Geology and Hydrocarbon Potential of the Berry Mountain Syncline, Central Gaspe (Matane, Matapedia, Gaspe W

Documents complémentaires / Additional files Licence / License

Ministère des Richesses Naturelles, Quebec SEWCE DE LA DOCUMENTATION TECHNIQUE

Date: No ~?. -,376

GEOLOGY AND HYDROCARBON POTENTIAL OF THE BERRY MOUNTAIN SYNCLINE, CENTRAL GASPE (MATANE, MATAPEDIA, GASPE W. AND BONAVENTURE COUNTIES), QUEBEC

A. HAKIM SIKANDER MAY, 1975 ii

ABSTRACT

The Berry Mountain Syncline consists of a wide oval shaped asymmetric structure, the northern limb of which is gently dipping, and the southern limb steep to upright. The central portion of the Syncline is underlain by the Lower-Middle Devonian Gaspé Sandstone series.

The Gaspé Sandstone, conformably overlying the Lower Devonian Gaspé Limestone series, is divided into: The 2,000 to over 6,000 foot thick, marine, York River formation (Emsian, Lower Devonian) consisting of greenish grey, fine to very fine grained, poorly sorted, grey, feldspathic, and muddy sandstone with intervening shale and siltstone. A 0-5,000 foot thick middle unit, the Lake Branch formation, of deltaic interface facies, consisting of red silty shale, with minor fine grained but relatively high energy sands (late Emsian?, Lower Devonian). And the 8,000-10,000 foot thick, alluvial Battery Point formation (extending into Eifelian, Middle Devonian), consisting mainly of greenish grey, fine to medium grained, highly cross-stratified, (pink) feldspar-rich sandstone, and a red sandstone and shale.

Although detailed correlation of the Gaspé Sandstone horizons across the Syncline is difficult, the 5,000 foot thick Lake Branch interval consisting of shale with minor sand, is absent in the southern limb sections: Also, the York River Formation contains more shale interbeds in the southern sections than to the north. Thus, stratigraphic trap possibilities are envisaged, especially on the gently dipping northern limb. Prospective structural traps consist of normal faults on the northern flank.

Owing to a lack of organic matter, the York River is considered a,shaving poor source-rock potential. Maturation studies, (vitrinite reflectance and organic matter carbonization) suggest that the York River, and the Lake Branch formations are situated at a favourable level of organic metamorphism for oil and gas generation; the western 111 part of the area having a greater possibility for oil than the eastern part; the latter attaining a higher regional metamorphism due to the presence of a great thickness of volcanics, and intrusives. The metamorphic effects along the volcanic and the sedimentary rock contacts are of an extremely local nature.

The field work did not reveal the presence of sandstones with interesting reservoir possibilities. The low porosity development in the Lower Devonian sandstones is attributed to the presence of illite, chlorite, rare kaolinite, altered feldspars, and occasional calcite and silica cement. The effect of surface weathering, and the formation of authigenic illite and chlorite on the potential reservoir sand is not clear.

Judging from the poor source rock, reservoir and trapping possibilities, and a favourable level of organic metamorphism, the hydrocarbon potential of the area, as evaluated from the surface collected samples, is rated as poor to fair. It is the qualified opinion of the author that the rock exposure in the area is too poor to make a categoric judgement on the potential parameters, such as source and reservoir. Furthermore, owing to an absence of wells in the area, a correspondance of the surface data with those of the subsurface is not clear. iv

CONTENTS

Page

1. GENERAL DESCRIPTION 1

1.1 INTRODUCTION AND PURPOSE OF STUDY 1 1.2 ACKNOWLEDGEMENTS 2 1.3 PREVIOUS WORK 2 1.4 METHOD OF STUDY 6 1.5 ACCESS AND EXPOSURE 7 1.6 TOPOGRAPHY AND DRAINAGE 8

2. GEOLOGICAL DESCRIPTION 12

2.1 CAP BON AMI FORMATION 13 2.1.1 DISTRIBUTION 13 2.1.2 DESCRIPTION 14 2.1.3 CONCLUSIONS 16

2.2 GRANDE GREVE FORMATION 16 2.2.1 DISTRIBUTION 17 2.2.2 DESCRIPTION 17 2.2.2.1 North Brandy Brook 18 2.2.2.2 Cascapedia Salmon Branch 18 2.2.2.3 Cascapedia Lake Branch 19 2.2.2.4 West Lake Branch 20 2.2.2.5 Nouvelle River 21 2.2.3 CONCLUSIONS 21

2.3 YORK LAKE FACIES 22 2.3.1 DISTRIBUTION 23 2.3.2 DESCRIPTION 23 2.3.2.1 Brandy Brook 24 2.3.2.2 Cascapedia Salmon Branch 24 2.3.2.3 Go-Ashore Brook 24 2.3.2.4 Cascapedia Lake Branch 25 2.3.2.5 West Lake Branch 25 2.3.2.6 Nouvelle Road South 25

Page

2.3.3 CONCLUSIONS 26

2.4 YORK RIVER 26 2.4.1 DISTRIBUTION 28 2.4.2 DESCRIPTION 28 2.4.2.1 Northern Area 29 2.4.2.1.1 Brandy Brook 29 2.4.2.1.2 Cascapedia Salmon Branch 29 2.4.2.1.3 Cascapedia Lake Branch 31 2.4.2.1.4 West Lake Branch 32 2.4.2.2 Southern Area 34 2.4.2.2.1 Caron Brook 34 2.4.2.2.2 Marcil West Brook 35 2.4.2.2.3 Charles Valley 37 2.4.2.2.4 Nouvelle South 39 2.4.3 CONCLUSIONS 40

2.5 LAKE BRANCH FORMATION 41 2.5.1 DISTRIBUTION 41 2.5.2 DESCRIPTION 42 2.5.2.1 Nouvelle South 42 2.5.3 CONCLUSIONS 44

2.6 BATTERY POINT FORMATION 45 2.6.1 DISTRIBUTION 46 2.6.2 DESCRIPTION 46 2.6.3 CONCLUSIONS 49

3. CORRELATION AND. ENVIRONMENTAL PALEONTOLOGY 51

4. PALEOGEOGRAPHY 54.

4.1 INTRODUCTION 54 4.2 DEPOSITIONAL ENVIRONMENT 55 4.2.1 YORK RIVER FORMATION 56 4.2.2 LAKE BRANCH FORMATION 57 4.2.3 BATTERY POINT FORMATION 57 4.3 CURRENT DIRECTIONS 58 4.4 CONCLUSIONS 60

5. VOLCANIC AND GRANITIC ROCKS 62

5.1 VOLCANIC ROCKS 62 5.2 DEVONIAN GRANITIC ROCKS 65 5.3 DIABASE INTRUSIVE 66

6. STRUCTURE 67 vi

Paae

7. ECONOMIC POSSIBILITIES 71

7.1 HYDROCARBONS 71 7.1.1 SOURCE ROCK POTENTIAL 73 7.1.2 MATURATION POTENTIAL 74 7.1.2.1 Clay Composition and Crystallinity 74 7.1.2.2 Vitrinite Reflectance 76 7.1.2.3 Organic Matter Colouration 79 7.1.3 RESERVOIR POTENTIAL 79 7.1.4 TRAPPING POTENTIAL 82 7.1.5 SUMMARY 83 7.2 MINERALS 84

8. REFERENCES 86

9. APPENDICES 92

9.1 FOSSIL IDENTIFICATION 93 9.2 PALYNOSTRATIGRAPHY 95 9.3 FIELD PHOTOGRAPHS 104 vii

LIST OF ILLUSTRATIONS

ENCLOSURES

1. Compilation geological map.

2. Stratigraphic section, northern limb of the Berry Mountain Syncline.

3. Stratigraphic section, southern limb of the Berry Mountain Syncline.

4. Structural sections A-A' and B-B,.

5. Important geological columns.

FIGURES

1. Previous studies.

2. Correlation of Lower-Middle Devonian formations by previous workers in the Gaspé Peninsula.

3. Transportation and general situation map.

4. Generalized topographic map.

5. Table of formations.,

6a. Northeast-Southwest diagrammatic section illustrating regional correlation.

b. North-South diagrammatic section illustrating regional correlation.

7. Geographic distribution, Cap Bon Ami formation.

8. Geographic distribution, Grande Grève formation.

9. Geographic distribution, York Lake facies.

10. Geographic distribution, York River formation.

11. Geographic distribution, Lake Branch formation.

12. Geographic distribution, Battery Point formation.

13. Compilation of environment models for clastic sedimentation viii

14. Frequency listing of lithological and sedimentary features, Gaspé Sandstone.

15. Isopach map, paleo-current directions, York River formation.

16. Thickness estimates, paleo-current directions, Battery Point formation.

17. Illustrative diagrams envisaging sedimentary environment for the lithological units of the Gaspé Sandstone.

13a. General scheme of hydrocarbon generation.

b. Principal steps of kerogen evolution and hydrocarbon formation.

c. Examples of kerogen evolution paths.

19. Some scales of organic metamorphism after Hood and Castano (1974), and Hood et al (1975).

20. Vitrinite reflectance, index for level of organic metamorphism, York River formation.

21. Table of porosity and permeability analyses.

22. Summary of hydrocarbon potential, Berry Mountain Syncline.

I-1. Fossil locations, Berry Mountain Syncline. GENERAL DESCRIPTION

INTRODUCTION AND PURPOSE OF STUDY

The Berry Mountain Syncline area designates an area of approximately 900 square miles (33 x 27) situated in central Gaspé between lati- tudes 48°26'-48°52' N and longitudes 65°54'-66°38' W, located midway between the St. Lawrence River to the north, and Chaleurs Bay to the south. The central part of the area is situated some 50 miles from the village of Ste-Anne-des-Monts.

Broadly speaking, the area consists of a gently dipping northern limb which exposes the Silurian and lower Devonian rocks, and a steeply dipping southern limb. The axial area is occupied by a thick sandstone sequence of Lower to Middle Devonian age. A major facies change occurs across the syncline axis: A several thousand foot thick sand interval shales out along the northern limb.

The Devonian granitic intrusives are restricted to the northern part (Barren Mountain), and to the north of the area in the Hog's Back Mountain. Volcanic lava flows, both acidic and basic, and pyroclastic rocks are present in the lower Devonian, at various horizons. The contact metamorphic effects of these lava flows, appear to be limited in both horizontal and vertical extent.

Hydrothermal activity, north and east of the area, causes a widespread sulphide mineralisation, along anticlinal structures which usually expose the Gaspé Limestone, especially the Grande Grève formation.

No wells have yet been drilled for hydrocarbons in the area.

The purpose of the study is to: 1. Build several geological columns, in order to establish 2

lithological sub-divisions within the Gaspé Sandstone series, and investigate the possibility of reservoir sand in the sequence. 2. Investigate sedimentological aspects and the depositional environment of each lithological subdivision. 3. Using geochemical techniques define the hydrocarbon potential for the Gaspé Sandstone series in central Gaspé. 4. Improve the over-all geological knowledge of the Berry Mountain Syncline area.

ACKNOWLEDGEMENTS

I am indebted to Michel Leduc for continued assistance in the field. Richard Theroux worked in the field as senior geological assis- tant, and later helped construct the geological sections; his help was invaluable throughout the writing phase. I also acknowledge the close communication that was maintained with the INRS-Pétrole laboratories of the Université de Quebec.

Finally, I am indebted to Dr. J.A. Boucot, who identified the brachiopods collected in the field.

PREVIOUS WORK

Important previous studies in central Gaspé are shown in figure 1.

The first geological description of the area was included in the Geology of Canada (Logan, 1863). Logan described the sequence south of the Quebec Group outcrop area as consisting of sandstone followed upwards into low dipping fossiliferous limestone, which he tentatively, correlated with the "Anticosti Group".

The limestones, according to Logan, are overlain by grey, fine- grained sandstones, and red sandstones containing mud-cracks and ripple-

4rsoN LEGEF;OE-LEGEND

GEYONIEN-GEVONIAN A / ~/ J Grcoite et feisite Granite and felsite Yattinson, 1964 , Alcock, 19Z6 6 /i ~ . j n"3 ~:~~.~' kicGerrlgle, 1954 -11 1 ~..e.~~•$ :~, _/ ~~~ d. ~ /b// s Pcdesite Andesite 4 ~ /. 7 1= Î Battery Point Battery Point / \ - i + 1J ~~ J/ Facies de 'Squire Forks' Square Forks facies ~~~~ i 1 1 ~qt,,,,,/ Bcttery Point typique Typical Battery Point ~. ,~ ;-~ ~ ' ~~~ i t t k, g. jr.Ch Lake Branch /1./4 6~\ 4/\^~

Y'ori. R.iY2r York Pi ver ,t~?ti I t(o1c&,,ioues, rLyolite, Volcanics, rhyolite, X2 basalte, ardesite E_: basalt, ande,itc >tI r-7-1 Groupe de f% York ',eke York Lake Fortin / f~ I'1 -' ~ /~i <1_,:.. //- Sranda_9 '0ri!!ve ; •, __J Grande Greve ~/(/~ ✓ i .,, ~I Cal Bor Am; r•77-`i Cn^ Bon :01",:01", ~/` 7 `.t, l_ J ~r ~. %~ï Y SIL'JRIEN DEVCNIEN-SILURIAN DEVONIAN Carbonneau, 1559 8 ~ .a s0' St. Leon (2a, .,,;r de Caldwin (2a; ü%.'dvin mbr. , +7 CAM3nD-ORuDVICIO ,-C.1M;C-ORCN IC!Av f 7 ,~ ` ` t Gro,;-_ d- Sr;i_xsncck i' r-/--1 Sh'ckshock Group '— ~ 2Q J• htasdic.entalres, mkta- C--- J Mctasediments, neta- ))) 7 / ~ SAREP, 1971 vol:an,Ç,ies YOlcdnici ~a ~j~7/ !'' 1_ 1 7 ~ , ti ras ~o u es° os°ssrv Faille Fault

Axcs de plis i' Fold aces —t— Contact g4ologi;ue FIGURE 1: ETUDES ANTERIEURES, SYNCLINAL 0E Geological contact BERRY MOUNTAIN, QUEBEC. PREVIOUS STUDIES, BERRY MOUNTAIN SYNCLINE, QUEBEC. Milles 0 4 g Miles

Kil,mêtres 10 4 Kilometres ECHELLE-SCALE 3 marks (p. 412). Although Logan's lithological descriptions are excellent, his thickness estimates are too low.

Ells, in 1883, did a reconnaissance along the Lake Branch and Salmon Branch, the two important tributaries of the Cascapedia river (Ells, 1885). The same year, Low ascended the Ste-Anne river to Lake Ste-Anne. He crossed over to the head waters of the west Branch of the Little Cascapedia river, and descended to the south shore of Gaspé.

Lead and zinc-bearing veins were discovered in Lemieux township in 1919, and Mailhiot mapped an area around the Federal zinc and lead mine.

In 1918-19, Coleman investigated the Berry Mountain area in a glacial and physiographic study of the Gaspé peninsula.

Alcock (1926) mapped the Mount Albert area, a part of which overlaps the northern area of the present study. Alcock's observations on the Gaspé Sandstone appear to be limited: However, he considered the lower part of the Gaspé Sandstone to be marine, and the upper as continental (deltaic and fluvial).

Jones (1930) investigated the central Gaspé area: he divided the sequence into a lower, basic volcanics; and an upper, Gaspé Sandstone division. He subdivided the Gaspé Sandstone into a lower unit ("Lower to Middle Devonian"), which resembles the York River; a middle unit, predominantly consiting of red shales; and an upper unit consisting of highly cross-bedded, grey, hard sandstones.

Jones attributed a total thickness of 7,700 feet to the Gaspé Sandstone (the name originally used by Logan in 1863 for the rocks found along the eastern Gaspé coast). A large part of the sequence was considered to be deposited under terrestial conditions as deltas. Owing to marine biota (p. 22), the basal part was considered to be marine. 4

Alcock (1945) reported the presence of solid bitumen in the amygdules, up to 2 inch in diameter, in basic volcanic rocks (within what is now known as the Lower Devonian York Lake), 1 mile west of Squaw Cap Mountain, along a tributary of the Salmon Branch (approx. loc. lat. 48°48'48", long. 66°18'30"). The bitumen saturation presumably took place before the precipitation of secondary calcite and quartz.

Alcock recommended a stratigraphic drilling program to investigate the presence of petroleum in local structures; but he noted a general absence of oil shows in the area.

McGerrigle (1946) found a contradiction in the paleontological age of the lower 3,000 feet of the Gaspé Sandstone series in eastern Gaspé. The brachiopods in the interval suggest Oriskany, while the molluscs, particularly the pelecypods, suggest a Middle Devonian Hamilton age.

Kindle (1938) postulated that the Gaspé Sandstone series should be divided into York River and Peninsula subdivisions. The York River being marine, and the Peninsula, non-marine; the two being essentially contemporaneous. However, McGerrigle (1946) suggested that although this may be valid to some extent, the presence of 4,000-5,000 feet of York River under 7,000 feet of Peninsula (Battery Point) makes this concept difficult to understand.

Using the paleontological data of Cooper (1942), and Kindle (1938), and judging from structural and geographic positions, McGerrigle (1946) suggested that the Heppel Sandstone, in the Matapedia Valley in western Gaspé, and the Gaspé Sandstone, in eastern Gaspé, are identical in age.

Carbonneau (1953, 1959) adopted the name "Big Berry Mountains" for the main topographic feature east and west of the Cascapedia River as indicated on the topographic maps of the topographic division of the Department of Mines and Technical Surveys, Ottawa. He systematically 5 mapped the Big Berry Mountain area. His study consists of an excellent work on the Gaspé Sandstone in which he extended McGerrigle's (1950) observations in eastern Gaspé, to central Gaspé.

Carbonneau (1959) subdivided the Devonian sequence into a Cape Bon Ami - Grande Grève limestone unit, a transitional limestone-sandstone interbedding called York Lake facies; grading upward, through a volcanic sequence, into the Gaspé Sandstone. He divided the Gaspé Sandstone into the York River, Lake Branch and Battery Point formations. A volcanic sequence preceded the Battery Point. The Devonian formations, according to him, range in age from middle Lower Devonian to lower Middle Devonian.

He concluded that the Lake Branch was a facies equivalent of the marine York River formation.

A re-study of the Gaspé Sandstone fauna in eastern and western Gaspé by Boucot et al (1967) revealed that at least the lower 2,000 feet of the strata are Lower Devonian in age. In eastern Gaspé, the York River is to Etymothyris zone age, and in western Gaspé it is of Etymothy- ris and Amphigenia age. Other brachiopod genera suggest an equivalence of the upper part of the Lower Devonian. Gastropods (Nylanderina n. genus) from the Gaspé Sandstone suggest a Lower Devonian age. They also indicate that the Lake Branch formation in western Gaspé (upper Heppel) is equivalent to the Battery Point of eastern Gaspé. The base of the York River formation in the west, according to the workers, is older than its equivalent in eastern Gaspé.

Figure 2 shows the published opinions of various recent workers regarding correlation and age of the Gaspé Limestone and the Gaspé Sand- stone series in the Gaspé Peninsula.

McGerrigle (1954) mapped the Tourelle-Courcelette areas, which form the northern part of the present study area. His maps are used in the present study. Figure 2: Correlation of Lower-Middle Devonian formations by previous workers in the Gaspé Peninsula, Quebec.

Region Western Gaspé Central Gaspé Eastern Gaspé

Author Boucot et a1,1967 Carbonneau,1959 Present Study McGerrigle,1950 Boucot et a1,1967 McGregor,1973

Battery Point le

1, d v - fp S Battery Point Battery Point ------d Lake Branch York River Mi Battery Point LE.ke Branch

• York River_ York Lake'

ONIAN Lake Branch York River G 7 T N Battery Point

r ~(erk Lake DEV we 'York Lake ' York River

Lo Fortin Series York River •

Grande: Grève Q (D ~ l Grande Grève Grande Grève • Grande Grève Grande Grève

~J~ 6

Mattinson (1964) mapped the northwestern portion of the present study. The southern part of his area is relevant to the present study.

Recent detailed mapping by Robert (1966a, 1966b, and 1967) covering the Mount Vallieres-des-Saint Rial, Mount Hog's Back, and Ruis- seau Lesseps regions respectively; and de Rdmer (1969), covering the Lac Madeleine area are relevant to the present study.

B.A. Oil Company (Gulf) and SAREP (Société Acadienne de Recher- ches Pétrolières, an affiliate of Texaco), have made general photo-geological reconnaissances of the Gaspé peninsula. These studies, especially the latter, in the files of the Direction générale de l'Energie, are interesting; their major shortcoming, however, is a lack of ground control.

METHOD OF STUDY

At each outcrop, usual lithological, structural, and sedimentary characters (bedding, sedimentary structures, and directional features) were noted. Lithological units were sampled for laboratory analyses on source, maturity and reservoir possibilities.

Stratigraphic thicknesses were computed by pacing or by direct measurement. Thicknesses were also estimated by geometric reconstruction on aerial photographs. The error in thickness reconstruction owing to a distorsion in aerial photograph scale was minimized by plotting the data, as much as possible, in the central portion of each photograph. A cor- rection factor was also applied, whenever a significant distorsion in the aerial photograph scale was noted.

In the text, the location of outcrops, and sections is shown by an approximate latitude and longitude coordinate. 7

ACCESS AND EXPOSURE

The area is accessible by a good asphalt surface all-weather- road (Trans-Gaspé Highway), completed during 1974. This road connects Ste-Anne-des-Monts, to the north, with New Richmond to the south (see figure 3).

Within the area, the main access was along gravel roads. These roads are good while under utilization for various forestry operations, but rapidly deteriorate when not in use. The fish and game clubs aggra- vate the situation by setting up barriers, or demolishing bridges to restrict free passage.

Exposure, in general, is poor. The vegetation is thick, the streams are often blocked by fallen timber. Good exposures are available only along the new road cuts and large stream valleys. The latter are accessible by canoe, at low water. Two Ford Econolines, a Ford Bronco (with a powerful winch), and a 16 foot canoe were used as means of transportation.

Main access roads (see figure 3) are described below. The Square Forks road, connects the Berry Mountain region with the Matapedia valley, via Nouvelle river; the Berry Mountain Lake road extends northeast and joins the road to Ste-Anne Lake. The Brandy Brook road crosses the Lemieux anticline and extends north toward Isabelle Lake.

The Salmon Branch road extends into the north and north-western part of the area. In the past, this road connected the Berry Mountain area with the town of Cap-Chat, situated to the north-west, and also the Matapedia valley to the west. At present, the Consolidated Bathurst and the Lacroix Lumber Companies are cutting timber along the ridge situated between the Salmon Branch and Lake Branch rivers; a good road extends for 7 miles into this operation from the Brandy Brook Lacroix Camp.

46°50'N 1 • ACARREN MIN • • \ ASq°w Cop MI ♦ \t.6 i ~Mt~ 1 ♦p ed ~~~ I:IL,JOEERE ~~kAJ \ n / • r c / fM âfr 45 . / e.J r_j: - _I '' r0! / ~ ~ ~.a/ / 1 ° ( tifs„~ 0 a ~/ •`l~~''`• (

L.6ERRY MIN f./ ♦ / ♦\♦ 9L C ONICAL MIN ~ RU,. MINER .• F/ W-•" ~\~- u LA ,♦ NOOIE MIN y ' 0.~ Iz CO to

/N►En• A .\ c/ u\ 1 0 1 35' a- / [ 50U'RE JOR,rs ;/~ F♦.~ • - -~ ~ifvj, r~ 3-- ,p YC 11 / c .,:4».. ` f1 \ t,'.5 ..J S` w i ~ ; e~` ~ I ~ j' 1p' ~ ~ ~ 1((S/ 1 r .,....-- Y:'.:;

~~ LO NEE É tiuçE T Ô • >'

Rp \♦ 4_ ~.`_ -.✓• . A11575 \L .'♦♦ f.•P 1 ~ 1 46 ° 25' 66 ° 65°55'W 66°39' 30• 1: 51°IJ Leçende/Legend Milles 0 4 8 Miles Route asphaltde Kilométrees ~~ 10 Kilometres ° Asphalt Road E.CHELLE-SCALE Ruute de Gravier Gravel Road d9°

Figure 3: L'accessibilite et la situation generale, 45° 6660° 66° 64° 62'W synclinal de Berry Mountain, Quebec.

Transportation and general situation map, Berry Mountain Syncline, Quebec. 8

A gravel surface road, which serves the current Consolidated Bathurst operations, exists in the eastern part of the area. It joins the Berry Mountain Lake and Charles Vallée road, which ultimately connects the eastern area with the Trans-Gaspé Highway.

In the north-western and western part of the area, an excellent road connects Nouvelle village, on the south shore, with the Canadian International Paper (CIP) camp, situated to the west of the area. This road finally joins the Causapscal-Cap Chat road, through Bélanger camp, situated in the northwestern part of the area (Loc. lat. 48°41'00", long. 66°31'20").

A road shown on the map as connecting Brandy brook with the Salmon Branch, parallel with the 17-Mile brook in the northern part of the area, is barely passable with a four-wheel vehicle.

A major road, presently under construction in the southwestern part of the area, will connect the CIP operations in the west, with Nouvelle village to the south.

Access in the southern part of the study area, situated between the Cascapedia and Nouvelle rivers, is extremely poor.

TOPOGRAPHY AND DRAINAGE

The Berry Mountain Syncline area consists of a rugged highland encircling a central lowland, a large part of which drains into Chaleurs Bay. The northeastern part is drained into the St. Lawrence by the Ste- Anne river. The western and extreme southern areas are drained, by a series of streams that join the Cascapedia to the east, or the Nouvelle to the west, into Chaleurs Bay.

The area is divided up into the following major topographic features, outlined in figure 4:

43'50.N v + ,AaEN C.ti-CYçC ,~ ~ ~ ~~.~- i5'uawCo ~~3arn Shope

Ân A5'

OIL N

431-4BIG 8ERR1 'y!oüNjAIN$ 4 *~ ~ HiC4LAN0~—: ~ ~ '. ~: ~ ~~" .~ j •~ ~ ..J~ ,. i~ .-~aS~lE 35' S o. •. `~`oS~ `,1i~tiS1 .Q(JARE FORK$ As L04JLAND ~ J ~Y~VL~ ~~0 : ...... " f/ ) ~ 1~ ~~. ~~ ~ ~~~ UQ~ ~~ ~.5 O ~ ,,.~:1 FOF~ -~~,~... ~~,-`~!t e~ ~ 1 ',,`~ P~ 07v ✓ <, 1? ` ,5 t`':- r4^~ ~,~::.t~ ."..1. .~n` ea:P ,r,. ~,~11pP"~ f p01`'~\ ~~.-~ :t-)

/GO ~~Et~~t

'•L ÂHS 75 A8°25' 66°37' 30. 15' 6 6 5° 55'W

Milles 0 ... . + 2, 000' 4 8Miles . . 1 A 10 mM?! +1,000 , vi1cmares Vilca,2trrs ~,.....i ECHELLE-SCALE -1,000'

Figure 4: Carte topographique generalises, Synclinal de Berry Mountain, Quebec.

Generalized topographic map,. Berry Mountain Syncline, Quebec. 1. SHICKSHOCK HIGHLAND: Situated in the northwestern part of the area, this highland reaches an elevation of 3,000 feet and a relief of 1,500 feet. The topographic feature, largely made up of pre-Ordovician rocks, is beyond the scope of the present study.

2. CAP CHAT LOWLAND: This topographic feature is situated south of the Shickshock Mountains; the topograhy varies between 1,000-2,000 feet elevation, a large part being lower than 1,500 feet. The area is made up of low-dipping Silurian and Devonian rocks.

3. DUNIERE UPLAND: This is a northeast-southwest trending, slightly arcuate, 6-8 mile wide, topographic feature in the central north-western part of the area. The elevation exceeds 1,500 feet.

This feature is dissected by several major southeast-flowing river systems, that cut across the regional strike. These rivers are Salmon Branch, Go-Ashore, and Miner, the valley floors of which are usually lower than 1,000 feet. Large parts of this area are underlain by the volcanics and the Devonian limestones.

4. BARREN-LYALL MOUNTAINS HIGHLAND: Situated in the northern part of the study area, this highland exceeds 2,500 feet at several peaks. Important peaks are Barren Mountain, Squaw Cap Mountain, and Barn-Shaped Mountain. Lyall Mountain is situated in the southeast extension of this highland trend. Most of the peaks are underlain by basic and acid volcanics and granitic intrusions.

Several small streams drain the southern slopes of this highland; these include the "Squaw Cap", Indian, North Brandy, and Brandy: All join the Cascapedia river. The northeastern slope of this highland is drained into the St. Lawrence by the Ste-Anne river, and the northwestern slope into Chaleurs Bay by the Seventeen Mile brook. The relief exceeds 1,500 feet. 10

5. MONT VALLIERES DE ST-REAL HIGHLAND: Situated in the northeastern part of the study area, the highland for the most part, exceeds 2,000 feet elevation: Sterling Peak reaches an elevation of 3,000 feet. The southwestern part of this highland is highly dissected, and drains into the Ste-Anne river, that flows into the St-Lawrence; and the Little Cascapedia river, discharging into Chaleurs Bay. The relief is of the order of 1,500 feet.

6. BALDWIN HIGHLAND: This feature represents an area to the west of the Little Cascapedia river valley, and south east of Lyall Mountain. The eastern part of the highland discharges into the Little Cascapedia, and the western part into Berry Mountain brook.

