the hole produced no natural gas. The log of this well is given in Appendix A.

Pontgravé River Formation

No exposures of this formation are known in the Upton area. However, in the log of the St-Gérard well (Appendix A) there is record- ed a thickness of 220 feet of Pontgravé River grey shale and limestone.

Nicolet River Formation

Rocks of this formation occupy a belt stretching diagonally from northeast to southwest through the west-central part of the area. Although the Nicolet River formation is very thick (2,491 feet on Nicolet river), only the lower part, the Breault member (1,020 feet thick on the Nicolet) outcrops here. Exposures are common along Yamaska river from near the southern margin of the area to about a mile below St-Hugues, and are richly fossiliferous in places. Some of the exposures along St-François river definitely should be referred to the Breault member although all are relegated to the St-Germain complex as mapped. The lowest exposure, riverwise, on the left (south- west) bank definitely belongs to the Breault member, and is so mapped (see Figure 2).

Yamaska River Exposures. Along both banks of Yamaska river below the mouth of Chibouet river in the vicinity of St-Hugues the Cryptolithus zone (Breault member) of the Nicolet River formation is exposed (Figure 2). On the east bank there is a small exposure less than a quarter of a mile from the mouth of Chibouet river; after a gap of half a mile, thin-bedded shales with half-inch thick sand- stone beds occupy the shore for another half mile. There is no - 7 - limestone here, although Foerste (1916, p. 50) implied in his descrip- tion of these beds that argillaceous limestone, in places abundantly supplied with fossils, was common. On the west bank of the river the exposures begin immediately opposite the mouth of Chibouet river, and about 500 feet below the ferry landing. Thence they are more or less continuous for three quarters of a mile, and consist of shales with a few beds of limestone, and here and there, a thin bed of sandstone. One 4-foot bed of sandstone occurs about a quarter of a mile down- stream from the beginning of the exposures. One or two small faults, and one zone of contorted beds extending for 90 feet along the stream bank, are the only small-scale disturbances noted. The description of the structure of these beds is deferred to the section on "Struc- tural Geology". The fossils collected by Foerste and by the present writer are given in the following list.

) Nicolet River d

C -- Identified by the writer on (Lorraine)

e hm

F -- Identified by Foerste e n o n

o

(Ric z ton z

e ber ha n em o List of fossils from exposures hus ber ber morp z m s em on Yamaska river near St em lit -Hugues e Tren é River r do ir tu to immediately below mouth of m e la lt m rav o

Chibouet river ila bly Pro tg Pho Crvp H eau n St- Po Cham Br Utica

Favistella sp. C Crinoid columnals C F Bryozoa C Coeloclema commune X F Linqula sp. C Pholidops subtruncata XXXX C Glvptorthis sp., cf. G. fissicostata C G. sp. F Holtedahlina sp., cf. H. varsensis C Resserella roqata X X X X C R. testudinaria X X F Sowerbvella sericea XXXX X C F Leptaena invenusta F L. moniquensis X X C Catazvga erratica F - 8 -

Nicolet River C - - Identified by the writer (Lorraine) F - - Identified by Foerste v 0 E -C a) U C N C O C o C0 N o ~ H N C a) ~ a) H ' A .Ç a) N H v E C H List of fossils from exposures on a) H m o a .,~ E o N A E E E.~ Yamaska river near St-Hugues a) O o.) a) r H `Q) H 'O E 0 E o immediately below mouth of .r.1 ~ m (6 ~ >- a~i ++ .-1 O i O r-I Chibouet river rn a x â ~â C O U ro a) 0 -i-> .0 H ~ M U M Cornulites sp. C Byssonychia radiata X X X X C F Ctenodonta hvacinthensis X X C C. borealis X X Cymatonota recta X X X X C Clidophorus praevolutus X X X X C G. postvolutus X C Whitella huquesensis X X C W. complanata X X X F Ç. planulatus X X X F Cymatonota pholadis X X X X F Colpomya faba X X X F Rhytimya oehana X X C Archinacella oulaskiensis X X X F Sinuites cancellatus X X X X X C F Liospira sp. C Hormotoma qracilis X X X C Pterotheca sp. F Cryptolithus bellulus X C C. tesselatus X F Triarthrus becki F T. huguesensis X C Calvmene sp. C Isotelus sp. F Lepidocoleus iamesi X X X X X C - 9 -

~► TO ST. HUGUES 1 MILE

o

SCALE IN FEET

FIGURE 2

Map of outcrops (solid black) along Yamaska river near St.Hugues. All rocks belong to the Breault member of the Nicolet River formation.

D.N.R.Q. 1962 NO. 1430 - 10 -

The presence of species of Cryptolithus and a dozen species elsewhere known only from the Cryptolithus zone, and the almost complete absence of species found exclusively outside the Crvptolithus zone, make it certain that these beds belong to the Breault member of the Nicolet River formation.

One mile upstream from the ferry landing nearly vertical isoclinally folded shales occur on both sides of the river for about half a mile. The shales on the east bank contain the following fos- sils: Poor graptolites Resserella sp. Geisonoceras sp.

On the west bank, exposures of soft, crumbly shale contain the follow- ing: Resserella sp. Clidophorus neplectus Triblidium (Vallatotheca) sp. Geisonoceras sp. Cryptolithus bellulus Such shales, with Geisonoceras, are elsewhere generally found in that part of the Nicolet River formation below the base of the measured section along Nicolet river, and may be part of the Breault member, or possibly part of the Leclercville formation.

These beds differ considerably from those of the sections downstream from the ferry in two respects: first, they are devoid of the calcareous fossiliferous beds, and, second, they are isoclinally folded. Less than half a mile separates the two lots of exposures across the strike, and it is probable that a fault, possibly a thrust, intervenes to bring the two quite different rock types so close together

St-Germain Complex

To the southeast of the exposures whose Lorraine age is not in doubt, and extending as far as the thrust which bounds the folded Appalachian terrane to the southeast, there exists a complex of in- tricately folded and faulted shales, slates, limestones and sandstones (Figure 3), in which there are practically no fossils. Lithologically, some of this complex is similar to the dark grey silty shales with sandstone beds the Breault member of the Nicolet River formation; some parts consist of soft silty shales, finely (1-5 mm.) colour banded, and probably represent either the Leclercville shale (lowest Lorraine) or the Lotbiniére shale (Utica); there are also developments of hard, thin-cleaving shale, or in places slate, containing poorly preserved graptolites, with interbedded buff- or orange-weathering magnesian limestone in beds a few inches thick, almost certainly of Utica age; and, lastly, there are developments of dark calcareous shales and limestones unlike the above but similar to Trenton limestones found elsewhere. Although it is possible in some exposures to find charac- teristics which allow the allocation of such exposures to one of the four varieties described, most exposures defy such treatment. It seems best, therefore, to group these highly disturbed beds together as a structural unit. The writer has chosen the name "St-Germain Complex" (Clark, 1947, p. 15) for this, because of the great development of these rocks along St-Germain river and over several square miles of fields west of St-Germain village. When one considers the complexity of the structure, it is by no means impossible that representatives of two, three, or even four formations may be present in any particular area. However, mapping separate formations within this complex has proved to be impracticable but, because more detailed interpretation of the structure may eventually be desirable, a few additional charac- teristics of the four types follow.

The Breault member of the Nicolet River formation is a silty shale with a few light to medium grey, fine-grained sandstones. The latter appear to have given a certain competence to the shales with the result that the Breault member beds have,in many places•, resisted the strong deformation that has affected the other and dominantly shaly formations. Not only does the Breault appear largely as little deform- ed beds, up to a few hundred feet thick, but they are almost sure to yield Resserella and Crvntolithus. It is in many places a difficult matter to decide, as one progresses upstream (southeastward) along St-Frangois and similar rivers, where to cease mapping exposures as belonging to certain formations and to allocate them to the St-Germain complex.

The Leclercville shale, first described from the Portneuf area (Clark, 1947, p. 8) is a thick (1,000 feet more or less) develop- ment of silty shales with thin sandstone beds rarely more than 1 inch thick. Fossils are very scarce, and include Triarthrus, Geisonoceras, and poor graptolites. Its lower part contains less silt, and,because of its small-scale colour banding (1-5 mm.),is referred to here as variegated shale. - 12 -

The Utica shale elsewhere in the lowland is usually a thin- bedded carbonaceous shale, noticeably bituminous in its lower part. Fossils are scarce, though graptolites may be common on certain bed- ding planes, and Leptobolus, Triarthrus,Geisonoceras, and Dicranonraptus may be present throughout. At irregular intervals (10 to 20 feet) there are slightly magnesian limestone bands, up to 1 foot thick, weathering buff or orange. Some of these limestones have a strong fetid odour. There may also be present large concretions, several feet across, weathering buff or orange. All of these characteristics can be seen here and there within. the rocks mapped as the St-Germain complex.

