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 CANADA 
 
 DEPARTMENT OF MINES 
 How. Maktin Bubbux, Ministib; R. G. McConmm.l. Dimjty Ministm. 
 
 GEOLOGICAL SURVEY 
 
 WiLUAM MclNNBt, UlUCTINO GBOLOGIST. 
 
 v 
 
 MEMOIR 1«9 
 
 No. 94, GSOLOOKAL SBBIBS 
 
 The Harricanaw-Turgeon Basin, 
 Northern Qwebec 
 
 BY 
 
 T. L. Tanton 
 
 ».- 
 
 ( 
 
 OTTAWA 
 
 J. DC LABROqUERIE TACH£, 
 
 PMNTER TO THE KING'S MOST EXCELLENT MAJESTY 
 
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CANADA 
 
 DEPARTMENT OF MINES 
 
 HoM. Makhm Buinti Mimtna; R. G. McCommbix, Dinnv MiNimi. 
 
 GEOLOGICAL SURVEY 
 
 William McInmbs. Dirbctino GBouiom. 
 
 MEMOIR IM 
 
 No. 94, GiOLOoicAL Sbbies 
 
 I 
 
 The Harricanaw-Turgeon Basin, 
 Northern Quebec 
 
 BY 
 
 T. L. Tanton 
 
 OTTAWA 
 
 I. Di LABROQUERIE TACHfi, 
 
 PKL IR TO THE KINO'S MOST EXCELLENT MAJESTY 
 
 m* 
 
 No. 1735 
 
 69813—1 
 
CONTENTS. 
 
 CHAPTER I. 
 
 IntroduetkM 1 
 
 OMtonl tutemmt Mid ■eknowledgment* 1 
 
 tioemtion and mtp* ? 
 
 McUM of commuBkathm 1 
 
 History 1 
 
 Pnvioua work S 
 
 BibUocnphy 4 
 
 CHAPTER II. 
 
 8ummMy mmI eoneliwkxM 
 
 Topography 
 
 OenMlkl leolncy. . « 6 
 
 Eeooomie leoiafy 7 
 
 CHAPTER III. 
 
 General character of the district t 
 
 Topography S 
 
 General account 8 
 
 Relief • 
 
 Drainage » 
 
 Climate 1! 
 
 Agriculture 12 
 
 Flora and fauna 13 
 
 Water<pawen 14 
 
 CHAPTER iV, 
 
 General geology IS 
 
 General itatement 18 
 
 Table of formation* 18 
 
 Abitibi group 18 
 
 GenenU character and aubdiv'^ioaa 18 
 
 Basic and intermediate voir >iu" IS 
 
 Gabbro, diabase, and br ' IB 
 
 Character ami distribution 10 
 
 Lithological character IS 
 
 Origin 20 
 
 Diofite, andcsite, and daeite 20 
 
 Distribution 20 
 
 Lithological character 20 
 
 Metamorphism 22 
 
 Amygdaloidal structure 22 
 
 Ellipsoidal structure 22 
 
 Origin 23 
 
 59813— li 
 
 . • ' '• t'« t ■■ i^ 
 
M 
 
 M 
 
 Intermediate pyroclastira and banded mica achiste '^°^ 
 
 General character and distribution «. 
 
 Agglomerates ~* 
 
 Lava agglomerates 
 
 Tuff agglomerate „ 
 
 Stratified tulTs ^ 
 
 Lithological character 
 
 Metamorphism „^ 
 
 Origin y/^y^y^y.'.'.'.'.'.::::: l\ 
 
 Banded mica schists ^ 
 
 Distribution r" 
 
 Lithological character _^ 
 
 Structure *" 
 
 Origin ;■;;!!!;;::;:::::::; 11 
 
 Rhyolite and quartz porphyry... 
 
 Quarti porphyry ^ 
 
 Acidic pyroclastics, ri-latcd rocks, and-iron formation 09 
 
 Acidic agglomerate 
 
 Banded acidic tuffs iT 
 
 Distribution | ^ ?? 
 
 Lithological character 2q 
 
 Metamorphism _. 
 
 Field relations ^ on 
 
 Carbonaceous slate _. 
 
 Lithological character .^^ 
 
 Field relations rr 
 
 Origin yyyyyyyyyyyy.'. , 
 
 Carbonate rock : 
 
 Distribution 
 
 Rest Lake occurrence «, 
 
 Harricanaw Kiver occurrence 30 
 
 Authier River occurrence .j. 
 
 Chikobi I.,ake boulder. . . ,. 
 
 Origin ^ 
 
 Chert rock ,„ 
 
 Origin '^'!'^!';!'';!;::;:::;: I? 
 
 Iron formation 
 
 Distribution „_ 
 
 Lithological character 3. 
 
 bv. acture __ 
 
 Field relations „_ 
 
 Origin 37 
 
 Structure of the Abitibi group y. 
 
 Age 
 
 _^* ■ OQ 
 
 Harricanaw series ^" 
 
 General character and distribution og 
 
 Arkose 
 
 Limy greywacke j« 
 
 Conglomerate j- 
 
 Banded greywacke !!!... 40 
 
 ^092U28 
 
m 
 
 PAcn. 
 
 Structure 41 
 
 Origin *1 
 
 Age « 
 
 Granite and gneiss 42 
 
 Distribution 42 
 
 Lithological character 42 
 
 Structure 43 
 
 Ck>ntact metamorphism 43 
 
 Origin 44 
 
 Age relations 44 
 
 Postrbatholithic intrusives 45 
 
 Lamprophyre 45 
 
 Age 45 
 
 Keweenawan (?) diabase 46 
 
 Distribution 46 
 
 Lithological character 46 
 
 Structure 47 
 
 Metamorphism 47 
 
 Origin 47 
 
 Age 47 
 
 Pleistocene and Recent 4o 
 
 Glacial " ' 48 
 
 Boulder clay 48 
 
 Moraines 49 
 
 Fluvioglacial deposits 50 
 
 Lacustrine deposits 50 
 
 Recent 51 
 
 CHAPTER V. 
 
 Economic geology 52 
 
 General statement 52 
 
 Gold 62 
 
 Silver 54 
 
 Copper 54 
 
 Tremblay claim 55 
 
 Lead 66 
 
 Iron 57 
 
 Molybdenite 57 
 
 Asbestos 57 
 
 Clay 68 
 
 APPENDIX. 
 
 Kienawisik gold district ^ 
 
 General statement ^ 
 
 Location and transportation "' 
 
 General geology °* 
 
 General statement ^^ 
 
 Table of formations *** 
 
 Banded schist complex 81 
 
 AbitibI volcanic complex •* 
 
' I f 
 
 ill 
 
 ti 
 
 it 
 
 Ormite and gneiM. 
 
 Quatenuuy...... ^^^ « 
 
 Economic geology *"• 
 
 Gold... 66 
 
 ^eha^eterordepo^it..;::;::::;:::;:;;;;;;;;;::^ S 
 
 Prospects ^ 
 
 Sullivan claims! ^ 
 
 I* Blanc claim ^ 
 
 Gale claim ^ 
 
 Ciowe.^^„;and^^^ S 
 
 Cassidy claim.. 1° 
 
 Sisco claim ' '" 
 
 Benard claim ^^ 
 
 71 
 
 Index " '^ 
 
 81 
 
 J, Hlustratlong. 
 
 ni.A:n:.^/^^^^f'-k««eastwa«,;.;;. 73 
 
 ". cis^rristr-*'"''^*-::: ■ " 
 
 VII. AandB ConCr u ^*"^* "^» '8 
 
 Vni. A.andB. Cont^rett^Vtt'^''^ "^^ °'''«-'^i«t comp^^^ !J 
 
 2.Geolog.XtrmTorKe^n°'^'----:-----^ ^ 
 
 map of Kienawisdc gold district. 2 
 
 60 
 
tOK. 
 
 as 
 
 65 
 66 
 65 
 65 
 
 65 
 
 66 
 
 66 
 
 66 
 
 S8 
 
 » 
 
 ro 
 
 
 
 1 
 1 
 1 
 
 The Harricanaw-Turgeon Basin, 
 Northern Quebec. 
 
 CHAPTER I. 
 INTRODUCTION. 
 
 GENERAL STATEMENT AND ACKNOWLEDGMENTS. 
 
 The district described in the following report is that part of north- 
 western Quebec which lies between the Harricanaw and Turgeon rivers 
 northeast of lake Abitibi. Very little was -known about this area until 
 recently on account of the difficulties of access; but with the coming of 
 the National Transcontinental railway, an active interest has arisen in 
 the character of this new country which has been opened for development. 
 It lies in the so-called clay belt and consequently is a promising field for 
 agricultural development, and the occurrence of gold in the adjacent 
 district to the south suggests the possibility of further deposits of that 
 mineral. 
 
 Field work was carried on during the summers of 1914 and 1915. 
 Practically all of the navigable streams of the district were traversed, and 
 micrometer and track surveys were made of those not shown on the base 
 map. Land traverses extending from 3 to 9 miles back from the water- 
 ways were run, by pace apd compass, at intervals of 10 miles or less, into 
 areas which could not be reached by canoe. 
 