The area is underlain by the Devonian clastics and volcanics, which give rise to a rugged and irregular topography. The relief is of the order of a thousand feet.

7. BIG BERRY MOUNTAINS HIGHLAND: This prominant feature is situated in the south central part of the study area and reaches an elevation of 2,400 feet: it has a relief of approximately 1,500 feet, and joins the Baldwin Highland to the east.

The highland situated to the west of the Cascapedia Valley, gradually subdues westward, across the Lake Branch river. Here, it attains an elevation of approximately 1,500 feet.

8. LITTLE BERRY MOUNTAINS HIGHLAND: This highly dissected highland forms the southern part of the study area. It trends in a west-southwest - east-northeast direction, and is drained by the Cascapedia and Josué rivers. The highest elevation exceeds 2,500 feet: The relief is approximately 2,000 feet. The area is largely made up of the Gaspé Sandstone.

9. SQUARE FORKS UPLAND: This subdued topographic feature is situated to the south of the Dunière Upland. The highest point exceeds 2,000 feet elevation; the relief is 1,500 feet. The area is largely made up of 11

York River sandstones.

10. HUARD LAKE-LAKE BRANCH LOWLAND: This wide arcuate topographic feature forms a wide area of an subdued relief (700 feet), and in general, has an elevation of less than a thousand feet.

Most of the streams in this depression drain into the Cascape- dia river. The lowland is underlain largely by the Devonian Lake Branch shale and silt, and poorly consolidated sandstone.

11. SQUARE FORKS LOWLAND: This lowland separates the Big Berry Moun- tains from the Little Berry Mountains. It is drained by the Square Forks river that joins the Cascapedia river near the Square Forks bridge (loc. lat. 48°34'-42" N, long. 66°08'-58" W). 12

GEOLOGICAL DESCRIPTION

The Shickshock Fault forms the northwestern limit of the area. The fault is near vertical, and represents an offset of the order of several thousand feet. It separates the pre-Ordovician to the north, from the Silurian rocks to the south.

South of the fault, the Silurian and Devonian rocks are exposed in a low dipping monocline, which forms the northern limb of the broad, oval shaped Berry Mountain Syncline. West of the study area, this monocline is folded into several northeast-southwest-trending, open, elongate folds.

The Lower Devonian Gaspé Sandstone is exposed along the centre of the basin-shaped syncline. South of the area, it is underlain by the Fortin Group facies.

The Fortin Group, consisting of tithtly folded slightly calcareous and silty shales with minor silica-cemented sandstone and volcanics, is the lateral basinward equivalent of the Gaspé Limestone and the lower part of the Gaspé Sandstone (Figure 5). The tightly folded nature of the Fortin Group, does not permit the construction of precies stratigraphic sections. Also, owing to the general fine-grained nature of the group it's hydrocarbon potential is considered to be minimal. Thus, although the Fortin was traversed in many areas, it's detailed description is excluded from the present report.

In eastern Gaspé, the Gaspé Limestone is considered to be the source for the widespread occurrence of hydrocarbon seeps and shows. Recent studies (INRS, 1973 and BEICIP, 1974, Sikander, 1974) suggest that the York River and Grande Grève formations are interesting in terms of hydrocarbon potential. The York River, on the basis of maturity indicators (reflectance, and carbonization indices), is considered favourable 13 for the generation of oil. On a chemical basis, it has also been suggested that at the Sunny Bank test, the oil shows in the York River formation, are possibly derived from the underlying carbonates.

The Gaspé limestone consists mainly of argillaceous lime-mud with little prospect for a primary carbonate reservoir. Therefore, in order to dilineate and examine the reservoir possibilities in the area, the study was focussed mainly on the Gaspé Sandstone.

The table of formations (figure 5) briefly summarizes the stratigraphy of the study area.

CAP BON AMI FORMATION

The type section of the Cap Bon Ami formation is located in the Forillon Peninsula, in eastern Gaspé, where according to McGerrigle (1950), it consists predominantly of dark, soft limestone and shale. The formation is enclosed above the soft limestone of the St. Alban formation, and below dark to light grey, hard siliceous and cherty limestone of the Grande Grève formation.

In eastern Gaspé, a westward, and southward thickening of the Cap Bon Ami from over a thousand feet to 3,500 to 4,000 feet (and even 6,000 feet, south of St. Jean River anticline) is documented by McGerrigle (1950). However, unresolved difficulties exist in correlation between the type section of the Cap Bon Ami (and the Grande Grève) and the interior (Skidmore, personal communication). Thus, an attempt to correlate the Cap Bon Ami formation in the area with that of eastern Gaspé, in the absence of a detailed study, is not advisable. The Cap Bon Ami formation in this report is described after McGerrigle (1954) and Carbonneau (1959).

DISTRIBUTION: Within the study area, the Cap Bon Ami varies in thickness and lithology. Only a restricted northwestern part of the area was studied for the Cap Bon Ami formation in view of its hydrocarbon source rock FIGURE 5. TABLE OF FORMATIONS, BERRY MOUNTAIN SYNCLINE, QUEBEC

13-a•

PERIOD EPOCH STAGE FORMATION LITHOLOGICAL DESCRIPTION 1 J

Red, motled red and green, medium ks to very 'fine grained sandstone con- W " --, s twining cross bedding, ripple-marks, EIFELIRH For ms ie mud-crocks rain-prints: shale and

a: are elasts and pebbles; rare conglome- fac u rate beds: channels rare.

BATTERY "Sq + 1,000 ft.

POINT Greenish grey to grey, medium to , fine-grained, pale pink to reddish ;a maroon weathering, sub-angular to m subroundcd, medium to poorly sorted, n Â medium to massive-bedded, highly 7,4- cross-bedded, pink feldspar rich -' sandstone: rare pebbles. Minor Sn7, chocolate brown shale end silty r--- shale. Upto 10,000 ft. 'P 7

Bright red to brownish red silty shale, siltstone. Common ripple- LAKE marks, and micro-cress bedding in siltstone. Gradual lower contact in ' ' send units: Lenses BRANCH of mottled greenish-grey to red, festoon cross-bedded sandstone u- nits upto 50 feet thick, abrupt lower contact. Upto 5,000 ft.

EYSiAN Grey to dark grey, prism weathering shale; grey to greenish grey, fine YORK grained subrounJed medium sorted sandstone: Inclined bedded, rarely laminated reddish brown, highly RIVER ripple-marked, and frequently mud- crackeu siltstone.

2,000 - 6,000' n: W DEVONIAN of Basalt, diabase 2 pyroclastics 0 - 2,000' .0

w- irtcrbedding of York River-type Ÿ sandstone, and siv.e, with Grande

11 Grkve type limestone, volcanics and tone,

pyroclastics. ds e s. lc

Upto 1,250 ft. san an tz lc ar u d vo q s. an

Bluish grey to grey, yellowish grey te s,

argillaceous limestone. la GRANDE te a Lower part consisting of banded ar- s SIEGEü1AN gillaceous and silty limestone, and r rey calcareous shale in southern sec- me

GREVE lo tior.s. Basic volcanics of vaiiable k g

thickness. Chert rare. ong c

t 3,000 Dar P:

• OU GR

Basalt, end coarse to medium grai- IN

ned pyruclastic rocks. Thickness RT O

variable end unknown. F

Dark grey to black shale, ergilla- CAP ceous end silty calcareous icterbeds GEDIREAN grading upwards into thin to medium BON ANI bedded, dark grey argillaceous limestone, minor tough calcareous siltstone. 1,500 - +3,000'

Andesite, basalt, rhyolite, tuff breccia ± 2,000'(Baldwin mbr)

ST-LEON Red, greenish grey to grey laminated slightly calcareous mudstone, „ silt;tone, sandstone, and limrstona. + 2,000' SILURIAN JI wr.'.:.;•`~»•i.,.r• ti~•.:z+..i.,.... i ;;è•:.,..a. r~:•;. ...,.-.ti. . .. -w~....s"c~ .. • ^A.. . . _ ~.,.,. ~:~~~- re •' - ., ~,Yz ..~ ,•_~:...,,.J-..._x_~.... -.a. ~ ...... 2 , ,ry-•y.

~ TOPO- NORTH R-i-S1130tl 88ANCH R. CINTRE -CE RTRRU RUTS. BRANDY N. BROOK R. LAKE BRANCH R. LAKE BRANCH LOWLAND ROUTE SQUARE FCRXS ROAD BIG BERRY MTN. OUEST - WE ST R. NOUVELLE $ R. R. NOUVELLE V.R.

--'~ p,O0o' ,j(prerumi- presumed)

Battery Point (faciis typique Typical facies) 5' 8,000' • • 3.000'

00 N.,4( à` c~ Q0 So` mii ~ Vo‘ i,o0o'

7""' ~ Lake Branch 13.000' 000' Niveau de retirence:tamm•t du York River Datum; top York River '--~-=••D 2.000'

York River 4,0 0 p' • ,000'

Yank Lake

23000' Grande Grive 2,300' Grande Grin• et/ou and/ er Fortin t

Fortin ~ Cap Bon Ami

ECHELLE V2gTlCALE/VERTICAL SCALE 0 2.000' 4.00~ i--- 0 • 100Q ni.

FIGURE 6A: Est-Ouest: Coupe illust.rai,t les correlations regionales, Synclinal de Berry Nount1lin, Quebec. East-West: Diagrammatic section illustrating regional correlations, Berry Mountain Syncline, Quebec. V.311 tibrli RANCH II. ilTirt7AWN ROOK BUIS BRANDY N BROOK BUIS MARCIE P/W !snook BIC BERRY MOUNTAINS DIG FURY IAGUNIAINS S-E liErRESSICS tAKE BRANCH LOWLAND

lottery ~° typicol

~^ ~

Surface * .^°~~~~mel^ York "°..~-~ rdm~w"~~

R0,11.4.

OmAdo 'w"

Cop Non Ami ~~~~

. | EMILE VERT IC/LE/VERTICAL SCALE C ,eoCic' 4.00= v 1mw M. FIGURE 6Bi Nord-Sud: Coupe illustrant les correlations regionales, Synclinal de Berry Mountain, Quebec. North-South: Diagrammatic section illustrating regional correlations, Berry Mountain Syncline, Quebec. 14

potential. For geographic distribution see figure 7.

DESCRIPTION: The Cap Bon Ami formation attains a thickness of 500 feet in the Mont Vallières de St-Réal area, situated in the northeastern part of the present area. Here, it essentially consists of dark argillaceous limestone (Robert, 1966). In the adjacent Lake Madeleine area, the Cap Bon Ami consists of soft, dark grey to black, shaly limestone (de Rdmer, 1969). It weathers greyish or brownish in colour. The rocks when altered by volcanic activity tend to be graphitic, and calcite veined. The middle part of the Cap Bon Ami contains approximately 300 feet of acidic volcanic rocks and several lithic tuff beds. In the Madeleine river area, further northeast, McGerrigle (1959, p. 53) assigns a thickness of 2,000 feet to the Cap Bon Ami.

The formation is best exposed in the northwestern part of the area, west of the Salmon Branch along the 14 Mile brook; and east of the Salmon Branch along the 17 Mile brook (approx. loc. lat. 48°49'40" N, long. 66°20'40" W), and along the escarpment immediately to the east of the broken bridge (near 14 Mile brook confluence, loc. lat. 48°49' N, long. 66°20'30" W).

The lithology consists mostly of dark grey, or brownish grey limestone, generally soft, argillaceous, and finely arenaceous. Shale interbeds are common, particularly toward the top. Quartzose and calcareous sandstones were also observed at various stratigraphic intervals. Along the Seventeen Mile brook section, a compact, well-bedded limestone was observed, but its thickness is not known owing to a diabase intrusion.

Along the 14 Mile brook, 1,500 feet of a low-dipping Cap Bon Ami section was measured above the andesite intrusive. This section is shown in enclosure 2.

Immediately above the igneous contact, approximately 300 feet of Cap Bon Ami consists of thin-bedded argillaceous limestone, calcareous shale, and calcareous siltstone, with minor dolomite. The Upper 1,100 LEGENDE-LEGEND

DEVONIEN-DEVONIAN

Granite and felsite Granite et felsite 13

Andesite Andesite 12 1 Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point 10 I Lake Branch Lake Branch 9 York River York River 1 Volcaniques, rhyolite, Volcanics, rhyolité, 6 basalte, andesite basalt, andesite 8 Groupe'de York Lake .York Lake 5 Fortin

Grande Grive Grande Greve 4

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN St-Léon St. Leon 2 (2a) llbr de Baldwin (2a) Baldwin n>br. CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickshock Group Métasédimentaires, méta- Metasediments, meta- volcaniques volcanics

Faille COUPES ETUDILES -- Fault so•N SECTIONS INVESTIGATED Axes de plis Fold axes , ( 5 -l•rr•„ Ruisseau Brandy et Brandy N. 7 Nouvelle N. et Cascanecla branch 1 Brandy and Brandy N. brooks. du Lac O. Nouvelle N. and Cascapedia Lake Branch. Contact géologique Geological contact Cascapedia Bras aux Saunons. 2 Salmon Branch. Ruisseau Laron. 8 Caron Brook. Ruisseau Quator2leme 11111e 3 Ruisseau liarcil O. Milles D 4 8 Miles Fourteen rile Brcok. 9 Marçi 1 i:. broc4. 1 •r• Ruisseau Go-Ashore. Kilomètres 10 Kilometres fi -"‘‘w 2 •• aNw ECHELLE-SCALE 4 Go-Ashore Brook. Ruisseau Charles val lee. 10 Charles Valley Brook. Ruisseau liner 5 Miner Brook' Route Square Forks, et les Lacs Josué. FIGURE 7 : DISTRIBUTION GEOGRAPHIQUE, FORMATION DE Cap Bon Ami 11 Snuare Forks Road, and Josue Lake, SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Riviére Nouvelle S. GEOGRAPHIC DISTRIBUTION, Cap Bon Ami Formation louveile River S. BERRY MOUNTAIN SYNCLINE, QUEBEC. ..Z ~ 15

feet consist of a monotonous dark grey to black silty shale and medium to thin bedded brownish grey weathering argillaceous limestone, with thin calcareous interbeds. Locally, the shale is splintery.

Along the Salmon Branch, near the 17 Mile brook confluence, dark grey andesite intrudes a thin to medium bedded argillaceous limestone. The latter is recrystallized along the igneous contact. Thin andesite dykes intrude the host rock. A description of the traverse is included in the following:

The lower part consists of a dark grey to black, thinly bedded, splintery calcareous shale; often containing upto a foot thick of argillaceous and silty limestone beds. The shale grades upwards into thin to medium bedded argillaceous limestones, interbedded with irregularly bedded calcareous shale and calcareous siltstone. The limestone (lime-mud) contains isolated corals, brachiopods and crinoid stems.

The upper part of the formation consists of medium to thick bedded, dark grey, brown weathering argillaceous limestone, containing thin shale beds. The calcareous content diminishes upward in the section. Some cliff sections expose 200-300 feet of interbedded calcareous shale and shaly limestone in spectacular outcrops.

The uppermost Cap Bon Ami, directly underlying the Grande Grève, is exposed along the eastern slope of the Salmon Branch (loc. lat. 48°48' 45" N, long. 66°20'35" W) valley. It consists of tough and splintery, thin to medium-bedded, micaceous calcareous shale and siltstone. Approx- imately 400 feet of the Cap Bon Ami is exposed in this section.

Carbonneau (1959) mapped a black, argillaceous, tough splintery limestone in the southeastern part of the area. This limestone unit was encountered in the Ruisseau Caron, and in the Charles Vallée traverses. It is bounded to the south by yellowish-pink, brown weathering rhyolite volcanics (Silurian). Not enough outcrops of the unit were examined to 16

justify a definitive conclusion. However, the recrystallised limestone has little resemblance with the Cap Bon Ami exposed in the northwestern part of the study area.

CONCLUSIONS: The limestone in the Cap Bon Ami formation is cryptocrystalline argillaceous lime-mud. Few floating corals and brachiopods were observed in the argillaceous limestone facies. Partial dolomitization, and floating silt-size-dolomite crystals are common.

Argillaceous limestone units in the lower part of the formation, and dark coloured, thin shale interbeds, are possibly rich in organic matter. In the vicinity of the Salmon Branch, the andesite intrusive causes the overlying Cap Bon Ami shales to develop a splintery fracture. Axial plane cleavage was not observed in the area. None of the examined Cap Bon Ami outcrops showed primary porosity development.

GRANDE GREVE FORMATION

The Grande Grève formation is conformable with the Cap Bon Ami formation in the area. It is exposed in the northern part, in the Mont Vallières de St-Réal, Lemieux anticline area; and in the northwestern part of the area, in a northeast-southwest trend extending from the Barren- Lyall Mountains, southwest ward, to the Lake Branch area in Dunière and Boutet townships.

The formation was defined by Clark (1908, p. 39) in the Forillon Peninsula, eastern Gaspé, as a 550 foot limestone unit comprising: a lower, in part cherty and fossiliferous (100 feet thick), massive bedded, drab hydraulic limestone, followed by an impure grey cherty limestone (400 feet), and capped by a 50 foot thick pure, grey-blue, non-cherty limestone. Russell (1946) measured approximately 900 feet at the same section.

The Grande Grève reportedly increases in thickness, westward from the Forillon section, to 2,000 feet within a few miles. To the west, 17

but south of the northern band of exposure, along the Bald Mountain and Mississipi anticlines, the Grande Grève increases to 4,000 feet. The formation, in the Malbaie and Fortin Townships, is 4,000-4,500 feet thick. Thus, it appears that, in eastern Gaspé, the Grande Grève rapidly increases from 2,000 feet in the northern area, to approximately 4,000 feet in the southern area.

Leaching of volcanic ash (from the volcanic centres situated to the west), was invoked by some workers, as the source of primary and bedded silica (Clarke, 1908, Park, 1929). However, the Grande Grève in eastern Gaspé in known to contain abundant sponge spicules (Skidmore, 1965), which presumably account for the primary silica in the limestone.

Although the Grande Grève in central Gaspé resembles that of eastern Gaspé in lithological features, it characterstically lacks bedded chert. The formation designation is based on the work of Carbonneau (1959) and McGerrigle (1954).

DISTRIBUTION: The Grande Grève formation is exposed in the northeastern, northern, and northwestern parts of the area, as shown in figure 8.

DESCRIPTION: In the extreme northeastern part of the area (north of 48° 48' N, east of 65°57' W), the Grande Grève (in the Lesseps syncline, Lake Madeleine area, de Rdmer, 1969), consists of a lower part which is 50-100 feet thick, well sorted, sub angular, fine to medium grained sandstone. It is peppered with limonite spots. Northeast of the study area, several tuff bands, with siliceous matrix, are observed approximately 500 feet above the base.

The upper part consists mostly of a siliceous limestone. In axial areas the Grande Grève contains an axial-plane cleavage (de Rdmer, 1969).

In the Hog's Back region, north of the study area, the basal Grande Grève consists of poorly exposed shelly limestone intercalated LEGENDE-LEGEND

DEVONIEN-DEVONIAN

Granite and felsite Granite et felsite 13

Andesite Andesite 12

Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point 10 Lake Branch Lake Branch 9 York River York River r 1 Volcan4ques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite basalt, andesite 8 Groupe de York Lake ,York lake Fortin r 5 Grande Grive Grande Greve 4 1

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN St-Léon St. Leon 2 (2a) Iibr de Baldwin (2a) Baldwin nlbr, CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickshock Group Métasédimentaires, meta- Metasediments, meta- volcaniques volcanics

44.7f' so' Faille Fault COUPES ETUDILES SECTIONS INVESTIGATED Axes de plis Fold axes ~ s~ Ruisseau brandy et Brandy N. 7 Nouvelle M. et Cascaneeia Cranch 1 Brandy and Brandy N. brooks. du Lac O. Nouvelle N. and Cascanedia Lake Branch. Contact géologique Geological contact' Cascapedia Bras aux Saumons. 2 Salmon Branch. Ruisseau Laron. 8 Caron Brook. 3 Ruisseau Quatorzieme gille Milles 0 4 8 Miles Fourteen hile Brcok. Ruisseau Marcil D. 9 tlarci I i:. Broc'<. Kilomètres 10 Kilometres Ruisseau Go-Ashore. ECHELLE-SCALE 4 Go-Ashore Brook. Ruisseau Charles Vallee. 10 Charles Valley Brook. Ruisseau Y.iner 5 Miner Brook Route Square Forks, et les Lacs Josué. FIGURE 8: DISTRIBUTION GEOGRAPHiQUE, FORMATION DE Grande Grève 11 Snuare Forks Road, and Josue Lake, SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Rivitre Ibuvelle S. GEOGRAPHIC DISTRIBUTION, Grande Grève Formation rouvetle River S. BERRY MOUNTAIN SYNCLINE, QUEBEC. 18 with conglomerate beds, limestone, and white orthoquartzite. The remaining section largely consits of a competent light grey limestone. The limestone is often silty and siliceous (cherty), and contains intrafor- mational breccia.

The Grande Grève in the Lemieux Anticline area, along Brandy brook (loc. lat. 48°49'5" N, long. 66°10'38" W), contains pink to white, quartz porphyritic rhyolite veins. These mineralized veins are the objective of mining exploration activity in the area.

The following description sums up the traverses made on the Grande Grève formation (Enclosure 5).

North Brandy Brook: (approx. loc. lat. 48°45' N, long. 66°12'45" W): This traverse reveals a medium-thin, well bedded, argillaceous and silty limestone with thin argillaceous beds. Rock exposure is poor. A white volcanic ash bed (previously described in Lemieux township as a kaolin bed) is poorly exposed in a collapsed outcrop (loc. lat. 48°45'20" N, long. 66°11'10" W) near the base of the formation. A trilobite was collected in this bed.

The lower Grande Grève, along the western tributary of Brandy brook, contains banded argillaceous limestone, and slightly calcareous shale, resembling the Fortin group.

Cascapedia Salmon Branch: (approx. loc. lat. 48°47' N, long. 66°19' 30" W): The Grande Grève, poorly exposed along the road section, consists of 2,800 feet of a rather monotonous succession of grey, light brownish grey weathering, medium to thin bedded, often splintery limestone. The lower 900 feet, concordant with the black calcareous Cap Bon Ami shales, are argillaceous and thin bedded.

The upper 1,900 feet are grey, medium to thick bedded, splintery, argillaceous limestone with thinly laminated calcareous shale and silty limestone. The limestone weathers to a typically yellow- 19 brownish grey colour.

Notable in this section is the total lack of the volcanics within the Grande Grève. The volcanics are present in the overlying York Lake section (see enclosure 2).

Cascapedia Lake Branch: (approx. loc. lat. 48°36'40" N, long. 66° 31'30" W): The Grande Grève is exposed to the west and southwest of Huard (Loon) Lake, along a forestry road extending westward into the Dunière Reserve. The formation is approximately 3,000 feet thick.

It is described in the following:

5. Grey, light yellowish grey weathering, irregularly but thinly bedded; interbedding of argillaceous limestone and calcareous shale. 400 feet

4. Black, brown to dark weathering basalt. 650 feet

3. Grey, light yellowish-grey weathering, argillaceous, silty limestone. Typically weathering into small yellowish grey fragments. 750 feet

2. Interbedding of dark calcite-infilled amygdaloidal lava with grey to dark grey, highly argillaceous limestone; and dark grey slightly calcareous shale, containing shale and silt laminations: resembles Fortin Group shales: white silicified ash bed (3-5'). 400 feet

1. Grey to dark grey, brown weathering, medium to thin bedded (typically Grande Grève) limestone. +800 feet

Owing to poor exposure, and a variation in bedding dips in units 1 and 2, the thickness calculations are at best approximate. 20

The thickness of the volcanic rocks, in view of poor exposure, is ambiguous. The neighbouring sedimentary rocks lack any apprecia- ble contact metamorphic effect.

West Lake Branch: (approx. loc. lat. 48°33'02" N, long. 66°35135" W): This section is very poorly exposed along the forestry road to Lacroix Camp (loc. lat. 48°33'03" N, long. 66°35'35" W), and along a new International Paper (CIP) road in the Dunière Reserve (approx. loc. lat. 48°33'35" N, long. 66°36'05" W).

The lower section presumably includes a 350 foot thick basaltic volcanic flow in a slightly disturbed contact with the overlying shaly limestone. The Grande Grève consists of a thin-bedded calcareous silty shale containing thin argillaceous beds. The limestone is characterstically dirty lime-mud.

The middle part of the Grande Grève consists of grey, medium to thick bedded, argillaceous and silty limestone, and minor calcareous silt: the upper part is characterstically Grande Grève, and consists of light grey to (bluish) grey, thin to medium bedded, pale yellowish grey weathering shaly limestone. It breaks into charac- teristic small, weathered splintery fragments.

In view of poor exposure, thickness estimates have not been made.

The lower part of the section is extremely poorly defined. Thus, no attempt was made to include it in the column shown in Enclosure 5. Following are the notable aspects:

The York Lake facies (interbedding of Grande Grève type limestone and York River type sandstone) of the Lake Branch section is missing (or so thin as to have escaped notice) in the poorly exposed west Lake Branch section. A correlation of the volcanics in the two areas on the basis of lithology alone, was not 21

attempted in the field.

A thick to medium-bedded, very dark coloured, calcite veined limestone which contains less than a foot thick shale interbeds is present below the upper volcanics. Several abrupt changes in dip render the thickness estimates imprecise.

Nouvelle River: Southwest of the area, along the Nouvelle River (east branch), and south of the bridge (loc. lat. 48°26' N, long. 66°31'25" W), the section underlying the York River, consists of dark grey, slightly calcareous shale (argillite), and silty shale, along with up to 10 foot thick beds of fine grained, silica cemented sandstone, and siltstone, and relatively minor, (5-10 foot thick) beds of Grande Grève-type limestone. The lithology here suggests a near-complete basinward shale-out of the Grande Grève limestone (see enclosure 3). Some volcanics are also present, but owing to structural complexity, their vertical extent and stratigraphic position are not clear.

CONCLUSIONS: Exposure in the area is too poor to enable a better dilineation of facies. However, following are the conclusions regarding the lithology of the Grande Grève:

1. In the northern part of the study area, the Grande Grève contains coarse clastics (mature sandstone) in the lower section, as described by de Rdmer (1969) and Robert (1966). The formation has been described as being siliceous and silty. In Lesseps and Lemieux anticlines (the latter situated along Brandy brook), the Grande Grève is intruded by acidic volcanic rocks, and hydrothermal mineralisation.

2. Basic volcanic flows and pyroclastics occur locally at different levels in the Grande Grève: for example, the Grande Grève lacks volcanics in the Salmon Branch section: On the other hand, several basic volcanic flows are present in the Lake Branch section. 22

In the West Lake Branch area at least 350 feet of volcanic and pyroclastic rocks are present in the lower Grande Grève: And an enormous thickness of volcanics may be present at the Cap Bon Ami - Grande Grève contact.

3. The sections in the western, and the northwestern part of the area (Enclosure 2) suggest that a gradual shale-out of the Grande Grève takes place southwestward or southward. The change is notable between the Nouvelle and Lake Branch sections. Fortin Group facies, calcareous siltstone and calcareous shale develop to some extent in the lower Grande Grève section in the West Lake Branch, Lake Branch and Brandy Brook sections. The Nouvelle road section contains minor Grande Grève limestone.

4. The Grande Grève lithology, in a large part of the area, consists of a grey to "bluish" grey, massive, light yellowish-brown weathering, usually, shaly, less commonly silty limestone. The limestone is a compact mudstone (Dunham, 1962). Chert and siliceous content is conspicously lacking, especially in the (southern) sections that contain the lava flows. Thin, dark coloured argillaceous bands are common. Calcarenite, bioclastic or biogenic limestones were not observed.

5. Primary limestone porosity, or secondary fracture or vuggy porosity were not observed in any of the outcrops. The Grande Grève in the northwestern part of the area is gently inclined, and lacks fractures other than widely spaced jointing. De Ramer (1969) reported axial-plane cleavage in axial areas of tight folds northeast of the area.

YORK LAKE FACIES

The York Lake has been defined by Jones (1935, p. 15) as an interbedding sequence between the Grande Grève-type shaly limestone, and the York River-type muddy, grey coloured sandstone. McGerrigle (1946, 23 p. 47) suggested that these rocks should be included in the York River formation. Because of its local nature, and both lateral and vertical gradation of the unit into the York River and Grande Grève formations, this interbedding is referred to as a facies (Carbonneau, 1959).

McGerrigle (1950) described the York Lake facies in the York Lake area of eastern Gaspé. Here, it consists of shale, sandstone, and limestone. The sandstones are fine grained, argillaceous, buff to greenish-buff in colour, as against the greenish grey of the York River formation.

The total thickness of the facies is variable in eastern Gaspé. Jones (1935, 36) mapped 2000-4000 feet of York Lake in Holland and Fletcher townships. McGerrigle (1950, p. 74) stated that there is no evidence that the York Lake facies develops at the expense of the Grande Grève formation.

Carbonneau (1959, p. 23) described three sections of the York Lake sequence to the east of the area, in the vicinity of the Little Cascapedia river. Here the Grande Grève "lenses", upto 500 feet thick, are interpreted to occur within the York River formation.

DISTRIBUTION: The facies best develops in a band of outcrops extending southwestward from Mount Squaw Cap (figure 9). The York Lake is also exposed in a synclinal structure along the western limit of the area; and along a poorly exposed local trend in the eastern part of the area.