Lastly, the Trenton beds west of the St-Lawrence are mostly fossiliferous limestones, but east of,the river both limestone and fos- sils are absent from at least the upper part of the rocks of that group Instead, they are chiefly calcareous shales and slates, e.g. the Stony Point shale in the ;St-Jean (Clark, 1955) and the Lacolle (Clark, 1934) areas. In the Upton area, calcareous shales and slates, with here and there beds of dark grey, grey-weathering limestone, make up much of the southeasterly part of the St-Germain rocks. ,Within these beds, no.. limestone can be definitely assigned to any of the Trenton formations, and there are no Trenton fossils in the. shales. ,However, this develop- ment occurs southeast of recognized Utica components of the St-Germain complex, and is certainly not Breault,• Leclercville, or Lotbiniére. It is, therefore, not unreasonable to designate it, provisionally, as being composed of calcareous shales and limestones of Trenton age. This type is chiefly exposed along St-François river, as indicated above, and also in the widespread pasture outcrops west and northwest of St-Germain.

St-François River Exposures. The outcrops of Lower Lor- raine shales which occur on both banks of St-Francois river in the Yamaska area are continued upstream to the Upton area where, out of a course of about 9 miles, the lower 7 miles show almost continuous exposures on both sides of the river (Figure 3). The upper 2 miles are barren of rock outcrops. Throughout all but a few short stretches, the rocks are accessible at low water. In spite of this sequence of exposures very little correlation can be achieved between the various parts. First, fossils are exceedingly scarce and rarely helpful; second, the strata of these parts are more or less strongly folded and faulted, and this deformation becomes more and more intense upstream toward the southeast. Although several faults complicate the structure of these exposures it is not felt that any one of them is of great disruptive importance. In fact, many of them show a displacement of but a few

FIGURE 3A Northeast corner of Upton area showing, in black, the outcrops on both banks of St. Francis river. The sections shown in Figure 3b are adjusted to appear as they would if the river ran in a straight line from D to A. The scale indicated is in miles. The lines marked with the mile counts are, in effect, strike lines.

N w //,17~,t"////////%rfJ// \\ AR • M P5K P, DR iC 1 t I- -1 I • up~ SCALE IN MILES A I1 1 I I 1 I l I I I B 2 Q3 4 5 6 7 8 9 10 ; 11 12 13 Z F SCALE IN THOUSANDS OF FEET F a,r% uu • 77 /11111M1 I11\1N NlIA1C AL w BL rc

FFFF F FF `07At rr ILAWAV0~~.R1 vS?11nnI\\ NÎiLh\ Aulu,.. DR t .4111111111' 111111111\ CR i T 3 B 13 14 15 '16 17 18 19 20 22 23 . 24 25 F F YAMASKA I DRUMMOND Y511111\\V5illl\\\\Illllll ' DL ,tQ1111ItO1\\\4 \Ut\aR, CL F T County line

St. Joachim church F F tF F F F F F FF F F 'if \\ t r , `1 N l'• +611\VI 1 "S, CR DR 6 5 ISLAND 7 1 ),1 C 1 1 1 1 1 D 26 2 27 28 29 30 31 32 33 34 35 36 7 F F F F F FF F F ra\\ \ anC-~\ CL � DL Î FIGURE 38 Sections along right (AR--BR, BR—CR, CR--DR) and left (AL--BL, BL--CL, CL—DL) banks of St. Francis river. Large numbers are miles, corresponding to miles in Figure 3a. Smaller numbers indicate thousands of feet. The strike is at right angles to the lines A—B, B--C, C—D. Note the general lack of concordance of structures of the rocks on one bank with those in line of strike along the opposite bank. "r indicates observed fault.

D.N.R.O. 1962 NO. 1431 - 14 - feet or tens of feet, although in some cases there may be no corres- pondence between the beds on the two sides of a fault within the height of the cliff. Another peculiarity which not only gives a clue to the regional structure but emphasizes the difficulties in correlation, is that no close, and little general, similarity between strata or struc- tures on the two banks can be made out. This anomalous condition persists downstream into the Yamaska area. The river is 1,200 to 1,500 feet wide, and therefore within such a distance the structure so chan- ges along the strike as to reveal different strata and structures on the two sides of the river. Only general structural and stratigra- phical trends can be carried from one side of the river to the other. This can best be seen by referring to Figure 3b, where the structures on both sides of the stream are shown in close relationship. These sections, taken from carefully recorded structural and stratigraphic observations along every foot of both banks, have been redrawn to ap- pear as they would were St-Frangois river to present a perfectly straight course, at about N. 500 W., which is approximately perpendic- ular to the regional strike of about N.40°E. There are, of course, numerous disadvantages and inaccuracies involved in carrying out such a conversion, but in places, such as around the big bend of the river, a running section would be distorted and very misleading. The section along the southwest bank has been drawn as it would appear looked at from the southwest and both bank sections are, in that respect, in harmony. Furthermore, because the redrawn section is perpendicular to the strike, beds and structures mapped on the north bank should be seen imm3diately thereunder on the south bank. That such correspondence is not general can be explained in part as being due to the plunge of folds thereabouts, and in part to the fragmentation and large-scale dislocation, possibly in places on a formational scale, thus prohib- iting the continuity of a structure or a bed for very far along the strike. There is the possibility that one or more faults do traverse the river bed, though no compelling evidence of such continuous struc- tures was seen.

In the entire section along St-Frangois river there are, lithologically, several types and associations of rocks. There are three chief developments. The beds exposed farthest downstream are largely sandy shales and shaly sandstones, here and there with Res- serella, Crvntolithus, and a few other fossils. These accord well with the lowest beds in Foerste's Nicolet river section (1916, p.14), and may be correlated with them. A second type of rock is a very argil- laceous shale, finely (1 to 5 mm.) and evenly banded, the banding showing very plainly in various colours when the rock is wet. This - 15 -

variegated shale is common between the northern boundary of the map and St-Joachim-de-Courval. It may be the same as the Leclercville shale (Clark, 1947, p. 8), and if so would lie stratigraphically below the Lower Lorraine type first described above. The third type consists of black shale, interbedded with a fine-grained, magnesian limestone. The shale is not distinctly banded but on some bedding surfaces bears poorly preserved graptolites. The limestone is medium grey when fresh and buff- or orange-coloured when weathered. In one or two places orange-coloured septarian concretions up to 5 feet across occur. This third type has a counterpart in the shales exposed along the shore above Pointe Platon (Portneuf area, Clark, MSS.) where interbedded, buff-weathering, grey limestone and black to dark grey shale, in part variegated, occur to- gether. At Pointe Platon itself the limestone beds are separated by greater thicknesses of shales, usually about 20 feet, than is the rule along •St-François river, where 5 to 10 feet seem to be usual.

There is a remarkable section of this third type of rock along the cliffs of the right bank of St-François river from 5/8 mile below the, church at St-Joachim-de-Courval upstream for more than a quarter of a mile. In this stretch the cliffs are from 10 to 30 feet high, and bedrock is exposed without a gap. It consists largely of dark grey to black shale, cleaved and veined, that rarely shows bed- ding within itself but that includes interbeds of the buff-weathering magnesian limestone. Calculations made from measurements taken along 1,360 feet of the river bank show that a total thickness of 940 feet is exposed, of which 109 beds of limestone from 1 to 20 inches thick make up 60 feet, leaving a balance of 880 feet composed of shale or slate. Hence the proportion of limestone to shale (and slate) is 1: 14.7. The prevalence of cleavage and slickensides in the slate indica- tes a probable thinning of the original shale in its transformation to slate, so that the original proportion of limestone to shale would probably have shown a greater figure for shale than that given above. Moreover, it is certain that much duplication by isoclinal folding, and probably by faulting, has occurred, but such deformation would probably not modify the proportion of the two kinds of rocks. The peculiar lithologic combination, together with a few fragments of fossils, indicates without a doubt that these shales and buff-weather- ing limestones are of Utica age.

Lastly,a fourth type, that possibly may represent the Trenton, is a hard, thin-cleaving shale unknown elsewhere, associated with a dense, dark grey limestone, weathering grey. This is commoner above St-Joachim than below. From the beginning of this development going upstream, strong rapids begin and persist as far as the exposures - 16 - last. This is another reason for supposing that a different rock type occurs here. Constant reminders of both Utica and what may be Leclerc- ville are to be found for nearly 2 miles above St-Joachim-de-Courval; these include the variegated shale, the buff-weathering limestone and concretions and, very rarely, graptolite fragments in the shale. Toward the upstream limit of the exposures on the right bank the beds are mostly c lcareous shale with, here and there, beds up to 6 feet thick of grey-weathering sandstone.

It should be clear that it is impossible to generalize concerning this St-Germain complex. It contains much that seems defi- nitely to belong to the Lower Lorraine Breault and Leclercville beds, and also to the Utica, together with a good deal of material which seems to have no counterpart in either of the above, and may possibly belong within the Trenton group. The unravelling of the stratigraphic sequence seems a remote possibility, but its accomplishment would cer- tainly lead to a better understanding of the structure.