 In 1914, the writer was assisted in the field by L. Clermont and L. I. 
 Walker, and in 1915 by G. Hanson, C. B. Dawson, and R. K. Carnochan. 
 
 The resultant geological map, scale 4 miles tc 1 inch, which accompanies 
 this report, includes an area along the National Transcontinental railway 
 which was examined by W. J. Wilson* and M. E. Wilson.' 
 
 The map of the Abitibi district, 1911, scale 4 miles to 1 inch, issued 
 by the Department of Lands and Forests, Quebec, was used as a base map. 
 
 LOCATION AND AREA. 
 
 The ff.ap covers a rectangle 1 12 miles by 82 miles in the northwestern 
 part of Quebec, in the county of Timiskaming, and the territory of Abitibi 
 (Figure 1). I^ake Abitibi is situated in its southwest corner. The principa. 
 stream in the district is Harricanaw river which flows across the eastern 
 part. 
 
 MEANS OF COMMUNICATION. 
 
 Prior to the construction of the Transcontinental railway, the district 
 was accessible by a canoe route from Ottawa river into the headwaters of 
 
 '"Oeokniial reeo iin« i «i»iH» »long the line ol the NatiomI Tramnoatiiientol railway in wwtern Quebeo"; Geol. 
 Siirv., Can., Mem. 4, 1»I0. 
 
 •"The Kawacama Lake map-area, Quebec": Geol. Surv.. Can., Mem. 3«. 1«13. 
 
ill 
 
 Bam'caoaw river or hv . 
 
 I I I i" I ' 
 
 li 
 
 waters. Amos is 0+''^ connect by portaee tr«nf ^i^^?"^ '^'^'ch flow 
 offers a good canoe i!^X\V^^^:'-^'^' «" ««Sana"J' T^^^J^l 
 
 HlSTOfti'. 
 
8 
 
 hunting ground by Indians for many years, but there is evidence that it 
 was never well populated nor extensively tra\elled. An Indian cemetery 
 is situated on Otter lake in which some of the crosses appear to be over 
 thirty years old, but in parts of the district more remote from Abitibi 
 post, only a few old winter camps give evidence of previous occupation. 
 Harricanaw river is not considered a good canoe route to James bay on 
 account of the numerous falls and rapids below Turgeon junction, and, 
 until recent years, there was no trading post in the Harricanaw-Turgeon 
 basin. 
 
 A reported discovery of gold on Patten river in 1912 caused a number 
 of prospectors to investigate this section and signs of prospectors' camps 
 are abundantly found along the whole course of this stream. No valuable 
 deposit was found, however, and all workings have been abandoned. 
 
 At present, agricultural settlements are growing up along the railway, 
 and several trappers have located in the district recently. 
 
 Very little intensive prospecting has been done as yet, and only one 
 mmeral deposit of economic interest has been found; this is a copper 
 deposit carrying gold and silver values, 3 miles northeast from Amos. 
 
 PREVIOUS WORK. 
 
 The first important contribution to knowledge of the district was 
 made by the Quebec Department of Lands and Forests, which issued a 
 map in 1911, 4 miles to 1 inch, showing the course of all the larger water- 
 ways in the district, together with notes on the character of the adjoining 
 land. 
 
 National Transcontinental Railway surveys were made across the 
 southern part of the district in 1910, and since that time a considerable 
 amount of accurate geographical information has been accumulated in 
 the vicinity of the railway through the subdivision of townships. 
 
 It is of historical interest to note that an early mention of Il^rricanaw 
 river is given in a report by R. Bell' whose assistant, A. S. Cochrane, 
 was told by the Indians on Nottaway river that that stream emptied into 
 Hannah bay. In 1895, Dr. Bcll= mentioned that Harricanaw river (then 
 called Hannah Bay river or Wash-a -how-si pi) was known to his Indian 
 guides, b;.t it was not known until the following year that Nottaway river 
 belonged to e different river system. In 1900, T. B. Speight.' O.L.S., 
 traversed Turgeon river (Hannah Bay river) from the confluence of Burnt- 
 bush river up to Ninemile portage. In 1906, T. J. Patten, O.L.S., made 
 a track survey of Patten (formerly Woman) river, from which circumstance 
 it derived its name.* From a personal communication the r.-riter learns 
 that, in 1907, Mr. J. J. Sullivan made a winter trip from Rupert House 
 on James bay to Abitibi post, crossing the Harricanaw basin. He noted 
 the general scarcity of lakes in the district. The record of this trip was 
 given to Mr. F. H. Clergue of Montreal. Other early geographical notes 
 and surveys were made in connexion with the geological explorations 
 listed below. 
 
 'Geol. Surv., C«n., Ann. Rept., vol. III. pt. I, new «r.. 1887-*. p. 21A. 
 KJeol. Surv., Can., Ann. Rept., vol. VIII, new ser . 1S95. p 7«A. 
 'Report on the purvey and eiplomtion of ncrtherp. Ontario, 1900, p. 4. 
 <Tbe Canada Oaaette, CSwcraphic-Baatd deciiioui. May 18, 1918. 
 
f M I 
 
 •!l 
 
 (I I 
 
 in- 
 
 
 This work included' th^ ' ^*P*- o' Pro« 
 
 Johnston, J. K E — " p..* '" ^''^ «««« diacuwed 
 
 western Quebep" p ^^ ^^^^^'onal Transcontin^^^^^^ f"*^ Nottawav 
 
Jen 
 
 «■> 
 
 ke 
 
 ed 
 
 Wilson, M. E.— "Kewagam* Lake map-area, Quebec": Geol. Surv., 
 Can., Mem. 39, 1913. This report deals in a comprehensive manner 
 with the results of field w ork performed in 1910 and 191 1 . The accom- 
 
 ¥inying geological map, 4 miles to 1 inch, adjoins the Harricanaw- 
 urgeon map sheet on the south. 
 Tftnton, T. L.— "The Harricanaw basin iK^rth he Grand Trunk Pacific 
 railway, Quebec". Geol. Surv., Can., Su.n. Rept., 1914, pp. 96-98; 
 Sum. Rept., 1915, pp. 168-170. , ^^ ^ 
 
 Brief accounts of field work performed in 1914 and 1915. The Sum- 
 mary Report for 1915 contains a geologically coloured diagram of 
 Harricanaw-Turgeon b:.sin, 20 miles to 1 inch, on which is marked the 
 • mineral occurrences in the district. 
 
 :^' 
 
 *^* 
 
 ^ 
 
ilif 
 
 CHAPTER II. 
 SUMMARY AND CONCLUSIONS. 
 
 TOPOGRAPHY. 
 
 The Harricanaw-Turgeon basin forms parts of the Rreat Pre-Cambrian 
 peneplain of northern Canada. The country slopes gently northward to 
 James bay, with a slight inclination toward the east, as shown by the 
 greater number of tributary streams joining Hurricanaw river from the 
 west than from the east. In the 1 14 miles between the railway and Turgeon 
 junction atthe north end of the map-area, the fall on Harricanaw river 
 is from 1 000 to 600 feet above sea-level. This descent is accomplished 
 by a number of irregularly spaced falls and rapids with stretches of sluggish 
 water between. All the large streams in the district make their descent 
 in a similar way, but the small streams are characterized by swift currents 
 and fairly evenly graded valleys, due to the fact that they run through 
 unconsolidated matenals and have not yet cut through to the irregularities 
 of the rock floor. The northern half of the map-area is a great musk g 
 plain with a few widely scattered rocky or clay-covered hills rising above 
 » *i?^"i- . 'r^'u Numerous hills and ridges occur in the southern half 
 of the district, the highest of the hill- T. ing Plamondon hill which rises 
 800 feet above the surrounding count v There are only a few lakes in 
 the district and these are, for the most part, small. The majority of the 
 lakes occur near the headwaters of small streams and are not arranged 
 as a chain of nyer expansions, es is commonly the case in the rockier parts 
 of the Laurentian plateau. 
 
 GENERAL GEOLOGY. 
 Pre-C " b^^ ^"'**^ ™*'''^ observed in the Harricanaw-Turgeon basin are 
 
 The oldest rocks, hereafter referred to as the Abitibi group, include 
 a complex series of lava flows, which range in composition from basalts 
 to rhyohtes, water-lam tuffs of varying acidity, and a banded iron forma- 
 tion. Many of these types present evidence of widely differing meta- 
 morphic action, ranging from rather fresh-looking, massive varieties to 
 steeply inclined schists. 
 
 A sedimentar>- series of rocks, the Harricanaw series, unconformablv 
 overiies the rocks of the Abitibi group. The sediments have been largely 
 altered to schists, and are infolded with the older members of the basement 
 complex. 
 
 Approximately one-half of the map-area is underiain by granites and 
 gneisses. These rocks represent batholiths which intruded the Abitibi 
 group and have been exposed by erosion since that time. The granitic 
 rocks are by no means uniform in their lithological character, but no 
 evidence was found for regarding one type as different in geologic age 
 from any other. o » & 
 
 Au ..•u-^™**" minette dyke wa.s observed cutting a schisted member of the 
 Abitibi group. Since the dyke rock is not schisted, its age in given as 
 post-batholithic. -» s 
 
 IfcN 
 
Comparatively freah-looking dykes of quarti disbaae ami olivine 
 diabase cut the granites and older rockii. The dykes are not largr but they 
 are widely distributed through the district. The diabas*' intru«iv«'s are 
 believed to be of Keweenawan age on account of their similarity to dykes 
 which occur at numerous localities between this district and lake Superior 
 and whose age has been determined in the latter locality. 
 