DESCRIPTION: The York Lake represents an interbedding of the York River- type fine grained, greenish grey, salt and pepper, muddy sandstone, and a yellowish grey-weathering Grande Grève-type argillaceous limestone. The sequence is capped by a basic volcanic and pyroclastic unit in several sections (see enclosure 2). Important York Lake sections are described in the following: LEGENDE-LEGEND

DEVONIEN-DEVONIAN •

Granite et felsite r 13 Granite and felsite

Andesite 112 Andesite

Battery Point Battery Point facies Facies de 'Square Forks' 11 Square Forks Battery Point typique Typical Battery Point 10 Lake Branch Lake Branch 19 I York River York River ` 7 Volcaniques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite f basalt, andesite 8 Groupe de York Lake .York Lake L Fortin 5

Grande Grève Grande Greve 4 Cap Bon Ami 3 1 Cap Bon Ami SILURIEN DEVONIEN-SILURIAN DEVONIAN St-Léon 1 St. Leon 2 (2a) libr de Baldwin 1 (2a) Baldwin mbr. CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickshock Group Métasédimentaires, méta- J Metasediments, meta- volcaniques volcanics ~o COUPES ETUDILE$ Faille _.._ Fault SECTIONS INVESTIGATED Nouvelle M. et Cascaneeia Branch Axes de plis Fold axes Ruisseau brandy et Brandy N. 7 1 Brandy and Brandy N. brooks. du Lac O. Nouvelle rl. and Cascanedia Lake erahch. Contact géologique Geological contact Cascapedia Bras aux Saunons. 2 Salmon Branch. Ruisseau Caron. N Caron Brook. Ruisseau Quator:ieme ilille 3 Fourteen file Brook. Ruisseau Marcil O. Milles 0 4 B Miles 9 Farci I V. broc'c. • 4 ,4 ♦ Ruisseau Co-Ashore. Kilomètres 10 Kilometres ♦a 4 2•W 4 Ruisseau Charles Vallee. ECHELLE-SCALE Go-Ashore Brook. 10 Charles Valley Brook. Ruisseau liner 5 Miner Brook Route Square Forks, et les Lacs Josué. 11 Forks Road, and Josue Lake. FIGURE 9: DISTRIBUTION GEOGRAPHiOUE, Facies de York Lake Souare SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. Cascapedia Branche du Lac. 6 Lake Branch. Riviére llouvelle S. 12 S. GEOGRAPHIC DISTRIBUTION, York Lake Facies Couvelie Hiver BERRY MOUNTAIN SYNCLINE, QUEBEC. N Lk/ 24

Brandy Brook: (loc. lat. 48°50' N, long. 66°10'38" W). It consists mainly of a York River-type grey to greenish grey, fine grained, inclined and thinly parallel-bedded sandstone. The lower part of the section consists of grey to dark grey slightly calcareous shale containing wisps of micro-cross-bedded silt, and shaly limestone. The total thickness of this interval is approximately 1000 feet. Robert (1966) mapped several thousand-foot-long sand lenses, but the exact dimensions are not clear owing to poor exposure.

Cascapedia Salmon Branch: (loc. lat. 48°46'30" N, long. 66°18'22" W). Poorly exposed York Lake outcrops along the roadside, and the Salmon Branch river. It occurs as a thick sandstone unit above the Grande Grève (exposed along the Salmon Branch and Squaw Cap brook intersection), and below a 125-foot-thick upper, basic volcanic and pyroclastic unit.

The York Lake consists of greenish grey, fine grained, thinly, and horizontally-to-inclined bedded, muddy sandstone. Sharply truncated cross-bedding is relatively rare. Some calcareous (argillaceous limestone) beds are inferred from highly weathered outcrops and local boulders.

A basic volcanic bed approximately 100 feet thick is exposed 450 feet above the base of the section. A mainly greenish grey sandstone section is interpreted to occur between the two volcanic beds on the basis of extremely weathered outcrops.

A few localities yielded isolated coral and brachiopod fossils.

The total thickness of the York Lake unit is 1,250 feet.

Go-Ashore Brook: On the basis of a few outcrops, and the distribution of boulders, the York Lake is interpreted to contain mostly York River-type sandstone below a basic volcanic unit. Owing to a lack of precise outcrop data, the lithologic details and thickness 25 estimates are lacking.

Cascapedia Lake Branch: (loc. lat. 48°36'30" N, long. 66°31' W). The York Lake consists of a yellowigh grey, argillaceous limestone, calcareous shale, and greenish grey, fine grained thinly bedded, muddy, often bioturbated, sandstone, and siltstone. This interval is approximately 600 feet thick. The sand units gradually increase in thickness from 5 feet thick in the lower part, to 20-40 feet in the upper part.

Poor exposure does not allow a detailed examination of the sand- intercalations, but the stratigraphic relationship between the limestone and the sandstone is summarized in enclosure 2. It appears that the sandstone does not develop in the section equivalent to the lower York Lake of the Salmon Branch section. The York Lake facies is only approximately half as thick as that of the Salmon Branch.

West Lake Branch: (approx. loc. lat. 48°30'40" N, long. 66°35'30" W). Exposure is poor, but along the new forestry road near the Lacroix lumber camp (upstream Lake Branch river) the Grande Grève and, York River lithologies are exposed. The Grande Grève limestone is typically developed as bluish grey, yellowish-brown-weathering shaly limestone. It is overlain by greenish grey, muddy, and bioturbated silty sandstone, which is occasionally crinoid and brachiopod bearing. Interbedding of the two lithologies is absent, or is too thin and escaped attention due to poor exposure.

There is a conspicuous lack of volcanics in the Grande Grève and the York River contact in this section.

Nouvelle Road South: (approx. loc. lat. 48°28' N, long. 66°33'40" W). The section is exposed near the bridge on the road to Nouvelle, and is partly situated outside the designated area. 26

The York Lake development along the southern limb of the Berry Mountain Syncline is poorly understood owing to a shale-out of the Grande Grève limestone, and poor access.

CONCLUSIONS: The Grande Grève-type limestone and the York River-type sandstone interbedding varies in measured thickness from non-existant in the western part, through 600 feet in the Lake Branch river section, to 1250 feet in the northern part (Salmon Branch river). Carbonneau (1959) reported a York Lake thickness of 2000 feet in the Berry Mountain Lake area.

On the basis of poorly identified fossils, McGerrigle (1950, p. 74) suggested a York Lake age closer to the Grande Grève (Oriskany) than the York River, but he concluded that it is closely related to the York River. Actually the discussion, to an extent, is superfluous since the York Lake represents a gradational contact between a largely calcareous, Gaspé Limestone sequence and a predominantly clastic Gaspé Sand- stone sequence. These sand bodies represent the first influx of offshore sands on to a southeast sloping carbonate platform.

The sandstone and shaly limestone interbedding of the York Lake facies provides stratigraphic (sand pinch-out) trapping possibilities in the area. Attempts to study the interbedding along Go-Ashore, and Minor brooks were futile due to poor exposure and bad access.

The reservoir development in the York Lake facies (intergranular porosity in the fine grained sandstone) is poor due to the presence of clay matrix. The clay content appears to increase in the westerly sections: the porosity development, and the nature of clay content, are further discussed in the Economic Possibilities chapter of this report.

YORK RIVER FORMATION

The York River formation in the study area, consists of a clastic sequence of a wide lithological range. Basically, it forms a 27 broad rim around a central trough, the Berry Mountain Syncline; and extends westward into the Matapedia Valley; where it is exposed in a tight syncline.

The York River formation is generally defined as the lower marine part of the Gaspé Sandstone series. In eastern Gaspé, it occurs outside Logan's Gaspé Sandstone type section (Logan, 1863).

Williams (1910, p. 688-698) referred to these sandstones as the "basal calcareous marine and fossiliferous zone of the Gaspé Sandstone" McGerrigle (1950, p. 78) included in the York River formation all rocks in the section having the same lithology as the "general series of York River beds".

In eastern Gaspé, the York River formation consists of a grey to greenish-grey, fine to medium grained, inclined - to gently cross- bedded, grey (plagioclase) feldspar-rich sandstone containing rare conglomerate. The York River, also contains upto 20-foot-thick, grey-coloured monotonous shales. The thickness generally increases from north to south: It is 1,300 feet thick in the northern outcrop band, north of Gaspé Bay; and increases to 6,000 feet, approximately 20 miles to the south, in the Malbaie Bay area (McGerrigle 1950, p. 79).

Carbonneau (1959) in central Gaspé, observed that the York River thickens from 2,000 feet in the north, to 10,000 feet to the south. North of the synclinal axis, Carbonneau included, in the York River, a section overlying a volcanic sequence.

In the Matapedia Valley region, situated to the west, the York River occupies two NE-SW trending synclines in the Lake Cassault, and the Causapscal areas. The latter is in strike extension of the Berry Mountain Syncline (Stearn, 1965).

The York River formation crops out in three bands in the Causapscal area in western Gaspé (Stearn, 1965), and is best described in the central part of the area. It consists of a more than 3,000-foot- 28 thick basal unit composed of structurally deformed, dark grey, very fine grained sandstone and siltstone; a 900-foot-thick middle unit (Joliet Brook beds) made up of interbedded, fossiliferous, dark brownish grey siltstone, shale, and sandstone; and a 3,500-foot-thick upper unit consisting of greenish grey, fine to medium grained, thick-bedded sandstone.

The York River sandstones are feldspathic. The sandstones and siltstones near the base are, however, calcareous and less feldspathic. The York River is overlain by increasingly friable siltstones and sandstones of the Lake Branch formation.

The calcareous siltstones contain a marine fauna which includes brachiopods, pelecypods, bryozoa, trilobites, gastropods and corals, and local "biohermal masses" (Stearn, 1959, p. 8). The green and red siltstones contain poorly preserved plant remains, and in some cases, mats of carbonized plant material along bedding planes.

DISTRIBUTION: The York River forms a rim around the axial area of the Berry Mountain Syncline. Narrow synclinal structures also contain the York River in the eastern part of the area (figure 10).

DESCRIPTION: Lithologically the York River formation varies widely across the study area, and demonstrates interesting facies changes.

In the northern and northwestern part of the area, the York River includes a greenish grey, fine grained sandstone, grey shale, reddish brown to maroon siltstone and shale, and calcareous sandstone. It overlies a volcanic (basalt) and pyroclastic unit; and underlies the Battery Point and/or the Lake Branch formations.

In the southeastern part of the area the York River sequence is more shaly than that described above; the section is usually structurally deformed. In some areas, there is a basic volcanic unit in the upper York River ( Caron brook , loc. lat. 48°36'45", long. 66°00'35";

LEGENDE-LEGEND

DEVONIEN-DEVONIAN

Granite and felsite Granite et felsite 13

Andesite Andesite 12

Battery Point Battery Point Facies de 'Square Forks' 11 1 Square Forks facies Battery Point typique Typical Battery Point 10 1 Lake Branch Lake Branch 91 York River York River i 7 1 Volganiques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite basalt, andesite 8 Groupe de. York Lake ,York Lake 5 Fortin

Grande Grève Grande Greve 4

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN St-Léon St. Leon 2 (2a) ilUr _ de Baldwin (2a) Baldwin mbr. CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickphock Group Métasédimentaires, méta- Metasediments, meta- volcaniques volcanics 3o Faille Fault COUPES ETUDILES SECTIONS INVESTIGATED Axes de plis Fold axes -L...... Ruisseau Brandy et Brandy N. 7 Nouvelle N. et Cascapedia Qranch 1 Brandy and Brandy N. brooks. du Lac O. Nouvelle M. and Cascapedia Lake Branch. Contact géologique Geological contact Cascapedia Bras aux Saunons. 2 Salmon Branch. Ruisseau l.aron. 8 Caron Brook. Ruisseau Quatorzieme Mille 3 Ruisseau liarcil O. Milles 0 4 8 Miles Fourteen rile Brcok. 9 1 ' rarcil U. BroC4. Kilomètres 10 Kilometres .\2 Ruisseau Go-Ashore. ECHELLE-SCALE 4 Go-Ashore Brook. Ruisseau Charles Vallee. 10 Charles Valley Brook. Ruisseau l'.iner 5 (liner Brook Route Square Forks, et les Lacs Josué. FIGURE 1 0: DISTRIBUTION GEOGRAPHiQUE, FORMATION DE York River 11 Souare Forks Road, and Josue Lake. SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Riviére louvelle 5. GEOGRAPHIC DISTRIBUTION, York River Formation rouvelle Hiver S. BERRY MOUNTAIN SYNCLINE, QUEBEC. 29 and along the upper most stretch of the Marcil brook, loc. lat. 48°36' 25", long. 66°03'25").

The observed sections are described in the following (see enclosures 2 and 3).

Northern Area:

Brandy Brook: (approx. loc. lat. 48°45' N, long. 66°11' W) The section, poorly exposed along the flanks of the Lemieux anticline, combines data from several traverses in the general area.

The York River is underlain by a 100 foot thick lava flow. The contact metamorphic zone is thin and limited to a few feet.

The lower part of the section contains approximately 650 feet of grey to greenish grey, fine grained, slightly muddy, and very slightly calcareous, thin, inclined-and gently-cross-bedded rusty brown-weathering sandstone.

The middle part, in general, is finer grained, and consists of a greenish grey, very fine grained sandstone, and siltstone. This unit is 400 feet thick.

The upper part consists of a grey coloured, fine to very fine grained sandstone. It is typically thin, parallel-to-inclined bedded, and capped by a calcareous sandstone. The unit is approximately 700 feet thick.

The total thickness of the Brandy Brook York River section is approximately 1,750 feet.

Cascapedia Salmon Branch: (approx. loc. lat. 48°44'50", long. 66°17'10"). The section is low dipping (10-15°) to the south and south-east; the lower part, immediately above the base, is poorly 30 exposed. It is conformable with a 120-125 foot thick basic volcanic and a cross-stratified pyroclastic interval.

There are only two exposures of the lower part of the section: these consist of reddish brown weathering, very fine grained sandstone and siltstone, and a dark grey to black fossiliferous mudstone. The latter is rich in pelecypods, brachiopods, and bryozoan-like stems, exposed 250 feet above the base.

The middle part contains, less than 100 feet thick grey, fine grained, thin, inclined-bedded sandstone. This unit is partly exposed along the Salmon Branch river bed. The thickness of the unit is undetermined.

The remaining 500 feet consist of an interbedding of red and green shales, siltstone, and fine to very fine grained, silty, calcite-cemented sandstone. Some beds are rich in brachiopod and pelecypod fossils. Bedding is lenticular over a distance of a hundred feet. The "typical" York River (that is, light greenish grey, fine- grained, thin and inclined-bedded light grey weathering) sandstone occurs as a minor constituent.

The red siltstones contain symmetrical ripple-marks, rill-marks, mud-cracks, and are commonly cross-bedded. The cross-bedding lacks flagrant erosion surfaces. The current directions and ripple-mark ridges in adjacent beds are often highly divergent. Convolute bedding, although present, is rare. The sediments appear to represent a wide tidal flat type of depositional environment, characterized by occasional submergence, and deposition of sand bars.

The upper-most 300 feet consist mostly of greenish grey to grey, fine to very fine grained, inclined bedded, and calcite cemented sandstone. This lithology is also observed in the upper York River along other sections in the western part of the area (such as the 31

Cascapedia Lake Branch section).

The total thickness of the York River formation is approximately 2,000 feet. The lithology in the upper part largely consists of an interbedding of shale, siltstone and very fine calcareous sandstone, with minor amount of "typical" light greenish-grey York River sandstone. The lower part is poorly exposed.

Cascapedia Lake Branch: (approx. loc. lat. 48°35'25" N, long. 66° 29'25" W). This section is exposed between a broken bridge on the Lake Branch river southwest of Huard Lake (coordinates shown above), and the abandoned Lacroix (Tank) lumber camp.* The bedding is inclined, at between 15 to 45° southeast. The section is reasonably well exposed along the forestry road.

The York River overlies a poorly exposed, approximately 100 foot basic volcanic interval. A poorly exposed shale bed below the volcanics is apparently slightly baked but this effect is local. The well bedded shales (typically York River) are grey to dark grey on fresh surfaces, weathering into small brownish cleavage fragments. They have a uniform composition, and contain rare brachiopod fossils.

The basal shale grades up into a dark-grey brachiopod-bearing shale, and a greenish-grey fine-grained, medium to thin and inclined- bedded sandstone. The sandstone units are 10-50 feet thick, with intervening 5-10-foot shale beds.

The middle unit, 1,350 feet thick, is poorly exposed (only collapsed boulders are observed along the roadside). It is interpreted to consist mainly of light greenish-grey, thin to medium and inclined-bedded, fine grained sandstone; the sand matrix is argillaceous. Reasonably clean, and well sorted sandstones are relatively rare. Shale interbeds are minor.

*Identified as Tank Lumber Camp: because of an abandoned armoured vehicle on the site. 32

The upper unit, approximately 1,200 feet thick, consists of an interbedding of grey to greenish-grey sandstone, red to reddish brown siltstone, sandstone, and red shale. Some red silty shales, towards the top, contain thin beds, extremely rich in leached-out pelecypod and brachiopod shells. The uppermost exposure, included in the York River, consists of a grey to greenish grey, thinly bedded calcareous sandstone and partly bioturbated shale, containing abundant pelecypod fossils.

The York River is approximately 3,500 feet thick.

The red units are included in the York River for the following reasons:

1. The red shale, siltstone, and sandstone, represent an interbedding of the Lake Branch-type red shales, and reddish stained greenish-grey York River sandstone.

2. The red facies contains stunted brachiopod and pelecypod- rich beds. The Lake Branch formation, on the other hand, has been defined as being typically non-fossiliferous (Jones, 1930).

3. The fossiliferous calcareous siltstone, and sandstone unit, overlying the red facies, is considered to be upper York River. Red colouration is also observed in the Salmon Branch section.

4. The red beds in the York River, in the Lake Branch section, are rather silty, and the bedding is far less regular (bioturbated in places) than usually observed in the Lake Branch formation. The red colour alone cannot be used as a correlation criterion.

West Lake Branch: (approx. loc. lat. 48°30'40" N, long. 66°35'30" W, and lat. 48°31' N, long. 66°37'30" W). The section is poorly exposed along the forestry road. The best exposures are along the 33 new CIP road, leading to the Lacroix Camp.

The lower part of the York River formation consists of 1,100 feet of a thin bedded greenish grey, fine grained, muddy sandstone. This interval contains inclined-bedded, bioturbated shaly and silty crinoid-bearing sand units. It grades westward into a grey to greenish dark grey, prism-weathering shale.

The middle part of this section, which forms the ridge to the south of the Lake Branch river (approx. loc. lat. 48°32' N, long. 66°35' W), is approximately 2,200 feet thick, and consists of greenish-grey, fine to medium grained feldspar-rich, medium to poorly sorted, thin - to medium - bedded sandstone altering to a pinkish grey colour. It resembles the "typical" Battery Point. These poorly exposed sandstones are, in general, flat or inclined - bedded, lacking the trough cross-bedding and erosion surfaces that are frequently observed in the Battery Point exposed to the east (in the Big Berry Mountains area). The lithology is presumably much more varied than that described.

The upper part is exposed one mile southeast of Chasseurs Lakes (loc. lat. 48°32' N, long. 66°37' W) along the Nouvelle river. It consists of approximately 800 feet of grey to greenish-grey, fine to very fine grained sandstone, with grey to dark grey siltstone, and brown weathering shale. The contact between this unit, and the underlying sandstone is faulted.

This interbedded section grades upward into a very thinly bedded, red coloured silty shale, and siltstone.

The total thickness is interpreted to be 4,000 feet. However, faulting and poor exposure render this estimate highly speculative. 34

Southern Area: The York River formation forms a band of sandstone, siltstone, and shale along the steeply dipping southern limb of the Berry Mountain Syncline. The outcrops are usually along the steep stream valleys in a rugged terrain. Several traverses along the south-eastern part of the area, such as Charles Vallée, Caron, and Marcil West brooks yielded a reasonable amount of information. Others, especially along the southern parts of the area, yielded little data. Many could not be completed owing to poor access. A general description of the southern traverses is included here.

The York River formation, south of the Berry Mountain Syncline, attains a great thickness, although the thickness estimates are imprecise owing to poor exposure, and structural complications. It is for this reason that some of the sections (such as that of Charles Vallée) shown in Enclosure 3, lack a vertical reference.

Caron Brook: (approx. loc. lat. 48°36' 10" N, long. 66°00' W). The York River is gently dipping along the northern part of the traverse, but steep to vertical, and faulted along the southern part. The structure is interpreted to be a tight syncline, the southern limb of which has been complexly deformed.

In the southern part of the traverse a black splintered argillaceous limestone (resembling Cap Bon Ami limestone), underlies the York River. This limestone is flanked to the south by acidic volcanics (Baldwin member). The contact in the southern part is presumed to be faulted.

The tectonically complex part of the section, south of the synclinal axis, has been excluded from stratigraphic computations. Thus, the thickness shown in the enclosure 3 is considered as minimum. 35

The lower section consists of an alternating sequence of sandstone and shale. The sandstone is characterstically pale greenish- grey to grey, fine to very fine-grained, thin to medium and usually flat bedded, and is partially silica, and rarely calcite-cemented. It contains shale and volcanic rock fragments. The middle part of the section contains a similar lithology to that described above, except for more frequent thin lenticular grey shale.

The upper part consists largely of dark-grey to black slightly calcareous shale containing thin silt stringers. A basic volcanic unit, present here, is absent along the Marcil West brook (approx. loc. lat. 48°35'50" N, long. 66°46' W), situated 4 miles to the south west. The sandstone at the base of the upper section is highly cross-bedded.

The fairly homogeneous, usually thin to medium-bedded nature of the sand, the planar and low angle cross-bedding, the presence of glauconite in some of the units, and a lack of flagrant erosion surfaces suggest a marine shore-face to offshore depositional environment. The shales are characteristically well bedded, and contain fine silt and sand laminations, suggesting a distal to fringe environment in the deltaic depositional model.

Marcil West Brook: (approx. loc. lat. 48°34'30" N, long. 66°04' W) This section is exposed along the south-flowing stream, east of the Charles Vallée lumber camp. Although the section is well exposed, owing to a fault of unknown displacement (intersecting the Marcil West brook, 1 mile southeast of the camp), the total thickness is unknown. The traverse crosses the York River - Battery Point contact, which provides a reference datum for the section.

The section above the fault consists of the following:

The lower part, approximately 1,300 feet thick, consists mostly of grey, fine to very fine grained, salt and pepper, usually flat 36 bedded, less commonly cross-bedded, sandstone.

The middle part consists of a thinly laminated, dark grey to black, splintery shale, frequently containing upto 10-foot-thick, grey, fine grained, flat and inclined bedded sandstone. This fossiliferous section is exposed in a road section one-half mile east of the Charles Vallée Consolidated - Bathurst camp (approx. loc. lat. 48°34'42" N, long. 66°5'12" W). The sandstone, is well jointed, compact, and silica-cemented. The thickness is approximately 1,150 feet.

The upper part consists of approximately 1,350 feet of thin to medium-bedded, fine grained, silica-cemented, compact sandstone. A minor shaly interval consists of approximately 150 feet of dark grey shale with thin sands. The stratification, on occasions is thick, and inclined-bedded.

The Marcil West Brook York River section imperceptibly grades into highly cross-bedded Battery Point sandstone.

The York River sandstones, exposed along the Marcil West brook, on the basis of parallel and inclined cross-bedding*, presence of shale fragments in the sandstones, absence of fluviatile (such as point-bar) characters of sedimentation, and the presence of abundant brachiopods, is considered to be marine. The sandstone, uniformly medium to fair-sorted, fine-grained, and parallel bedded, appears to represent an offshore depositional environment. The "Flaser" bedding in the shales suggests alternating current and wave action and calm periods in a coastal-shelf environment (Reineck and Wunderlich, 1968).

Owing to the presence of a major fault, the southern part of the Marcil West brook section is of dubious relevance for thickness estimations. Approximately 4,300 feet of York River (see geological

*Occurrences of massive inclined-bedded fine grained sands were observed at Locality 8.29.118: approx. loc. lat. 48°45'30" N, long. 66°04' W. 37 map, enclosure 1), and volcanics are exposed south of the fault.

Lithological reconstruction and a tentative correlation across the fault suggest a displacement of the orderof a thousand feet.

The total stratigraphic thickness of the York River formation in the Marcil West brook, north and south of the fault is interpreted to be of the order of 7,000 feet.

Charles Vallée: (approx. loc. lat. 48°33'50" N, long. 66°05'40" W). The highest exposed Charles Vallée road section is interpreted to be situated some 2,000 feet below the York River - Battery Point contact. The lower 400 feet is excluded from the measured section owing to faulting.

The steeply inclined, and at times slightly overturned, lower part of the section, approximately 600 feet thick, consists of a dark grey to black shale interstratified with grey, fine grained, medium to thick bedded, tough and compact, silica-cemented sandstone; and grey laminated silt. The sandstones are rarely cross- bedded. The shales are typically splintery, presumably due to an increased metamorphism.

The middle unit, approximately 700 feet thick, consists of fine to very fine grained, flat and cross-bedded sandstone units upto 50 feet thick. The silica-cemented sandstones are typically grey in colour, thin to very thin bedded, with smooth bedding surfaces and occasionally contain oscillation ripples, and worm-burrows. They contain shale and carbonized wood fragments. The sands are interstratified with a dark-grey to black, occasionnaly highly brachiopod-rich shale (loc. 7.5.51, lat. 48°33'47" N, long. 66°05' 48" W). 38

The upper part of the section contains a typically grey to light greenish grey, fine to very fine-grained, inclined-bedded sandstone with muddy matrix, and lacking in the silica cement observed in the underlying sandstone. The beds are generally 5 feet thick and are interbedded with dark grey silty shale. The lower contact of these sandstones is abrupt, but non-erosional. This unit is approximately 400 feet thick.

It should be noted that the "typical" grey to light greenish grey York River sandstone facies develops only in the upper-most 400 feet of the exposed Charles Vallée road section.

The sandstone is a minor constituent in a predominantly grey to dark grey shale, siltstone and fine grained sandstone sequence. Total exposed thickness is more than 1,700 feet along the Charles Vallée road.

The sandstones are horizontally bedded, rarely oscillation- rippled. In general, there is a lack of cross-bedding with frequent erosion surfaces. The shales contain thin wisps of silts and sands, (flaser bedding). On the basis of these features, a neritic shelf depositional environment is suggested. The sands were presumably deposited by wave and current action during frequent clastic in- fluxes in a marine environment.

The presence of the "typical" York River sandstones in the upper part of the section presumably suggests a shallowing of the sedimentary basin, and the deposition of offshore sand bars or shoreline sands.

Lithologically, the shaly lower York River section, resembles the Fortin Group facies exposed south of the study area. 39

Nouvelle South: (approx. loc. lat. 48°28' N, long. 66°33'40" W) The York River formation is exposed south of the synclinal axis, and to the north of the Fortin shale development, near the Nouvelle bridge (loc. lat. 48°26'20" N, long. 66°31'30" W). The section is consistently steeply northwest dipping.

The York River consists of fine to medium-grained, grey to greenish grey, rarely reddish, light grey to pink - weathering, thick to massive, inclined to cross-bedded, sandstone with thin shale lenses.

The sandstone often contains small shale clasts, pink subrounded feldspar, and has a greenish clay matrix.

The York River, as elsewhere in the southern part of the area, is typically tough and massive, and resembles the Battery Point sandstone of the Big Berry Mountains. The main obvious difference lies in it's lack of frequent trough-type cross-bedding, and an abundance of pebbles in the sandstone. Minor, grey to dark grey shales and siltstone beds are brachiopod-bearing.

The massive sandstones are also exposed along a road section to the west of the Nouvelle road (loc. lat. 48°28'10" N, long. 66° 33'20" W).

Minor, grey to very light-grey, fine to very fine-grained, thin and inclined-bedded sandstones each upto 25 feet thick, occur in silty shales. The total thickness of this unit is approximately 250 feet.

The minimum thickness of the York River is 2,400 feet, but assuming that the red facies are a part of the York River, it may be upto 4,500 feet thick. 40

The York River overlies the grey to dark grey shales, siltstone, and quartz sandstone and minor grey, light tan weathering argillaceous limestone. However, there is a good thickness of dark grey shale, and siltstone, which lack limestone beds. These could be the shaled-out equivalents of the York River and/or the York Lake.

CONCLUSIONS: The following summarizes the observations on the York River lithology.

1. The York River formation is relatively flat lying and undeformed in the northwestern part of the area. Here, it overlies a basic volcanic unit. In the southern sections, on the other hand, the York River is often complexly deformed, and reaches an enormous apparent thickness. It some southeastern sections, it contains basic volcanics toward the top.

2. The uppermost York River unit, in the northwestern outcrops (Salmon Branch and Lake Branch areas), consists of a pelecypod-rich calcareous sandstone and siltstone, which caps a transitional zone, an interbedding of the typical Lake Branch and York River facies.

3. The York River formation represents a marine sedimentation. The lithology varies from a typical greenish grey, fine grained muddy sandstone, through reddish, ripple-marked siltstone and sandstone, to grey and reddish shales. The sandstones represent a shore-face to near-shore bar environment. The red ripple-marked, and mud- cracked siltstones presumably represent a tidal flat environment. Red, and grey "flaser" bedded shales and silts represent a "fringe" to a shelf type of marine environment.