St-Germain River. Dredging carried out about 1943 to deepen the river for drainage purposes exposed fresh rock along St-Germain river from the crossing of Route 20 downstream almost as far as the lowest bridge above its mouth. Although the actual rock now lies for the most part below water level there are a few localities, such as upstream and downstream from the cement bridge one half mile west of the eastern boundary of the area, and three miles south of St-Frangois river, where good sections of the rock can be seen. Almost everywhere the rock is a black, slaty limestone with a brownish streak, or a slaty shale with a few beds of black limestone and of buff-weathering magne- sian limestone. Some of the rocks of this section have an oily odour. The sum of their characteristics seems to point to their being of Utica age.

On both sides of the cement bridge mentioned above the rock is thinner cleaving than elsewhere. On the west bank, 600 feet above the bridge, there are thin cleaving shales with poor graptolite frag- ments similar to those met with on both Chibouet and David rivers. Downstream from this bridge the black shales and shaly limestones con- tain buff- and orange-weathering limestones characteristic of the Utica. About 1,500 feet above the lowest bridge there is a 3-inch bed of grey, crystalline limestone in which, however, no fossils were found.

Everywhere the cleavage is steeply inclined, and the bedding, where it does not coincide with the cleavage, may have any attitude. In most of this section, however, bedding and cleavage coincide. - 17 -

Slickensides, quartz veins, and pyrite crystals are common throughout. Some of the slickensided black rock could well be mistaken for coal by the uninitiated (Weston, 1899,p. 9). Below the lowest bridge the buff- weathering magnesian limestone is still to be seen, although consider- ably brecciated owing, in part at least, to folding.

Fields West and Northwest of St-Germain. Over several square miles of farm land westward from St-Germain and northwest of Sir-Wilfrid- Laurier boulevard there occur scattered outcrops of calcareous shale and shaly limestone, black when fresh but weathering medium grey. The south- ernmost of these, almost exactly 4 miles west of St-Germain, is nearly pure limestone, coloured as above. Elsewhere calcareous shales seem to predominate. Most of the exposures are low, weathered, and consist of cleaved rock, so that satisfactory descriptions are impossible. One exposure (2 1/2 miles northwest of St-Germain) which covers an acre or so and stands 10 feet above the general level of the field, shows, in addition to the usual calcareous shale, a bed of grey crystalline lime- stone 8 inches thick with fragments of unrecognizable graptolites. Rusty-weathering limestone, possibly magnesian, accompanies these rocks. Immediately north of this exposure and on the north side of Route 22, the rocks have a slight oily odour. Two miles southeast of St-Edmond- de-Grantham there is a cluster of small exposures in the fields near the road corners. Calcareous shales and shaly limestones predominate, but in the cut exposed in the stream bed below the road bridge there are several beds of massive dense limestone and one of crystalline limestone, in neither of which, however, did thorough search reveal fossils. In all, about 60 feet of beds are exposed here, including what appears to be rusty-weathering magnesian limestone.

Almost midway between St-Germain and St-Edmond-de-Grantham there is another cluster of exposures, mostly of calcareous shales. One of these, however, is composed of crystalline limestone together with some conglomeratic material. This occurs as a low ridge 100 feet or more long. Brachiopods, including Resserella, and small fragments of bryozoa were found here. None of the fossils is specifically iden- tifiable, however, and hence there is no paleontological evidence as to the age of the containing formation.

There is little here to influence a reference of these ex- posures definitely to any one of the Lorraine, Utica, or Trenton form- ations. Little, if any, of the hard, thin-cleaving slate, or of the typical buff-weathering limestone can be seen, and there is therefore scant evidence of the presence of rocks of the Utica group, insofar as - 18 - those criteria are valuable. However, the black colour and the rusty weathering limestone indicate a possible Utica age. There is nothing to rule out the assignment of these rocks, or at least a large part of them, to the Lorraine. Crystalline limestone is rare, but not unknown, in the Lower Lorraine, and the exposures of such rock in the fields west and northwest of St-Germain cannot be considered good evidence for barring these exposures from the Lorraine and relegating them to the Trenton where crystalline limestones are common.

David River. For a few hundred feet upstream and for a mile or more downstream from the bridge over David river at St-Edmond- de-Grantham there are exposures of shale and slaty rocks. Above the bridge the rocks are mostly grey sandstone. Below the bridge shaly types predominate, with orange-weathering magnesian limestone common for half a mile downstream. About 500 feet below the junction with the tributary from the east there are some brown, thin-bedded shales with indefinite, graptolite-like fossils, similar to those found along Chibouet and St-Germain rivers. The exposures as a whole are similar to those found along Chibouet river, and it seems best to relate them, provisionally and without division, to the Utica and possibly the upper part of the Trenton formations.

Chibouet River. Between the bridge at Route 20 and the dam upstream, thin-cleaving hard graphitic slates occur on both banks of Chibouet river. Near the road, bedding and cleavage coincide, whereas farther from the road they diverge. Where small folds can be seen the cleavage is parallel to the axial planes. The shales contain poor graptolites, unidentifiable as to species or genus. In addition, there are a few beds of unfossiliferous limestone and one 6-inch bed of sandstone. The limestone beds have been disrupted by folding and solution and appear as dissociated fragments of strata. These rocks are considered to belong to the Utica group.

About 2 miles upstream exposure's begin again, and extend interruptedly for about 2 miles. The rocks farthest downstream are the variegated shales, probably belonging to the Leclercville form- ation. Farther upstream, about three-quarters of a mile above the sawmill, and at the end of a woods road, the exposures begin with hard, thin-bedded, thin-cleaving shales containing abundant fragments of graptolites. These are correlated with the Utica. Associated with them, and becoming the dominant type going upstream are the brownish- weathering variegated shales characteristic of the Leclercville. The last exposures along this stretch of the river are limestones, - 19 - weathering both grey and buff. Although they resemble the fine-grained Upper Trenton limestones around Montreal, there is insufficient evidence to remove them from within the Utica formations.

Road Cuts Along Sir Wilfrid Laurier Boulevard. The few, low, gutter exposures to be seen along Route 9 between the southern border of the area and the vicinity of St-Germain show little that is not seen inthe pasture exposures to the northwest. Limestone conglom- erate occurs southwest of St-Germain, and in many places the rocks are severely slickensided. These exposures are limited in length to a few tens of feet, and in no case can more than a few feet of beds be seen in undisturbed stratigraphic succession.

Formations East of the Champlain Fault

In the southeast corner of the area are two formations known elsewhere to belong definitely to the region east of the boun- dary fault which separates the Appalachian mountain-built terrane from the St-Lawrence Lowlands. These are the Sillery sandstone and a lime- stone which might be the Lévis or possibly one of the subdivision of the Philipsburg succession. It is here Provisionally correlated with the Lévis limestone formation.

Lévis Limestone

Three and a half miles due west of Wickham there is a group of small exposures of massive and crystalline limestone showing poorly. developed bedding. Such observations as could be made indicate that the beds form part of a shallow syncline plunging toward the north- east, a structure entirely in accord with the regional pattern. The exposures consist of a combination of dark, crystalline limestone weathering to a medium grey, rough surface, and a pure, light dove- grey to white limestone weathering white. Both types carry a network of calcite veins 1 to 2 mm. wide. The eastern end of one of the ex- posures is a mass of breccia, possibly tectonic in origin although it might be the result of the filling of a cavity or might mark an erosion- al unconformity. All of the fragments in this breccia are of limestone, and none exceeds 2 inches in diameter. No trace of fossils was seen. This rock might well become the source of a local agricultural lime industry. - 20 -

Sillery Sandstone

Northeast and southeast of Wickham, just to the west of the highway and immediately beyond the limit of the Upton area, there are exposures of a coarse, "dirty" quartz grit and a medium-grained sandstone. Within the Upton area the same rock occurs 2 miles west and also 3 1/2 miles north of Wickham. These are parts of the Sillery formation, which outcrops from the vicinity of Quebec City southward to Granby. Northeastward, within the Aston area, this rock is well exposed at Notre-Dame-du-Bon-Conseil where it is being quarried main- ly for road material. Neither cleavage nor stratification was seen in any outcrop of the Sillery within the Upton area.

STRUCTURAL GEOLOGY

The structure of the rocks in this area runs the gamut from gently inclined beds at St-David and St-Hugues to the intensely folded, faulted, and deformed beds along St-François and St-Germain rivers. The axis of the Chambly-Fortierville syncline passes close to St-David; thence toward the southeast the rocks become more and more intensely folded. In addition, the southeast corner is cut by the Champlain fault by which rocks belonging to the Appalachian moun- tain-built province are brought into contact with the Ordovician rocks of the lowland.