 A mantle of unconsolidated materials now covers the lowlands of the 
 d-'ply eroded Pre-C;ambrian rock-floor. These deposits of Ixjulder clay, 
 SI ivel and sand, and stratified clay and sand, were deposited by the 
 continental glaciers which passed over the district in Pleistocene times, 
 and by the waters from these melting ice-sheets as they retreated. 
 
 ECONOMIC GEOLOGY. 
 
 When the National Transcontinental railway was built, very little 
 was known of the natural icsources of the Harricanaw-Turgeon basin 
 except that it lay in the cls" belt. The best of this land along the railway 
 was speedily taken up by ugricultural pioneers. , .^u u 
 
 Very little prospecting has been done in the region as yet, although 
 approximately one-half of the basin is underiain by rocks of the schist 
 complex. The only parts of the district altogether unsuitable "»>" pros- 
 pecting are the large interstream areas north of the Mistawak bathohth, 
 which are known to be almost entirely occupied by muskeg, and the interior 
 parts of the batholithic masses of granite, which are characteristically 
 
 Quartz veins are abundant in the rocks of the Abitibi group, especially 
 
 . in the vicinity of the granitic intrusives. Several such veins showed the 
 
 presence of small amounts of gold when assayed. Some quartz stringers 
 
 in the ferruginous dolomite on Harricanaw river, just north of the Mistawak 
 
 batholith contact, showed a high gold contact upon assay. » , ... . 
 
 Silver values have been found in pegmatitic quartz veins m the Abitibi 
 greenstones near the granite contact, a few miles southeast of Okiko and 
 
 on Chikobi lake. . , . . ^ * 
 
 Chalcopyrite has been found in considerable amount, near Amos, in 
 a quartz vein cutting a schistose rhyolite tuff, and a small occurrence was 
 found near the mouth of Patten river in a quarts, »ein cutting the Abitibi 
 greenstone. , , . .. , 
 
 Small amounts of galena have been found in a pegmatitic quartz vein 
 in the Abitibi greenstone near the granite contact and also m a quartz 
 vein associated with a post-batholithic minette dyke. 
 
 Banded iron formation was observed about 10 miles northwest from 
 Chikobi lake, and boulders of this rock and strong local magnetic deflexions 
 testify to its presence in the Abitibi greenstone area in the northern part 
 of the sheet. , , . ^.^. . 
 
 A small amount of molybdenite was observed in a pegmatitic quartz 
 vein in the Abitibi schist on Plamondon hill near the granite contact. 
 
 Considering the accessibility of the district, the. numerous rock 
 exposures between the railway and the Mistawak batholith and along the 
 waterways to the north, and the fact that casual prospecting already has 
 shown the presence of valuable minerals, it is evident that the district 
 merits the attention of prospectors. 
 
CHAPTER III. 
 
 ill 
 
 i,i; 
 
 GENERAL CHARACTER OF THE DISTRICT. 
 
 TOPOGRAPHY. 
 
 OBNBRAL ACCOUNT. 
 
 The Harricanaw-TurKPon baiiin formB part of the Pre-Cambrian 
 plateau which oceupieB a wide, V-shaped area around Hudson bay. 
 ThrouRhout this physioftraphic province the surface is characteristically one 
 of low relief and the old rock structures are truncated, indicating that the 
 whole area was at one time reduced by erosion to a peneplain. Evidence 
 that this peneplain was raised and subjected to erosion long before Glacial 
 times is found in the old river channels which now appear as rock gorges 
 where the present streams have followed the same course, and in the cliffs 
 and minor topographic irregularities which are found in the higher parts 
 of the area where the rock is exposed. The erosive action of the continental 
 glaciers which passed over the area during the Glacial epoch is to be seen 
 on the polished and grooved rock surfaces and the rounded character of 
 the hills when viewed from a distance. Glacial rock flour and boulders 
 have been deposited over the whole Pre-Cambrian plateau in an irregular 
 manner, and in a large area in northern Quebec and Ontario, known as 
 the clay belt, a depositional plain of considerable thickness has been 
 formed by stratified lake clays and sands which were laid down in the waters 
 derived from the melting glaciers. 
 
 The map-area lies within the clay belt and consequently its topography 
 differs from the greater part of the Pre-Cambrian plateau. An abundance 
 of drift materials, a large part of which were laid down in glacial lake 
 waters, covers the lowlands of the district and hides the minor irregularities 
 in the rock surface. The rivers are consequent on the drift plain and have 
 cut V-shaped valleys in the unconsolidated materials. There are only a 
 :ew lakes in the district and these are for the most part at the headwaters 
 of small streams. Such a drainage system is in marked contrast to the 
 mesh of rock-basin lakes which spill into one another by streams character- 
 ized by falls and rapids, as described in the Pre-Cambrian plateau outside 
 the clay belt. The northern half of the Harricanaw-Turgeon basin, which 
 lies between the Harricanaw, Wawagosik, Thco, and Turgeon rivers, is 
 occupied by great muskeg plains in which the vegetation has prevented 
 the development of the drainage system. The southern half of the map- 
 area is of comparatively high relief. Muskeg areas of considerable extent 
 occur between the hills and ridges, but the drainage system is much better 
 developed than to the north (Plate II B). 
 
 RELIEF. 
 
 The Harricanaw-Turgeon basin has an average height of 700 to 1,100 
 feet above sea-l^vel, this being somewhat lower than the general elevation 
 of the Laurentian plateau. Hills and ridges are scattered through the 
 
■outhern part of the iheet an thew rii« to heifthii of • few hundred feet 
 •bove the lurroundinR country. The hiffhest point in the dJrtrirt ii 
 riamondon hill, with an approximate height aiwvc wa-level (aneroid 
 determination) of 1,880 feet; the lowert point is on Harrieanaw river at 
 
 the extreme north end of the sheet, the elevation here MnRapproximatery 
 
 / 1 r«o« , "7 ■- ■ •'' *'^*"* ■ vertical range for the district of approxi- 
 mately 1,280 feet. 
 
 600 feet above sea-level. 
 
 Plamondon hill is situated 18 miles due n«)rth of lake Chikobi It is 
 the highest hill in a long irregular ridge which runs through this "part of 
 the sheet in a northeast-southwest direction. Plamondon hill and Hebert 
 hills, which nse from the same ri<lge to the northeast, are composed of 
 highly metamorphosed green schists near the granite contact, whereas 
 southwest of Plamondon hill, the ridge terminating in the three Nissing 
 hills and Oditan hill, is composed of granite near the greenstone contact 
 At Oditan hill this major ndge meets the divide between the Harrieanaw 
 and Abitibi waters, which runs west-northwest and east-southeast The 
 naost prominent elevations «n this divide are the Abitibi hills near the west 
 side of the sheet. Other prominent hills occur in various isolated positions 
 throughout the southern part of the district; practically all of these are 
 near the contact between granite and greenstone. The only hills of anv 
 prominence in the northern half of the sheet are two diabase massi-s stand- 
 ing about 200 feet above the general level, west of Harrieanaw river 9 
 miles above its junction with the Turgeon. 
 
 The following elevations are taken from the "Altitudes in Canada" 
 and from aneroid observations by the writer. 
 
 Uka AbHibi hishwater level T**r 
 
 Makamik lake (low water) gi; 
 
 Robertaon lake (low water) i |mi 
 
 Heitht of land, eart of Robertaoo lake t'mk 
 
 Davylake ,'niX 
 
 Beauehamp lake l'^ 
 
 Harrieanaw atation. 
 
 1.002 
 
 Harrieanaw river (highwater) at N.T.R. bridge 979 
 
 Harrieanaw river (low water) at N.T.R. bridie am 
 
 Lake Obaliki Sm (.n«».u\ 
 
 Lake Chikobi iSs*^.'"^ 
 
 Otter lake '•"* 
 
 Lake Joe 
 
 Abitibi hills 
 
 Oditan hUl 
 
 Tansinanhill J'TS 
 
 Plamondon hUl ,'JS 
 
 Riftedhill {'SS 
 
 Plu« hill ' • ^ 
 
 910 
 1.040 
 1.300 
 1.408 
 
 820 
 
 DRAINAGE. 
 
 With the exception of a small part of the Ottawa River basin in the 
 southern part of the sheet, the district drains into James bay. The major 
 ^l"^.!®- !", ^'"^ Harncanaw-Turgeon basin, and the remainder drains into 
 Abitibi lake, mainly through La Sarre and Okikodosik rivers. 
 