4. The York River sandstone is tough, compact, and often silica-cemented along the southern limb: north of the Berry Mountain Syncline axis, the York River is less indurated. It is friable and thin bedded with abundant interstitial clay. 41

5. Sand and shale interbedding within the lower York River formation forms a favourable configuration for source and reservoir possibilities in some sections. However, as observed in the field, owing to the presence of clay in the matrix, the possibility of a good sand reservoir is considered unattractive. Clean and well sorted sandstone are relatively rare.

6. On the basis of field examination, the York River formation developed south of the Synclinal axis appears to attain a relatively higher degree of organic metamorphism. This metamorphic effect appears to be regional.

LAKE BRANCH FORMATION

The term "Lake Branch" formation was introduced by McGerrigle (1950) to the middle, red shaly unit of the Gaspé Sandstone series (Jones 1930). Carbonneau (1959) used the term to include the poorly exposed red shale and siltstone, north of the Big Berry Mountains, along the Salmon Branch, and the Lake Branch (the two principal tributaries of the Cascapedia river), Miner, Go-Ashore, Brandy, and Berry Mountain brooks. A similar lithological interval, but restricted to the upper part of the Battery Point formation, occurs in the Square Forks Valley. The differences between the two, will be enumerated later, in the report.

In the Causapscal area in the Matapedia Valley the Lake Branch formation is 4,000 feet thick and consists of red siltstones intercalated between the more resistant sandstones of dark to dusky red and green colour. Ripple-marks, and ripped-up clay clasts are common.

DISTRIBUTION: The Lake Branch formation, is poorly exposed in an arcuate trend, along the Hyard Lake - Lake Branch Lowland, north of the Big Berry Mountains (figures 4 and 11). LEGENDE-LEGEND

DEVONIEN-DE VON IAN

Granite et felsite 4 13 Granite and felsite 1 Andesite Andesite 12

Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point 10 Lake Branch Lake Branch 9 York River York River 7 Volcaniques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite basalt, andesite 8 Groupe de York Lake ,York Lake S Fortin

Grande Greve Grande Greve 4

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN St-Léon 2 St. Leon (2a) flbr de Baldwin (2a) Baldwin mbr. CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickshock Group Métasédimentaires, méta- Metasediments, meta- volcaniques volcanics

•4. 1•' 10' Faille Fault COUPES ETUDILES SECTIONS INVESTIGATED Axes de plis Fold axes -to . ,, Ruisseau brandy et Brandy N. 7 tlouvelle H. et Cascanec'ia trench 1 Brandy and Brandy N. brooks. du Lac O. Nouvelle n. and Cascaneoia Lake Branch. Contact géologique Geological contact Cascapedia Bras aux Saumons. 2 Salmon Branch. Ruisseau Laron. 8 Caron Brook. 3 Ruisseau Quator:ieme i',ille Milles 0 4 . 8 Miles Fourteen file Brcok. Ruisseau Marcil O. 9 l:arci I l:. broc'c. u• Ruisseau Go-Ashore. Kilometres 10 Kilometres •a w 64 •1•w 4 ECHELLE-SCALE Go-Ashore Brook. Ruisseau Charles Vallee. 10 Charles Valley Brook. Ruisseau liner 5 Miner Brook Route Square Forks, et les Lacs Josué. FIGURE 1 1: DISTRIBUTION GEOGRAPHiQUE, FORMATION DE Lake Branch 11 Souare Forks Road, and Josue Lake. SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Riviére Nouvelle S. GEOGRAPHIC DISTRIBUTION, Lake Branch Formation Couvelie River S. BERRY MOUNTAIN SYNCLINE, QUEBEC, 42

DESCRIPTION:

Huard Lake - Lake Branch Lowland: The Lake Branch is typically red or brownish red in colour with some mottled green or grey streaks. It consists of shales with discretely cross-bedded fine silt or very fine-grained sand laminations. The bedding surface is characteristically irregular. In general, there is a lack of mud-cracks, rain-prints, and rill-marks. Ripple-marks are also relatively rare. There is a pronounced lack of macro or micro-fossils.

The lower contact of the Lake Branch with the York River is gradational, and was observed in the Lake Branch river traverse (approx. loc. lat. 48°35'45" N, long. 66°29'30" W). The York River sandstone (grey to greenish grey, partly oxidised to a brownish colour) is interbedded with red to reddish brown shale and silty shale. This interfingering is approximately 400 feet thick. The red siltstone and silty shales contain numerous beds extremely rich in stunted brachiopod fossils.

Along the Salmon Branch, the York River - Lake Branch contact is poorly exposed, but is interpreted to be more abrupt than that exposed in the Lake Branch area.

Similar gradation is interpreted in the poorly exposed section along the intersection of Miner and Cruiser brooks (loc. lat. 480 39'45" N, long. 66°26' W). Here the red shale is exposed below the uppermost York River sandstone.

Nouvelle South: As shown in enclosure 3, approximately 1,300 feet of section is unexposed above the York River sandstone. This section is presumed to consist of red silty shale. Above this interval, red coloured siltstones and shales attain a thickness of approximately 1,100 feet. This portion contains a red, fine-grained, inclined bedded and ripple-marked sandstone, interbedded with silty 43

shale, and siltstone (200 feet); followed by an approximately 900 foot thick red-weathering silty shale and siltstone.

The red coloured silty shale, siltstone, and sandstone section is included in the Lake Branch formation. The contact is difficult to place due to poor exposure.

The Lower Lake Branch is characterized by a sandstone development which reaches a total thickness of up to 50 feet. One such sand develops near Lake Huard in the west-central part of the area (approx. loc. lat. 48°37'20" N, long. 66°25' W; photograph 15); the other is exposed along Miner brook, near the Cruiser brook confluence (loc. lat. 48°39'45" N, long. 66°26' W). The red coloured sandstone in these outcrops is typically fine to very fine-grained, fairly well sorted, poorly cemented, and festoon-cross-bedded. It is characterized by the presence of shale clasts. The sandstone appears slightly porous on field examination.

Another such sandstone intercalation is exposed a mile south of the Berry Mountain road intersection, along the Trans-Gaspé Highway. Here, the red coloured Lake Branch shales grade from siltstone, into 3-5 foot thick fine-grained, discretely micro-cross-bedded sandstone containing rare evidence of sub-aerial exposure (such as mud-cracks). There is a gradual upward coarsening in the section.

The above mentioned sand units within the Lake Branch shales are differentiated from the red facies equivalents of the Battery Point formation on the following criteria:

1. The Lake Branch sandstone units are characteristically fine to very fine-grained: they lack quartz and igneous rock gravels (above the erosion surfaces) and the shale conglomerate beds 44

frequently encountered in the red facies of the Battery Point.

2. The erosion surfaces in the cross-beds are less frequentin the Lake Branch, than in the Battery Point formation. Also, mud- cracks, rain-prints, rill-marks, or ripple-marks are more frequent in the Battery Point. Small channels are rare in the Lake Branch.

3. The lower sandstone units often contain small shale clasts, but the quartz grains show better sorting and rounding than those of the Battery Point.

4. No point-bar type fluvial cycles are observed within the Lake Branch sandstones.

5. The sandstones do not exceed a possible maximum of 50 feet; average thickness is approximately 25 feet.

6. The Lake Branch lacks fossils.

CONCLUSIONS: Despite poor exposure, and an absence of a continuous section (which could be referred to as the type section), a composite section can be built for a reasonable vertical extent. A fairly good picture of the nature of these sandstones can be formed from the available exposures.

It is considered that the Lake Branch sediments were deposited in a delta fringe and/or lower deltaic plain environment. In this respect it is important to note the lack of widespread sub-aerial exposure, the presence of discretely micro-cross bedded silt and sand laminations, gradual coarsening of the shales into silts and sands, and an absence of channels development.

The fine-grained sands, fairly well sorted, festoon-bedded, containing ripped-up clasts totally enclosed in shales, probably represent 45

distributary channel facies in a delta mouth. In these channels, the energy regime was high and conducive to the deposition of sands in an otherwise (low-energy) shale facies.

The lower Lake Branch sandstones are an interesting objective for stratigraphic trap possibilities in view of the possible presence of intergranular porosity, and the fact that they are enclosed in shale. However, no hydrocarbon shows, seeps, or pyrobitumen were observed in the sandstone outcrops.

The oxidised nature of the Lake Branch shales is unfavourable for the preservation of source organic matter.

BATTERY POINT FORMATION

In eastern Gaspé, the Battery Point formation forms the upper part of the Gaspé Sandstone series. The type section of the formation situated near Gaspé town (in eastern Gaspé), was described in 1863 by William Logan.

A description of the eastern Gaspé Battery Point development is considered relevant to this study. The formation there consists of two distinct parts: The lower part consists of a bright greenish-grey, fine to coarse grained, highly cross-bedded, occasionally pebbly sandstone containing subrounded quartz, granite and quartzite pebbles in a medium to coarse grained sand matrix. Thin conglomerate beds and flat sub-parallel erosion surfaces are common. Feldspar is typically pink in colour.

The upper part of the formation in eastern Gaspé, consists of variously coloured red and brown sandstone, shale and conglomerate. Some beds are mottled to streaked red-brown and green. This portion of the section contains frequent ripple-marks, mud-cracks, rain-prints, trough-cross-bedding, and channel development suggesting a continental 46 sedimentation with periodic exposure.

DISTRIBUTION: Within the study area, the Battery Point sandstones are best developed in the Big Berry Mountains Highland (extending across the Cascapedia river), along the central part of the Berry Mountain Syncline. Exposures are extremely poor, and inacessible. Relief is high, and the steep slopes are often covered with boulder debris (photograph 17).

South of the Square Forks river, a similar sandstone development takes place, which in view of the stratigraphic and structural re- lations, is considered to be equivalent to the Battery Point. On the southern limb of the Syncline, the Battery Point directly overlies the York River (figure 12).

DESCRIPTION: The Battery Point lighological characters as developed along the Big Berry Mountains ridge are considered as typical. The formation consists of a greenish grey, less commonly brownish maroon, highly trough-cross-bedded, fine to coarse-grained, subrounded to subangular, light grey to pinkish grey weathering, pink-feldspathic sandstone. It is tougher than the underlying York River sandstone. The Battery Point is monotonous in sedimentary features. It lacks extensive gravel or pebble and shale interbeds.

In the eastern part of the Big Berry Mountains, north of the Charles Vallée Camp (approx. loc. lat. 48°35'10" N, long. 66°5'50" W), the Battery Point consists of bright greenish grey, medium to coarse grained, slightly conglomeratic, thick to massive bedded, and highly cross-bedded silica-cemented sandstone. Bedding is low dipping, but the true inclination of bedding is difficult to estimate. The base of the cross-beds is marked by a coarse sandstone, and less commonly by fine granules and shale conglomerates, usually 4 inch in diameter, consisting of white to pink quartz, igneous rock, and quartzite. Small, floating, well rounded pebbles are also observed in the sand matrix (Photograph 18). Only the lower 750-1,000 feet of Battery Point is exposed. LEGENDE-LEGEND

DEVONIEN-DEVONIAN

Granite and felsite Granite et felsite 13

Andesite Andesite 12 1 Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point 10 Lake Branch Lake Branch 9 York River York River 7 Volcaniques, rhyolite, Voltanics, rhyolite, 6 basalte, andesite basalt, andesite B Groupe de York Lake .York Lake 5 Fortin

Grande Grève Grande Greve 4

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN St -Léon St. Leon 2 1 (2a) iibr de Baldwin (2a) Baldwin mbr. CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickshock Group Mdtasédimentaires, méta- Metasediments, meta - volcaniques volcanics

Faille Fault COUPES ETUDItES SECTIONS INVESTIGATED Axes de plis Fold axes Ruisseau brandy et Brandy N. 7 Nouvelle N. et Cascanec'ia L'ranch 1 Brandy and Brandy N. brooks. du Lac O. Nouvelle N. and Cascanedia Lake Branch. Contact géologique Geological contact Cascapedla Bras aux Saunons. 2 Salmon Branch. Ruisseau Laron. 8 Caron Brook. 3 Ruisseau Quator:leme Lille Milles O 4 •g Miles Fourteen file Brcok. Ruisseau Marcil O. 9 Mardi I:. broc'<. Kilomètres 10 Kilometres Ruisseau Go-Ashore. ECHELLE-SCALE 4 Go-Ashore Brook. Nvisseau Charles Vallee. 10 Charles Valley Brook. Ruisseau liner 5 (liner Brook Route Square Forks, et les Lacs Josué. FiGURE 12 DISTRIBUTION GEOGRAPHiQUE, FORMATION DE Battery Point' 11 Square Forks Road, and Josue Lake, SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. b Cascapedla Branche du Lac. Lake Branch. 12 Riviere l!ouvelle S. GEOGRAPHIC DISTRIBUTION, Battery Point Formation l'ouvelle River S. BERRY MOUNTAIN SYNCLINE, QUEBEC. 47

The traverses made east of the Cascapedia river, along Cold- water, and Indian Falls brooks, reveal a Battery Point lithology similar to that exposed north of the Charles Vallée Camp.

Square Forks Valley contains Battery Point of a similar lithology to that described above. One-half mile west of the bridge, along the Square Forks river (approx. loc. lat. 48°34'45" N, long. 66°13'55" W) several 5 foot thick chocolate brown shales develop in the Battery Point (Photograph 22). These shales are overlain by a massive, highly cross- bedded channel sand. A conglomerate bed characterizes the base of the overlying sands. Poor exposure does not permit further elaboration, but it appears that this exposure may represent a point-bar type fining-upward sedimentation.

The traverses made along the south flowing streams, in the central Big Berry Mountains ridge (approx. loc. lat. 48°37' N, long. 66° 20' W) reveal a south dipping section consisting of a typical lower Battery Point sandstone development. It consists of a greenish-grey, less frequently brownish maroon coloured, fine-to medium grained, subrounded, massive bedded, extensively trough-cross-bedded, tough, pink weathering, feldspar (orthoclase)-rich sandstone. The base of the individual cross- beds is marked by white to pink quartz and igneous rock granules. These beds grade upward into thin to thick bedded, fine grained sandstone, and siltstone; and greenish-grey silty shale containing dark grey shale clasts (Photograph 19), which in turn, are overlain by a red, thinly laminated silty shale, referred to as "Square Forks facies" in this report.

The red silty shales, and sands with minor silt, cover the width of the Square Forks Valley: they attain a total thickness of approximately 1,500 feet.

These shales contain a 100 foot thick, very fine-grained sandstone unit, exposed half a mile east from the Josué Lake road Junction, along the Square Forks road (approx. loc. lat. 48°34'38" N, long. 66°17' 40" W). The sandstone is typically red to chocolate brown in colour; 48

frequently cross-bedded and mud-cracked, occasionally ripple-marked, and contains thin pebble beds, and shale conglomerates (Photographs 24, 25).

Similar sand units are exposed along the West Square Forks Road, approximately 7 miles west of the outcrop described above. Here, the lower part of the unit grades downward into thinly bedded shales and siltstones of chocolate brown colour, which are in turn underlain by greenish grey and brownish maroon coloured Battery Point sandstones overlying the York River sandstone. A fault may separate the York River from the Battery Point. Thickness calculations in the west Square Forks Road area hazardous due to poorly exposed large foreset beds coupled with structural complications, especially in the southern part of the area. The total thickness of the typical Battery Point sandstone is estimated to be 8,000 feet in the central Big Berry Mountains area.

A subdued east-west trending Big Berry Mountains ridge crosses the Lake Branch river to the west. Although the geological contacts are poorly exposed, this ridge (loc. lat. 48°36', long. 66°28'), as observed along the stream traverses, is made up of the typical greenish Battery Point sandstone. It appears that the sandstone markers in the Lake Branch abut against the Lake Branch - Battery Point contact, suggesting an uncon- formable or a faulted contact. Thus, a pre-Battery Point warping of the central Gaspé area is a possibility. Poor exposure does not allow further elaboration.

Along the western part of the Square Forks road (loc. lat. 48°34', long. 66°26' W; and lat. 48°31'30" N, long. 66°35' W) several red silt and fine grained sandstone units are exposed within the red shales.

Along the west Square Forks road (loc. lat. 48°31'30" N, long. 66°33'30" W), fine grained red sandstone, siltstone, and shale are exposed in a strike section. These sandstones show evidence of a shallow water deposition with occasional subaerial exposure. 49

Further west, along the road to Nouvelle, the Battery Point sandstones are mainly red to reddish brown, highly cross-bedded, ripple- marked, mud-cracked, and contain rain-prints. They also show channel development and scouring. The sandstone contains 3-5 foot thick conglomerate beds with abundant shale clasts. The shale beds are highly lenticular. No cyclic sedimentation is evident.

A northerly direction, is suggested from rill-marks (Photograph 28).

CONCLUSIONS: A high energy shallow-water fluvial deposition with frequent subaerial exposure in the upper part of the Battery Point, suggests a sedimentation process markedly different form that of the lower Battery Point.

The red sandstones and shales constitute the upper Battery Point, best exposed in the western part of the area. In the absence of time markers, it is difficult to define precise lateral facies variations. However, the red facies appears to attain a greater thickness in the western part of the area than to the east; this seems to occur at the expense of the typical Battery Point facies. It is illustrated in Enclo- sure 3. Figure 6a outlines the author's ideas on the mutual relationship between the two facies in an east-west direction. The following lithological subdivisions are proposed for the Battery Point.

Unit 2. "Square Forks facies" consists of streaked red to brownish red, green, fine to medium grained, frequently cross-bedded, medium to thick bedded silty sandstone. It contains minor shale, and conglomerate. Ripple-marks, rain-prints, mud- cracks, and channels are common. It is 3,000 feet thick in the Nouvelle River area. In the Square Forks River area, the facies consists of approximately 1,500 feet of red shale and siltstone, and red, fine grained, cross-bedded silty sandstone with minor shale clasts. 50

Unit 1. "Typical" Battery Point Sandstone consists of a monotonous bright greenish-grey, rarely reddish, fine to medium grained, trough-cross-bedded, pink-feldspar-rich sandstone. It attains a thickness of 8,000 feet in the central Big Berry Mountains but thins westward.

The "Square Forks" facies resembles the Lake Branch in gross lithological characters. However, it is lithologically more variable and its depotisional environment is envisaged as distinctly different (possibly continental fan as against a deltaic fringe and/or lower deltaic plain environment for the Lake Branch). The Square Forks facies presumably forms stratigraphically the highest exposed Battery Point in the south-western part of the area. The development of the upper, red facies, appears to be similar to that in eastern Gaspé (McGerrigle, 1950, p. 85). Tr CORRELATION AND ENVIRONMENTAL PALEONTOLOGY

The following macro-fossils were identified by Dr. A.J. Boucot (written communication, 1975) through the cooperation of Dr. P.-A. Bourque of Université Laval.

York River formation: Spirifer gaspensis, Cypricardinia, Pterineoid, Globithyrid, Globithyris sp., Loxonema sp., Rhenorensselaria: Siegenian or Emsian.

Greenish-grey (York River-type) sandstone in dark grey shale along the Nouvelle road section contains Etymothyris.

Grande Grève formation: Leptocoelia cg. L. flabellites (from bentonite bed), Acrospirifer murchisoni.

Cap taon Ami formation: Leptocoelia, Protochonetes, Cypricardinia, and crinoidal debris. Occasional isolated corals were obser- bed in the Cap Bon Ami, Grande Grève, and York Lake formations.

Boucot (1970) has used various Early Devonian brachiopod communities to characterize the bathymetry for the Siegenian and Emsian basins. According to him, the Costellirostra community characterizes deep water, the Chonostrophia-Chonostrophiella represents relatively shallow water, and the Globithyrinid community represents an extremely shallow environment normally unfavourable to other brachiopod taxa, and is characterized by carbonaceous and pyrite-rich facies.

The first two communities contain numerous fossils restricted to the Etymothyris zone which separates the relatively shallow from the deep marine environment. The Globithyrinid community consists of abundant Globithyris and/or Rhenorensselaeria, normally associated with abundant pelecypods in the Appalachian biogeographic province. It is also highly restricted in taxonomic diversity compared with other coexisting communities. 52

It is significant that in the Charles Vallée road section, the genera belonging to the Globithyrinid community were observed in the York River formation below a frequently sandy, and presumably relatively shallow water unit (described as "typically" York River in the text), and above a predominantly shaly section interpreted to have been deposited in relatively deeper marine conditions.

The presence of Globithyris below the thick upper sandstone interval in the Josué Lake section suggests similar conditions as interpreted for the Charles Vallée road section.

In the Nouvelle South section, Etymothyris was identified in a "York River-type" sandstone unit in a dark shale (resembling Fortin lithology) at the gradational lower contact of the York River. Thus, relatively deeper conditions are invoked for the basal York River sedimentation.

Globithyrid was also observed in the upper York River of the Lake Branch Section (identified in the field as SW Lake Huard Section), and the upper part of the Salmon Branch Section (characterized by abundant divergent ripple marks, and dessication structures).

The Rhenorensselaeria, noted in the lower part of the York River formation (exposed in the Lake Branch section), suggests a shallow water sedimentation in the early York River time.

The overall facies interpretations based on the brachiopod communities are in general agreement with sedimentological observations. The early York River in the southern part of the area was characterized by a relatively deeper marine environment, which rapidly regressed into shallower marine facies before being overcome by a continental deposition in Battery Point time. 53

In the northern part of the Syncline, the York River was deposited mainly in a shallow coastal to near-shore marine, or brackish- transitional facies. It was followed by a deltaic sedimentation in Lake Branch time, and a continental fluvial sedimentation in Battery Point time.

The Lake Branch and the Battery Point were found to be barren. Stunted brachiopods, and bivalves were observed in an interbedding zone between the Lake Branch and the York River. Fossils, other than plant fragments, are generally absent from the Battery Point formation.

Carbonneau (1959) included a complete list of macro-fossils collected in the Richard-Gravier map-area. No attempt is made to improve on this list in view of a different aim of the present report. A list and location map of fossils identified in this report is included in the Appendices.

Preliminary palynostratigraphic work on the field samples was undertaken by the INRS-Pétrole staff (Dr. J. Utting). A lower Devonian, Siegenian-Emsian age is evident for the York Lake and York River formations. The Battery Point extends into the Eifelian (Middle Devonian) stage. The Lake Branch is therefore interpreted to be Emsian-Eifelian in age. The palynostratigraphy chapter of the INRS-Pétrole report is reproduced in the appendices of this report. PALEOGEOGRAPHY

INTRODUCTION

The paleogeographic setting for the Gaspé Sandstone series in the area is derived from the following considerations:

1. Regional stratigraphic considerations of the underlying formations. 2. Regional stratigraphic considerations of the Gaspé Sandstone series. 3. Clastic deltaic models interpreted on the basis of sedimentary character as outlined in this report. 4. Current directions and gross lithologic characters within the Gaspé Sandstone.

Regional stratigraphic considerations are largely based on the outlines of the regional basinal configurations in the Paleozoic as described by Skidmore (1970).

During the Silurian, the area was the site of a continued basinal sedimentation of fine grained clastics and limestone. Along the platform edges to the northeast and west, some reefal and bioclastic limestone were locally deposited: However, within the study area and immediately to the north, shale, siltstone, and very fine sandstone, with minor limestone were deposited.

The Silurian ended with a siltstone and limestone platform surrounding a central elongate shale basin. This central basin accumul- ated approximately 9,000 feet of fine clastics and volcanics.

The Lower Devonian commenced with a similar basinal configuration, with the exception that the siltstone and limestone were replaced by shallow open marine, shaly limestone, siltstone and shale in the 55 peripheral areas, surrounding a central shale (with minor carbonates and volcanics) basin. This northeast-southwest trending elongate basin existed through a greater part of the Lower Devonian (Cap Bon Ami - Grande Grève), and toward the end of the Grande Grève the limestone platform was inundated by a clastic influx through coastal accretion (in York Lake and York River times). These sands were deposited in interdeltaic areas; the source of the sediments is presumed to be distant.

The coastal sands were overridden by the deltaic interface sediments of the Lake Branch and were followed by the fluvial sands of the Battery Point. It appears from the regional considerations that the central shale basin, which existed in the early lower Devonian times, may have been filled up by Lake Branch - Battery Point times. This aspect is further discussed later in this chapter.

DEPOSITIONAL ENVIRONMENT

The depositional models envisaged for the clastic environment are summarized in Figure 13. The general ideas on the paleo-environment concepts in this report are based on a number of works, largely undertaken on Recent sediments along the Gulf Coast, and on the Cretaceous clastic basins of the mid-western United States. The works published by the following workers are relevant to the discussion on environmental interpretation: Allen (1965b), Berg and Davies (1968), Bernard et al (1970), Davies et al (1968), Fisk (1961), Fisk et al (1954), Hoyt (1967), Lane (1963), LeBlanc (1972), Pettijohn and Potter (1964), Potter (1967), Sabin (1963), Visher (1965), and Weimer (1966).

Figure 13 is included to provide a reference to the framework of nomenclature used in this report, and to better identify the suggested model. The illustrative diagrams are based on the known modern clastic depositional models. It is difficult to fit a thick rock sequence, deposited over a large geographic area, into specific depositional models, especially a unit as variable as the Gaspé Sandstone. An

Cy ENVIRONMENTS fNti'IRQS:T£ MEN TS ..••~~

1 ''• ALLUVIAL FANS ,- 2 CHA:NELS • ///\I\` ALLUVIAL FANS }` 'i.YNES ALLLY:ACX ' + CSF"wUX J \ - CCTS ALLWI:LX •'a '~ \ ( •\~ IVVV I , PAVEHENT lHHJSA f~ \\` F1:T!_ 5•' Â 4 ALLUVIAL 2 CnAHNElS , BARS ,, ~~ ~ ~ 5k1~ ' (RVYIFL) BRAIDED STREAMS 2 `. ~'~~i ' CHANNELS [XEA'AUX, 8.7:.F_S BRAIDED 1 ~,•~FE ~ STREAM ; -.~ ~• '4 ,:11./1. FLO'ODBASINS 1 ''~~!!! ' û"n {' CHENAUX ALLLH'IAL CHENAUX E.T `{ I ~1lt ! TP SSES PAS.: CUE EN v I.}~p, ij{` D'IhD.S'DA7:0.4 \`•e , \~ (FLUVIATILE) ThESSES • I 2 CHAL:NELS [~ 1 I r ~.

L..7-Tr. J

.. Z 2 RID .;Ta PE.ACHES•d" u ` .' é INNER CARRIERS FRINGE

TA f511'.4RINE

N I ~Ivlc' ` DnLR INE NT DEL AI

R ?XIUIRBARS, - - - RO U M

BORDURE F D PLACES A :.ARR_f SES - OPA DUTER 1 - ` ~ DE:LTil A- S 'YI ME- EXTEF.'.T ~ D'ESTL'AR:EN RC; ELT Fü D F. 0151AL 1 FU ELCISNEE ~ ~ 1 2 3 BARRIER BEACH ti BARRIER ISLANDS Plc". d. row. BURLIER ILL'S-BA.RIERES BA.RRIEYLS PLACES Tidal not -- ISLAND COMPLEX =v.' COASTAL PLAIN y \~__ COASTAL 2 BEACH ~ -% 4 INTER- CHEFLILR P:~ITS f i ~, Cc.yLEXS DELTAIC .... PLAINE CLYIIEE3' TIDAL FLATS C Lo.~~;:•e'~

Wy 1 CANYChS CANTONS 1 ....„.,..._...... _7<::`~~ • ~ ~ CFNSITT ~ } G, CU•N6ENTS SLOP[ d CEEB 2 ..%f'.•~~~ ~~~N 'TU78IDITE2' • TURBIOl1E5" )L'ATë A F.'ND ,/~_\ ~ BARS & NLTAS _ _- • ••Ï:> , ' ".YaI(:T£S" CY'CBAN,'.^ 3 • . IT LLTSI'YE Q:£S A Id'ITAS ., '' <•p°Y "IL'h91D:7£S" iPENCH d ~~~ ~l~~~ :hA.S:R.'EFS r`~

!3 1- INURE 2B: SOYtAIRE DES MRIDELES D'BNVIRCM:HEMFNT POUR LA SED IY.ENTAT ION [LANE 10...E

.CCMDIIAT ION OF EPVIRONY,EII1 YA)DELS FOR CLASTIC SEDIMENTATION.

.oY9Rln_..rm'v.trmYfY1Yt3T•1TTi►SYSl.Y1J!1 !FJ' Figure 14: Frequency listing of lithological and sedimentary features

Gaspe Sandstone Units •

o te ion ion O tes t t ding te, a ra tes, a dding cyp a a d r ta br

in le be

ds te lome

FORMATIONS be l, s- r

ks lomer lome ng lam

Pe dimen r ion ve ts ts os ous war

ks d, ng t co in se cr ra in d ve dding o ba cong co t ma up rac r Pr tone op cas le h g on be

W O V) O ing h an e ts tr te tu r- L rC .0 c

in d ac CO U r S- l - r LL [L) Fin Fis bio Flu Ripp Be Gas Ra Dun Disc Si Mu N - CD CONTINENTAL TRANSITIONAL MARINE

Battery Point Square Forks R AMT A C C C. X C A A C R C X A A C X X X X X X X R R X C X X X C X X X X facies Typical Bat- XRMTAXXCXX XAAACRAP AXX X X X X X X X X XXX XXXX X X tery Point

Lake Branch X A L C X X R X X R C C C X X/ C/ X X X X X X X C C R A A A X A X X X X

York River X R. TH R X X X. R X X R R X X X C R R X X X X A C X C A C A C C/ A R C R C

,"York Lake" X . X TH X X X X X X X X X X X X C R X X X X X X X X C A/// X A A R R R R

Bedding: M = massive, T = thick, M = medium, TN = thin, L = lamination

Frequency: A = abundant, C = common, R = rare, / = very rare, X = absent or not observed 56 attempt, nevertheless, is made in proposing environmental models for each major lithological unit.