Chamblv-Fortierville Syncline

The axis of this fold is drawn so as to pass through St- Louis-de-Bonsecours and to the west of Massueville and St-David. It crosses Yamaska river a mile or so south of Massueville. The dip of the red Bécancour River shales and sandstones at St-David makes it necessary to place the axis west of that locality. The course of this axis southwestward is controlled largely by the regional strike. There are no exposures of the Bécancour River save at St-David, but its presence in many water wells around St-Louis-de-Bonsecours and nearby in the neighbouring Verchéres area makes it likely that the regional strike is the correct one. Actually, there are no records of red rock east of Salvail river, so that placing the axis close to St-Louis-de- Bonsecours seems justified. There is nothing to which to tie the south- ern end of the axis, and it is therefore placed so as to be in harmony with its position in the northeast corner of the Beloeil area (Clark, 1955). Plate I

A- St-François river looking downstream (N.W.) at island 1 mile above St-Joachim-de- Courval.

aw ,.,.~ ],.. ~" ` r. M~ sw+. ~ I► , 14111.M•• . a .WNW. - _._ ,'. ~ r~d~~H•`W~ ,r :;!-~~^ .. . _ - _*+.

B- Bed of St-François river, right bank, opposite island 1 mile above St-Joachim-de-Cour- val. St-Germain complex exposed at extreme low water. Looking S.W. Plate II

A- Thin-bedded Utica slate with buff-weathering limestone beds. Part of St-Germain com- plex. Right bank of St-François river 3/ mile below church at St-Joachim-de-Courval. Looking E.

B- Same as A. Detail of limestone bed. C- Same locality as A. Calcareous sla- Note transverse tension cracks. te, either Utica or Trenton, cut by system of closely spaced tension cracks. Plate III

A- Felsenmeer developed on calcareous slates of the St-Germain complex, probably Lor- raine, 3 miles northwest of 5t-Germain-de-Grantham.

B- Detail of above. Plate IV

~~ '. r~—'~~ .R ~ ! ~ ~:.... - + - - ~4,; .4 - Zdar.". i`.. . ~•~. . .+x^ — • ~ • ~. :e " - - .j . :::}

• - .2'1'41644 I. w11e 10 ‘s. ~~ ~ ` ~ ~ ~ ~g_-~ •

. ~ :S:y ~-j ' •Zw. -

~~•

Landslide near St-Louis-de-Bonsecours (1945). 15' scarp in left middle distance; slide material breached by Yamaska river. - 21 -

St-Hugues Structure

Reference to Figure 2 will show the distribution and struc- ture of the beds in the vicinity of St-Hugues. These beds belong to the Breault member of the Nicolet River formation, and contain the characteristic fossil Cryptolithus bellulus throughout. The exposures were first exploited by Foerste (1916, p.52) but the map, prepared by Harvie, is in error both as to scale and compass direction. Two anti- clines and the intervening syncline are indicated by the observations made during the present work. All of the structures plunge to the southwest. Though the angle of plunge could not be measured directly in the field, it must be more than 5° and less than 10°, probably near- er the smaller figure.

Thickness of the Sedimentary Section

No significant information followed from the examination of the rocks of this area concerning the thickness of the Ordovician strata here. Only one deep well has been drilled in this area, the St-Gérard well near the northern border of the map. An abbreviated log (See Appendix A) of this well is taken from DeBlois (1959, p. 25) as follows:

Depth Formation Thickness

O - 50 Overburden 50 50 - 1280 Bécancour River 1230 1280 - 1500 Pontgravé River 220 1500 - 410 Lorraine-Utica 3310 4810 - 5770 Trenton 960 5770 - 5840 Black River 70 5840 - 6070 Beldens 230 6070 - 6160 Beauharnois 90 6160 Bottom of hole

Except for an expected thickening toward the east and thin- ning toward the west, these thicknesses probably represent what would be found throughout the Chambly-Fortierville syncline area. Although the Bécancour River elsewhere reaches 2,000 feet in thickness it is hardly likely to be found much thicker than shown in the St-Gérard well. There is no information concerning the total thickness of the Beauharnois, or if the March and Potsdam formations be present. - 22 -

The St-Barnabé Fault

The continuation northward of this fault, well documented in the rocks of the St-Hyacinthe area (Clark, in press), is corrobor- ated by the presence in water wells of red Bécancour River beds to the west of the plotted position of the fault, e.g. all along the north- northeast road passing through Danoueville. There would be no room between those occurrences and the Lower Lorraine exposures west of St- Hugues for the Middle and Upper Lorraine and the Pontgravé River beds, hence a fault is necessary. There is no evidence for its presence much farther north, and it is shown as failing to reach St-David.

The St-Germain Complex

Although the structure of any small part of the St-Germain complex shows great variety in detail, a community of structural deform- ation pervades the rock unit. In order to bring out some of the details of structure a short account of the structures of the rocks in the fol- lowing areas is given: Chibouet river, St-François river, and St-Ger- main river. Other exposures contribute little to an understanding of the internal economy of the complex.

Chibouet River. Immediately above the bridge where Route 20 crosses Chibouet river, there is an exposure of black graphitic slates described above (p. 18). Bedding and cleavage coincide except in parts of the exposures farthest from the road. Where the cleavage is separate from the bedding it strikes N.35°E. and dips•450E. In several places it can be seen to be parallel to the axes of small folds. The few limestone beds have been pulled out in the folding, brecciated, and partly dissolved (boudinaged). In only one place could the plunge, 25° S.W., be identified.

Farther up Chibouet river, about 2 miles due east of the above described exposures, there are extensive showings of slates on both banks of the river for nearly 2 miles. Toward the lower end of these exposures some of the rocks are brownish with a faint oily odour, both characteristics indicating a Utica age. Farther upstream the rock is largely a thin-cleaving, hard, black shale, with abundant unidenti- fiable graptolite fragments in certain layers, again a Utica indicator. Going upstream, the cleavage and stratification become more and more independent, and folds with axial plane cleavage are common in the last mile. Throughout the 2 miles the dips are steep to the east or vertical, and the strike ranges from N.20°E. to N.60°E., with one exceptional read- ing of N.45°W. All folds plunge to the southwest at about 10°. It - 23 - would be impossible to give an adequate representation of the structure on any convenient scale.

The same general conditions obtain along David river below St-Edmond-de-Grantham. High dips (700 to 90°) predominate, all to the east, although all gradations between verticality and horizontality occur. The strike. is more constant than along Chibouet river, and ranges from N.45°E. to N.60°E.. Pencil cleavage in some shale beds, the result of two intersecting directions of cleavage, is common.

St-Francois River. It is apparent in Figure 3 that the folding is less intense at the downstream end of the river within this area. This is in accord with the findings on the Yamaska area (Clark, in press) where open folds are common. However, within a mile of the northern edge of the map, and going upstream, the structure becomes characterized by steep dips, close folds, drag folds, and faults. These complications, yielding in places to isoclinally folded beds, continue as far as the exposures last. The last (upstream) mile or so appears to be characterized by a simplicity of structure, but this apparent simplicity is probably due to the sketchiness of the exposures in this upper part.

In detail, starting at the zero mile mark at the downstream end of the section, there is nothing on the right bank to correspond to the exposures along the left bank for the first three-quarters of a mile. There follow half a mile of strata dipping to the northwest along both banks. The fault at AB-9500 (Figure 3b) is not seen on the right bank, nor is the anticline just west of the fault recognized on the right bank. From this point upstream only very general similarities can be made out.

In several places approximately the same attitude is borne by the rocks for a distance of half a mile or so. It might appear that in such places one would have a chance to measure an unbroken section of the strata. However, close scrutiny of crossbedding and drag folds shows that parts of such sections are overturned. The rapid alternation of overturned and normally inclined beds indicates that what appears to be a simple stratigraphic succession is, in reality, a series of iso- clinal folds.

Because it is rarely possible to project a fault across the river from one bank to the other, it is concluded that the faults are of local importance only. The compression responsible for the folding - 24 - resulted in a multitude of minor intraformational faults rather than in faults of regional importance. In fact, the same may be said of the folding and of most of the contorted zones. This is not only apparent after a study of the sections shown on Figure 3, but it is also obvious to a remarkable degree in the field. One can stand on the axis of a fold on one bank, and look along the projection of the axis to the other bank, and search in vain for any expression of such a fold. Because these structures, both faults and folds, do not carry across 1,500 feet of river-covered terrane, it is impossible to consider them to be of regional significance.

St-Germain River. In the black slates and slaty limestones exposed along this river, bedding and cleavage may or may not coincide. The cleavage for the most part strikes N.60°E. and dips 500 to 60°E.,the dip rising in places as high as 75°E. The strike of the bedding ranges between N.20°E. to N.40°E., with no uniformity in dip. No faults are visible, probably because the cuts are for the most part only a foot or two high. Most of the rock, however, has been strongly slickensided.

Elsewhere, only a general idea of the structure can be de- duced. From the pasture exposures west of St-Germain and from the ex- posures along Route 9 it can be seen that the rocks are closely folded, with cleavage striking N.60°E., steeply inclined to the east. Along Route 9 many of the low gutter exposures show considerable slicken- siding. Few of the pasture outcrops reveal anything of their struc- ture.