 The depressions in the rock surface are filled with glacial boulders 
 sand, and clay, so that the rivers are consequent on this depositionai 
 surface. Where a stream runs through sand and clay, the valleys are 
 y-shaped and graded. Where belts of boulders too large for the streams 
 to roJI have been encountered, rapids occur. In many places alfuy the 
 
10 
 
 ffil 
 
 •traMM have inoiwd their chMinela down to the ruck floor and have expoaed 
 irregularitim Which now show in falls and cascades. These irregularities, 
 toward whose Rradinx very little profress has been made, serve to give the 
 stream courses a step-like character, that is long stretches of qui*tly 
 flowing water alternate with falls and boulder dams. The headwaters of 
 the brge streams and the small tributaries are normally more swift and 
 meandering than the main streams and are rharartcrised bv fewer falls. 
 The scarcity of falls is doubtless due to the fact that the smaller amount of 
 water in these streams has taken longer to cut through the upper sand and 
 clay deposits; whereas the swiftness is due to the more even grade and 
 the head uf water found between the high lanas and the main river channels. 
 All the stream valleys are vouthful. The main streams have valleys much 
 larger than is warranted by the amount uf discharge during the greater 
 part uf the year. In the spring after the breakup, however, there is an 
 enormously augmented run-off, the floating ice leaving its record in chafe 
 marks on the trees often 10 fe?t alwve river-level in July. The rivers when 
 in flood erode actively and where their beds afc in clay, they scour their 
 bottoms in places deeper than their locnl bane level. This is illustrated 
 in the case of the La Sarre which has a depth of 25 to 30 feet; whereas 
 lake Abitibi is 15 feet shallower. On Wawagosik river above the 18-foot 
 falls the bed of the river hatt been scoured deeper than the lowest point on 
 the brink of the falls and at several points on Plamondon river the clay 
 has been washed awav from above as well as below the boulder belts, 
 leaving prominent boulder dams. 
 
 Unlike the Laurentian plateau in general, lakes are lot .lumerous. 
 Besides lake Abitibi there are only fourteen known lakes in the wbole 
 district, and the majority of these are comparatively small. Ah the 
 larger lakes of the district occur in the southern half, which v more hilly 
 than the northern half. The lakes owe their origin to the combined 
 effect of irregularities in the rock floor and the ' deposits. The domin- 
 ant influence of the drift deposition in forming lake basins is seen in such 
 lakes as Makamik and Newiska which arc very shallow and have clay 
 Irattoms and few rock exposures along their shores. Lake Chikobi has 
 been caused by the damming of a depression in the rock floor by a wide 
 boulder and sand belt which is lo he seen at the numerous rapids at the head 
 of OctRve river. In the case of Otter lake the hollow in the rock floor 
 has been the dominant factor, though a small part of the lake's rim is 
 defined by drift deposits. Other lakes show to a varying extent the 
 influence of the old rocky irregularities and the uneven glacial accumula- 
 tions. 
 
 The more important lakes in the regioi and their areal extent are 
 given in the following table: 
 
 Squai* 
 
 miles. 
 
 Abitibi 3S8 
 
 MkkMntk 18 
 
 Otter 8 
 
 Nawi«k» 4 
 
 Mirtawak 9 
 
 Wawacouk 4 
 
 Chikobi 10 
 
 Kobertaon 2) 
 
 ObiOiki • 
 
11 
 
 In the ain ■outhern part of lake Chikobl throUKh a distance of 
 about 5 milM, the Bhoret of the lake n>ughly parallel the irhiitoiiity Rtrike 
 of the Pre-Cambrian rock-flo«r. In loukinn for evidence of the old prc- 
 
 !;lacial drainaxe nyatem tt was noted that practtc-ally all ot the rock gorRca 
 n the district tr«>nd north-northwest, soutn-suuthoast. 
 
 Linear valleys which are so characteristic of the district to the south 
 and southwest are lacking. There is, however, a general parallelism to be 
 observed in the major directions of the main streams, and the more or less 
 ■inuous course of one stream often finds its counti-rparts in the adjoininK 
 streams. A general survey of the map reveals two major directions to the 
 main channels, one being «lue north and south, the other north of northwest. 
 The northerly «lirection is normal, ilue to the slope of the nlain toward 
 James bay, tl.'j northwesterly direction corresponds closely with the 
 direction from which the main ice-cheet advanceil and its tlirectioiml 
 influence is due tu the linear arranuement of its morainic deposits along its 
 coi se, and possibly, in pan, to the influence of preglacial channels as 
 seen In gorgos. The southern half of the district is characterised by rock 
 hills, and rolling sand and clay land. The drainage is on the whole much 
 l>etter developed than in the northern half of the district which is so neariv 
 flat that the vegetation does not permit the incision of channels by small 
 streams. Moss has accumulated to a depth of from to 10 feet and in wet 
 seasons this forms a saturated spongy mass from which the seepage into 
 the streams is very slow. Numerous ponds with no defined stream leading 
 from them are encountered in the muskeg areas and many of these «lry up 
 during the late summer months. The streams which run through the great 
 northern muskeg Iw-lt are entirely consequent ^n the glacial dep«)8its, there 
 being no sign of influence from the preglacial topigiaphy. Following the 
 general slope of the plain the stn-ai"* maintam a very constant main 
 direction of flow. Theo and VVawagosik rivers are bniught to the Horri- 
 canaw by the abrupt turn to the east of the lower Turgeon river. The 
 sudden change of direction of the Turgeon, which up to the Orand Bend 
 has been north for over 28 miles, is due to a gr<>at iMiulder sand belt which 
 strctt hes across the north end of the district in a direction slightly north 
 of east. 
 
 CLIMATE. 
 
 The climate of the Harricanaw-Turgeon basin is the chief drawback 
 to what would otherwise be a splendid agricultural district. Although 
 the area explored extends over a distance of 114 miles north of the railway, 
 the altitude diminishes goinp north, so tiiat there is sufficient uniformity 
 to allow for the consideration of the most northerly part of the area along 
 with t'.e most southerly. On an average, it might be said that the opening 
 of the waterways in the spring occurs at the latter end of April, and that 
 the freeze-up comes near the beginning of November. Frosts are liable 
 to occur during all of the summer months. Annual precipitation is about 
 28 inches. The Harricanaw valley is annually visited by cyclones of 
 varying intensity, during the summer months. These appear to sweep 
 down from the north or northwest following hot, dry spells. Their 
 approach is signalized by a strong wind which increases to a gale, often 
 
 59813—2 
 
( ,' 
 
 
 (if 
 
 i 
 
 ' i< ii 
 
 12 
 
 high wind and pr"ip SJon usuX ui !' *''""^^[ *."'' HRhtning. The 
 though during SepteSVof 1915 « it?'"' f JJf"*^i°' twenty-four hours, 
 days. The close of The storm I mf 13 t **"' '^t'^'^^l ^^^^ 'or five 
 the low scudding clouds af™ whToh f^. n^ * "f"^'' *''?^ '^"'^ breaks in 
 and blue sky ap^are *'''' "°™"' **'«t«''-'y ^inds prevail 
 
 du4te siTmrer^olTo^lsnt'U-^iotti^T^^^ -»-y 
 
 19-20 was sufficient to raise the waters inKfn95T ^'^ ■ 1"™ °^ ^""^ 
 just below the confluence of Burnthn«h ri, ^4 hours in Turgeon river 
 of the season an.l the one of ^Zst ,1 1„ T""- 1 T''^ ?""* ^'"'"'* «torm 
 to September 19. *^ ** duration lasted from September 14 
 
 in 19?5T^ur7S^l"To tlvT™T """^'^^ "" ^he following days 
 
 September 2Tand'Se"ptUber "2 J SnotTelfin'/"?"^* '«} ^u^Sst 3^ 
 23, and August 30. The onlv hails?«rl i '" ""."les on June 8, Julv 
 
 vegetation o'ccurred on Julys' Th «* w™s l^^^TKV'^K''' ''^"^^ 
 nver in the west central part of the dTstrict ''T'^^'''' ^hile on the Corset 
 of Its having passed overly' agri. dttaV^U^toTelS'' '" "'*''*"^' 
 OctoS '^""*"* """""* °^ -- ^'^"^ ''"ring late September and early 
 
 ^o^^^^^.^lZr^r::tZ^' - — "^ ve^ 
 
 AGRICULTURE. 
 
 -^^r.tTsi::^riVt,^7,:^^^^^^^ /«««" - the experi. 
 
 drained support a heavTgrowth of'^S?^l T' 'f ^' ''''^■'' ?"^ '"""^ ^^hen 
 as to the excellence of theTnd for Sr^J"^'*^*"'"' ^"^ '^*^« »« d«"bt 
 to determine the limitatiLs imi)osed brfh*^ P^rpoj^es. It only remains 
 The growing season is short biTKo * ^ '"r"*"" '^*'«t'''' ''onditions. 
 
 r=,f if„s- fft3 "=J«H '"-"'- w«S 
 
 sri--s «f s^-i^"« S.i K -iSar^S 
 "' T^r^^sd'XS^ K^^^^^ '"^"^* 
 
 camp. The locTtS is ^ it^*^fP"^""!|;« ^^ ^he Spirit Lake detention 
 
 a muskeg and rock aroihraviv colored wUh It. H''' '" T^ *^'^ ^«« 
 a considerable depth of moss Thn T • mfdium-sized spruce and 
 
 sections in this district req.i res a conS«^l T^ '""^ '1 ''i' ^'^^ ""''"'""t 
 long pe iod of time. The onlv income whnh ';.?"""""* "^ ^"''^ o^''''- « 
 
13 
 
 to be drained and boulders removed before ploughinf^. Locations near 
 waterways by which pulpwood and timber can be sent to mills are being 
 most actively developed by settlers. This gives especial importance 
 to the areas adjoining the streams flowing into lake Abitibi and Harrioanaw 
 river near the railway. 
 