YORK RIVER FORMATION: The York River consists mainly of very fine to fine grained, low angle-cross bedded, poorly to medium sorted sandstone containing flat erosion surfaces. These sand units with gradational lower contacts, and very thin to thin stratification, represent a near-shore coastal plain environment. Evidence of subaerial exposure, oxidation, or leaching are generally lacking in the upper parts of the sand units.

The sands are accompanied by grey to dark grey marine shales, presumably representing open marine to partly restricted "lagoonal" conditions. A general lackof layered organic matter or pyrite-rich shales in the York River suggests that the lagoonal conditions, as observed in the Gulf Coast region, were not widespread.

Highly ripple-marked siltstone and silty shale with asymmetric to symmetric ripples (with highly divergent axes in adjacent strata), occasionally mud-cracked, and slumped, represent shallow marine to subaerial conditions in a broad shallow shelf to a tidal-flat environment.

Thus the York River, at least in the northern part of the area, was deposited in a barrier island-bar complex environment. A lack of good sorting, and the presence of abundant clays in the matrix, however, are difficult to account for in terms of the experience in Modern examples, but these may be partially explained by invoking low energy marine currents, with insufficient capacity to winnow away the finer fractions. A diagenetic origin of the clay (illite-chlorite) matrix cannot be completely ruled out (see Reservoir Potential, chapter 7.1.3).

The lower York River in the southern part of the area, which consists mostly of grey to dark grey shale, flat to inclined, and cross bedded sandstones with planar erosion surfaces, and laminated shales containing "flaser bedding", was probably deposited in an interdeltaic, 57

normal marine shelf or neritic (1.2.3.3) to possibly coastal plain chenier (2.1.2.2) environment. It would be appropriate to emphasize that the York River in the southern area does not demonstrate turbidity current features, such as graded bedding.

The upper York River in the southern area, on the other hand, contains thin to thick bedded "typical" York River sandstones and shales. The abrupt, but non-erosional lower contacts of the sand units, gentle cross-bedding, and gradational upper contacts suggest that these were presumably deposited as offshore marine bars in a neritic environment.

LAKE BRANCH FORMATION: The Lake Branch consists mainly of silty shales with very fine grained sand and silt interbeds, which are frequently' micro-cross-bedded. The shales are often irregularly bedded, and bioturbated. The sandstones generally show gradational, but occasionally erosional,lower contacts. They are cross-bedded on a large scale, with smooth bottom-sets, and partly eroded foresets. Evidence for sub-aerial exposure, although present, is not common.

The Lake Branch formation is considered to have been deposited in a lower deltaic plain environment, inter-distributary area (2.2.3.1) and/or the inner-fringe (2.2.2.2) of a delta (Figure 13). The shale with minor silt is the main lithology, and encloses 25 to 50 foot thick high energy sandstone lenses, presumably formed in mouth bars or distributary channels.

The Lake Branch formation in the area represents a transitional facies edge of a north or northwestward prograding, presumably arcuate shaped delta.

BATTERY POINT FORMATION: The typical, greenish grey, Battery Point sandstones were deposited in meander belts or braided stream channels, either in the upper deltaic flood plain (2.2.4.2) or in the fluvial continental (3.2.1 or 3.2.2) environment (Figure 13). 58

This depositional environment characterizes the upper deltaic plain, in a transitional environment (2.2.4.2), or the lower part of a meandering system in a continental fluvial environment (3.2.1 or 3.2.2). A lack of shale interbeds and fining-upwards cycles (Allen, 1965) suggests that the classic point-bar depositional cycles are poorly developed.

The red-bed facies of the upper, highly cross-bedded Battery Point sandstone, containing minor conglomerate, channels, dessication cracks, and rain prints, suggests that these were deposited as alluvial fans (3.2.3), possibly in the upper reaches of a widespread arid to semi- arid flood plain.

A slight flexuring of the area may have occurred prior to the Battery Point deposition.

CURRENT DIRECTIONS

The current directions were mainly derived from the foreset bed inclinations. The cross-bedding observations were corrected to the horizontal with a stereographic net. The corrected directions are shown as mean directions in Figures 15 and 16.

Insufficient data were collected on flute and groove marks to serve as plaeo-current indicators: also, the ripple-marks observed in the area were largely of oscillation type, which did not permit current direction interpretations, especially beause a divergence in the ripple trends in adjacent strata is frequent in the York River formation.

The paleo-current directions show a high degree of variation. On a rosette diagram, they are bimodal or polymodal.

The inclined-bedding directions in the York River, despite a high degree of variation, suggest a southerly to southeasterly average. This possibly indicates an E-W to NE-SW trending coastline. This coastal

>.9

,e25 66 CO 65 35 W

50°N COUPES ETUDIEES/SECTIOIS INVESTIGATED: York River I. Ruis. Brandy, Brandy N. 171 Brandy, Brandy N.Br. 49° Volcaniques 2. Cascapedia aras aux Saumons. Volcanics Salmon Branch. 48° Localisation d'une coupe 3. Cascapedia Branche du'Lac. Location of section Lake Branch.

"O Faille / Fault 68° nao 6 6t°w -- 4. Branche du Lac 0./ Lake Branch W.

Isopaque approximatif 5. Ruis. Caron / Caron Cr. Nombre d'observations Approximate isopach 43 Number of observations 6. Ruis. Marcil 0./ Mardi W. Br.

Milles 0 4 8 Miles 7. Ruis. Charles Vallée Br. Kilomètres Kilometres ECUELLE-SCALE ,1h B, Riv. Nouvelle S./ Nouvelle R. S.

FIGURE 15: CARTE. 1SOPAQUE, DIRECTIONS DES PALEO-COURANTS, FORMATION DE YORK RIVER, SYNCLINAL DE BEkRY MOUNTAIN, QUEBEC.

ISOPACH MAP, PALEO-CURRENT DIRECTIONS, YORK RIVER FORMATION, BERRY MOUNTAIN SYNCLINE, QUEBEC. 59

trend is also inferred from a regional southward shale-out of the York River sandstones. The York River also shows a westward or southwestward fining in grain size within the area (Théroux, 1974).

A few cross-bedding directions on the Lake Branch sandstones, indicate a northeasterly flow. Thus, it is suggested that the central Gaspé shale basin, as outlined earlier in the report, was filled up by Lake Branch time; and from here on the deltaic systems extended northwestward and northward across the central shale basin. The northeasterly direction observed in the Lake Huard locality may been situated on a northeasterly flowing channel.

The Battery Point paleo-current directions are extremely variable owing to the obvious fluvial character of these sandstones. The composite diagram of over 200 observations shows a predominant westward average (figure 16). In the individual localities the direction is extremely dispersed and at times meaningless, but a westerly to southeasterly trend is apparent. Such a diversity in current direction is presumably owing to the deposition of the sands in braided channels, where the streams meander in all many directions. It is possible that more data on the Battery Point paleo-current directions would yield a more definitive average direction.

Thus, a southwestward or westward progradation of the Battery Point fluvial system is apparent from the cross-bedding. The area was situated downstream from the eastern Gaspé area. This is suggested also by the fact that the Battery Point in central Gaspé is finer grained than that observed in most outcrops visited in eastern Gaspé during the summer: It also lacks conglomerate and gravel beds. Mason (1971) also noted generally westward current directions in the Battery Point in eastern Gaspé.

The Battery Point sedimentation terminated with an alluvial fan type of sedimentation (as discussed earlier in the chapter). Poor available data suggest a northward current direction in this facies.

48%0N DIP MAMME COMPOSE COMPOSITE DIAGRAM

• as•

• • • N

.., X. ti ....- \ / --- ‘ \ / ‘ • OBSERVATIONS ..'757.775777-1gM - „..:— s/s ‘ 206 / ...... ,... .... .. a..... " \ : ...... 7?..? • -**..A:..,'...... -,...f.f..,im..m ,f.:...i,, .0

30'

A11375 l 4 B'25 i 6°39 30' 66°00W 1 1

56'113ATTERY POINT CoupesttUdié6s/Sections investigated: 1 FACIES SQUARE FORKS , FACIES DE SQUARE FORKS Big Berry Mountains centrale 1 i Central Big Berry Mountains 1 TYPICAL BATTERY POINT i BAT1ERY POINT TYPIQUE Rivi6re Square Forks F-1 2 River i Square Forks , Faille • Fault Les lacs Josu6 3 Josue Lakes Localisation ddune coupe :48a8881 i 68° 6 6e Location of section i 1 Epaisseur calculée I 7.400 2 I Thickness calculated Milles 0 4 çMiles 2 Nombre d'observations 1 34 KilomOtres 10 Kilometres I Number of observations ECNELLE-SCALE

Direction moyerne du courant Mean current direction

FIGURE 16: EPAISSEUR ESTIMEE, DIRECTIONS DES PALE0- COURANTS, FORMATION DE BATTERY POINT, SYNCLINAL DE BERRY MOUNTAIN, QUEBEC.

TPICKNESS ESTIMATES, PALEO-CURRENT DIRECTIONS, • BATTERY POINT FORMATION, BERRY MOUNTAIN SYNCLINE, QUEBEC. 60

CONCLUSIONS

It is thus concluded that the Gaspé Sandstone series was deposited in a complex variety of sedimentary environments associated with an overall regressive phase in the Lower to Middle Devonian. In pre-York River time, the area was situated on a southeast sloping platform, where calcareous shales, accompanied by silty and argillaceous limestone containing frequent brachiopods and isolated corals were deposited. The platform constituted the northern flank of a marine embayment (opening to the southwest) that succeeded the Silurian trough, and extended parallel with the Gaspé Peninsula (Burke, 1964, Lajoie et ai, 1968, and Skidmore, 1970).

A continued shallowing of the marine basin shelf characterized the upper Gaspé Limestone series, suggested by the replacement of the shale-silt interbedding by argillaceous and silty lime-mud, especially in the northern part of the area. To the south and southeast, however, the equivalent basinal sediments consisted of shale, silt, volcanics and minor limestone.

The first coarse clastic incursion into the carbonate platform was presumably carried from the east and northeast by weak marine currents, and sand and limestone interbeds were deposited in the shallow parts of the basin, situated to the north.

The time-equivalent sediments in the central part of the area, consisted of argillaceous limestone, and in the southern part, the above mentioned basinal sediments.

In York River time poorly sorted sandstone, siltstone, and shale were deposited in a shallow marine environment in the northwestern part of the shelf. Tidal-flat and lagoonal conditions persisted into the upper York River in the coastal areas. 61

The central marine trough appears to have been filled in by the end of York River time. A northwestward to northward prograding delta advanced into a rapidly west-receding marine embayment. The delta mouth possibly occupied the northern limb of the Berry Mountain Syncline, and resulted in the deposition of bioturbated shale and silt, and high energy sand lenses.

In Battery Point time, the area was overrun by a west or southwest flowing fluvial system. The sedimentological and lithological characters suggest that, generally speaking, an upper fluvial environment prevailed over the area. A meandering and braided stream system occupied largely the eastern part of the Berry Mountain Syncline; whereas the southwestern part was occupied by an alluvial fan system. The lateral and vertical transition between the two environments (characterized in this report by the "typical Battery Point facies" and the "Square Forks facies"respectively) is gradual.

The above ideas on paleogeography are summed up in the illustrative diagrams in figure 17. YC!K LAVE TûRK ERT.R ruin. fF.al.f.,.. a+,ilia..) ( .orl...) (r.'.,ilil .6.If I 1Ca+,.o1

A A

:EEiK,

WILE Ce71 SILT CASSIN.ry M SILT

VtS A OqIN FIN ME WINES SANnr:t

LI141T'Jt ~ 1 Il5? EBAB_H 'ExTRY P:1NT iFlaia. J.Ilaia.. iafiri..n) Ita...a.. ..1:...., .~ a,J..d CtAtTIatS AFt DEt FSNITS Q CL:t7I1-3 SIN /CRIpCIC (S,.id.d ..d .•1.41,s . ~ll.a~,) :E .-'.5i TAllm; +' l'E. X Cf55IC+T:w: Ti.t FLATS. II

SCI'iNT. R3 COINS II;JL •ALLVAIAL FIS• STSIIÇAI NSA~. l FLL•.I,7iLL3 ~ES nln/u•~fA tFA1CC1 SIV C.E\!N fA ittlït sm:rs ""44

Fil YL.:C.SF /MS: ...YE

FIGURE 17: DIAGRAMES ENVISAGES ILLUSTRANT L'ENVIRONNEMENT SEDCiE ITAI RE POUR LA SERTE DES GRES DE GASPE, SY`CLINPL DE BERRY MOUNTAIN, QUEBEC. A ILLUSTRATIVE DIAGRAMS ENVISAGING A 6 SEDIMENTARY ENVIRON1ENT FOR THE LITHOLOGIC.AL UNITS OF THE GASPE ~ ~ — _— v~-- SANDSTONE SERIES, BERRY MOUNTAIN SNCLINE, QUEBEC. VOLCANIC AND GRANITIC ROCKS

VOLCANIC ROCKS

Because of the obvious petroleum-oriented objectives of this report the volcanic rocks have only been given a cursory attention. However, the volcanic rock contacts have been examined as closely as permitted by the generally poor exposure. The following description is a compilation of the previously published reports, and field descriptions. The interpreted thicknesses are shown in the geologic sections (Enclosures 2 and 3).

1. The oldest volcanic rocks in the study area, described by Burke (1964) as the Baldwin member of the St. Léon are exposed along the flanks of the Josué anticline. These were traversed mainly along Josué brook (loc. lat. 48°28'20" N, long. 66°11'10" W), Marcil brook (loc. lat. 448°35'50" N, long. 65°59'20" W), and further to the east, along Caron brook.

The volcanics consist of andesite, rhyolite, and basalt with minor tuff. Andesites, being by far the most common constituent, are medium to fine grained, porphyritic, and ophitic in texture. In some areas, such as to the south of Charles Vallée, pillows are observed. Rhyolite flows and volcanic breccia are frequent in the southern limb of the Josué anticline.

Carbonneau (1959) described the presence of small dykes and various other small igneous bodies in the Silurian rocks.

Faint pyrite mineralization was observed in a grey rhyolite flow along the Caron brook section (loc. lat. 48°35'50" N, long. 65° 59'20" W): Mineralized stringers on the average are 5 mm long, and 1 mm thick. 63

2. An enormous thickness of volcanics and pyroclastics is present in the western part of the area, presumably at the Cap Bon Ami Grande Grève contact: It appears that they occur along the structural nose of a regional fold north and northwest of the Lacroix Lumber Camp (loc. 48°39' N, long. 66°34' W; and lat. 48°34'30" N, long. 66°37' W). These low-dipping, and poorly mapped volcanic rocks are widespread, but appear to be restricted along strike. The brown weathering rarely amygdaloidal basalt, occasionally shows pillow structures along the new CIP road cut (photograph 3).

Grey to dark greenish-grey, medium to coarse grained, crumbly basaltic pyroclastic rocks are partly silicified. The fragment edges show chilling effects; silica growth rings are also evident. Greenish chalcedony is common. White to pinkish white secondary quartz appears to constitute upto 20% of the rock.

The limestone in the vicinity of the volcanics is recrystallized, and locally calcite veined.

3. Yellowish cream to reddish coloured cryptocrystalline rhyolites intrude the Grande Grève and Cap Bon Ami calcareous shales in the northern part of the area (Lemieux Anticline).

The acidic rocks consist of light green, grey-pink, or reddish feldspar porphyry. The groundmass consists of cryptocrystalline quartz, and feldspar. The latter is occasionally highly altered. Quartz crystals, showing growth rings, are apparently formed by a later introduction of silica. Apatite and zircon also occur as small crystals in the rhyolite groundmass.

4. The geologic interval between the Grande Grève and the York River, that is, the York Lake in many sections, is frequently occupied by volcanic rocks. 64

In the northern and northeastern part of the area, the volcanics cover a large territory, situated to the north of the lower boundary of the York River, and exposed around the Lemieux anticline (loc. lat. 48°48' N, and long. 68°10' W). They are often intruded by acidic intrusives.

5. Along the northwestern part of the area, the York Lake volcanics form a rugged arcuate northeast - southwest trending ridge. Several local peaks, such as Conical Mountain and Squaw Cap, occur in this trend. These rocks were observed along Go-Ashore, Cruiser, and Miner brooks and the Salmon and Lake Branches.

Along Cruiser and Miner brooks, the volcanics consist of basalt, with intrusives of diabase. Limestone in contact with the diabase is baked (Carbonneau, 1959, p. 27).

Along the Salmon Branch, several outcrops of York-River-type sandstone (of the York Lake facies) are observed between two basic volcanic intervals: The volcanics are poorly exposed, but the uppermost exposure, at the base of the York River formation, consists of greenish coloured igneous breccia, stratified, and medium to coarse grained pyroclastics.

These volcanics do not cause any visible alteration of the enclosing sediments: The York Lake sandstone exposed below the volcanics is unmetamorphosed.

6. Greenish grey to black, brecciated basic volcanics are exposed in the low-dipping upper York River along Caron brook (loc. lat. 48°37' N, long. 66°00'50" W). Here, Carbonneau (1959) interprets a fault between the volcanics and the York River. The York River shales are splintery, and develop an axial- plane cleavage inclined at 78° SE. 65

In the eastern part of the area a similar volcanic interval, consisting of basalt and pyroclastics, occurs near the York River - Battery Point contact, along the Charles Vallée road, west of the Caron brook section (loc. lat. 48°36'25" N, long. 66°03'30" W).

Carbonneau (1959) mentions that the volcanics exposed along the axial area of the Berry Mountain Syncline are more acidic than those exposed to the north, and the north-west. Predominant, however, are dacite, and porphyritic rhyolite.

7. The northern escarpment of the Big Berry Mountains contains a 5-mile-wide, and 2,000-foot-thick volcanic body, along the Lake Branch and Battery Point contact. Carbonneau (1959) reported that the rocks in the eastern part of this lens are predominantly acidic, and in the western part, basic. Poor exposure does not allow better dilineation of the two. These are frequently impregnated by a sulphide mineralisation, and are presently actively explored for minerals.

DEVONIAN GRANITIC ROCKS

Devonian granite intrusives occuring in the northern part, in the Barren Mountain and Hogsback Mountain areas (approx. loc. lat. 48° 50' N, long. 66°16'10" W; and lat. 48°51'20" N, long. 66°06'30" !J), consist of a grey to pink coloured prophyritic granite. The phenocrysts consist of quartz, feldspar, and biotite in a fine grained groundmass (Alcock, 1922, p. 87 D).

Feldspar phenocrysts consist of albite (An 4) and oligoclase (An 14). Secondary constituents consist of iron oxides and apatite (McGerrigle, 1954, p. 59). 66

South of Barren Mountain, the porphyritic granite grades into white to pale pink coloured, tuffaceous, and brecciated rhyolite at Barn- Shaped Mountain, and Squaw Cap Mountain. The contact between these acidic and the neighbouring basic volcanics is interpreted by Alcock (1945) to be faulted. However, the acidic volcanics are regarded by McGerrigle (1954) to be intrusive into the basic rocks. The rhyolites contain feldspar phenocrysts in an aphanitic groundmass of quartz and feldspar.

DIABASE INTRUSIVE

A large diabase sill, 3 mile long, approximately a mile wide, and 1000 to 1500 feet thick, occurs along the Cascapedia Salmon Branch (approx. loc. lat. 48°49' N, long. 66°21'20" W; McGerrigle, 1954). The rock consists of greenish grey, fine to medium grained diabase of an ophitic to sub-ophitic texture. The feldspar phenocryst laths are identified by McGerrigle (ibid) as plagioclase or andesine occurring in a pigeonite, biotite, apatite, and epidote matrix. Magnetite and chromite occur as opaque minerals. The overlying Cap Bon Ami shales are baked into splintery slates. The contact metamorphic effects are local. STRUCTURE

The area is situated on the broad northeast-southwest trending Berry Mountain Syncline, the southern limb of which is steeply dipping, faulted, and locally tightly folded. The northern limb is low dipping. Enclosure 4 shows the regional structure of the area.

The southern limb of the Berry Mountain Syncline shows low angled, to vertical, to slightly overturned dips. Tight folds are inferred from the variable dip directions. However, individual fold hinges are rarely observed in outcrops. Carbonneau (1953) mapped several such folds, within an exceptionally wide York River outcrop belt in the Marcil West Brook, Charles Vallée, and Josué Lake areas. The York River outcrop belt also contains several steep strike faults with a variable southeasterly throw of upto a thousand feet. Such faults are observed in Caron, Marcil West, and Charles Vallée traverses.

Carbonneau (1953) interpreted the York River, and possibly the Cap Bon Ami (?) to be in a fault contact with the Silurian volcanics (andesites and basalts) along the northern limb of the Josué anticline, to the southeast of the Berry Mountain Syncline.

Local fractures frequently develop near fault zones, but there is no rigorous pattern of cleavage development, and secondary fractures. Locally, axial-plane cleavage develops in the southern part of the area, in the tightly folded Fortin group shales. The Fortin group rocks, are however beyond the scope of the present study. Jointing is common.

The regional structure of the eastern part of the area is poorly understood owing to poor access and exposure. A NE-SW trending syncline contains the Gaspé Sandstone in the axial area.

The northern limb of the Berry Mountain Syncline is gently inclined. Local structures are broad and open. The Lemieux anticline 68

(approx. loc. lat. 48°47' N, long. 66°10' W), in the northern part of the area, exposes the Grande Grève, and the Cap Bon Ami limestone at the centre, rimmed by the volcanics, and the York River sandstone. In the central part, hydrothermal mineralization (mainly lead and zinc) affects the Grande Grève. This mineralization has been the objective of many now-abandoned mining operations.

The dips rarely exceed 25° in the northwestern part of the area. Here, broad northeast-southwest-trending folds are observed within the Gaspé Limestone. The York River formation, exposed along the "Cassault Lake - Boutet Syncline", extends into the study area. Occasional normal faults were encountered in the traverses along Seventeen-Mile brook. These have been mapped by McGerrigle (1950). These structures are illustrated in the Compilation Geological Map (Enclosure 1).

Structurally speaking, the southwestern part of the area is relatively simple. A strike fault, which may be of regional significance, exposed under the Nouvelle bridge (loc. lat. 48°30' N, long. 66°36'26" W), causes a noticeable disturbance and induration of the York River sandstone along the northern flank of the Berry Mountain Syncline. The Battery Point "Square Forks facies" is exposed in the axial area.

In the Gaspé-Sandstone-covered northern limb of the Berry Mountain Syncline, a fault has been interpreted along the Battery Point contact with the Lake Branch. The contact, exposed along the eastern wall of the Cascapedia river valley (loc. lat. 48°39' N, long. 66°09'40" W), is marked by a contorted, and isoclinally folded Battery Point sandstone containing minor shale. The fault, in view of the extent of deformation, is suggested to be compressional.

The fault contact is traced by Carbonneau (1953) and La Société Acadienne de Recherches Pétrolières (SAREP 1971) along the foot of the northern slope of the Big Berry Mountains. 69

South and southwest of Huard Lake (loc. lat. 48°38' N, long. 66°24'18" W), the contact between the Battery Point and the Lake Branch may be faulted, but owing to poor exposure, further investigation was not possible.

Photographic interpretation suggests the possibility of an important topographic lineament aligned parallel with the Battery Point - Lake Branch contact, south and southwest of Huard Lake (loc. lat. 48°37' 10" N, long. 66°23' W), the southern block presumably downfaulted towards the axis of the syncline (situated to the south): see the geological map, Enclosure 1.

Several small normal faults were observed along the northern limb of the Berry Mountain Syncline. The faults are topographically poorly expressed. A fault with a throw of approximately 15 feet, observed along the Cascapedia Salmon Branch, was not expressed on the aerial photographs. Similar faults, if associated with greater offsets, could be significant for hydrocarbon trapping possibilities in the northern limb of the Syncline.

Local secondary fracturing is generally absent in the northern limb of the Berry Mountain Syncline. Axial plane cleavage is absent in the low inclined northern limb of the Syncline.

Local anticlines, within the low dipping northern limb of the Syncline, were not observed during the field work.

The following sums up the structural aspects of the area:

1. Prospects of secondary fracture porosity development are poor in the area. 2. Although block faulting possibilities are poor, some structural lineaments have been mapped on the basis of photogeological interpretations. These may offset the possible reservoir development 70

in the lower Lake Branch sands, and the York River formation, in the subsurface. 3. Local anticlinal structural reversals within the low dipping Battery Point, Lake Branch, and York River formations were not observed along the northern limb of the Syncline. 4. Tight local folds on the southern limb of the Syncline are of little interest for hydrocarbon possibilities. ECONOMIC POSSIBILITIES

HYDROCARBONS

It is now widely accepted that organic matter disseminated in sediments served as the source of hydrocarbons (Phillippi, 1965, Hood and Castano, 1974). The resistant proto-petroleum, called kerogen, is the degradation product of the organic matter, which by a thermal alteration accompanied by various other secondary processes, is transformed into petroleum products. With subsequent increase in temperature, it is further broken down into simpler hydrocarbons, and finally into methane.

Kerogen is defined as a complex organic molecule which is insoluble in petroleum solvents, and on thermal alteration during burial forms hydrocarbons.

A general scheme of kerogen transformation is suggested in figures 18 a, b, and c. The organic matter of a given composition, as expressed by the hydrogen/carbon, and oxygen/carbon atomic ratios, breaks down in its own peculiar manner. The transformation paths are suggested in figure 18b, and c (Tissot et al, 1974). Hydrogen-rich (lipid-rich) organic matter, usually amorphous and of an algal source, rich in fatty acids, gives rise to a wide range of complex hydrocarbons associated with petroleum: this is shown by path I. On the other hand, the hydrogen-poor organic matter, with a lower H/C atomic ratio, usually humic rich, of a continental source, breaks down in a manner shown by path III, ultimately yielding methane with little possibility of generating petroleum-related compounds.

Organic matter, with a sapropelic composition, between the two extreme cases, transforms somewhat similar to path I, along the path indicated by II.

The physico-chemical breakdown brought about by temperature changes is due mainly to burial. The generation of hydrocarbons is influ- enced by the paleothermal gradient, along with the duration for which the PRINCIPAL PRODUCTS rltly,I4tQ II.11310 I.I.... IIlII16 OF KCROOEN EVOLUTION cot, KO OIL I UM 00 n r I I n ~ 1.50 Incr.atin0 .volution S U ® IMnOfi1.Q IYOiullall E é n ~ ré'i o

1.00

� InnlOtup IYOIIIWn

~ CH4 • 0.50 4-

• • 0 010 0 20 Atomic 0/C ( Fig. 18a-General scheme of hydrocarbon gene- Fig. 18b-Principal steps* of kerogen evolu- ration. Depth scale represented is tion and hydrocarbon formation. based on examples of Mesozoic and Flat parts of curves indicate Paleozoic source rocks. It is only mostly oxygen loss as CO, and indicative and may vary according to N 0.. Steep parts show loss of nature of original organic matter, hydrogen and hydrocarbon gene- burial hi.tory, and geothermal ration. Evolution paths I or II gradient. correspond to kerogens able to generable abundant oil, whereas evolution path III is represen- tative of hydrogen-poor kerogens, ., producing mostly methane at depth.

. ~ 0 + Algal I(orogsn (Botryococcus, etc...) .0 ~t- o Cretaceous, Arabic Gull t. Increasin(i burial •1 sir 1..Toarclan, Paris Basin

1.50 O Upper Paleozoic-Triassic, Spitzbergen o Silurian, Sahara * U. Cratacocuc, Douala Basin 00 _ 00 ~.~ Incraksing n L. Monnville, W.Canado (Mc Ivor, î9E;7) • bvrici Ay-o~ / 1. Other: ~1 l+ I.00 - LJ" t„ "O r—• x x Q k-~.. X *>• Increasing ~ burial

0.50 -

0.25 L_ t ~, 0 0.10 0.20 . 0.30 ATOMIC 0/C Figure 18c-Examples of kerogen evolution paths. Path I includes ttïgal kerogen and excellent source rocks from Middle East; path II includes. good source rocks from North Africa and other basins; path III corresponds to less oil-productive organic matter, but may include gas source rocks. Evolution of kerogen composition with depth is marked by arrow along each particular path. 72

temperature is maintained (thermal history).

The thermal gradient depends on the thermal conductivity, and the temperature difference between the surface and subsurface.

Phillippi (1965), in a study of the depth and time of petroleum generation in the Los Angeles and Ventura basins, demonstrated that the bulk of oil generation takes place below 8,000 feet and 12,000 feet with temperature gradients of 3.91°C/100 m (2.15°F/100 ft) and 2.66°C/100 m (or 1.46°F/100 ft) respectively. In both cases, oil generation appears to have taken place at 115°C (239°F).

Considerable discussion has taken place over the depth of burial and oil generation. However, it is now generally agreed that oil formation is a non-biological thermal process, and that the depth at which it occurs also depends on the nature and the richness of the source organic matter.