The Appalachian Terrane and Champlain Fault

The presence in the southeast corner of the area of rocks belonging to the Sillery and the Lévis formations betrays the exis- tence, between these rocks and those of the St-Germain complex, of a boundary between the St. Lawrence Lowlands to the west and the Appala- chian mountain-built terrane to the east. No direct evidence of the position of this boundary can be seen. It is probably a low angle thrust, and was doubtless responsible for the complications which have beset the incompetent shales of the lowland area, transforming some of them into what is here called the St-Germain complex. The Sillery and Lévis rocks are, on the other hand, not particularly disturbed. The Lévis limestone is exposed in a shallow syncline with no dips of more than 20°. Within the Upton area the Sillery does not show any struc- ture, but elsewhere it is characterized by open folds, as one would expect in the case of a competent bed. - 25 -

ECONOMIC POSSIBILITIES

Oil and Gas

The one deep well drilled expressly for the purpose of obtaining gas or oil proved to be a dry hole (See Appendix A). There is a well at the Péloquin garage in St-Guillaume d'Upton which, in 1944, yielded enough natural gas to heat one building and to cook with. Al- though piped to a tank, the proprietor made no use of it. In the south- west corner of the area, 4 miles southwest of St-Hugues, gas occurs in the well of Joseph Leblanc, and his neighbour, Adrien Fontaine, has noticed bubbles of gas in his well. Remarkably enough these three oc- currences line up with the strike of the St-Hugues anticlinal structure, and provide an incentive for the exploration of that structure as a possible gas trap.

Limestone

An exposure of limestone, which might be used as a source of agricultural lime, has already been described (Lévis limestone,p.19) • from Wickham.

Miscellaneous

Some of the limestone in the St-Germain complex west of St- Germain might be suitable for road material or concrete aggregate. Probably none of the other rock types would be suitable for either pur- pose on account of their slatiness. Nowhere are the slates of the St- Germain suitable for the production of roofing slate.

At St-Bonaventure, the Quebec Peat Moss Company carries on a good business in the production of peat.

There are several gravel pits, which provide gravel barely sufficient for local use. - 26 -

APPENDIX A

REGISTER OF DEEP WELLS

Extracted from DeBlois (1959), page 25.

Company: Canadian Seaboard Oil and Gas Well Name: Canadian Seaboard St-Gérard No. 1 Well Location: Lot: 593 Concession: St-Antoine Parish: St-Gérard County: Yamaska Seigniory: Yamaska Coords: 198' from west lot line, 522' from south lot line Ground Elevation: 1031 Rig Floor Elevation: 105' Spudded: Nov. 19, 1931 Completed: Jan. 25, 1933 Type of Rig: Cable and Rotary Result: Dry hole Log by Belyea:

Formation Depth interval (in feet)

Overburden 0 - 50 Richmond (Bécancour River) 50 - 1280 Richmond (Pontgravé River) 1280 - 1500 Lorraine-Utica 1500 - 4810 Trenton (Upper) 4810 - 5390 Trenton (Montreal) 5390 - 5770 Black River (Leray-Lowville) 5770 - 5830 Black River (Pamelia) 5830 - 5840 Chazy (Beldens) 5840 - 6070 Beekmantown 6070 - 6160

Quoted from Report of the Minister of Mines of the Province of Quebec for the Fiscal Year 1932-1933. Part A. 1933.

Page 48. "The last deep boring was performed at St-Gérard, in Yamaska county, by the Canadian Seaboard Oil and Gas, Ltd. This well was aban- doned as a dry hole in December, 1932. It was drilled with standard cable tools to a record depth, in this Province, of 6,160 feet. The site for a new well was chosen in the parish of St-Angéle de Laval, Nicolet county, and drilling was in progress in February, 1933." - 27 -

LCG OF CANADIAN SEABOARD OIL AND GAS, LTD., WELL Page 50 Cadastral lot "573", range St-Antoine, St-Gérard parish, Yamaska county

Formation Footage Surface deposits 0 50 Queenston sandstone 50 90 Queenston red shale 90 1,190 Queenston grey shale 1,190 - 1,280 Lower Richmond grey shale and limestone 1,280 - 1,530 Lorraine grey shale with thin limestone bands 1,530 - 2.260 Lorraine medium grey sandy shale 2,260 - 2,670 Lorraine dark grey shale 2,870 - 4,400 Utica dark grey and brown shale (1) 4,400 - 4,840 Lower Utica dark grey shale with limestone bands 4,840 5,330 Lower Utica and Upper Trenton 5,330 - 5,540 Trenton and Black River limestone 5,540 5,980 Basal sandstone Trenton group 5,980 - 6,000 Chazy limestone 6,000 6,030 Chazy (2) shale and sandstone 6,030 - (bottom of well) (1) Contact between Lorraine and Utica is not sharply defined

Extracted from Belyea (1952), pages 54-60

CANADIAN SEABOARD ST-GERARD NO. 1 WELL

Location: lot 593, concession St-Antoine, Parish of St-Gérard, Yamaska county, Quebec Elevation: 90 feet Depth: 6,160 feet Rig: standard cable to 3,170 feet; rotary, 3,170 to 4,490 feet; and cable, 4,490 to 6,160 feet Drilling started: November 18, 1931; completed: December 24, 1942 Samples examined by H.R. Belyea, 1946; revised in part, 1950

Depth (Feet) Lithology 0-40 Clay 40-50 Grey-brown sand Richmond Bécancour River Formation 50-60 Sandstone, reddish brown, coarse-grained 60-90 Sandstone, reddish brown, fine-grained, and about 10 per cent fine-grained, greenish grey sandstone 90-120 Shale, reddish brown, micaceous, and about 10 per cent red and grey. sandstone 120-130 Sandstone, greenish grey, fine-grained; some greenish grey shale 130-140 Sandstone, reddish brown; about 10 per cent greenish grey sandstone; trace of red shale 140-150 Sandstone, greenish grey 150-160 Sandstone, fine- to medium-grained, red and greenish grey 160-170 Sandstone, light greenish grey, fine-grained; traces of greenish grey shale 170-180 Shale, dark grey, sandy; about 10 per cent.light greenish grey sandstone 180-240 Shale and sandstone: dark grey and light grey sandstone and grey shale, all micaceous 240-250 Shale, dark grey, sandy 250-260 Sandstone, dark grey; grey shale 260-300 Sandstone, mostly light grey; minor light grey sandstone and grey shale studded with pyrite 300-330 Shale, brownish red; a little gypsum in nearly every sample; minor greenish grey sandy shale and sandstone at 310 to 320 feet 330-370 Shale, brownish red, as above; 30 to 40 per cent sandstone, greenish grey, grading to sandy shale; traces of gypsum 370-750 Shale, brownish red, as above; greenish grey, sandy shale and sandstone in small amounts at 380 to 390, 440 to 450, and 470 to 480 feet; spots of white to pink gypsum - 28 -

Depth (Feet) Lithology

Bécancour River Formation (cont.)

750-770 Shale,.greyish green, silty, and sandy; trace gypsum 770-790 Shale, grey, silty, slightly calcareous; trace gypsum 790-810 Shale, reddish brown, with about 30 to 40 per cent green, sandy shale, and light grey, calcareous, fine-grained sandstone; trace gypsum 810-980 Shale, reddish brown, with spots of gypsum 980-1,020 Shale, reddish brown, with gypsum, as above; greenish grey, silty, calcareous shale forming nearly 50 per cent of samples 1,020-1,190 Shale, reddish brown, spotted with gypsum 1,190-1,280 Shale, green mudstone; about 20 to 30 per cent red shale, spotted with gypsum

Pontgravé River Formation

1,280-1,290 Shale, greenish grey, slightly calcareous, more fissile than above, pyritic in part; calcareous siltstone, grey with calcite and quartz in varying proportions, grading to silty, fine limestone 1,290-1,300 Shale, as above; grey, finely crystalline, very silty limestone; grey, micaceous, argillaceous siltstone; brachiopod fragments 1,300-1,320 Silty limestone, blue-grey, finely crystalline; siltstone and shale as above 1,320-1,330 Shale, grey, calcareous, as above; less limestone and siltstone than above; bryozoa; pyrite 1,330-1,340 Shale, as above; siltstone and blue-grey limestone, as above; a few ostracods 1,340-1,380 Siltstone, limestone, and shale, as above; shale less abundant 1,380-1,390 Shale, as above; a few fragments grey limestone, with ostracods 1,390-1,400 Siltstone grading to limestone, as above; grey shale, as above 1,400-1,410 Shale, siltstone, and limestone, as above; brachiopod fragments 1,410-1,450 Shale, as above; siltstone grading to limestone; scattered fossil remnants 1,450-1,470 Limestone, grey, finely to medium crystalline, silty; grades to calcareous siltstone; shale, as above; brachiopods and ostracods 1,470-1,500 Limestone, grey, finely to medium crystalline; grey, shaly, micaceous siltstone; grey shale; brachiopods, 1,490 to 1,500 feet