 An interesting experiment in gardening has been carried on by Mr. 
 J. J. Sullivan on lake DcMontigny. Potatoes, beets, parsnips, radish, 
 lettuce, cabbage, and other market garden produce have been raised with 
 success and also a great variety of garden flowers, but the proximity to- 
 the large expanse of water has been undoubtedly a mixierating influence 
 on the climate. 
 
 FLORA AND FAUNA. 
 
 The principal trees and shrubs occurring in the district are: black, 
 spruce, white spruce, jack pine or banksiun pine, white birch or canoe birch, 
 poplar, balsam, balm of Gilead, tamarack, white cedar (Upper Harricanaw, 
 Otter lake, and Abitibi lake), red pine (Abitibi only), yellow birch, black 
 ash, mountain ash, maple, wild red cherry, alder, willow, moosewood 
 or mountain maple, blueberry, high bush cranberry, low bush cranberry, 
 meadowsweet, red osier dogwood, saskatoon berry fir sugar plum, hazel, 
 moosewood or leatherwood. 
 
 Black spurce is commercially the most important tree in the district. 
 It occurs in all the clay areas and reaches a diameter of 2 feet or more 
 in the well-drained strips along stream channels and the prominences of 
 the roiling southern part of the district. This wood was extensively used 
 for ties on the Transcontinental railway and is now the chief tree cut for 
 pulpwood. The only red pine observed in the district was on some rocky 
 islands in lake Abitibi; this appec-s to be the northward limit of pine 
 in this part of the country. The northward limit of maple occurs in the 
 upper Harricanaw basin a few miles south of the map-area. The farthest 
 point north at which cedar was observed was in Otter lake. The northern 
 half of the district is largely muskeg. Practically all of the timber in the 
 district, which is of suflicient size for commercial purptise, is founil along 
 narrow strips bordering the streams an<i in the hilly southern part of the 
 sheet; but this timber cannot be utilized under present conditions liecause 
 the streams flow north away from the railway and the settlements. The 
 timber in Abitibi basin at the southwest part, however, is not under this 
 disadavantage and con.siderable quantities of pulpwoo*! and lumber are 
 being cut around Makamik lake. La Sarre river, and the Okikodosik. 
 The lumber trade of Amos draws its supply from the forests on the banks 
 of upper Harricanaw river. 
 
 Land traverses through the district frequently show a strikingly 
 sharp boundary between different types of forest, due to the peculiarities 
 of their habitat. In well-drained clay areas the predominating trees 
 are white and black spruce, and balsam; on sandy clay, poplar and birch; 
 on sand areas, jackpine. On rocky hills a mixed forest of these trees 
 and various large shrubs is found. On old burnt areas poplar and birch 
 saplings dominate in the clay areas, jack pine on the sand areas, and in 
 the muskeg stunted black spruce and tamarack are sparsely scattered. 
 
 59813— 2i 
 
■'i 
 
 The'Sratebe™"'? 'i:t'' S.^ZZ'^'^^l ''"•" » «>« — 
 
 district is becoming a favourite ri?,^ 5 "u*®^ ""•'*• attention that the 
 
 abundant in the Scinity ofnlSdon' hln"*'"^* ^^^ deer are locU?; 
 
 Hamcanaw junction. Caribou "?eiti ^^ ''™"°^. *^« Tur«eon- 
 
 though none were seen by the writer's Srty ^ '"■'"'°* '° ^''^ '^«°' 
 
 and tt SruKSUrthTrilL^^ ^"'^T ^ay posts 
 
 *»? tapped very little until recent Zre so that th^f *"''k' ''•'"" *'""*«d 
 
 are still present in their normal abnX'n.^ ^u*''^^ '"'■"*'^*"''8 a°imal« 
 
 the beaver are more numero^at tho iITh . The dams and houses of 
 
 %Y °*'^«': P'^rt of theTorth eountJ^ 5ha? the' whI *^' '*'^?'?« ^'^^^ '» 
 
 other fur-bearing animals of the S incLo ^^' ^^^ ''f^^^' The 
 
 fisher lynx, wolf, black bew SJf liT i,''"Tu?''°''' f"''' ™arten, 
 
 squirrel, and flying squiirel '""^^™*' s''""''. 'abbit, chipmunk, red 
 
 in thl^^ntX'rortreSct" "''' '''''"^^ '" '"^^ "-»>-, especially 
 pickerS::StSi^^^^^^^ 
 
 peripSteXSol""o'f "A/° ifthtSm^e'fk*'"^ T "« «°-^« -^ the 
 muddy, hence, no bass or troS inhJTT ^^^ }^^ ^""^^^ constantly 
 bait fishing are of little value forTLf.l- I u*'" ^*''^«"«- Trolling and 
 of the district, i.e. Otter, MiLwafS^^ '""^^^ deeper lakes 
 
 ing in the district is doifwS^tiii^Sets^^^ Practically all the fish- 
 
 c'ear stream flowing across Ninem/le nnr^;„ ^^^l Makamik river and a 
 Abitibi is the only place in f hi hE^^T u°"**'" ^^^ t^out. Lake 
 extensively and fish from tZe Ire "^'IjK''' ^«*^'"| *« ^"^ied on 
 station to southern mar^ts ^^^ ^^"""^ ^* ^^rre (Wabikin) 
 
 WATER-POWERS. 
 
 and I'n't^es'^i^^Son!^!^^^^^^^^^ tftC^'^^y *« '^^ ™'-y 
 La Sarre river falls 120 feet beTw^n Ail i t development of power, 
 greatest single drop in its couree il at a^^ J^i''' ^° ^ '^H ^^'^^'- The 
 ship, range IX, lot 48. The Sh banks nn ^A'^' •5''^ '" ^ ^arre town- 
 permit of the construction of I dam wHhoutfl't "* *^'' P"''^* ^°»'d 
 Another falls of about 18 feet occu^ Thnnf 4 m'*'"? ?"y ^^™ '^'^ds. 
 miles from the town of La Sarre o^ thori '"''es be ow this, only 3 
 Makamik on the upper parts of tW ? ^'''^^-''- ^'''^ '^ke and lake 
 of water throughout the year *'^*'" ^"'"'■'^ « considerable flow 
 
 hills,l?aTrL"Vf'LnsS:L^^^^^^ ""^ ''' — - the Abitibi 
 
 9 miles north from the "of Okiko tL 7''"' «t^ distance of about 
 The supply of water is probab y iSs c'onstL/^^ ^'^^^H'^ ^^""^^ ^^ f«^^t. 
 
 jndicatVo; fcprmoTof\S:eV^* ^'^^^^^ '^"^^ ^^"« -^^-h are 
 be of any economic valu^fn the near f?.f°° ''T^' ™" settlements to 
 rapids about 5 miles in length wS t^^l' 'f'"' ''^ "''''"'des and 
 
 eiigm, wfticft appear very favourable for power 
 
 *,' 
 
16 
 
 development (Plate IIIA), occurs on Harricanaw river between 21 and 
 26 miles below Harricanaw village. The total drop is over 75 feet. A 
 dam could be built in the granite gorge which would not cause the flooding 
 of any farm land. The three rapids on Harricanaw nver between the 
 railway and lake Obalski deserve immediate attention before the lands 
 along the banks become of too much value. The total drop is approxi- 
 mately -14 feet, divided as follows: 4 feet, 2 J feet, and 7 J feet. A dam 
 at the foot of the third rapid, with a lock, would add 20 miles to the 60 
 miles of the upper Harricanaw waters which are already navigable for 
 power boats. Power might be developed from the drop, which would 
 reduce the cost of transportation north of the track and make the land 
 around Obalski lake more desirable for settlement. 
 
16 
 
 CHAPTER IV. 
 GENERAL GEOLOGY. 
 
 \\m 
 
 
 II H-^ 
 
 If;; 
 
 GENERAL STATEMENT. 
 
 The solid rocks of the Harricanaw-Turgeon basin arp all Pre-Camhrian 
 and are classified under the following headings: (1) Abitibi group, (2) Harri- 
 canaw series, (3) granite batholiths, and (4) post-batholithic intrusi . '•s. 
 
 The Abitibi group embraces the oldest rocks in the district. It 
 consists of basic, intermediate, and acidic lavas and tuffs, also hornblende, 
 chlorite, and mica schists, which are regarded as the metamorphosed 
 equivalent of the volcanic and pyroclastic members, together with ferru- 
 ginous dolomite, and banded iron formation. Certain banded mica schists, 
 the ferruginous dolomite, and the banded iron formation may he sediments; 
 but, considered as a whole, the Abitibi group is one in which the volcanic 
 and pyroclastic members predominate. 
 