A depth of approximately 10,000 feet has often been used as optimal for oil generation for average thermal gradients. A generalized figure (18 a), presented by Tissot et al (1974), shows that oil is generated at a depth greater than 1 km, and a maximum generation takes place at a burial of approximately 2.6 km (8500 feet).

Several geological indicators to the thermal history of rocks are utilised to evaluate the maturation of the sedimentary rocks (Hood and Castano, 1974, p. 91). Among the physical methods, the commonly used are: clay crystallinity, vitrinite reflectance, carbonization, and fluo- rescence of the organic matter: Among the chemical maturation scales, many modern techniques are now available (Philippi, 1965), none of which were utilised in the present study.

The Gaspé Sandstone was extensively sampled for laboratory work to determine the organic carbon content to evaluate the source rock potential; the clay crystallinity, spore carbonization, and vitrinite reflectance 73 were studied to assess the level of organic metamorphism. Porosity and permeability analyses were undertaken to assess the reservoir possibility.

SOURCE ROCK POTENTIAL: A source rock is generally defined as a fine grained organic-rich rock, which on maturation generates petroleum. Thus, the rocks with good potential for source rocks are organic-rich shales.

The organic carbon was chemically determined to evaluate the organic content. A ratio of organic carbon and the insoluble residue, after the removal of carbonates, is also used to assess the organic matter that can contribute to hydrocarbon generation on maturation. The organic matter content can be obtained by multiplying the total organic carbon content by a factor of 1.6.

The organic content of the shales in the marine York River is poor. Five geological sections were sampled; these include the Cascapedia Lake Branch River, Nouvelle River, and West Square Forks Road sections in the western part; and the Marcil West, and Caron Brook sections in the eastern part.

Only six samples show a total organic carbon content in excess of .5%; the highest value is 1.4% in a York River shale unit (INRS, 1975, Figure C3).

Experience in the ancient sediments in petroliferous provinces shows that the organic content in source rocks is generally at least of the order of 3% by weight. Snowdon and McCrossan (1973, p. 2) suggest the potential source rocks to contain 1.57% total organic carbon. The organic content in organic-rich sediments, reaches 5% (Phillippi, 1965, p. 1023). Some well known, exceptionally organic-rich shales, such as the Green River Oil Shale in Colorado, and the Mississippian shales in New Brunswich, contain upto 20% or more organic matter by weight (Bradley, 1970; King, 1963; Cameron, 1969). 74

The York River contains black coaly streaks within sandstones. These sapropelic (mega-spore and algae-rich) laminations were rarely observed in the northern and northwestern parts of the area. In eastern Gaspé the organic matter mixed with red brown leptinic substance, huminite, sporinite, cutinite, and inertinite (INRS, 1975, p. 67, personal communication, Dr. Pittion, 1975), forms local source laminae within the York River sand units. In the study area their actual frequency is difficult to judge owing to poor exposure.

It is thus concluded from the total organic carbon analysis that the source rock potential of the analyzed shale samples is poor. The area, however, lacks good exposure and since the poorly exposed sections are likely to contain shale, a categoric judgement on the source rock potential for the central Gaspé area in this report would be premature.

MATURATION POTENTIAL:

Clay Composition and Crystallinity: Detailed x-ray diffraction analysis was carried out on the York River, the Lake Branch and the Battery Point formations, primarily to study the clay composition of the rocks, and subsequently, to study their diagenetic evolution.

Increased organic metamorphism results in better ordering of the clay crystals. Illite crystals, studies as a maturity index by utilizing the width of the 001 peak at half the height (Weaver, 1960; Kabler, 1968), provide a reasonable tool for maturity evaluation.

To sum up the x-ray results, it appears that kaolinite is rare but unique to the York River; corrensite is only present in the Lake Branch and smectite is restricted to the Battery Point. The York River contains the least amount of illite (55%), the Battery Point the highest (62%); the Lake Branch contains an average of 57% illite. However, these differences are too slight to 75 be used as a criterion to distinguish the formations from one another. The fine fractions are richest in mixed layer clays and poorest in chlorite. The importance of corrensite lies in that it is found in a level of maturation favourable to the generation of oil (Kdbler, 1973).

The crystallinity indices for the <2p fraction have an average value of .67°20 ± 0.13°20 in the Battery Point, 0.52°20 ± 0.15°20 in the Lake Branch, and 0.54°20 ± 0.11°20 in the York River formation. There is no difference in the crystallinity of the last two formations in the examined sections. The low crystallinity could be attributed to either a low thermal evolution, or a fresher detrital influx.

A considerable amount of work has been done on the diagenetic alteration of matrix clay (Grim, 1968, p. 563). The emphasis on diagenesis of clays in the sandstone has been on the formation of interstitial kaolinite, and on the transformation of smectites to an illite-chlorite assemblage.

The presence of precipitated kaolinite suggests an invasion of relatively fresh ground water recharge in the outcrop belt which is rich in dissolved silica (Pettijohn et al, 1973, p. 430). The presence of kaolinite is relatively rare in the Gaspé Sandstone. Only three samples in the York River formation contain significant quantities of kaolinite. The fact that the kaolinite content is variable in different samples, reaching more than 50%, and that it is restricted to a relatively small part of the section, suggests that it may be of a non-diagenetic nature.

The formation of a stable clay mineral assemblage of illite and chlorite in sandstones, as in shales, may be a result of duration and/or depth of burial. It is related to the long term substitution of K and Mg for Na and Ca in clay minerals (Siever, 1968) in moder- ately concentrated pore waters. The total process involved is a result of an interaction of many factors which include temperature, 76 its duration, and pore-chemistry, and is not clearly understood (Pettijohn et al, 1973).

The relatively stable ratios of the clay constituents in the York River, and the Battery Point, and a lack of systematic variation in the crystallinity within the geological column possibly suggest that the illite-chlorite is, at least in part, of a diagenetic origin. Thus, a regional maturation picture is difficult to deduce from the clay crystallinity index. None of the analyses made on clay crystallinity suggestsan overmature (anchizone) level of organic metamorphism. The reader is referred to figure A-1 of the INRS-Pétrole (1975) report.

Vitrinite Reflectance: The relationship between coal rank and the occurrence of oil and gas was noted many years ago (Suggate, 1959). Fairly recently coal petrography, especially the reflectance of an incident light on polished organic macerals, has been utilized as a measure of the thermal history of sedimentary rocks. The technique, applied on the dispersed organic matter in sedimentary rocks (phytoclasts, Bostick, 1971), provides a quick and reliable index to evaluate the organic metamorphism, and estimate the maturation potential for oil and gas.

The relationship between coal rank and thermal alteration of organic matter, and vitrinite reflectance is shown in figure 19. The range of values for oil and gas generation varies from a reflectance (Ro) of 0.5 to 3.0%. (Reflectance is the ratio of the quantities of reflected and incident lights bounced off a polished organic maceral surface, expressed in percentage.)

The cut-offs used by various workers for oil and gas generation somewhat similar. Alpern (1970), Teichmüller (1973),and Vassoevich et al (1970) indicate a principal oil phase between a reflectance (Ro) of 0.5 to 1.35%, a wet gas and condensate phase between 1.35 to 2.0%, and a principally gas phase at reflectance values greater than 2.0%. 77

On the other hand, Hood et al (1975) propose an initial maturity stage at a reflectance range of 0.7 to 1.3, a mature stage between 1.3 to 2.1, and a gas prone, post-mature stage with values of greater than 2.0%.

The cut-offs used in this report are those proposed by Vassoevich et al (1970), and are shown in figure 19.

The sections in this study were made from palynological prepa- rations; some were made from crushed rock samples. Approximately 50 random measurements were made on each preparation immersed in oil.

The reflectance observations made on the Gaspé Sandstone in the area suggest that there is a tendency for a lack of systematic vertical variation in a given section. For example, in the Cascapedia Lake Branch section Ro means range from .61 to 0.9% (INRS-Pétrole, 1975, Figure 4). The histogram peaks are well defined and allow a reliable interpretation. A detailed section shows a similar variation in reflectance, where the higher values do not necessarily occur below the lower ones. The Salmon Branch section (ibid, 1975, Figure 7) shows a similar tendency.

The Nouvelle River and Caron brook sections (INRS-Pétrole, 1975, Figures 1, 2 and 12) show a reasonable gradual increase in the Ro values with lower stratigraphic position (i.e. a greater depth of burial).

Several observations made from the same locality show fairly consistent values and a low scatter. Ten samples from the Lake Branch section collected from 500 feet of stratigraphic interval demonstrate an average Ro of 0.74%, and a standard deviation of .07.

The reflectance data from the fluvial Battery Point sandstone is highly variable. Although the histograms do not appear to show 97 _a,

F I G.• 11 SOME SCALES OF ORGANIC METAMORPHISM

(AFTER HOOD AND CASTANO, 1974, ,AND HOOD ET AL, 1975)

COAL SPORE- THERMAL VI TRI N- STAGES OF HC GENERATN. CARBON- . ALTERA- ITE a RANI: BTU Ivr~ ) (6) -~ ~ ~A.TION TION , FFLECT . (5 _ (1 ) (2) (3) (4 ) 2 -LIGN. SLIGHT EARLY 4B(:Ot~Jy1- — 8 METHANE YELLOW - SUB C ' I ivi~iATUI•',É 6 — — —~ YELLOW — 10 BIT. g ~ 11 a5 2-5 .5 ' S — C -- — n' PRINCIPAL - HV F— 13 .— 40 _ O I L .. -- --- — 14 - FORP~ATION BIT. JS 10 — YELLOW — 1 ~ -- 35 .:-1. O PI -LASE -- 30 DARK -3V01). 12 INJ TIT = — 20 ----,` 13I2N •\ BROWN . WET GAS g 3.5 ~ 1.5 "r~:`;T~Rc ,LV Bill — 15 CONDENSATE ► ~3.7 — 2,p 14 ---r SEMI HIGH , ri)5 ~_ - AN11-I . `- 10 BLACK STRONG ~_ 2 . ') TEMP. 16 - \ BLACK .f ~.TU.ïE _I 4.0 = r ~THAId E

ANTH. 18

(1) SUGGATE, 1959. (2) GUTJAHR.,1966. (3) CORREIA,1967. (4) INTERNATIONAL HANDBOOK ON COAL PETROGRAPHY,1971. (5) VASSOYEVICH et a1,1970. (5) HOOD et a1,1975. 78 such a spread (XNRS..Pftrole, 1975, Figure 4), it is possible that the organic matter in the analyzed sample is ancient and reworked.

In order to reveal any geographic variation, the averages of the arithmetic means for each area were plotted and contoured in Figure 20. The figure sums up the vitrinite reflectance results, on the York River formation, but lacks good control in some parts of the area. Also, owing to the absence of data, similar maps could not be prepared for other formations.

It is obvious from the figure that in the eastern and the northeastern parts of the area, the level of organic metamorphism, as suggested by the values of 1.45 to 2.19%, is considerably higher than that in the west and the southwest, where the Ro values are lower than 1.26%. Thus, a greater potential for oil exists in the western part of the area, where the reflectance values do not exceed 1.35%.

The high regional metamorphic effect in the eastern part of the area is evident in the field. The York River sandstones in this area, such as along Marcil West and Caron brooks are tough and compact with a conchoidal fracture. The shales in these locations contain an axial plane cleavage.

The regional variation of the organic metamorphism within the York River should depend on the York River basin configuration as suggested by the isopach map (Figure 15). Assuming that the thickness of the overlying beds was uniform in the area, the York River metamorphism should increase toward the south and southeast.

This effect, however, appears to have been modified by the regional igneous activity, and the presence of a great thickness of volcanic rocks in the lower Devonian section in the eastern and northeastern part of the area. f~> Ka/ 48.56N

r- Potentiel pétrolier et gazier L...I ,Oil, and gas potential

.' — 1 Potentiel gazier L _ J Gas potential 65'

00'

I 68'25 20' 6600 S'SS W COUPES ETUDIEES SECTIONS INVESTIGMTED: York River 1. Nuis. Brandy, brandy N. Volcaniques Brandy, Brandy N. Br. Volcanics 2. Cascapedia Eras aux Saumons. Salmon Branch. Coupe étudiée Section investigated 3. Cascapedia branche du Lac. Faille/ Fault Lake Branch. • 68^ 66. 64. 62.W Contour d'égale 4. Cascapedia branche du Lac O. Pouvoir réflecteur Lake Branch W. en pourcentage réflectance 1.46 Percentage reflectance Contour of equal reflectance 5. Ruffs. Caron/ Caron Brook. /6 Nombre d'observations Number of observations 6. Ruffs. IMarcil O./ larcil N. Br.

7. Ruis. Charles Valley. Milles 0 4 B Miles Charles Valley Brook. Kilomètres Kilometres ECHELLE-SCALE 10 B. R. Nouvelle 5./ Nouvelle N. S.

FIGURE 20: REFLECTANCE MOYENNE DE l.A VITRINITE, INDEX •POUR LES NIVEAUX DE METAMORPHISME ORGANIQUE, FORMATION DE YORK RIVER, SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. VITRINITE REFLECTANCE, INDEX FOR LEVEL OF ORGANIC METAMORPHISM, BERRY MOUNTAIN SYNCLINE, QUEBEC. 79

On a smaller scale, as observed in the western, and northwestern sections (Salmon Branch and Lake Branch rivers), the contact metamorphic effects, due to the presence of the volcanic (lava) beds, are restricted and extremely local. The contact zone, owing to extremely poor exposure in most sections, could not be successfully sampled for a detailed study.

Organic Matter Colouration: Organic matter content is generally poor in the Gaspé Sandstone. Important organic constituents in most samples in the York River are brown amorphous, black angular, and finely dispersed debris. Plant tissues are relatively minor in occurrence.

Trilete spores occur in the Grande Grève, York Lake, York River, and Battery Point units. Marine palynomorphs occur in occasional samples in the Grande Grève, York Lake, and York River units.

In general, the degree of carbonization throughout the area is fairly advanced. In terms of Correia's scale (Figure 19), the carbonization is in excess of 3.5; the exception being the northwestern part of the area, where, although the Gaspé Limestone shows advanced carbonization (possibly owing to a regional igneous activity). The York River formation, along the Lake Branch section, shows a yellow brown (slight) to moderate brown colouration.

In summary, the maturation trend suggested by the carbonization of the organic matter confirms the results of the vitrinite reflectance technique.

RESERVOIR POTENTIAL: A reservoir rock is defined as a rock with visible grains (very fine grained and coarser sandstone) containing sufficient intergranular porosity and permeability; or a rock with secondary (possibly fracture) porosity and permeability. 80

Field observations on intergranular and vugular porosity were made with a hand lens and a binocular microscope. A petrographic study was made to supplement the field examinations. The porosity measurements were made on a selected, but a limited number of samples.

In the field, the porous sandstones were assigned a porosity of less than 5%. These York River and York Lake units consisted of fine to medium grained, sub-rounded to sub-angular, salt and pepper, poor to medium-sorted sandstone.

The porosity and permeability determinations were made with a Ruska porosimeter, and permeameter, on the most promising samples only. Figure 21 sums up the results of the analyses. It is apparent that the sandstones contain poor (2-4%) porosity. Only two samples from the York River formation showed a porosity of the order of 9%. The permeability in all measurements is less than 13.4 md.

Figure 21. Porosity and Permeability Analyses

No. MRN Nom localisation Formation Lithologie Porosité Perméabilité Loc. NO. Locality Name Lithology Porosity Permeability md.

6.19.52 Cascapedia Lake Battery Point Sandstone 3.19 11.23 Branch 6.19.55 West Square Forks Battery Point Sandstone 3.95 12.96 6.19.57D West Square Forks York River Sandstone 2.69 12.12 6.19.59C West Square Forks York River Siltstone 0.18 11.66 7.8.60A4 Cascapedia Lake York River Sandstone 9.58 13.39 Branch 7.3.62.6 Cascapedia Lake York River Sandstone 3.38 9.72 Branch 7.8.62.3 Cascapedia Lake York River Sandstone 2.78 12.96 Branch 7.8.62.14 Cascapedia Lake York River Sandstone 2.03 11.23 Branch 7.8.62.21 Cascapedia Lake York River Sandstone 9.07 11.23 Branch 8T

An important aspect to note is that although the porosity of the rocks varies between 0.18 and 9.58%, the permeability in all cases varies only slightly, between 9.72 and 13.4 md. The high porosity (9.58%) was observed on a local 18 inch thick, relatively clean, medium grained sandstone bed.

A petrographic study on the Gaspé Sandstone (Théroux, 1975) points out the following aspects:

The York River sandstone consists of sub-rounded to sub-angular quartz, chert, and volcanic fragments, and grey and frequently perthitic feldspar. It is more arkosic than the Battery Point sandstone. However the difference between the two is slight.

The Battery Point is poorly sorted, sub-rounded to sub-angular and consists mainly of pink potassium-feldspar, quartz, chert, and volcanic fragments. The York River sandstones are relatively finer grained than those of the Battery Point.

The matrix of the two type of sandstones is mostly clay. The cement on some occasions is calcitic and rarely siliceous.

The Lake Branch sandstones resemble those of the York River in gross lithological characters except colour which is mottled grey and red. These sand members in the lower Lake Branch are considered slightly porous in field examinations.

From the above observations, it appears that the lack of good porosity in the Gaspé Sandstone is largely due to the presence of an interstitial clay, an alteration of the feldspars into clays, occasional calcite, and rare silica cementation. Although in the field, extreme care was taken to assure freshness of samples, the true effects of the surface alteration on the porosity and permeability are not clear. 82

Thus the present study suggests that the reservoir development in the Gaspé Sandstone is poor. It should be noted here that the Devonian sandstone reservoirs in western Canada have an average porosity of the order of 15% (for example, Gilwood Sandstone); and Cretaceous sandstones contain a porosity of between 20 and 30% (AERCB, 1973).

A poorly porous sand development within the lower Lake Branch formation appear to be relatively better sorted. The sandstone reaches a maximum gross thickness of 50 feet. No porosity determinations are available on this unit.

TRAPPING POTENTIAL; The northern limb of the Berry Mountain Syncline (Lake- Branch Monocline) does not contain prospective local structural closures. Here, the possibility of fracture porosity development is minimal due to slight deformation and gentle bedding inclinations. Prospective traps are considered to be stratigraphic (sand) pinch-outs and normal faults.

Along the southern limb, owing to extensive faulting, and near- vertical dips, secondary fracture possibilities exist. However, in view of the tight nature of local folds, a high degree of organic metamorphism, and the presence of silica cementation, the hydrocarbon possibilities are considered to be poor. In the eastern part of the area, the cores of regional folds expose the underlying Gaspé Limestone series, which lacks primary and secondary porosity development.

Correlation of individual markers is possible in adjacent sections, but it is tenuous across the Berry Mountain Syncline. Figure 6B summarizes a north to south change in lithological variations.

The figure diagrammatically demonstrates that the York River formation, consisting of a 6,000-foot-thick sand-shale sequence to the south, thins northward to an approximately 4,000-foot-thick York Lake and York River sequence. The latter sequence is predominantly sandy at the base but shaly and silty in the upper part. 83

The figure also shows the Battery Point sandstone along the southern limb, partly changing to the north into a shale and siltstone with minor sandstone of the Lake Branch formation.

Thus, although the lateral facies variations of individual beds can not be demonstrated, there is an ample lithologic variation across the Berry Mountain Syncline to warrant stratigraphic trap (sand pinch-out) possibilities, especially along the low-inclined northern flank.

The York River and the York Lake, along the northern limb, although poor in source potential, are situated within an LOM range that is conducive to the formation of oil and gas. The fact that bitumen occurs in the area (Alcock, 1945, p. 13-19) suggests that oil was probably generated in the York Lake - York River interval.

These stratigraphic traps are difficult to map by conventional exploration techniques, but high-resolution reflection seismic, and direct exploration methods, such as magneto-telluric, may help dilineate them.

Photo-geologic interpretations suggest the presence of several structurally controlled lineaments in the Huard Lake - Lake Branch Lowland. These are possibly due to block faults of unknown displacement. Notable among these is the southwest-northeast trending lineament, south and southeast of Huard Lake (Enclosure 1). A reflection seismic line across this structure may reveal a displacement of the sub-surface markers, especially since a velocity contrast is anticipated at the York River/Lake Branch, and the York Lake/York River contacts.

SUMMARY: In summary, the hydrocarbon potential of an area can be summarized as the sum total of the equally important source rock, maturity, reservoir, and trapping possibilities. The following table sums up the results of the laboratory analyses undertaken on the samples collected in the 1974 field season in the central Gaspé area. 84

Figure 22. Summary of hydrocarbon potential, Berry Mountain Syncline, Quebec.

HYDROCARBON POTENTIAL FORMATIONS POTENTIEL D'HYDROCARBURES Source Rock Maturation Reservoir Trap Roche mère Maturation Réservoir Piège

v r re nne nne re ée

w r r - en v h e -d .0 .0 e r;JQ S- a~ o ir ir o 0 0 ir 3 •" 0 C •r- >) 0 •r •r- 0 MS0 0 rQ O 0 0 Po Pauv Pau Poo Fa Elev Poor Pauv Fa Moy Fa Hig Moy &CC Moy Jû_ C7 CO LLM CD 03

BATTERY X X X X X POINT

LAKE X X X X BRANCH

YORK X X X ? X RIVER

The present study suggests that, with the exception of a favourable to poor maturation potential for the hydrocarbons, the source, reservoir, and trapping possibilities are considered poor for the area. On the basis of the analyzed samples, it is the qualified opinion of the author, that the hydrocarbon potential of the area, at best, can ''only be rated as poor to perhaps fair.

MINERALS

The studies of Robert (1966 and 1967), McGerrigle (1954), Carbonneau (1959, p. 55-57), and Mattinson (1964) adquately describe the mineral possibilities of the area, and are recommended to those interested. A compilation on the important mineral possibilities is summarized in the following.

The best known region for base metals, is situated along the hinge area of the Lemieux anticline. Here, hydrothermal activity has caused a mineralization in the Cap Bon Ami and Grande Grève carbonates. 85

The Federal Metal Corporation mine which exploited the lead and zinc sulphide deposits (galena and sphalerite) has now been abandonned. Trenches and drill-sites are widely scattered in the Brandy brook area.

Carbonneau (1959) reported submicroscopic chalcopyrite mineralization in the porphyritic rhyolite in the northern escarpment of the Big Berry Mountains.

McGerrigle (1954) reported a minor occurrence of sphalerite, 3,000 feet upstream from the broken bridge, and 4 mile downstream from Salmon Branch falls (approx. loc. lat. 48°48'45" N, long. 66°26'10" W). It is associated with the Cap Bon Ami formation.

Silurian volcanics (rhyolite and andesite of the Baldwin member), exposed in southwest-northeast trending bands along the flanks of the Josué anticline, show a faint mineralisation. The rhyolite encountered in the Caron brook traverse contains faint disseminated pyrite. These volcanics deserve further attention.

E 67 N LEGEIIDE-LEGEND ,s I. 8 _.

^EVON19N-DEVONIAN

Granite et felsite Granite and felsite j 13 1 16• Andesite Andesite ~4-3-5sa 12

Battery Point Battery Point 4 Facies de 'Square Forks' 11 Square Forks facies . ~ ~ \ 2attery Point typique ~ Typical Battery Point !4.„ ~ • 10 jw ~/ 5 \ ~ V Laie Branch Lake Branch JJ -k;5 9 ;. /------~6` ~~4 A/ //j f Yo'-:: River i 10 ---- cv 'I t/ o York River 1 ‘\ //`1./' / 7 / ~9F r %c 6- 46, a 1'/ ( ~ , ° o, - - ,~~.,;" ~ tioica'',l +es. rhyoiite, ~ ;/yi?-7-;-/2/ Volcanics, rhyolite,i »6—. : ~i~ -...:).,/,' basalte, ar.desite 5 w'3.53'S`1 ~~ ^~ ' , basalt, andesite r g, ~, p C ~ 10 7J / , ~ .6 ^ , ~1 ..nrk Lake a Groupe de r • / F :ork Lake Fortin ' I ~ - j < r ~ - ~-/ ~ Grande Gr@ve G.ande Greve •r,. 4 // / i ~~ 5:~7,4/>%;/:> /:/..... /.(7),/' : ~l`'~ P-2:-1 1~r /~ / — • .1 1 /t `j ~ /` Cal, Ben Ami % Cap Bon Ami ~ l ô~ / ~~-~ f % { f _ //'~ j À ,J}~ izi 1 / ~ -„~ ' \/J 8 SILURIEN L`EVONIE:;-SILURIAG DEVONIAN p s-,-s,a Arcjle, siltstene, i.,~ ~ gras j 1 Shale, siltstone, sandstone ,~/ ,~' ~~\ (2a Volcaniques [ 2 (2a) Volcanics / .~.7 E. c ~, "~ ~ ~\12 ` / / lU O ~ 1 ~/ 1 C."Sç0-,RDOVICIE'1-CABRO-GROOVICIAN _~~~f L Grcupe de Shicksho,:'r. I r Shickshock Group c ,~~~ ~taS di,entaires, m6ta- t t'etasediments, meta- ~ t•-i14 ~ + vcicaniques volcanics ' AHS 75 $ 7/ ~ ~ I I 1 ~ 1 ~t°1S 66°39' ]O' IS 66 ° 6c"

REFERENCES

AERCB (Alberta Energy Resources Conservation Board), 1973, Reserves of crude oil, gas, natural gas liquids and sulphur, Province of Alberta: ERCB 74-18.

Alcock, F.J., 1922, Geology of Lemieux Township, Gaspé Country, Quebec: Geol. Surv. Canada, Sum. Rept. 1921, pt. D, p. 71-96.

1926, Mount Albert map-area, Ouebec: Geol. Surv. Canada, Mem. 144.

1945, Oil residuals in Volcanic rocks in Gaspé: Trans. Roy. Soc. Canada, vol. 39, sec. IV, p. 13-19.

1948, in Summary of investigations on New Brunswick oil Shales: Bur. of Mines, Dept. Mines and Resources, Rept. no. 825, 24 p.

Allen, J.R., 1965, Fining upwards cycles in alluvial successions: Geol. J., vol. 4, pt. 2, 1965.

1965b, A review of the origin and characteristics of recent alluvial sediments: Sedimentcloay, vol. 5, p. 89-191.

Alpern, B., 1970, Classification pétrographique des constituents organiques, Fossiles des roches sédimentaires: Revue de l'Institut Français du Pétrole et annales des combustibles liquides, vol. XXV, no 11.

Alpern, B., B. Durand, J. Espitalié, and B. Tissot, 1971, Localisation, caracterisation et classification pétrographique des substances organiques, sédimentaires fossiles: Adv. in Org. Geochem., Pergamon Press, Oxford, p. 1-28.

BEICIP, 1974, Etude de géochimie et de pétrographie organiques sur des échantillons de sondages du Québec oriental, Files of Energy Branch, Quebec Dept. Nat. Resources, 69 p.

Berg, R.R., and D.K. Davies, 1968, Origin of Lower Cretaceous muddy Sand- stone at Bell Creek field, Montana: Bull. Am. Assoc. Pet- roleum Geologists, vol. 52, no. 10, p. 1888-1898.

Bernard, H.A., B.S. Parrott, and R.J. Leblanc Sr., 1970, Recent sediments of South Texas - Afield guide to Brazos alluvial and deltaic plains and Galveston barrier island complex: Texas Bur. Econ. Geology, Guidebook II, 24 p.

Bostick, N.H., 1971, Thermal alteration of clastic organic particles as an indicator of contact and burial metamorphism in sedimentary rocks: Geoscience and man., vol. III, Oct. 1, 1971. 87

Boucot, A.J., 1970, Practical taxonomy, zoogeography, paleoecology, paleogeography and stratigraphy for Silurian and Devonian brachiopods: Proc. N. Am. Paleont. Conv. Sept. 1969, pt. F, p. 566-611.

Boucot, A.J., L.M. Cumming, H. Jaeger, 196/, Contributions to the age of the Gaspé Sandstone and Gaspé Limestone: Geol. Surv. Canada, paper 67-25, 27 p.

Bourque, P.A ., manuscript, le Silurien et le Dévonien Basal de l'Est de la Gaspésie: Quebec Dept. Nat. Resources, Special Study, 178 p.

Bradley, W.H ., 1970, Green River Oil Shale - Concept of origin extended: Geol. Soc. of Am. Bull, v. 81, p. 985-1000.

Cameron, R.J ., 1969, A comparative Study of Oil Shale tar sands and coal as Source of Oil: Journal of Petroleum Technology, Mar. p. 253-259.

Carbonneau, C., 1953, The Big Berry Mountains map area, Gaspé Peninsula: PhD thesis McGill University.

1959, Richard-Gravier area, Gaspé Peninsula: Quebec Dept. of Mines, Geol. Dept. 90, 63 p.

Connan, J., and A. Giraud, 1968, Caractérisation de la matière organique de quelques sédiments marins récents: Bull. Centre Rech. Pau-SNPA, vol. 2, no. 1, p. 117-130.

Cooper, G.A., 1942, Correlation of the Devonian sedimentary formation of North America: Geol. Soc. Am. Bull., vol. 53, p. 1729-1794.

Davies, D.K., F.G. Ethridge, and R.R. Berg, 1971, Recognition of barrier environments: Bull. Am. Assoc. Petroleum Geologists, vol. 55, no. 4, p. 550-565.

Dunham, R.J., 1962, Classification of carbonate rocks according to depositional texture: Bull. Am. Assoc. Petroleum Geologists, Mem. 1, p. 108-121.