Lorraine and Utica

1,500-1,510 Shale, grey to greenish grey, in part silty; grades to green, micaceous, argilla- ceous siltstone; some grey, fine, silty limestone; fossil fragments; calcite veins 1,510-1,530 Shale, greenish grey, very slightly calcareous; siltstone, greenish grey, micaceous, calcareous, argillaceous 1,530-1,670 Shale and siltstone; light grey, soft, flaky shale, breaks into rounded fragments, in part micaceous; lighter grey, slightly'calcareous, laminated siltstone, with black carbonaceous specks, grades to sandy shale, in part fossiliferous, with fragments of bryozoa, brachiopods, crinoid disks, and secondary calcite forming in places a sandy shell limestone 1,670-1,680 Shale and siltstone, as above; 10 per cent with brown stain 1,680-1,780 Shale and siltstone, as above; fossil fragments; a little medium grey, micaceous, fissile shale 1,780-1,790 Shale and siltstone, as above, but 50 per cent with a brownish stain; bryozoa; greenish metabentonite; slickensides 1,790-1,830 Shale, as above; about 30 per cent siltstone; brachiopods, bryozoa, and crinoid fragments in all samples 1,830-1,870 Shale and siltstone, as above 1,870-1,890 Shale and siltstone, about 10 per cent with brown stain 1,890-1,920 Shale, light grey and medium grey, as above; about 30 to 40 per cent siltstone, as above; fossil fragments, especially bryozoa, in all samples, forming in part a sandy shell limestone 1,920-1,930 Shale and siltstone, as above; 10 per cent with brown stain - 29 -

Depth (Feet) Lithology

Lorraine and Utica (cont.)

1,930-2,050 Shale, light grey, soft, flaky; medium grey, micaceous, fissile, well- laminated shale becoming more prominent with depth; about 30 per cent slightly • calcareous siltstone and silty shale; crinoid stems, brachiopods, and bryozoa in all samples 2,050-2,280 Shale and siltstone, as above; a little more medium grey, fissile shale than above; brachiopods and bryozoa in all samples 2,280-2,300 Shale, light grey; a little medium grey, fissile shale; a little light grey, calcareous siltstone; fossil fragments 2,300-2,420 Shale and siltstone: light grey, flaky shales gradually superseded by medium grey, fissile and silty shales; 30 to 40 per cent calcareous silt§tone, commonly with secondary calcite forming sandy, shell limestone; brachiopods 2,350 to 2,380 and 2,400 to 2,410 feet 2,420-2,650 Shale, medium grey, irregular partings, micro-silty, micaceous, brittle; 10 to 20 per cent siltstone, light grey, calcareous, with black carbonaceous specks, fre- quently interlaminated with medium grey shale; cross-lamination at 2,420 to 2,430 and 2,790 to 2,800 feet; pyrite 2,440 to 2,450 feet; metabentonite 2,480 to 2,490, 2,590 to 2,600, 2,720 to 2,730 and 2,840 to 2,650 feet 2,850-2,670 Shale and siltstone, as above; about 5 per cent with brown stain 2,870-2,920 Shale and siltstone, as above; about equal in amount 2,920-3,100 Shale, chiefly medium grey to dark grey, micro-silty, brittle, with rough fracture; some medium grey, fissile shale; up to 30 per cent light grey, calcareous, laminated siltstone, commonly interlaminated with shale; cross-lamination of silt and shale at 3,020 to 3,040 feet; metabentonite 2,920 to 2,930 feet 3,100-3,110 Shale and siltstone, as above; about 5 per cent with brown stain 3,110-3,180 Shale, same as above; a little siltstone 3,180-3,450 Siltstone and shale: light grey, variably calcareous, laminated siltstone, with black carbonaceous specks; shale partings; nearly an equal amount of shale, medium to medium dark grey, micro-silty, micaceous, fissile; about 10 per cent of shale, grey to slightly greenish grey, very fine, firm, smoothly fissile; interlaminae of shale and silt common; crinoid disk 3,180 to 3,190 feet 3,450-3,800 Shale, in part light medium grey, finely micaceous, fissile, with pyrite nodules, and in part micro-silty, medium to dark grey shale; 10 to 20 per cent siltstone, light grey, calcareous, interlaminated with shale; metabentonite 3,570 and 3,580 and 3,730 to 3,740 feet 3,800-3,840 Shale, as above; very little calcareous siltstone; metabentonite 3,810 to 3,820 feet 3,840-3,860.- Shale, light medium grey, fine, fissile, commonly with pyrite nodules; medium dark grey, fissile shale; medium grey, silty, rough shale; dolomite, light grey, silty, argillaceous, grading to dolomitic siltstone. 3,860-3,880 Shale, light medium grey to dark grey, as above 3,880-3,890 Shale, light medium grey to dark grey, as above; silty, argillaceous dolomite and dolomitic siltstone, as above 3,890-4,010 Shale, light medium grey to dark grey, as above; calcite veins 3,900 to 3,910 feet 4,010-4,020 Shale, as above; a little silty dolomite, as above 4,020-4,060 Shale, light medium grey to dark grey, as above; metabentonite 4,020 to 4,030 feet 4,060-4,070 Shale, as above; some brownish grey, silty dolomite; calcite veins 4,070-4,110 Shale, light medium grey to dark grey, as above 4,110-4,120 Shale, as above; brownish grey, silty dolomite 4,120-4,260 Shale, as above; pale green metabentonite 4,140 to 4,150 feet 4,260-4,320 Shale, chiefly medium grey and dark grey, fine fissile; a little dark grey, silty shale, and black shale with a brownish streak; a little siltstone 4,320-4,330 Shale, same as above; brownish grey, argillaceous, silty dolomite 4,330-4,360 Shale, as above 4,360-4,370 Shale, as above; dolomite, brownish grey, argillaceous, silty 4,370-4,450 Shale, as above; metabentonite 4,380 to 4,390 feet 4,450-4,460 Shale, as above; dolomite, greyish brown, dense, silty - 30 -

Depth (Feet) Lithology

Lorraine and Utica (cont.)

4,460-4,480 Shale, as above; pale grey metabentonite 4,470 to 4,480 feet 4,480-4,530 Shale, blackish grey to black, fissile, smooth, with light brownish streak; pyrite streaks and specks 4,530-4,550 Shale, black, as above; dolomite, dark brown, finely crystalline, finely silty; pyrite; calcite veins 4,516-4,570 Shale, as above 4,570-4,580 Shale, as above; dolomite, brown, silty, grades to dolomitic siltstone; pyritic 4,580-4,590 Shale, dark grey, in part with a dark brown streak 4,590-4,620 Shale, black, with a dark brown streak 4,620-4,630 Shale, as above; greenish buff metabentonite with small nodules 4,630-4,680 Shale, black, with a brown streak, as above, slightly calcareous; pyrite; calcite 4,670 to 4,680 feet; trace dark grey siltstone 4,680-4,750 Shale, black, with brown streak, slightly calcareous, becoming more calcareous with depth 4,750-4,770 Shale, as above; calcite; pyrite 4,770-4,810 Shale, very dark grey, more fissile than above, harder, micro-silty, calcareous, grey streak

Trenton

Terrebonne and Tetreauville Equivalents?

4,310-4,860 Shale and limestone; dark grey, calcareous, silty_shale; limestone, dark grey, argillaceous,silty, very finely crystalline, up to 5 per of samples 4,860-4,910 Shale and limestone: dark grey, calcareous shale; a little dark grey, argillaceous, silty, very finely crystalline limestone; metabentonite and vein calcite 4,860 to 4,870 feet; pyrite 4,870 to 4,890 feet 4,910-4,930 Shale, dark grey, calcareous, silty; pyrite; a little limestone, as above 4,930-5,030 Shale and limestone: shale, as above; about 40 per cent limestone, brownish grey, argillaceous, very finely crystalline, silty; vein calcite 4,980 to 5,000 feet; trace pyrite in all samples; metabentonite, brownish, 4,980 to 4,990 feet; slickensides 4,990 to 5,000 feet 5,030-5,040 Dark igneous rock 5,040-5,060 Shale,as above; a little brown-grey, shaly, fine limestone; thick metabentonite 5,040 to 5,050 feet 5,060-5,070 Shale and limestone: shale, same as above; pyrite; limestone, dark blue-grey, argillaceous, silty, very finely crystalline 5,070-5,080 Shale and limestone: shale, as above; much dark brownish grey, finely crystalline limestone; fossil fragments 5,080-5,090 Shale, as above; a little limestone 5,090-5,130 Shale and limestone: shale, as above; 10 to 20 per cent brown-grey, argillaceous limestone 5,130-5,210 Shale, as above; a little limestone, as above; pelecypod and ostracod 5,170 to 5,180 feet 5,210-5,230 Shale and limestone: shale, as above, with fossil fragments; 30 to 40 per cent limestone, grey, dense, finely crystalline 5,230-5,280 Shale, as above; less limestone than above 5,280-5,330 Limestone, grey, finely crystalline to brownish grey, argillaceous, in part silty; 40 per cent silty, dark grey shale 5,330-5,360 Limestone, grey, finely crystalline; some darker grey, very fine, argillaceous limestone as above; dark grey shale; fossil fragments 5,360-5,390 Limestone, grey, cryptocrystalline, dense, slightly silty; dark grey shale - 31 -

Depth (Feet) Lithology

Trenton (cont.) Montreal Equivalent ?