 Within a very restricted area, field evidence is found which indicates 
 that, after the deposition of the banded iron formation, uplift and subaerial 
 erosion of a part of the district took place. During this period a con- 
 formable series of sediments was laid down consisting of a thin bed of 
 quartzite and arkose followed by thicker beds of conglomerate and grey- 
 wacke. These rocks have been designated the Harricanaw scries. Among 
 the pebbles found in the conglomerate are representatives of a great 
 variety of rock types found in the Abitibi group and in addition there are 
 granite pebbles. The granite, which is a plutonic rock, must have been 
 exposed at the surface by erosion at the time of the deposition of the 
 Harricanaw sediments. 
 
 The classification of the Harricanaw series as a distinct entity rather 
 than as a member of the Abitibi group is based on the following considera- 
 tions: (1) these definitely recognizable normal sediments are the oldest 
 rocks of this type found among the pre-batholithic rocks, (2) they record 
 a period of unknown but possibly great duration when the normal processes 
 of erosion, transportation, and sedimentation were not masked by volcanic 
 activity (which ma.sking may have taken place in earlier times). The 
 period is probably much more important than might be inferred from the 
 limited distribution of these rocks in the Harricanaw basin, because they 
 occupied a stratigraphic position which exposed them in a particular 
 manner to the erosive agencies which have since planated the district. 
 (3) By distinguishing from the Abitibi group any series whose stratigraphic 
 position can be ascertained, the remaining group becomes less of a " com- 
 plex " and progress is made toward the orderly classification of the whole 
 pre-batholithic assemblage. 
 
 It is not known to what extent the rocks of the Abitibi group were 
 folded previous to formation of the Harricanaw series, but it is evident 
 that f Iding took place on a large scale at some later date and probably 
 contemporaneously with the great batholithic intrusion. The Harricanaw 
 sediments are infolded with members nf the Ahitihi group and in many 
 
 
17 
 
 of the stratified members of the Abitibi group also folds can be observed. 
 There has been a striking development of schists. It is inferred that the 
 whole pre-batholithic group was thrown into folds of huge dimensions 
 -and that numerous minor lolds were superimposed upon these. 
 
 This great folding or mountain-building process was accompanied or 
 followed by the intrusion of huge batholiths of granite. There are also 
 within the areas underlain by the Abitibi group a number of granite bosses 
 and dykes together with pegmatite veins; and since the rocks in these 
 smaller intrusives are lithologically identical with those in the batholithics 
 they are regarded as being of the same age and origin. Field evidence 
 indicates that mineralization is a much more prominent feature in the 
 numerous veins which occur in the vicinity of these smaller granite bodies 
 than in those near the contact of the large batholiths. This tact is of 
 significance in dincting prospectors to promising fields. 
 
 The next ivent following the great granite intru.sions appears to have 
 been the intrusion of minette dykes. These dykes are quite smail and 
 the few occurrences that are known appear to be disposed along a line 
 running south from Rest lake. 
 
 Other post-batholithic intrusives, whose age relation to the minette 
 and to each other is unknown, are diabase, quartz diabase, and olivine 
 diaba.se. These rocks as now exposed are massive and unaltered. Small 
 dykes of these rocks were observed at scattered localities throughout the 
 district, and at Plug hills the quartz diabase masses may be the erosion 
 remnants of volcanic necks. No diabase sills occur in the Harncanaw- 
 Turgeon basin. 
 
 The quartz diabase of this district is lithologically identical with the 
 quartz diabase which occurs in the form of dykes and sill remnants in the 
 vicinity of Cobalt and Gowganda. There, rich deposits of silver, etc., 
 are found associated with the diabase sills; but no mineralization of this 
 type is to be found in connexion with the smaller dykes. In the light of 
 this experience it appears that mineral deposits of ♦he Cobalt type are 
 scarcely to be expected in connexion with the diabasr intrusives of Ihe 
 Harricanaw-Turgeon basin. 
 
 The region was exposed to erosive agencies for a period of great 
 duration between the time of the mountain-building of the Abitibi and 
 Harricanaw formations and the deposition of the Pleistocene drift. A 
 planated surface resulted, in which was exposed the truncated structures 
 of all the solid Pre-Cambrian rocks of the district. No sediments of 
 Huronian or Palaeozoic age occur in the ma|)-area. But the study, in 
 neighbouring regions, of the field relations of the Huronian and the distri- 
 bution of the Palffiozoic sediments indicates that the Huronian rocks 
 were deposited on an old erosion surface of low relief, and that there was 
 a ces,sation of erosion during a period of marine submergence in Silurian 
 time. 
 
 In Pleistocene time, continental glaciers passed over the district 
 scouring bare the rocky uplands and depositing till in an irregular manner. 
 These deposits were evidentlv of greater volume than in that part of the 
 Pre-Cambrian shield which Ties outside of the so-ca!leil clay belt, and it 
 appears that much of the debris was subjected to the assorting action of 
 lake waters which covered a large part jf the district during the time of 
 glacial recession. 
 
18 
 
 TABLE OF FORMATIONS. 
 Abitibi grWtUt 7re«eSnlTtl;n°p£ ^"'^'^'^ «' ^^ 
 
 Stratified l«CTi»trine clay and aand. 
 Boulder clay, gravel, and sand. 
 
 Vnconformity 
 
 Ple-Canibrian 
 
 K^^ni'wt'w *-'™'^ISS;'jS.«'»'««.q«"rUdi.6«.. 
 
 Igneoiu conlaet 
 
 Batholithic intnuivea 
 uuirentian (f ) 
 
 Granite and granito^iieiu. 
 
 Igneoiu contact 
 
 Harricanaw series 
 
 Arkoae, conglomerate, greywacke. 
 
 Unoonformitg 
 
 Abitibi group 
 
 Fenuginous dolomite and carbonaceous volcanic 
 
 Acid oWlMtics (chert) iron formation. 
 Khyohte and quarts porphyry. 
 iBtennediate pryoclastics and banded mica schi>t« 
 IShirts""*'^''' '^'^^- •■"• '"'"'blende JIS cWortS 
 Gabbro, diabase, basalt, and schists. 
 
 ABITIBI GROUP. 
 
 GENERAL CHARACTER AND SUBDIVISIONS 
 
 the latter, the surfieial rocUTo „S/cLeWla'va ^wf ft* w'^l' 
 
19 
 
 found in the tuffs of the Rreenstone complex and these are intruded by 
 later granitic batholiths. 
 
 In the Lake Superior' region, where detailed geological work has been 
 done, volcanic rocks are found in eveiy Pre-Cambrian seKes of that reg" n 
 Hence, in this region it is possible that the suriicial igneous rocks belong 
 to more than one geologic age and it is evident that there are, or have 
 been, granites of two distinctly different ages. Consequently, the name 
 Abitibi group will be applied to the lavas and related surficial rocks of 
 the basement complex instead of the term Keewatin. thereby avoiding 
 a name which bears a definite age significance, and the plutonic granite 
 and gneiss (Laurentian?) will be referred to by special local names given 
 to each batholith. 
 
 The Abitibi group includes a great variety of lava flows, pyroclastics, 
 bi. dykes, surficial rocks for the most part, which make up a larpe part 
 of the basement complex of the Pre-Cambrian. The stratigrapbic and 
 structural relations of these rocks have not been wholly deternained, but 
 in accordance with the more pronounced lithological distinctions recognized 
 in the field, the complex may be divided, for the purposes of description, 
 into: (1) basic and intermediate volcanics, (2) intermediate pyroclastics, 
 and banded mica schists, (3) rhyolite and quartz porphyry, (4) acid 
 pyroclastics, chert, and iron formation, (5) ferruginous dolomite and 
 carbonaceous volcanic slate. 
 
 BASIC AND INTERMEDIATE VOLCANICS. 
 
 The basic and intermediate volcanics occupy large areas in the north 
 and south parts of the sheet, but the irregularity of their distribution 
 renders it impracticable to define their boundaries in detail. They com- 
 prise the greater part of the area which is coloured green on the accompany- 
 ing map. 
 
 Gabbro, Diabase, and Basalt. 
 
 Character and Distribution. These basic volcanics occur in various 
 small areas. They are represented by schists for the most part, but 
 occasionally dark green, massive phases are found. Those with an allo- 
 triomorphic texture are classed as gabbro, those with an ophitic texture, 
 diabase, and the fine-grained or glassy-textured members are called ba^ilts. 
 Secondary minerals have developed to such an extent that these names 
 are not in accord with the present essential mineral constituents of the 
 rocks. In some of the outcrops examined, these rocks are found to pa.ss 
 gradntionally one into the other, and in some cases the diabase is a phase 
 of a uasaltic lava. Flow structures were noticed in some of the basalt 
 outcrops. 
 
 Lithological Character. Microscopic examination of the gabbro and 
 diabase shows that the original feldspars have been replaced almost entirely 
 by sericite, epidote, zoisite, and cai ite ; and the original augite is only 
 seen in the central part of hornblende crystals, entire alteration into 
 hornblende being most common. Chlorite, actinolite, tremolite, calcite, 
 ilmenite, and magnetite form the interstitial material betweer the original 
 feldspar and augite crystals. 
 