Ells, R.W., 1883, Report on the geological formations in the Gaspé Penin- sula 1882: Geol. and Nat. Hist. Surv. Can., Rept. prog. for 1880-81-82, pt. DD, p. 1-32.

1885, Report on exploration and surveys in the interior of Gaspé Peninsula; Geol. Surv. Canada, Rept. prog. for 1882-83-84, part E, pp. 7-11.

Fisk, H.N., 1961, Bar-Finger sands of Mississippi Delta: Bull. Am. Assoc. Petroleum Geologists, p. 29-52.

Fisk, H.N., E. McFarlane Jr., C.R. Kolb, and L.J. Wilbert Jr., 1954, Sed- imentary framework of modern Mississippi delta: Jour. Sed. Petrology, vol. 24, p. 76-99. 88

Hood, A., and J.R. Castano, 1974, Organic metamorphism: it's relationship to petroleum generation and application to studies of anthigenic minerals: United Nations ESCAP.CCOP Technical Bulletin, V. 8, p. 85-118.

Hood, A., C.C.M. Gutjahr, and R.L. Heacock, 1975, Organic metamorphism and the generation of petroleum: Bull. Am. Assoc. Petroleum Geologists, V. 59, No. 6, p. 986-996.

Hoyt, J.H., 1967, Barrier island formation: Bull. Geol. Soc. America, vol. 78, p. 1125-1136.

INRS-Pétrole, 1973, Etude géochimique de la série Siluro-Dévonienne des sondages Sunny Bank 1 et York 1: Energy Br., Quebec Dept Nat. Resources, open files, 30 p.

1975, Analytical Investigation, mineralogy, geochemistry, palynology, and reflectometry of the Gaspé Sandstone Series of Central Gaspé, Quebec: Energy Br., Quebec Dept. Nat. Resources, open files, 80 p.

Jones, I.W., 1930, The Berry Mountains map-area, Gaspé: Quebec Bur. Mines, Ann. Rept. for 1929, pt. D, p. 1-41.

1931, The Lesseps Map-Area, Gaspé Peninsula: Quebec Bur. Mines, Ann. Rept. for 1930, pt. D, p. 195-226.

Kubler, B., 1968, Evaluation quantitative du métamorphisme par la crystal- linité de l'illite: Bull. Centre Rech. Pau-SNPA, vol. 2, no. 2, p. 385-397.

1973, La corrensite, indicateur possible de milieux de sédi- mentation et du degré de transformation d'un sédiment: Bull. Centre Rech. Pau-SNPA, vol. 7, no. 2, p. 543-556.

Lane, D.W., 1963, Sedimentary environments in Cretaceous Dakota Sandstone in northwestern Colorado: Bull. Am. Assoc. Petroleum Geologists, vol. 47, no. 2, p. Z29-256.

Lajoie, J., P.J. Lespërance and J. Béland, 1968, Silurian stratigraphy and paleogeography of Matapedia-Témiscouata region, Quebec: Bull. Am. Assoc. Petroleum Geologists, V. 52, p. 615-640.

.J., 1972, Geology of sandstone reservoir bodies in underground waste management and environment implications: Am. Assoc. Petroleum Geologists, Mem. 18, p. 133-19u.

Logan, W.E., 1863, Geology of Canada, Rept. prog. to 1863, 922 p.

Low, A.P., 1885, Reports on exploration and surveys in the interior of Gaspé Peninsula: Rept. of Prog. for 1882-1883-1884, part F.

Mailhiot, A., 1919, Geology of a portion of the projected township of Lemieux, County of Gaspé, Quebec: Que. Dept. Col. Min. Fish., Rept. Min. oper. 1918, p. 134-145.

Mason, D., 1971, Stratigraphic and paleoenvironmental study of the upper Gaspé Sandstone and lower Gaspé Sandstone groups (Lower Devonian of eastern Gaspé Peninsula): PhD thesis, Carle- ton University, Ottawa, 131 p. 89

Mattinson, C.R., 1964, Mount Logan area, Matane and Gaspé-North Counties: Quebec Dept. Nat. Resources, Geol. Rept. 118, 97 p.

McGerrigle, H.W., 1950, The geology of eastern Gaspé, Quebec Dept. Mines, Geol. Rept. 35, 168 p.

1954, The Tourelle and Courcelette areas, Gaspé Penin- sula: Quebec Dept. Mines, Geol. Rept. 62, 63 p.

1959, The Madeleine River region: Quebec Dept. Mines, Geol. Rept. 77.

Parks, W.A., 1930, Report on the oil and gas resources of the province of Quebec: Quebec Bur. Mines, Ann. Rept, 1929, pt. B, p. 7-56.

Pettijohn, F.J., and P.E. Potter, 1964, Atlas and glossary of primary sedimentary structures: Springer-Verlag, New York Inc., 370 p.

Pettijohn, F.J., P.E. Potter and R. Siever, 1973, Sand and Sandstone: Springer-Verlag, New York, Heidelberg, Berlin, 618 p.

Phillippi, G.T., 1965, On the depth, time and mechanism of petroleum generation: Geochim. Cosmochim. Acta, vol. 29, p. 1021-1049.

Potter, P.L., 1967, Sand bodies and sedimentary environments: A review: Bull. Am. Assoc. Petroleum Geologists, vol. 51, no. 3, p. 337-365.

Reineck, H.E. and F. Wunderlich, 1968, Classification and origin of Flaser and lenticular bedding: Sedimentology, 11, p. 99-104.

Robert, J.L., 1966, Géologie de la Région du Mont Hog's Back: Quebec Dept. Nat. Resources, Prel. Rept. 540, 27 p.

1966b, Géologie de la Région du Mont Vallières de Saint-Réal: Quebec Dept. Nat. Resources, Prel. Rept. 549, 19 p.

1967, Géologie de la Région du Ruisseau Lesseps: Quebec Dept. Nat. Resources, Prel. Rept. 562, 16 p.

Russel, L.S., 1946, The stratigraphy of the Gaspé limestone Series, Foril- lon Peninsula: Quebec Dept. Mines, Prel. Rept. 195.

Sabin, F.F., 1963, Anatomy of stratigraphic trap, Bisti field, New Mexico: Bull. Am. Assoc. Petroleum Geologists, vol. 47, no. 2, P. 193-228. SAW lkiaiinne de Recherchei Pêtrol ières) , 1971, photogeologlc mapping program of the Gaspe Peninsula: N. Zay Smith and Assoc. Ltd., Calgary, Alberta: Energy Br., Quebec Dept. Nat. Resources, open files. 90

Siever, R., 1968, Sedimentological consequences of a Steady-State*ttett- ailt . e: Seaimentstegy, v. 11, p. 5-29.

Sikander, A.H., 1975, Occurrence of oil in the Devonian rocks of eastern Gaspe, Quebec: Bull. Canadian Petroleum Geology, V. 23, no. 2, p. 278-294.

Skidmore, W.B., 1965, Gastonguay-Mousier area, Quebec Dept. of- Natural Resources; Geol. Rept. 105, 87 p.

1967, Geological map, Gaspé Peninsula, Quebec Dept. Nat. Resources; map no. 1642.

1970, Petroleum potential in the Gaspé region of Quebec: Ontario Petroleum Institute, 9th Ann. conference.

Snowdon, L.R. and McCrossan, R.G., 1973, Identification of Petroleum source rocks using hydrocarbon gas and organic carbon content: Geol. Surv. Canada, Paper 72-35, 12 p. Stearn, C.W. 1 i are, 4a and Matane counties, Quebec Dept. Natural Resources: Geol. Rept. 117, 42 p..

Teichmüller, M., 1971, anwendung Kohlen petrographischer. Methoden bei der Erdül-und Ergaspropektion. Erdül kdhlerdgas: Petro- chem, 24, p. 69-76.

1973, Generation of Petroleum-Like substances in coal seams as seen under the microscopic: Advances in organic geochemistry, 6th International Cong. of Geochemistry, p. 379-407.

Théroux, R., 1975, Etude de la pétrographie et des microfacies sédimen- taires sur la série du "Grs de Gaspé" (Devonien inférieur) de la Gaspésie centrale, Quebec: Energy Branch, Quebec Dept. Nat. Resources, open file, 23 p.

Tissot, B., Y. Califet-Debyser, G. Deroo, and J.L. Oudin, 1971, Origin and evolution of hydrocarbons in Early Toarcian shales: Am. Assoc. Petroleum Geologists Bull., V. 55, No. 12, p. 2177-2193.

Tissot, B., B. Durant, J. Espitalié, and A. Combaz, 1974, Influence of nature and diagenesis of organic matter in formation of petroleum: Bull. Am. Assoc. Petroleum Geologists, vol. 58, no. 3, p. 499-506.

Vassoevich, N.B. et al, 1970, Principal phase of oil formation: Moskov. Univ. Vestnik, no. 6, p. 3-27; English transl: Internat. Geology Rev., V. 12, p. 1276-1296.

Visher, G.S., 1965, Use of vertical profile in environmental reconstruction: Bull. Am. Assoc. Petroleum Geologists, vol. 49, no. 1, p. 41-61.

Weaver, C.E., 1960, Possible uses of clay minerals in search for oil: Clays and clay minerals, 8th Nat. Conf., p. 214-227. 91

Weimer, R.J., 1966, Time-stratigraphic analysis and petroleum accumula- tions, Patrick Draw field, Sweet water County, Wyoming: Bull. Am. Assoc. Petroleum Geologists, vol. 50, no. 10, p. 2150-2175.

Williams, H.S., 1910, Age of the Gaspé Sandstone: Bull. Geol. Soc. Am., vol. 20, p. 688-693. APPENDICES

APPENDIX 1

FOSSIL IDENTIFICATION

AHS-74-6-12-58B large, Lower Devonian type spiriferid fragment 58A fossil fragments 56B Siegen or Ems age globithyrid

AHS-74 Bentonite Ash Bed-Lake Branch-Cascapedia-Road Traverse-D. Grenon Siegen or Ems Leptocoelia cf. L. flabellites.

AHS-74-7-13-57F SW Lac Huard York River sandstone with bivalves.

AHS-74-7-30-151 Camp Belanger-Cap Bon Ami Fm. with Leptocoelia and Protochonetes.

AHS-74-8-13-D York River-type sandstone interbedded with dark grey shale with Etymothyris, indicating Etymothyris zone age. Location: lat. 48°23'52", long. 66°21'48".

AHS-74-7-5-51 Charles Vallée "Spirifer" as ensis indicating a Siegen or Ems age (York River ss. age

AHS-74-8-5-3A Cypricardinia, "Spirifer" gaspensis indicating a Siegen or Ems age.

AHS-74-7-23-17 Cypricardinia, crinoidal debris. Age uncertain.

AHS-74-6-13-103 Cascapedia York River Fm. pterineoid, globithyrid? probably Siegen or Ems. 104A (says "b" on specimen) blank.

AHS-74-7-5-51B Charles Vallée "Spirifer" gaspensis, pterineoid, Globithyris sp., Loxonema sp. Siegen or Ems age.

AHS-74-6-27-54b Cascapedia-Salmon Branch-York River sandstone globithyrid Siegen or Ems age.

AHS-74-8-3-150A Discomyorthis? sp., Platyceras sp., "Leptostrophia" cf. magniventra Siegen or Ems.

AHS-74-7-8-62A SW Lac Huard York River sandstone Rhenorensselaeria Siegen or Ems age. 62C SW Lac Huard York River sandstone or Ems age.

AHS-74-7-30-150D Camp Belanger Cap Bon Ami Formation Leptocoelia sp. 150E " " Protochenetes sp. 94

AHS-74-8-26-108 York River sandstone Cyrtina, crinoidal debris Devonian.

AHS-74-8-5-3A Lac St. Anne Grande Grève Limestone trilobite, Acrospirifer murchisoni.

AHS-74-7-8-67B SW Lac Huard York River Formation "Spirifer" gaspensis Siegen or Ems.

AHS-74-8-20-62A York River Formation plant fragments.

AHS-74-8-13-52A Lacs Josué York River Sandstone globithyrid Siegen or Ems. 52B Globithyris sp. Siegen or Ems.

AHS-74-7-8-60C SW Lac Huard York River Sandstone (red) globithirid?

AHS-74-7-24-9 York River Sandstone "chert" pebble. APPENDIX 2

PALYNOSTRATIGRAPHY (INRS-Pétrole, 1975)

Introduction

A total of 106 samples were investigated by standard palynological techniques and identifiable palynomorphs were found in 39 of the samples. All of these productive samples were from the York River Forma- tion with the exception of 4 from the Grande Grêve, 2 from York Lake and 4 from Battery Point rock units; the results of the investigation are summarised on figure P 1. All the productive samples were given filtra- tion treatment in Buchner glass funnels (porosity 2) to remove very fine organic and inorganic debris, and 29 of these samples also required further oxidation treatment by Schulze solution because the palynomorphs were too dark to be identified.

The palynomorphs found consisted mainly of trilete spores, but occasional acritarchs and rare chitinozoans and scolecodonts also occur. The preservation of the fossils was variable and in many cases very good, although in the few samples where carbonisation is advanced, preservation is very poor and generic identification impossible (see also Organic Matter section).

Description of assemblages

The forms recorded below have been listed in order of the lithostratigraphic units in which they occur, from older to younger, and brief comî nts concerning the probable age follow each list. More detailed information concerning the vertical distribution of palynomorphs found in each section is given on figures 1--13, and photographs illustrating some of the forms found, are given on Plates P 1-P 6 FIGURE P 1 SHOWING RESULTS OF SAMPT FS INVESTIGATED

SERIES STAGE FORMATION OR NO. OF PRODUCTIVE PALYNOMORPHS UNIT SAMPTFS SAMPTFS PRESENT

MIDDLE DEVONIAN Eifelian Battery Point 13 4 Spores ?Lake Branch 18 NIL NIL Emsian York River 65 29* Spores, Acritarchs, Chitinozoans, Sco- lecodonts - York Lake 5 2 Spores, Acritarchs, Chitinozoans, Sco- lecodonts LOWER Grande-Greve 5 4 Spores, Acritarchs, DEVONLAN Chitinozoans, Sco- Siegenian lecodonts

Cape Bon Ami NIL Gedinnian

L This'f.igure includes the 6 productive samples from "West Square Forks Road" (see 'Description of Asser^blages' section). 97

GRANDE GREVE FORMATION Lower part contains black carbonised spores and a single carbonised scolecodont.

Upper part (2 samples) contains:

Trilete Spores: Ap.i.cu,e.ati.spotc.bs sp., Ap,i.cutin.etuz-bspona sp., Ap.i,cu,P.vice- tc.usaponct ptica.ta, D.iboUzpoic,i,tu sp., Fmphavwsponi,tez nota.tuh, Kn.aeu~se.e,i)spon,i,tels gazpu.ien4tis, Punc,ta.tizpolc,i,te4 sp., R e,tuz ottc.i,i' etm sp., V etvcucoh-a pm,i,tu sp.

Acritarchs: Battivsphaerr.id.ium sp.,Cyma-Uasphae.7a sp., Mui%tf.p.P,i.c,izphaen.i- cLi,um sp:, Venylucch,i.um sp., V.sp.A V.sp. B, V. sp. C.

Chitinozoans: ?Angochitina sp.

Scolecodonts Probable Age: Upper part of formation - Emsian?

YORK LAKE UNIT

Trilete Spores: Ap.icuta-tirspohts sp., Ap.icu.?ihetws.i,00tca sp., A. minon, Dic- tyotn.i,e.e.ta sp . , Bmphan,ioon,i,tu no.tatu,s, Punc.iatiz po%zi,te4 sp., S-tenozonottc,i,ee.te% sp.

Acritarchs: Ba.?.ti..s phaetc.i.di.um sp., C ymatiois phaeha sp., MatipZiciis phaeh,i.- â,ium sp., Vehyhach.ium sp. A, V. sp. B, V. sp. C.

Chitinozoans : ?Arago cJtii,ti.na sp. Probable Age: Emsian

YORK RIVER FORMATION (Excluding "West Square Forks Road") Trilete Spores: Ap.icu.Ca.t,iispon.ils sp., Ap.icu.Cvice,tu4-i4pona sp., A. ga,5p-i.ejvs-its 98

Anapt.cuw~ pon.i,te's sp., Ae,i.nospon,i,te.s sp., Aunonas pona minuta, Ancynospona togan,i,i., A. ancynea, A. gnand.isp.inosa, C.ti.vo4-i4- pona venkuca,ta, De.P,to.idospona sp., D.ic.tyo.tn.ieetez sp., D. subgnani,sen, DiboWponites sp., D. 2chi.naeeu.s, D. ei6e,P.i.en- s.i,s, Ernplucn,ioon,i,tez no,ta,tws, E. annu,ea,tus, E. elvca.ticu/5, Gnand,izpona sp . , Gnand,ioona maetcotubencutata, Gnanu.ecLt,iis po - n,Lte's sp., Knaeus e.i%iA poh.i,te4 gas p Js.ien.s.i/s , Pune,tatiz pon,i,tez sp. Puiszu,eatiz pon.i tes sp., S-teno zonottt i,eete4 sp., ? Sp-cno zonota,c.- .ee.tes sp., Vettcuc,Uc.e,tuz.izpona nrutti.tubekeu-ea.ta, Vavtueosispon.i,tes sp.

Acritarchs: $a,Q..ti,sphaefc,i.d.i.urn sp., Cyna,tiosphaelca sp., Lophosphaeh,id.i,uxn sp . , M,ichh4pth,i.citusn sp . , Venyhacl2i.um sp. A, V. sp. B, V. sp. C.

Chitinozoans: ?Angoch,i.tina sp.

Scolecodonts: Probable age: Emsian

LAZE BRANCH FORMATION No palynomorphs found.

BATPERY POINT FORMATION

Trilete Spores: Apicu2at,b5 pm.f./s sp . , Apicu,P.iketaz,i.s pona sp . , Anap2an-i,s pon,i,tes sp., Aca:lthott.i.2e,te4' rnut,.ti,se,tu,s var. majon, Ancynospona .eogan,i-i. A. aneynea, Aunonaoona minuta, Diba,izpon,i,tes sp., D.ibo.?.i4- pon.i.te4 cf. D. eclzi,naceu4 , De.P.toidos pona sp., Emphan.i.spon.t,ta naia,tus, Ertii,grnophy.tospona sinp.2ex, Knafuse,E%iispo& i,te4 9aspa.iertis-i~s Pune.tatioon.i.te,s sp., Pwstu,@atvspon.i.tes sp., Re,tieu,ea,tizpo- n.i,tes sp., Re-tuso,tk,i.2e,tu sp., R. s-i.,np.eex, S,tenozono-th i,2.e-tu sp

Probable age: Emsian (to early Eifelian?)

In the list given above, the assemblage for "West Square Forks Road" has 99

not been included because of the uncertain stratigraphic position of the section. It seems probable that the beds are York River Formation although they are not completely typical (personal communication A.H. Sikander 1975). Thus, the assemblage found is listed below: Trilete Spores: Aazn xho.ttc.i.ee-teis mu.e,tiz e,tws , Apieuea-ti.s pon,bs sp., Aneyn000n.a .eogan,ü., A. ancyn.ea, ApicutUte,tuz-izpon.a. sp., A. p.e,ica,ta, Ca,eam000n.a sp., De.P.to-idowAa sp., Dibo2,bspon,i,ie's sp., Die,t yo-ttk,i,eete4 sp., Fmphan,ioon.i,tez n.otatu.s , Gn2nu.ea.ta pon,i- -te4 sp., Gn.cr.nd.i.spotta? macti.otubetcu.,e.ata, Puncta.tioon.i,te4 sp., Puustu.2aVlsponita sp., Re,tulso.tni.ee.ta sp., Rhabdo4pon,i.te4 .E.a.ngi, ? Spinozono-th i,eeta sp., S-tenozono.ttiie,tea sp., Vetvtu- coz.vs pon,i.tu sp. Acritarchs: M-ichny4ttr,id.ium sp., Vettyhach,i,um sp. C. Scolecodont: Probable age: Emsian? or Emsian (to early Eifelian?)?

Discussion of the Assemblages

Any comparison of the assemblages in the respective formations must take into account the wide variation in the numbers of productive samples; for example, the assemblage list for the York River Formation was compiled from more than 20 productive samples, whereas that from Battery Point from only 4, York Lake 2 and Grande Grève 4. Thus, the fact that more forms occur in the York River Formation than any other rock unit (see figure P 2 ) is almost certainly partly the result of this discrepancy, which can only be resolved by further sampling with possibly less eurphasis being placed on collec:,ing from York River Folviatiun.

In the following section, the results so far obtained are compared with the information available from the Eastern Gaspé Peninsular. FIGURE P 2

GENERAL COMPILATION CHART OF PALYNOMORP1 IS FOUND IN THE FORMATIONS .

~ 1 1 1 sl

X n. ~ e s es.

v N - r-,

is ta tu Ci • a ass o. ~ sp. lt ta sp. STAGE FORMATION OR ;~ N ~ (TI

ûs ta • sp. 0

~ sp. F

ta sp. ruc UNIT Q ora u ce tes

w la sp. mu m ne ro ro o7 1`-'~ v â s ¢ nora sp. U) ~ :-) ta ~ ~ ~ • C.1 sp. •• 1) ~ C1 • ' Q. is in ites G, .H 4-, sp. ites ites 0 0 0 0 M sp. O Q 1-) F. cd •.+ a! Q. c: la isp ile is r tes s r ;-. `17. ina dium -1

r-1 a .-1 W m•.1 ver rcu r C 4J •,-1 G; Q m r •r1 O i o ites o tes m

vi 1) U) o F. -H U) 1-) (n U) S-. 0.•' O C) • i Q. • . tr t ch e S r c Q. -H C G) er O bc o c ~ ites idium tus ra ile ceu l. o tus er N a rcu ora or cil Q, U S. Q) r l, CJ 1Â F. Q X•.1 .2 Û 'f -r-i isp isp

o i .- •

G) u O .H1 n O mi ,i c' •r1 O tu isp c

[ is isp oc U) dosp 0 O jor U D. G) 1= (11 Q RiU ro e '. ~i O O O Q r-I 0 la sp cy Q C~ lire asp la o ozon c c

hina i 'Cu . 1 C ri 4y Ç F •-i la ~ ~ •,-i en Q. C • • Û in u isi u tho itu vs f ' tu Ç in hry le han ma N+ Û~ G G. Et Ô o I; ~ (n ~i a i 0

ic ic ino ~- s lt an ivos tus ~ rru lt c ito

r t' CO p anu ae . mac ~ m ~ G an c ec

r •

c ~ 1-) ••F. û O CCu ~ ?Sp Ac Ap A. Auror A. Pu Sco 'i Cl Re ~ mu aa va D. D. Lnp Kr Ve Mi. Dn G? é Cl a, w ~ 7 Gr z x ~ .9 > -

~ An [ r I l I

Eifelian

Battery Point x x x x x x x x x x x x x x x x x x ?Lake Branch?

Emsian York River x x xx xxx xx x x x xx xx xx xxx xxx x x x x xxx xx xxx x York Lake x x x x x x x x Grande Grève x x X x x x x x xxx X X X X X X X X X X •x

Siegenian

Cape Bon-Ami

Gedinnian 101

Comparison of Central Gaspé Assemblages with those from Fa stern Gaspe Peninsula

The ages given for the respective formations shown on figures P 1 and P 2 are partly based on the. study of Devonian spores by McGregor and Owens (1966) (8) and McGregor 1973 (9), these workers investigated the palynology of the Devonian of the eastern-most tip of Gaspé Peninsula. No palynological investigation has, however, previously been carried out on Devonian spores from the Central Gaspé area of this report, neither has any systematic work been carried out on the acritarchs, chitinozoans and scolecodonts from either central or eastern Gaspé. In the following section general comparisons are made between these two localities:-

Cape Bon Ami Formation: a)E. Gaspé Few spore genera recorded Age: Upper Gedinnian b)Central Gaspé No samples available Grande Grève Formation: a)E. Gaspé Assemblage more diverse than Cape Bon Ami, but few forms in comparison to younger formations. Age: Siegenian, although upper most part of formation Emsian b)Central Gaspé Spores carbonised in lower part. In upper part spores relatively rare in the 2 productive samples. Age: Lower part not determinable. Upper part: The presence of Apicu- L i ketu.-pony pEicata and Knaeuis e- LL pon,i tes gazpuiert/s,r s favour an Emsian age. York Lake Unit: a) E. Gaspé Unit not recognised. 102

b) Central Gaspé Few diagnostic forms, but presence of ApicutiAe tuts . potca mJnon favours an Emsian age. York River Formation: a) E. Gaspé A very varied assemblage of Emsian age. b) Central Gaspé Similar to that of E. Gaspé, except (excluding 'West Square Forks Road") in upper part occur occasional spe- cimens of Ancy Loocna. Age: Emsian. Lake Branch Formation: a)E. Gaspé Formation not recognised b)Central Gaspé No identifiable palynomorphs. Battery Point Formation: a) E. Gaspé Lower part in general similar to York River and of Emsian age. Upper part characterized by large forms, especially Ancyn000na. Age: Emsian to early Eifelian. b) Central Gaspé Spores in any significant numbers found in only one sample towards the top of the formation and like E. Gaspé contains a number of Ancyhozposut. Age: Upper part of formation Emsian to early Eifelian.

'Conclusions

In general there are many similari_fies between the assemblages found in the Central Gaspé and the Eastern Gaspé areas. The most significant discrepancy appears to be that of the "West Square Forks Road" section, which on lithostratigraphic criteria has been tentatively included in 103 the York River Formation. However, the assemblage of palynomorphs found in the samples shows certain similarities to that recorded by McGregor and Owens (8) and McGregor (9) from the upper part of the Battery Point Forma- tion i.e. the frequent occurrence of Anclnaoona. However, Anclno4pona also occurs occasionally in the upper part of York River Formation in the Central Gaspé area, although it is apparently absent from this formation in Eastern Gaspé. The presence of acritarchs and scolecodonts in a few of the samples from "West Square Forks Road" indicates marine influence and similar forms also occur in the York River Formation. No marine palynomorphs were found however in the 4 fossiliferous samples from the RRttery Point Formation. 104

APPENDIX 3

FIELD PHOTOGRAPHS 105

Photograph 1: Thin silty and argillaceous limestone beds in dark grey calcareous silty shale, Cap Bon Ami formation along Seventeen Mile Brook. Locality 8-25-106.

Photograph 2: Thin bedded silty limestone and calcareous shale, Cap Bon Ami formation: Locality 8-'25-108A. 106

Photograph 3: Pillow-type structures in the pyroclastics and volcanics

Cap Bon Ami - Grande Grève contact (?), West Lake Branch area: Locality 8-23-110.

Photograph 4: A volcanic and pyroclastic unit underlying the York River formation, Salmon Branch road: Locality 6-13-101. :107.

Photograph 5: Thinly bedded calcareous siltstone, silty limestone, upper York River formation, Salmon Branch river: Locality 6-27-51.

Photograph 6: Ripples-marks, York River siltstone, Salmon Branch river: Locality 6-27-55. 108

Photograph 7: Brownish maroon coloured thinly laminated siltstone, York River formation, Salmon Branch river: Locality 6-27-53.

Photograph 8: Worm-burrowing, bedding surface, York River siltstone, Salmon Branch river: Locality 6-28-48. 109

Photograph 9: Rare mud-cracks in very fine-grained York River sandstone, Salmon Branch river: Locality 6-28-48.

Photograph 10: "Typical" grey to greenish grey, fine grained, inclined bedded York River sandstone, Salmon Branch river: Loca- lity 6-27-56. 110

Photograph 11: Inclined bedding in grey, fine-grained York River sandstone, Trans-Gaspe Highway: Locality 6-1Z-17.

Photograph 12: Rare convulate bedding, York River formation, Salmon Branch river: Locality 6-28-48. 111

Photograph 13: Bottom structures (worm-burrows?), York River sandstone Charles Valley road: Locality 7-5-53.

Photograph 14: Reddish brown to red, very fine grained, thinly bedded silty, highly fossiliferous sandstone and shale, upper York River formation, Lake Branch road: Locality 7-8-68. 112

Photograph 15: Festoon-bedded, red coloured, very fine to fine grained sandstone, Lake Branch formation, Lac Huard (Loon Lake) area: Locality 6-19-31.

Photograph 16: Battery Point Sandstone intruded by a basic sill near the York River Battery Point contact: Note rain prints. Charles Valley road: Locality 7-3-66. 113

Photograph 17: Battery Point sandstone covered scree slope, east valley wall, Cascapedia River: Locality 6-17.

Photograph 18: Cross-bedded Battery Point sandstone containing quartz, quartzite, and shale clasts, Cascapedia River eastern valley slope: Locality 6-17-101. 114

Photograph 19: Thin and small shale lenses presumably resulting from a flattening out of shale clasts within thinly bedded Battery Point sandstone, near the contact with the red Square Forks facies, north slope, Square Forks Valley: Locality 6-20-102.

Photograph 20: Massive cross-bedding in the Battery Point sandstone, Josué Lake road: Locality 6-17-52. 115

Photograph 21: cross-bedding, Battery Point sandstone, Josué Lake road: Locality 6-17-51. Photograph 22: A view of Battery Point shale outcrop in the foreground, cut into by a channel type, highly cross bedded fluvial sandstone. Arrow shows the basal conglomerate in the sandstone unit, Square Forks road: Locality 6-15-25. 117

Photograph 23: Greenish grey and red mottled colouration of the "Square Forks facies", Battery Point formation, Square Forks road: Locality 6-17-30.