5,390-5,410 Limestone, grey, very finely crystalline, in part with crinoid fragments; dark grey shale; brachiopod and bryozoa fragments 5,410-5,420 Limestone, grey, cryptocrystalline; some fragments crystalline limestone; dark grey shale 5,420-5,430 Limestone, grey,cryptocrystalline, as above; some lighter grey, coarsely crystalline limestone; dark grey shale, with crinoid disks 5,430-5,450 Limestone, dark grey, cryptocrystalline 5,450-5,460 Limestone, grey, finely crystalline, with more crystalline limestone than above; in part, possibly recrystallized fossil fragments; crinoids, brachiopods 5,460-5,470 Limestone, buff, finely crystalline; some darker, cryptocrystalline limestone; dark grey shale 5,470-5,500 Limestone, buff-grey, finely to medium crystalline, may be recrystallized fossiliferous limestone in part; dark grey, calcareous, silty shale partings 5,500-5,540 Limestone, grey, finely crystalline; buff, medium crystalline, in part recrystallized, fossiliferous limestone 5,540-5,560 Limestone, grey, finely to medium crystalline, as above; some light buff, coarsely crystalline limestone 5,560-5,580 Limestone, light buff, coarsely crystalline, fossiliferous, with brachiopods and bryozoa fragments (probably recrystallized foss limestone) 5,580-5,600 Limestone, dark brownish grey to light greyish bror,, dense to coarsely crystalline, pyritic in part, fossiliferous; brachiopod and bryozca fragments; dark grey shale partings 5,600-5,630 Limestone, greyish brown to brown, dense to coarsely crystalline, cherty, pyritic, in part slightly dolomitic, fossiliferous; chert, clear, smoky, and dark brownish grey to black; brachiopod fragments 5,630-5,640 Limestone, buff-grey and cream, medium to coarsely crystalline, fossiliferous; poorly preserved crinoid and brachiopod fragments; a little grey, dense limestone; trace pyrite 5,640-5,660 Limestone, creamy grey, coarsely crystalline; a little buff-grey to grey, dense to finely crystalline limestone; stylolites in cream limestone; pyrite; brachiopod fragments 5,660-5,680 Limestone, dark brownish grey, finely crystalline, slightly dolomitic, slightly argil- laceous; light grey, coarsely crystalline limestone, with smoky chert; fossil fragments, chiefly brachiopods 5,680-5,690 Limestone, light grey, coarsely crystalline, in part recrystallized fossils; recrystal- lized bryozoa or coral-like fossils; numerous brachiopod fragments; clear chert 5,690-5,720 Limestone, light grey, coarsely crystalline and darker grey, finely crystalline, slight- ly argillaceous, fossiliferous; brachiopods common; dark grey shale partings 5,720-5,730 Limestone, dark brownish grey, dolomitic, dense, cryptocrystalline, argillaceous, pyritic in part; in part finely to medium crystalline, as above. 5,730-5,740 Limestone, dark brownish grey, finely crystalline to smoothly textured, sublithographic, argillaceous, and in part micro-silty; pyritic 5,740-5,750 Limestone, cryptocrystalline to finely crystalline; in part argillaceous; brownish grey metabentonite 5,750-5,760 Limestone, brownish grey, sublithographic, argillaceous, micro-silty, slightly dolomitic; some brownish grey, crystalline, fossiliferous limestone, with secondary calcite; pyrite; chert, milky to smoky; a little dark grey shale 5,760-5,770 Limestone, dark brownish grey, slightly dolomitic, sandy; brownish grey, sublithographic limestone, as above; light grey, sandy limestone and calcareous sandstone; a little dark grey, calcareous, sandy shale

Black River

Leray and Lowville Formations

5,770-5,780 Limestone, dark brownish grey, cryptocrystalline, sublithographic, slightly dolomitic in part, argillaceous, sandy in part 5,780-5,790 Limestone, greyish brown, crytocrystalline, sublithographic, with white calcite; a little dark grey limestone, dolomitic, micro-silty -32-

Depth(Feet Lithology

Black Rive

Leray and Lowville Formations (cont.) 5,790-5,810 Limestone, dark brownish grey, cryptocrystalline, sublithographic, with white calcite; a little light grey, dolomitic, micro-silty limestone 5,610-5,820 Limestone, greyish brown,"cryptocrystalline, sublithographic, with white calcite as stringers and aggregates; a little grey limestone, dolomitic, silty, and sandy 5,620-5,830 Limestone, medium grey, cryptocrystalline, sublithographic, slightly micro-silty; a little dolomite, limy, medium grey, microcrystalline, silty to sandy 5,830-5,840 Dolomite, medium grey, finely crystalline, argillaceous, silty; grades to grey, dolomitic, calcareous siltstone; a little medium grey, sublithographic limestone

,Beldens. Formation ?

5,840-5,850 Limestone and dolomite: dolomitic, brownish grey, cryptocrystalline to finely crystalline limestone; medium grey, crystalline, micro-silty dolomite; a little cream limestone 5,850-5,860 Limestone and dolomite: brownish grey, slightly dolomitic, argillaceous, cryptocrystalline, limestone and medium brown, crystalline, micro-silty dolomite; a little dark grey shale 5,860-5',870 Limestone and dolomite: greyish brown, dense, sublithographic limestone; dark brownish grey to light grey, finely crystalline argillaceous, micro-silty dolomite; a few large, rounded sand grains; some dark grey shale; calcite veins in limestone 5,870-5,880 Limestone and dolomite, as above; a few sand grains; a little greenish grey, calcareous, micro-pyritic shale 5,880-5,890 Dolomite, light grey, crystalline to coarsely crystalline, finely silty to sandy, with large rounded, frosted sand grains; limestone, greyish brown, argillaceous; a little dark grey shale 5,890-5,900 . Dolomite, brownish grey, sugary, pyritic in part, sandy, with large quartz grains; some calcite may be from fossil fragments; shaly partings; a little greyish brown, argillaceous limestone 5,900-5,910 Dolomite, light grey, sandy, with large quartz grains; dark grey, shaly partings; pyrite 5,910-5,920 Dolomite, same as above; fossil fragments; a little dolomitic, light grey, fine- grained sandstone; dark grey, sandy shale 5,920-5,930 Limestone, brownish grey, cryptocrystalline, and grey, argillaceous, dolomitic, pyritic; a little dolomite, grey, finely crystalline, sandy; dark grey, dolomitic shale 5,930-5,940 Dolomite, creamy grey, crystalline, sandy, pyritic; greenish grey, argillaceous, pyritic limestone, and dark grey, fossiliferous, argillaceous limestone; dark grey, dolomitic shale 5,940-5,950 Limestone, dark grey, argillaceous, finely crystalline; brownish grey, dense, slightly dolomitic limestone; dark grey, dolomitic, pyritic shale; a few fossil fragments 5,950-5,970 Dolomite, grey, finely sugary, argillaceous, sandy, pyritic; a few large quartz grains; a little dark grey shale 5,970-5,980 Dolomite, sandy, as above; dolomitic sandstone; much interbedded dark grey shale 5,980-5,990 Sandstone, light grey, coarse-grained; chiefly rounded, frosted, and pitted quartz, well cemented with lime - - 5,990-6,000 Sandstone, as above; much light grey, fine-grained, dolomitic sandstone 6,000-6,010 Limestone, dark brownish grey, finely crystalline to cryptocrystalline, slightly dolomitic and argillaceous; a little secondary calcite; quartz grains (savings?). 6,010-6,020 Limestone, dark brownish grey, dolomitic, sandy, cryptocrystalline to finely sugary, large quartz grains (cavings?) 6,020-6,030 Dolomite, dark grey, silty, sandy, with large quartz grains, finely sugary; a little limestone, brownish grey, cryptocrystalline, as above - 33 -

Depth (Feet) Lithology

Chary (cont.)

'Beldens' Formation ? (cont.)