^ m 
 
 I 
 
 M 
 
 'liiMi 
 
 20 
 
 »Ki„r'*'" "*"*'"'"» «f »«««'* show a denso, fine-drained man of mineral. 
 
 ul^ u"* T"*'^ alteration products. No phenocrysts were oS^i^pH 
 
 although rods of secondary hornblende s, iTtlmes rive a MrS^tt' 
 
 enTX"'" 1*° t»J7<»ck in the field. The plagioeK 7.f the basaK'^JC 5 
 
 Krnf " '*'"* **'*' Pharaeteristic twinning lamell». The ferroma?nes an 
 ^«Xi T ••«'P':r''*'i^ ''.r ««•*"»«'!»«• and chlorite in small frrJ^ular 
 patches. Iron oxide is locally abundant in the thin sectionr ' ^ 
 Hornblende schists and amphibolitcs are the chief contact mpt«m«r„Ki„ 
 
 r/j^'Sgnaf ^''''"" "'■^'^"''^ "* ''^ b<,rdcrs ofihT;i:Strbrhoffis 
 
 ♦h„ SfTt^" ,"]l^''^"^- "^ *'>*' '*''*'''• mt'mbcrs of the Abitibi complex show 
 the effects of dynamic metamorphism. From the general contini^tvnnH 
 
 ZXT "^ ^""n'''\'" '^' ^™« ^'■'"^t^ i" the dis rict ifis BevSd 
 
 that the presence of schists among massive rocks (in some cases at a con- 
 
 siderable distance from any known batholith) is not due to local rock 
 
 naovements, but rather the n-sult of a great general compressive fo?eewhkh 
 
 «nffi ?lr'^ the weaker members in the series. The wSer rockryiddS 
 
 fhfn th„y *° "-eheve the strain, whereas the massive rocks were strong^ 
 
 than the force applied. In various parts of the region there are evidpn?™ 
 
 «LlrH'K^'^'"""lf*'°r' "^"vements."^ The basic rock" which have bee„ 
 
 oi^r^T^i^'K^*" Kreenish grey, calcite-chlorite schists. ''" 
 
 yrigm. The basic rocks of the Harricanaw-Turgeon basin are for the 
 
 most part ancient lava flows. The only exceptions to this were the labbro 
 
 which occurs on Turgeon river 17 miles below Corset islanJand is probabl? 
 
 as a dvke on Ihe lef? ?*"t' Tt^ " hornblende^hlorite schist whicCccS 
 
 SfTheo river. "'*'°" "''"' ^ '°''"« "^''''^ *''« confluence 
 
 Diorite, Andeaite, and Dacite. 
 
 r„„t ^'^'''(''"'^■o''- The greater part of the Abitibi complex is composed of 
 rocks of these types. Outcrops were observed in all thrgrecnst^re ^eas 
 
 imoT''"Trr'V''^ Zl'^' ^^''^ *» the farthest Joi^t north 
 Lithological Character. The diorite is a gr,.y or green rock w th a 
 fine, granitic texture in most cases, but that which is exMsed on Then 
 river 5 miles above its mouth is rather coarse. The amSe Z fine 
 grained equivalent of diorite, is a greenish-grev or grey rS in which the' 
 individual crystals can seldom be seen with the nakeTC though in a few 
 hDcahties a porphyritic development of feldspar crystals c' an be observed^ 
 The^andesite frequently has an ellipsoidal structure, in which cas^ it 
 ^rS^'"'^"^ 'r^*'"'''' in composition and textur^. Dacite a fine 
 Tf U^.v^""'"' -"k "^ n»«rtz diorite, resembles the andesite in the fiekl 
 It IS grey, greenish-grey, or pinkish grey in colour, and porphyrit c nhases 
 o this rock were more commonly found than in tiie case of th" and^ite 
 
 t^^n'^htif'* '■"'•'' ''^ ^^f ^""?''y ""'^ ™"'-h '""re abundant in the disTrci 
 than their coarse-graiued equivalents. aisirict 
 
 ^in "^1^ **^u" ^•*!:*'"" of the diorite is almost entirely composed of secondarv 
 minerals though a few remnants of primary minerals indicate that the 
 fresh rock was essentially made up of hornblende, biotite, and plaSoclase 
 JnrnKi P^r^*""* ^""^ition the rock consists of la;ge, irre^lar crvstals of 
 hornblende with fibrous terminations, biotite and chlorS crjSs also 
 
31 
 
 with irrPKular boundnripB; b««twe««n those rrystals the outline of altered 
 feldspars can be traced in a fine-drained mass of epidote, znisite, chlorite, 
 and kaolin. HectaiiKular masses of leucoxene with (K'casional cores of 
 ilmenite are plentiful. 
 
 The andesiti*H ranxe from types carrying abundant hornblende anil a 
 little plagioclase to types compo8«>d almost entirely of pUiKioi'luse with a 
 small amount of hornblende and some of the latter contain a Utile <|uartz. 
 In texture they vary from fine-nrained, holocrystalline typi's to porpliyritic 
 and glassy types. 
 
 The dacites show a similar variation in texture and composition, their 
 only difference lieing the presence of small amounts of orthcM-law and 
 quartz. It was frequently found that daeite occupied th«' central part of 
 andesite ellipsoids and elsewhere the connexion between these two rocks 
 suggests that both were derived from a common magma. 
 
 Microscopic examination shows that both the andesite ami daeite 
 have been highly altered, decomposition products usually being in excess 
 of the primary mineral constituents. The majority of the andesites examined 
 are porphyritic, cqiitaining small phenocrysts of oligoclase and oligocluwe- 
 andesine in a fine-grained matrix of plagioclase laths and smaller amounts 
 of hornblende. These minerals are largely replaced by calcite, chlorite, 
 zoisite, and sericite. Pyrite in small cubes is abundant in sj-veral of tins*? 
 rocks. Parallel streaks rich in chlorite in which the crystals are not 
 paral... show the direction of the original flow structure; broken frag- 
 ments of plagioclase phenocrysts were observed in one section strung out 
 in the same direction. Magnetite and tiny needles of apatite occur as 
 accessory minerals. 
 
 A spherulitic andesite outcrops on the portage on Turgeon river just 
 above where Patten river enters. It is composed of a recrystallized glass 
 full of small, stout crystals of hornblende. The spherules consist of 
 radiating microlites of feldspars. Similar spherulitic andesite occurs on 
 Turgeon river at CJorset island. 
 
 A massive, 8-foot dyke of porphyritic daeite cuts the slightly schisted 
 ellipsoidal andesite on the right bank of Woman river 3 miles above its 
 mouth. No other rock of exactly the same type was observed in the region. 
 In the field, the dyke material appears quite fresh; rectangular white 
 feldspars ranging from the size of pin heads up to one-third of an inch, 
 stand out clearly in a dense, greenish-grey matrix. Pyrite, in tiny cubes, 
 and a speck of gold were observed in a hand specimen. Under the micros- 
 cope, phenocrysts of badly altered plagioclase were seen, together with 
 hornblende and a feldspar which is not twinned. The matrix consists of 
 fine-grained quartz, feldspar, calcite, sericite, and zoisite. 
 
 A small dyke of biotitc andesite was found on the cast side of a small 
 bay on the south shore of Chikobi lake. This appears to be closely asso- 
 ciated with other andesites of the locality, but microscopic examination 
 shows that it is of a distinctly different type from any of the andesite 
 observed elsewhere. It is a porphyritic, dark, greyish-green rock slightly 
 schisted, carrying small phenocrysts of a dark micaceous mineral. Micros- 
 copic examination shows abundant green biotite phenocrysts embedded 
 in a fine-grained matrix composed of tiny rods and grains of biotite, chlorite, 
 plagioclase, and zoisite. The materials of the matrix show a distinct 
 parallelism. The biotite is regarded as partly primary and partly second- 
 
i 
 
 22 
 
 anr, u ■ome cryatals have a drawn out appearance conformini to the 
 •chwtoiity, whm«M other crystals with irregular boundaries have developed 
 witb haphasard orientation, and, in somt' eases merge into chlorite patches 
 which in«'hide ptiticles of the matrix. 
 
 Metamorphism. The andesites and relaU>d rocks are greatly kata- 
 morphosed. Sufficient evidence is not at hand to decide whether these 
 changes took place soon after consolidation, through the agency of heated 
 waters enaanating from the lava and possibly mixed with the sea watt-r 
 under which they were extruded, or by protracted weathering. Both pro- 
 cesses are believed to have been operative, but the former was probably the 
 more effective. Extreme alteration is found throughout the whole rock 
 material. The evidence that this alteration was carriwi on largely through 
 the agency of sulphur-bearing solutions is found in the abun<lant develop- 
 nient of pyrite in certain of the andesites, particularly on Harricanaw 
 nver at Tanbell rapids, and on the south shore of lake Chikobi; and in 
 the interstitial filling of quarts and calcite containing pyrite, which is 
 l)est seen at the Tanbell Kapids outcrop. 
 