Photograph 24: Shale conglomerate, "Square Forks facies", Square Forks road: Locality 6-17-30. 118

Photograph 25: Mud-cracks in the "Square Forks facies", Battery Point formation, Square Forks road: Locality 6-17-30.

Photograph 26: Reddish grey to dark grey shale and siltstone forming

the lower part of the "Square Forks facies", Battery Point formation, Square Forks road: Locality 6-17-30. 119

Photograph 27: Red, fine to medium grained medium to thick bedded,

highly cross-bedded sandstone. "Square Forks facies", Battery Point formation. Nouvelle road: Locality 7-15-4.

Photograph 28: Bedding surface "Square' Forks facies", Battery Point, showing northward current direction. Nouvelle road south: Locality 7-15-7. LEGENDE-LEGEND

DEVONIEN-DEVONIAN

Granite et feisite Granite and feisite 13 45 •

Andesite Andesite 12

Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point 110 1 Lake Branch Lake Branch 9 York River York River 7 Volcaniques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite basalt, andesite Groupe'de York Lake .York Lake F----1 5 Fortin

Grande Grève Grande Greve 4

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN 30 St-Léon I 2 St. Leon (2a) Mbr de Baldwin ` (2e) Baldwin mbr. CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickshock Group Métasédimentaires, méta- Metasediments, meta- volcaniques volcanics .825 30 IS •• e "s5 Faille Fault COUPES ETUDILES SECTIONS INVESTIGATED Axes de plis Fold axes Ruisseau Brandy et Brandy N. 7 Nouvelle M. et Cascanedia Branch 1 Brandy and Brandy N. Brooks. du Lac O. Nouvelle U. and Cascanedia Lake Branch. Contact géologique Geological contact Cascapedia Bras aux Saumons. 2 Salmon Branch. Ruisseau Caron. u 8 Caron Brook. 3 Ruisseau Quatorzieme aille Milles 0 4 B Miles Fourteen file Brcok. Ruisseau Marcil O. 9 llarçi I W. Broc'c. 47' Ruisseau Go-Ashore. Kilomètres 10 Kilometres •• • •7•vW ECHELLE-SCALE 4 Go-Ashore Brook. Ruisseau Charles Vallee. 10 Charles Valley Brook. Ruisseau t'iner 5 Miner Brook Route Square Forks, et les Lacs Josué. 11 FIGURE 7 : DISTRIBUTION GEOGRAPHiQUE, FORMATION DE Cap Bon Ami Souare Forks Road, and Josue Lake. SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Rivibre t!ouvelle S. GEOGRAPHIC DISTRIBUTION, Cap Bon Ami Formation lbuve le Hiver S. BERRY MOUNTAIN SYNCLINE, QUEBEC. .._

LEGENDE-LEGEND

DEVONIEN-DEVONIAN

Granite and felsite Granite et felsite 13

Andesite Andesite 12

Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point ~ 10 I Lake Branch Lake Branch 9 York River York River

Volcaniques, rhyolite. Volcanics, rhyolite, 6 basalte, andesite basalt, andesite 8 Groupe de York Lake ,York Lake Fortin 5

Grande Grève Grande Greve 4 1

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN St-Léon St. Leon 2 (2a) Mbr de Baldwin (2a) Baldwin mbr,

CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN

Groupe de Shickshock 1 Shickshock Group Métasédimentaires, meta- Metasediments, meta- volcaniques volcanics

64' 3r COUPES ETUDILES Faille Fault so°N SECTIONS INVESTIGATED Nouvelle N. et Cascapedia Eranch Axes de plis Fold axes Ruisseau brandy et Brandy N. 7 Brandy and Brandy N. Brooks. du Lac O. r 41° Nouvelle N. and Cascapedia Lake Branch. Contact géologique Geological contact' 2 Cascapedia Bras aux Saumons. Salmon Branch. 8 Ruisseau Caron. u Caron Brook. Ruisseau Quatorzieme Mille 3 Ruisseau tiarcil O. 4 8 Miles Fourteen Vile Brook. Milles 0 9 farci I W. Broc'<. u• Kilometres w Ruisseau Go-Ashore. Kilomètres 10 e6 61 s2° 4 Charles Vallee. ECHELLE-SCALE Go-Ashore Brook. Ruisseau 10 Charles Valley Brook. Ruisseau t'iner 5 Miner Brook Route Square Forks, et les Lacs Josué 11 Souare Forks Road, and Josue Lake. FIGURE 8: DISTRIBUTION GEOGRAPHIQUE, FORMATION. DE Grande Grève SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Rivière Nouvelle S. GEOGRAPHIC DISTRIBUTION, Grande Grève Formation t:ouvetle River S. BERRY MOUNTAIN SYNCLINE, QUEBEC. I 44 SO M / 4 LEGENDE-LEGEND / 2 DEVONIEN-DEVONIAN

Granite et felsite Granite and felsite 6 ' 13 45 '

Andesite Andesite 12 4 Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point ~ 10 Lake Branch Lake Branch 9 York River York River 7 4 Volcaniques, rhyolite, Volcanics, rhyolite, 6 6 basalte, andesite basalt, andesite 8 Groupe de .York Lake York Lake Fortin A 6 Grande Grève Grande Greve 4

Cap Bon Ami 3 Cap•Bon Ami 8 SILURIEN DEVONIEN-SILURIAN DEVONIAN 00 / St-Léon 2 St. Leon (2a) Mbr de Baldwin (2a) Baldwin mbr. 2 ~~tN/SV OE ? ~0 / J CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN • 6/ Groupe de Shickshock 1 Shickshock Group 2~, +~ ~ Métasédimentaires, méta- Metasediments, meta- volcaniques / L . volcanics AHS ]S 8 1 t ~ 44, 3 IS' 006 OS^SS'W 6A ° 39 30 Faille Fault COUPES ETUDIEES SECTIONS INVESTIGATED Axes de plis Fold axes .laure., Ruisseau Brandy et Brandy N. 7 Nouvelle M. et Cascapedia Branch ~ s' 1 Brandy and Brandy N. Brooks. du Lac O. Nouvelle N. and Cascapedia Lake Br3Mtn. Contact géologique Geological contact Cascapedia Bras aux Saumons. 2 Salmon Branch. Ruisseau Caron. ~ Caron Brook. 3 Ruisseau Quatorzieme Mille Milles O 4 8 Miles Fourteen Nile Brcok. Ruisseau Marcil O. 9 tlarci I W. Broc'c. 0 Ruisseau Go-Ashore. Kilomètres 10 Kilometres OP w 046 61.W ECHELLE-SCALE 4 Go-Ashore Brook. RL'isseau Charles Vallee. 10 Charles Valley Brook. Ruisseau Miner 5 Miner Brook Route Square Forks, et les Lacs Josué. FIGURE 9 : DISTRIBUTION GEOGRAPHIQUE, Facies de York Lake 11 Snuare Forks Road, and Josue Lake. SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Riviére Nouvelle S. GEOGRAPHIC DISTRIBUTION. York Lake Facies Nouvelle River S. BERRY MOUNTAIN SYNCLINE, QUEBEC. W t ~ LEGENDE-LEGEND

DEVONIEN-DEVONIAN

Granite et felsite Granite and felsite 13 ~

Andesite Andesite 12

Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point 10 Lake Branch Lake Branch 91 York River York River 7 Volcaniques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite basalt, andesite 8 Groupe de York Lake .York Lake 5 Fortin

Grande Grève Grande Greve 4

Cap Bon Ami 3 Cap Bon Ami

SILURIEN DEVONIEN-SILURIAN DEVONIAN 30 St-Léon St. Leon 2 (2a) Ilbr de Baldwin (2a) Baldwin ,nbr. CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock I Shickihock Group Métasédimentaires, méta- Metasediments, meta- volcaniques volcanics AHS 75 44.35' 65 39 ' Faille Fault COUPES ETUDILES SECTIONS INVESTIGATED Axes de plis Fold axes ( s Ruisseau brandy et Brandy N. 7 Nouvelle N. et Cascaneeia Branch 1 Brandy and Brandy N. brooks. du Lac O. ,r• Nouvelle N. and Cascanedia Lake Branch. Contact géologique Geological contact 2 Cascapedia Bras aux Saumons. Salmon Branch. 8 Ruisseau Caron. u Caron Brook. 3 Ruisseau Quatorzieme tille Milles 0 8 Miles Fourteen rile Brcok. Ruisseau liarcil O. 9 farci 1 1:. broC'<. 1 47 . Ruisseau Go-Ashore. Kilomètres 10 Kilometres 0• 60 '4 ♦2'w 4 ECHELLE-SCALE Go-Ashore Brook. Ruisseau Charles val lee. 10 Charles Valley Brook. Ruisseau riner 5 Miner Brook Route Square Forks, et les Lacs Josué. FIGURE 10: DISTRIBUTION GEOGRAPHiQUE, FORMATION DE York River 11 Souare Forks Road, and Josue Lake. SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Rivitre Nouvelle S. GEOGRAPHIC DISTRIBUTION, York River Formation i:ouvetle Hiver S. BERRY MOUNTAIN SYNCLINE, QUEBEC. oc‘

98° 50'N 1~~ • 4 LEGENDE-LEGEND 2 DEVONIEN-DEVONIAN

Granite et felsite Granite and felsite 13 45 •

Andesite Andesite 12 4 Battery Point Battery Point

Facies de 'Square Forks' Square Forks facies 11 Battery Point typique H0 I Typical Battery Point Lake Branch Lake Branch 9 York River York River 7 1 4 Volcaniques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite basalt, andesite Groupe de York Lake .York Lake r---1 5 Fortin

Grande Grève Grande Greve 4 7

Cap Bon Ami Cap Bon Ami 3 -11,)1(/' 8 SILURIEN DEVONIEN-SILURIAN DEVONIAN 30 St-Léon 2 1 St. Leon / C0 (2a) Mbr de Baldwin 1 (2a) Baldwin mbr. EN~ URE $ON CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN ? /• ~~~ Groupe de Shickshock 1 Shickshock Group 20 4+ ~ Métasédimentaires, méta- Metasediments, meta- 7 /. I volcaniques volcanics 6H5 75 8 / 5 ~ ••h5' • 64 la So is• • 0!°55 W Faille Fault COUPES ETUDILES SECTIONS INVESTIGATED

Axes de plis Fold axes s, Ruisseau brandy et Brandy N. 7 Nouvelle M. et Cascanec'ia branch 1 Brandy and Brandy N. brooks. du Lac O. •M Nouvelle N. and Cascanedia Lake Branch. Contact géologique Geological contact Cascapedia Bras aux Saumons. 2 Salmon Branch. Ruisseau Laron. 8 Caron Brook. 3 Ruisseau Qu.atorzieme Mille Millets 0 4 8 Miles Fourteen file Brook. Ruisseau Marcil O. 9 Mardi 1:. Broc`<. Ruisseau Go-Ashore. Kilomètres 10 Kilometres • i7 00 N ECHELLE-SCALE 4 Go-Ashore Brook. Rk'isseau Charles Vallee. 10 Charles Valley Brook. Ruisseau Finer 5 Miner Brook Route Square Forks, et les Lacs Josué. FiGUREI i: DISTRIBUTION GEOGRAPHIQUE, FORMATION DE Lake Branch 11 Souare Forks Road, and Josue Lake. SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Riviére i!ouvelle S. GEOGRAPHIC DISTRIBUTION, Lake Branch Formation tbuveile River S. BERRY MOUNTAIN SYNCLINE, QUEBEC.

3 4 LEGENDE-LEGEND

DEVONTEN-DEVONIAN

6 Granite et felsite Granite and felsite 13 45 ,

Andesite Andesite 12 4 Battery Point Battery Point

Facies de 'Square Forks' 11 Square Forks facies Battery Point typique Typical Battery Point 1 10 Lake Branch Lake Branch 9 York River York River 7 4 Volcaniques, rhyolite, Volcanics, rhyolite, 6 basalte, andesite basalt, andesite 8 Groupe de York Lake .York Lake 5 Fortin 6' Grande Grève Grande Greve ~ • —~ 7 4 \ Cap Bon Ami 3 Cap Bon Ami ,,/ ~11 ~IF 8 SILURIEN DEVONIEN-SILURIAN DEVONIAN 50' St-Léon 2 St. Leon (2a) Mbr de Baldwin (2a) Baldwin mbr. 1 CAMBRO-ORDOVICIEN-CAMBRO-ORDOVICIAN Groupe de Shickshock 1 Shickshock Group Métasédimentaires, méta- Metasediments, meta- 7 volcaniques volcanics 7 AM5 75 xe°IS' 15 ~ e 65°55'w 6.5° 59' ao Faille Fault COUPES ETUDILES SECTIONS INVESTIGATED Axes de plis Fold axes Ruisseau Brandy et Brandy N. 7 Nouvelle M. et Cascanec'ia Lranch 1 Brandy and Brandy N. Brooks. du Lac O. Nouvelle N. and Cascanedia Lake Branch. Contact géologique Geological contact f 2 Cascapedia Bras aux Saumons. Salmon Branch. Ruisseau Laron. 8 Caron Brook. Ruisseau Quatorzieme Fille 3 Ruisseau Marcil O. Milles O 4 Miles Fourteen rile Brcok. 9 Farci I l:. Broc'<. Kilomètres 10 Kilometres Ruisseau Go-Ashore. ECHELLE-SCALE 4 Go-Ashore Brook. Ruisseau Charles Vallee. 10 Charles Valley Brook. Ruisseau Miner 5 Miner Brook Route Square Forks, et les Lacs Josué. FIGURE 1 2 DISTRIBUTION GEOGRAPHIQUE, FORMATION DE Battery Point' 11 Souare Forks Road, and Josue Lake, SYNCLINAL DE BERRY MOUNTAIN, QUEBEC. 6 Cascapedia Branche du Lac. Lake Branch. 12 Riviére Nouvelle S. GEOGRAPHIC DISTRIBUTION, Battery Point Formation r:ouve:le River S. BERRY MOUNTAIN SYNCLINE, QUEBIC. 95 APPENDIX 2

PALYNOSTRATIGRAPHY (INRS-Pétrole, 1975)

Introduction

A total of 106 samples were investigated by standard palynologi — cal techniques and identifiable palynomorphs were found in 39 of the samples. All of these productive samples were from the York River Forma- tion with the exception of 4 from the Grande Grave, 2 from York Lake and 4 from Battery Point rock units; the results of the investigation are summarised on figure P 1. All the productive samples were given filtra- tion treatment in Buchner glass funnels (poroity 2) to remove very fine organic and inorganic debris, and 29 of these samples also required further oxidation treatment by Schulze solution because the palynomo.vphs were too dark to be identified.

Description of assemblages

The forms recorded below have been listed in order of the lithostratigraphic units in which they occur, from older to younger, and brief comments concerning the probable age follow each list. More detailed information concerning the vertical distribution of palynomorphs found in each section is given on figures 1--13, and photographs illustrating some of the forms found, are given on Plates P 1-P 6 FIGURE P 1 SHOWING RESULTS OF SAMPLES INVESTIGAThD

SERIES STAGE FORMATION OR NO. OF PRODUCTIVE PALYNOMORPHS UNIT SAMPTE S SAMPTFS PRESENT

MIDDLE DEVONIAN Eifelian Battery Point 13 4 Spores ?Lake Branch 18 NIL NTT, Emsian York River 65 29* Spores, Acritarchs, Chitinozoans, Sco- lecodonts York Lake 5 2 Spores, Acritarchs, Chitinozoans, Sco- lecodonts

LOWER Grande-Greve 5 14 Spores, Acritarchs, DEVONIAN Chitinozoans, Sco- Siegenian lecodonts

Cape Bon-Ami NIL Gedi nriian

This figure includes the 6 productive samples from "West Square Forks Road" (see 'Description of Asserblages' section). 97

GRANDE GREVE FORMATION Lower part contains black carbonised spores and a single carbonised scolecodont.

Upper part (2 samples) contains:

Trilete Spores: Ap.icu,2at,ioon4.4 sp . , Ap,i.ca itcetws-us pona sp . , Apieu,e.ih.e- Aus-vspon.a pZi.ca-ta, Dibo.?.vsponite4 sp., Emphanipon.i,tez nota.tuz, KnaeuzetZspon.i,tu gaou.i.enz.c4, Punc,tat.ioon,i.tez sp . , R etuz o.ttc.i,2etez sp., V etcnueo.s-bs pon.i.te4 sp.

Acritarchs: Ba,P.tts phaen.id,ium sp., C yma,tio4 phaena sp., Matipac,ivs phaetc,i.- dium sp. , V en yhach.i,um sp . , V . sp . A V . sp . B, V. sp. C.

Chitinozoans: ?Angochiti.na sp.

Scolecodonts

Probable Age: Upper part of formation -- Emsian?

YORK LAKE UNIT

Trilete Spores: Ap,icu.tati spo sp., Apicaiketcus.izpona sp., A. m.inon, V.i.c- t yotnit e a sp., Emphan,i s pote i t ers nota , Punc ta iz pok tu sp. StenozonotAi e,a sp.

Acritarchs: Ba,~tGt,i,s phaetr..i.dium sp . , Ca,t.t.oz phaena sp . , MuL tip.P i.e,iohaeh-i.- dium sp., Venyh.ach,ium sp. A, V. sp. B, V. sp. C.

Chitinozoans: ?Angoc iti.na sp. Probable Age: Emsian

YORK RIVER FORMATION (Excluding ''est Square Forks Road"

Trilete Spores: Apicu.Ca.tiz pon-bs 8p., Ap,icu,e itt.etuzipona sp., A. ecop-i.ewS,i.s 98

Anapaltii4pon.i,te4 sp., Ae,i.no4pon,i,teZ sp., Autcona4pona minuta, Ancyno4pona .2og.an.i,i., A. ancpnea, A. gnandi4pno4a, C.Zivo444.- pona v etvcucata, Datoido4 pona sp., Dic,t yotA i.2.ete4 sp., D. 4ubgnarii.6eh., Dibo.e,ioon,i,te,s sp., D. zchinaeeu4, D. e qe,Zi..en- 4a, Emplucn.izpon,i,te4 notatu4, E. annuX.atu4, E. etvcat,i,cu4, Gnand,ioona sp., Gnandizpona mactcotubetccu2ata, Gnanutat,voo- n,i,te4 sp., Knaeut~ e,~.i~s pot.i,tus ga4 p nlien4.i4 , Puaictat.ioon,ite4 sp., Pu4tu2atioon,ite4 sp., Stenozcnottc,i,e.ete4 sp., ? Spinozonottt,i.- Qete4 sp., Vetctcue,itcetu4.i.4pona muP.ti.tubetceu.eata, Vetvzuco4i4ponite4 sp. Acritarchs: Ba.2t,i4phaetc.i.d,i.u.m sp., C yrna,t.i,o4 phaetca sp., Lo pho4 phaetc,i.cti.um sp . , M-i.chn. y4ltr.icLi.cun sp . , V e1c yhach.ium sp. A, V. sp. B, V. sp. C.

Chitinozoans: ?Angoch,i.ti.na sp.

Scolecodonts: Probable age: Emsian

LAKE BRANCH FOPNATION No palynomorphs found.

BATTERY POINT FOR.PifATION

Trilete Spores: Apicutat,izpo4 sp., Apiccc2-ihetaz-c4pona sp., Anapaw,ioon,i,tez sp., Acao.thotn,i,2e,te4' rnutti.setuo var. majon, Ancyno4pona .2ogan,a A. ancynea, Aunona4pona minuta, Dibotizpon,ite4 sp., D-i.bo.P,izpon,i.ta cf. D. eclzi.nace.u4, Dettotido4pon.a sp., Empian,i.4pon.itu notatu4, Erzi.gmophyto4pona 4inptex, KnaEu4e,E;izpon,ite4 ga4pcztei144.4 PUnctatioon,i te4 sp., Puistutat.bspon.ite,s sp., Re.t.icuta-t.izpo- n,i,te4 sp., Re.tu4ottc-i,22te4 sp., R. 4ianptex, Stenozonoth.i,2e,te4 sp.

Probable age: Emsian (to early Eifelian?)

In the list given above, the assemblage for "West Square Forks Road" has 99

not been included because of the uncertain stratigraphic position of the section. It seems probable that the beds are York River Formation although they are not completely typical (personal communication A.H. Sikander 1975). Thus, the assemblage found is listed below: Trilete Spores: Aaznthottc itetez mat,i4etws, Aptcutat.izpotc.bs sp., Ancytcozpotca togan,i,i,, A. ancytcea, Ap-tcuP.iJcetuz.izpotuz sp., A. p.?.i.cata, Ca.E'am000tca sp., DeX.to.i.d000rca sp . , aibo-P.vootc.i,te4 sp . , Dietyottc,i,eete4 sp., Emphavwspojci,te4 notatua, Gtcanutat.iootc,i.- tu sp . , Gtcand.i..s po>ta? maetcotubeJc.cu.e.ata, Pune.tat:ih pote-i,ta :;p., Puztu.ea,ti4potc,i,te,s sp., Retuisott.i,e.etez sp., Rhabd000A,itez .Eangi, ? Sptinozonott.i.e.etu sp., StenozonotJc i,eete)5 sp . , Vetveu- cob-vs potcite2s sp. Acritarchs: M,i.cGvc y4tJc,i.dium sp . , V eJc. y6iaclzi,um sp. C. Scolecodont: Probable age: Emsian? or Emsian (to early Eifelian?)?

Discussion of the Assemblages

Any comparison of the assemblages in the respective formations must take into account the wide variation in the numbers of productive samples; for example, the assemblage list for the York River Formation was compiled from more than 20 productive samples, whereas that from Battery Point from only 4, York Lake 2 and Grande Grève 4. Thus, the fact that more forms occur in the York River Formation than any other rock unit (see figure P 2 ) is almost certainly partly the result of this discrepancy, which can only be resolved by further sampling with possibly less emphasis being placed on collec:,ing from York River Formation.

In the following section, the results so far obtained are compared with the information available from the Eastern Gaspé Peninsular. FIGURE P 2

GENERAL COMPILATION CHART OF PALYNOMORPHS FOUND IN THE FORMATIONS I 1

tus~

tn lex res.

ise ta tus C. • C. •

D. i sp. lt ta imp m STAGE FORMATION OR ~~~ ~ ~ ~. ~ i ta sp.

sp. • m sp. gas ta sp.

s ,) •) o w UNIT C; • c. c. a 1 n. ~ ora sp. an ceus mu rn la L~ G. ro C) CO 1) c., g M ~E E: Î U)

so. to •;i C) r) C.~) ~ u _ a is inu osa sp. ites tn W ora ites ites 6î ' C r-i •-1 U) C' •r CJ ..-4 of C). L: isp ites log

U) tes

verruca .r1 ites r • Qi ai Q) C) ,—. F, •r r1 `D F. v L IA or in

m r ites hina or

•r U) o J-, F. U) so. J-) ~ •^, F. O CO •r1 C) •ri a •r • or a

N ites

C~ bercu O O ~ or Q) C) 7,-.4-)~ :3 O F. Cr: F, U) T., ~ 1= ites

tus ~ ile 1, r x 4- Eli or tosp sp n 1 U~ Q) r a r, o ' F U ~ or

:) nora .r N i. icus ,-+ m M ora tu Cr O Q) M C, ~ o C. •r .P ec C tisp isp or rea tr or disp el • tisp 1 t t lisoor F-, O hy C, I-1 çlÛ O co f.-. .0 L ta ..0 +1 P .0 ~U• ire 'is soora 0 W n is D. isp `. ~ 1' TJ J~ r- NO•rZL.O r--1 U O ~ la ~+ l hinaceus •r r1 la la Ç • op O = 0 0 0+) c: •1 c C. >--.. cri. • • O c u la osp ro rasp ran tho lisoo f

r-t use +-i O disp ta to •r J Ô •-~ , O•r ~ = a C O c) ec tu G Eh major Q i han u ui •r .,--i i-) âj r 1- >, U c ~ .-i ic icu in ro cy r igm O r1 an anu .:) , ...-1 r1 C, ancy g macro 4- :J a GO O O c erra can • ,--1 C. • ? Q; • .- U ; Q) J Sr„' , ~ ~ C) ~7 An Ap Ac Au An A. A. va Clivos Pus

¢ ‹ Dibo D. D. S. Fn Gr C= iCrae Punc ~ Cr C~ rî, c• c• C!' Q ~ G! Emp W X .0,-. .5 ~ C Ù a z ~ 5 J• ) - Anap ~

Eifelian

Battery Point x x x X X X x x x x x x x X x x x x ?Lake Branch?

Emsian York River X X xx x x x x x x x x x X X x X X X X x X X x X X x X X X X X York Lake x x x x X X X X Grande Grève X X X x X X X X X X X X X x x X x X X X x XX X

Siegenian

Cape Bon-Ami

Gedinnian

Comparison of Central Gaspé Assemblages with those from Eastern Gaspe Peninsula

The ages given for the respective formations shown on figures P 1 and P 2 are partly based on the study of Devonian spores by McGregor and Owens (1966) (8) and McGregor 1973 (9), these workers investigated the palynology of the Devonian of the eastern-most tip of Gaspé Peninsula. No palynological investigation has, however, previously been carried out on Devonian spores from the Central Gaspé area of this report, neither has any systematic work been carried out on the acritarchs, chitinozoans and scolecodonts from either central or eastern Gaspé. In the following section general comparisons are made between these two localities:-

Cape Bon Ami Formation: a)E. Gaspé Few spore genera recorded Age: Upper Gedinnian b)Central Gaspé No samples available Grande Grève Formation: a)E. Gaspé Assemblage more diverse than Cape Bon Ami, but few forms in comparison to younger formations. Age: Siegenian, although upper most part of formation Emsian b)Central Gaspé Spores carbonised in lower part. In upper part spores relatively rare in the 2 productive samples. Age: Lower part not determinable. Upper part: The presence of Apicu- Likauzi.vma pava ta and Knaews e- tizpon,itus gais eziews favour an Eisi.an age. York Lake Unit: a) E. Gaspé Unit not recognised. 102

b) Central Gaspé Few diagnostic forms, but presence of Apicutiketuisapoka minor favours an Emsian age. York River Formation: a) E. Gaspé A very varied assemblage of Emsian age. b) Central Gaspé Similar to that of E. Gaspé, except (excluding 'West Square Forks Road") in upper part occur occasional spe- cimens of Ancytwoofuz. Age: Emsian. Lake Branch Formation: a)E. Gaspé Formation not recognised b)Central Gaspé No identifiable palynomorphs. Battery Point Formation: a) E. Gaspé Lower part in general similar to York River and of Emsian age. Upper part characterized by large forms, especially Ancyno4pona. Age: Emsian to early Eifelian. b) Central Gaspé Spores in any significant numbers found in only one sample towards the top of the formation and like E. Gaspé contains a number of Anc yno4 polLa . Age: Upper part of formation Emsian to early Eifelian.

Conclusions

In general there are many similarities bett,.rPeri the asCemb,lages found in the Central Gaspé and the Eastern Gaspé areas. The most significant discrepancy appears to be that of the "West Square Forks Road" section, which on lithostratigraphic criteria has been tentatively included in 103 the York River Formation. However, the assemblage of palynomorphs found in the samples shows certain similarities to that recorded by McGregor and Owens (8) and McGregor (9) from the upper part of the Battery Point Forma- tion i.e. the frequent occurrence of Ancyxo4pona. However, Ancyno4 pony also occurs occasionally in the upper part of York River Formation in the Central Gaspé area, although it is apparently absent from this formation in Eastern Gaspé. The presence of acritarchs and scolecodonts in a few of the samples from "West Square Forks Road" indicates marine influence and similar forms also occur in the York River Formation. No marine palynomorphs were found however in the 44 fossiliferous samples from the Battery Point Formation. 104

APPENDIX 3

FIELD PHOTOGRAPHS 105

Photograph 1: Thin silty and argillaceous limestone beds in dark grey calcareous silty shale, Cap Bon Ami formation along Seventeen Mile Brook. Locality 8-25-106.

Photograph 2: Thin bedded silty limestone and calcareous shale, Cap Bon Ami formation: Locality 8-L5-108A. 106

Photograph 3: Pillow-type structures in the pyroclastics and volcanics contact (?), West Lake Branch Cap Bon Ami - Grande Grève area: Locality 8-23-110.

Photograph 4: A volcanic and pyroclastic unit underlying the York River formation, Salmon Branch road: Locality 6-13-101. 107

Photograph 5: Thinly bedded calcareous siltstone, silty limestone, upper York River formation, Salmon Branch river: Locality 6-27-51.

Photograph 6: Ripples-marks, York River siltstone, Salmon Branch river: Locality 6-27-55. 108

Photograph 7: Brownish maroon coloured thinly laminated siltstone, York River formation, Salmon Branch river: Locality 6-27-53.

Photograph 8: Worm-burrowing, bedding surface, York River siltstone, Salmon Branch river: Locality 6-28-48. 109

Photograph 9: Rare mud-cracks in very fine-grained York River sandstone, Salmon Branch river: Locality 6-28-48.

Photograph 10: "Typical" grey to greenish grey, fine grained, inclined bedded York River sandstone, Salmon Branch river: Loca- lity 6-27-56. 110

Photograph 11: Inclined bedding in grey, fine-grained York River sandstone, Trans-Gaspe Highway: Locality 6-11-17.