6,030-6,040 Sandstone, light grey, coarse, well cemented, composed chiefly of large, rounded, frosted quartz grains; dolomitic cement 6,040-6,050 Dolomite, dark grey, finely crystalline, argillaceous, sandy, grading to dolomitic, fine-grained sandstone; a little white sandstone, fine-grained, with black fragments 6,050-6,060 Shale, dark grey fissile, and light grey, with black flecks, limy nodules, and laminae, sandy, pyritic 6,060-6,070 Dolomite, dark grey, finely sugary, pyritic, silty to sandy, with large quartz grains; some white sandstone, with dark streaks; greenish grey, pyritic shale; a few fossil fragments

Deekmantown

6,070-6,090 Dolomite light grey, argillaceous, finely sugary, silty; and dark grey, argillaceous, cryptocrystalline dolomite; dark grey, calcareous shale 6,090-6,110 Dolomite, shaly, medium grey, finely crystalline, silty; much greenish grey, dolomitic, pyritic shale 6.110-6,130 Shale, grey to slightly greenish grey, dolomitic; dolomite, grey, finely crystalline, shaly, silty, pyritic;. a few sand grains 6,130-6,140 Missing 6,140-6,150 Dolomite, light grey, shaly to finely crystalline, silty; considerable greenish grey to grey, dolomitic shale 6,150-6,160 Dolomite, dark grey, finely crystalline, silty, argillaceous; dark grey, dolomitic, silty shale

Mote. The Pontgravé River shales in this well have been separated from the Lorraine on the basis of their content of finely crystalline limestone. The contact may not correspond exactly with the actual contact as determined by faunal differences, but is probably very close to it.

As in other wells, the Lorraine-Utica contact cannot be determined. The black shales with the dark brown streak, typical of the Utica, appear to grade upwards to grey shales and to be interbedded with the lower part or the Lorraine.

The top of the Trenton has been selected arbitrarily at the highest occurrence of finely crystalline limestone, although there is little limestone in the upper 120 feet of the limestone-shale section in this well beneath the black shales of the Utica. This upper section, consisting of dark, calcareous shales and dark, argillaceous, silty limestone, from 4,810 to 5,390 feet, is believed to be a more shaly facies of the upper part of the Trenton, possibly corresponding with the Terrebonne and Tetreauville of the Montreal area and possibly including beds above or below these formations. It may be equivalent to part of the Utica. The lower crystalline part of the Trenton in this well appears to be thinner than in the St-Hubert or the St-Grégoire wells. The lower beds, from 5,720 to 5,770 feet, are dense to finely crystalline, and the crystalline, fossiliferous beds found just above the Black River in the other wells are missing. The base of the Trenton in this well, unlike the other wells examined, includes a fine-grained calcareous sandstone.

The Chazy in this well consists of finely crystalline dolomitic limestones, dolomites, and sandstones, and is not similar in lithology to the Laval formation of the Montreal area. It may be equivalent to the 'Beldens' formation, which it resembles, or may represent a change in facies of the Laval formation. It is possible that these beds between the Black River and the known Beekmantown do not correspond with either the Laval or the 'Beldens'. Moreover, there is no positive evidence that they are Chazyin age. - 34 -

APPENDIX B

INFORMATION CONCERNING QUARRIES

Name of Quarry : Rosaire Roy quarry Location : 3 miles northwest of (downstream from) St-Joachim-de-Courval ONner : M. du Coteau, St-Joachim Operator : M. Rosaire Roy, Baie du Febvre, Yamaska county Type of Rock : Dark grey to black silty slate, with minor amounts of thin beds of sandstone and limestone Approximate : 200 feet by 100 feet. Working face up to 12 feet Dimensions high Remarks : A few miles of the adjacent river road have been surfaced with stone from this quarry, with apparently satisfactory results. The quarry extends to the edge of a 75-foot precipice overhanging the right bank of St-François river. Name of Quarry : Enterprises Piexreville quarry Location : On Route 22; 2 1/2 miles northwest of St-Germain-de- Grantham, and 1'2 mile northeast of the road Operator : Enterprises Pierreville, St-François du Lac, Yamaska county Type of Rock : Argillaceous limestone and calcareous slate. All considerably cleaved Approximate : Several tens of acres cleared at present Dimensions Remarks : Land is at present (May, 1961) being cleared for quarrying operations. A few small excavations have been made, probably for testing purposes. Name of Quarry Quebec Peat Moss Company Location St-Bonaventure, .Yamaska county ONner Fafard et Frères Operator Fafard et Frères Type of Rock Peat Approximate Dimensions 1,500 arpents Number of Men Employed : 30 to 40 Equipment : No special equipment. Peat is cut by hand slicer, piled for drying by hand, transported to warehouse by truck. Production : 1,500 tons per year Remarks : Products sent as far as New York and Boston. Used mostly as agricultural aids. 35 -

BIBLIOGRAPHY

Belyea, H.R. (1952) - Deep wells and subsurface stratigraphy of part of the St.Lawrence Lowlands, Quebec; Geol. Surv. Canada, Bulletin 22. Clark, T.H. (1934)- Structure and Stratigraphy of Southern Quebec; Geol. Soc. Am. Bull. 45, 1, pp. 1-20. Clark, T.H. (1947)- Summary report on the St. Lawrence Lowlands south of the St. Lawrence river; Que.Dept. Mines,P.R.No.204.• Clark, T.N. (1947)- Two recent landslides in Quebec; Trans. Roy. Soc. Canada, 3rd. series, sect. iv, vol. 41. pp. 9-18. Clark, T.H. '(1951)- New light on Logan's Line; Roy. Soc. Canada Trans., 3rd series, vol. 45, sect. 4, pp. 11-12 Clark, T.H. (1955)- St.Jean-Beloeil area; Que. Dept. Mines,Geol.Rept.66. DeBlois, R. (1959)- Data on wells drilled for gas and petroleum in the St. Lawrence Lowlands area; Que. Dept.Mines, S. 49. Ells, R.W. (1896)- Report on a portion of the Province of Quebec com- prised in the south-west sheet of the Eastern Town- ship map (Montreal sheet); Geol. Surv. Canada, Ann. Rept. 1894, part J. Foerste, A.F. (1916)- Upper Ordovician formations of Ontario and Quebec; Geol. Surv. Canada, Mem. 83. Foerste, A.F. (1924)- Upper Ordovician faunas of Ontario and Quebec; Geol. Surv. Canada, Mem. 138. Logan, W.E. (1863)- Report on the Geology of Canada; Geol. Surv. Canada, Rept. of Progr. to 1863. Parks, W.A. (1931)- Natural gas in the St. Lawrence valley, Quebec; Que. Bur. Mines, Ann. Rept. 1930, part D. Quebec Bureau of Mines (1933)- Ann. Rept. for the calendar year 1932, part A.

Snider, L.C. and Farish, L.M. (1935)- Natural gas in Quebec and the Maritime Provinces; in Geology of Natural Gas, Amer. Ass. Petrol. Geologists.

Weston, T.C. (1899)- Reminiscences among the rocks in connection with the Geological Survey of Canada; Toronto ALPHABETICAL INDEX

Page Page Appalachian terrane 24 Formations east of Appendix A 26 Champlain fault 19 Appendix B 34 Formations exposed in Upton area 3 Bécancour River formation 5,27 Formations west of Beekmantown 33 Champlain fault 5 Beldens formation 32,33 Belyea, H.R.- Gas 25 Ref. to work by 2,27,35 Geology Bibliography 35 General 3 Black River 31,32 Structural 20 Breault member 11 Information concerning Canadian Seaboard Oil and Gas quarries 34 St-Gérard No.1 well 6,26,27 Chambly-Fortierville Leclercville shale 11 syncline 20 Leray and Lowville Champlain fault 24 formations 31,32 Chazy 32,33 Lévis limestone 19 Chibouet river exposures 18,22 Limestone 18,22,25,34 Clark, T.H.- Location of area 1 Ref. to previous work 2,11 Logan, W.E.- 12,15,20,22,23, 35 Ref. to work by 2,35 Log of Canadian Seaboard David river exposures 18 Oil and Gas Ltd. well . 27 DeBlois, R. Log of Canadian Seaboard Ref. to work by 21,26,35 St-Gérard No.1 well 27 Lorraine and Utica 28 Economic possibilities . 25 Ells, R.W.- Method of work 2 Ref. to work by 2,35 Montreal equivalent 31 Enterprises Pierreville quarry 34 Nicolet River formation 6

Férish, L.M.- Oil 25 Ref. to work by 2,35 Fields west and northwest Parks, W.A.- of St-Germain 17 Ref. to work by 2,35 Foerste, A.F.- Pontgravé River formation 6,28 Ref. to work by 2,7,14,21,35 Pontgravé River shales 33 Fossils 7,8,10,11,12 Préfontaine, Jean Field assistant 3

- 37 -

Pape Page

Previous work 2 Sillery sandstone 20 Snider, L.C.- Quebec Peat boss Co. Ref. to work by 2,35 Peat production by 25,34 Stratigraphy 5

Register of deep wells 26 Terrebonne and Tetreauville Richmond 27 equivalents 30 Road cuts along Sir Wilfrid Thickness of sedimentary Laurier boulevard 19 section 21 Rosaire Roy quarry 34 Transportation in area 2 Trenton beds 12,30,31 St-Barnabé fault 22 St-Frangois river exposures 12,23 Utica shale 12 St-Germain complex 10,22 St-Germain river exposûres 16,24 Weston, T.C.- Sandstone 18,20,34 Ref. to work by 17,35 Yamaska river exposures 6