 Dynamic metemorphism of the andesites gave rise to calc-chlorite 
 schists, in some of which sericite is an important constituent. These 
 rocks are best seen on Harricanaw river between Plamondon and Turgeon 
 junctions and on that part of the Wawagosik river which lies to the west 
 of tnis section. Shearing of ellipsoidal andesite gives rise to light and 
 dark grey, banded rock, the light-coloured bands representing the flat- 
 tened ellipsoids, the dark bands, the squeezed interstitial material. Petro- 
 graphically, the mam difference between the light and dark-coloured rock 
 lies in the greater abundance of chlorite in the dark part. Examples of 
 such rock outcrop at the first rapids below Obalski lake, on the left bank 
 of Harricanaw river; and also on the same stream 50 chains above the 
 <^o"V^"u*ncf .of Octave river. In the ellipsoidal ..n'jesite on the east shore 
 of Obalski lake fibrous hornblende, or stiff-fibred asbestos, has been 
 developed along local shear zones. 
 
 Amygdaloidal Structure. In a few localities amygdules are fouid near 
 the borders of ellipses in the ellipsoidal andesites. These vary in size 
 from one-quarter inch to an inch in diameter, the filling material usually 
 being quartz, though occasionally quartz with a central mass of calcite 
 was observed. An amygdaloidal structure is of remarkably rare occur- 
 rence in the lavas of the district. 
 
 Ellipsoidal Structure. A majority of the outcrops of andesitic lava 
 exhibit an ellipsoidal or pillow structure (Plate IVB). In some places the 
 interstitial material is weathered away and the pillow stands out distinctly, 
 but, as a rule, glaciation has smoothed the outcrops and prominence of 
 the structure depends on differences in colour or texture between the pillows 
 and the interstitial filling. The ellipsoids are elliptical, circular, or irregular 
 in section and vary from 3 inches up to 6 feet in maximum diameter, 
 though in any one outcrop the range in size is not so great. Sometimes 
 the ellipsoids are composite, that is, the interstitial material does not 
 completely close around an elMpsoidal mass, but allows two or more pillows 
 to join. In some oute.of, bun structure was observed, the pillows 
 being flattened on one side ' convex on the other. It is supposed that 
 the flattening is due to gravity, while the material was still molten, the 
 flattened sides thus representing the bottom of the ellipiwids at the time 
 

 38 
 
 oi their formation. At preront, the angle which the flattened Burfarea 
 maice with the horiiontai gives a clue to the structural relation* of the 
 flow. 
 
 Aa has b«'en previously stated, the rock material forming the ellipsoids 
 is usually a grey or grecnish-grev andesite, sometimes having an irregular 
 kernel of pale grey dacite or rhyolite repn-senting an acid differentiate 
 fmm the andesite. The rock is always fine-grained, <v<n when porphyritic. 
 A spherulitic development of radiatmg microlites of f«"ldHpar is character- 
 istic of the ellipsoidal andesite on Turgeon river near Corset island. 
 Amygdules, when preB«<nt, occur around the periphery of the ellipsoids. 
 The material which occupies the gore-like interstices between the ellipsoids 
 and which follows around their iMirders varies in different outcrops. At 
 Tanhell rapids at the northern limit of the mapp<'d area, it is cjuartz and 
 calcite. On Theo river 9 miles al)ove its mouth it is calcite und chlorite, 
 and elsewhere it is a dense, dark, fine-grained material which, when 8<'histed, 
 resembles slate. The original character of the dark filling material is not 
 known, though it probably represents fragmental igneous material. 
 
 Origin. A concise summary of some of the various hypotheses which 
 have been advanced in explanation of ellipsoidal structure is given by 
 M. E. Wilson.' He concludes that " the ellipsoidal structure in extrusive 
 rocks is always 8ul)aqueou8 in origin and is dep«'ndent on two factors : 
 (1) the flowage of the lava, and (2) the rapid cooling effected by contact 
 with water. Owing to this rapid cooling, and to the pressure of the lava 
 from within, innumerable fractures are formed in the surface of the lava 
 flows from which the fluid lava of the interior is ejected. This molten 
 material is immediately cooled by the water, however, to a viscous niass, 
 which by movement is later drawn out into ellipsoidal form. By repetition 
 of this process, great thicknesses of ellipsoidal lavas could be accunuilated 
 just as they are known to occur in various parts of the world." 
 
 This conclusion appears to be in accord with the writer's field evidence, 
 except in so far as lava movements are suggested as responsible for the 
 ellipsoidal shape. Though this may be true in some cases, there are 
 some occurrences where it is evident that the ellipsoid has merely sagged 
 imder its own weight, and there is also the case of interlocking ellipsoids, 
 which show that there has been vcr>- little, if any, flowage since their 
 formation. 
 
 Composite ellip.soids, which have l)een previously mentioned, indicate 
 that these globular ejections may be forced out from similar masses. This 
 would explain a considerable thickness of ellipsoidal lava without the 
 necessity of several sheet flows, though in all cases there would have to 
 be a lava connexion between the volcanic neck and the ejecting ellipsoid 
 in order to supply the necessar>' pressure and ejection material. 
 
 The volcanic vents through which the extrusions of andesite occurred 
 were probably located in numerous localities in this region. Dykes of 
 andesite cutting similar andesite were observed on Harricanaw river at 
 Tanbell rapids, at the gorge 6 miles above the confluence of Turgeon river, 
 and also near the middle of the south shore of lake Chikobi. 
 
 >0«ol. SuTT., Cu.. H«n. N. pp. Sl-M. 
 
INTEimmBUT. rTIIOClA.TIC. AND BANDRI, MICA KHim. 
 
 .nun's' t'X'';S!:;u^*''i:itr::s r,.-«'«»mt.^ .n.j ba„d«i. «„.. 
 
 rl««.|y r. Jm..le'S^^!l^rgnilt5 .'n'dSt'o 'th";, ^r?'" .««»«"« them 
 milium to fine^crBine«^Kr?v «iLt!.nin„ L ^'"^ '"""''I'' ""••» ■«'''"<» <"•». 
 
 Okikod,«ik river, and SnK H, 0.1? wL h^t'*"*'''- "''"'■• ['" *''•' "PP"' 
 ■outh«f(hik..hiandReit"JkS •^"* *™* '^''* P"«""K « -hort dirtance 
 
 I' 
 
 n'l 
 
 If*' 
 
 lake rhTklf IT;:^^ WW ?S'rZr^r*rP ?%*»•- -"^»' «h"«" «' 
 are north 27 d"KnVr;a.t^trnnrtWl "" *'"' *'P "' **"' ""»*" P^ninnulu 
 Wand in Turi^?n river ?u»t St^^^^^ "VT a pmall 
 
 IncluJin, pink ,„ „,te iSn rhZ .fl 1 1' '.'«""■"<■ •'";» net varirty, 
 
 fine. i« coarse enough to 'showThe '^XlI'.wS"' *"'' '** ^^V"--'-' ^'♦*'o"Kh 
 to the naked eve Theron^^l»\7 ^"""t'tu^'"* K"T" ""*' ^^'te minerals 
 
 tains wi,l,.iv ^epIVated r3ed Lm'J.n^^^^^ f '""* *'''' '?"'' '« *»"** '* ''""- 
 1 inch to 2 incCTn dXtr S^Z^nd "TTl^'^'T'^ ««"»*-. from 
 boundaries. It is »«'lieved t« heT liv i ^^"1^^ ""t P'-rft'ctly sharp 
 
 flow has intruded a nreiiHt 1 '«^'a «KKl«morate in which the andesite 
 
 assimilate.! a few fragmenTs ^ ''"'"*'' """^ •""""* ^^''^ «"^' P^^Iy 
 f.>m on^uarter ^n.^^S^^[^t^^ nSr/X J 
 
 (ffii 
 
rhiuritir material which probBbly is altcntl volranir ilurt. Tho mntrix tif 
 this riK'k i« not t>HM>ntially <liffi-ri>nt from thi* nmt nim-i- th«' whoU- in frag- 
 mi'ntal, but it in <iiiitinctly darker than the largrr frafuncntii. 
 
 Thp aRKlnmrratc in a nxk formctt tif vulcanic cjccta thmwn out by 
 a volcano of the cxplunvc type. Kince there in n«) evidence of tranMport- 
 ation of the materials, the iioaition of thin outcrop marks the approximate 
 site of the ancient volcano. 
 
 Strniifitd Tujfa. 
 
 Litholngicnl Chnraeter, Htratifi^l tuffs curreti|M)n(iinK to andiNitcs and 
 dacitett occur 4 miles east of the Harricnnaw-TurKeon junction, on TurReon 
 river 2 and 7 miles nlwve the Harricanaw junction, 3) miles Im-Iow the 
 EHttour River junction, and at several points bet »«-een 2) to 4 miles b«>low 
 Corset islai.d. 
 
 They are best seen on Turgeon river 3J miles lielow the confluence 
 of Detour river. They vary from pale grey to black, depending largelv 
 on the texture, the finer-grained varieties l)eing the darker. The Im'«1"m 
 vary in thickness from several feet to one f«M)t as a rule, but occasionallv 
 a much finer banding within the major Ix'ds is observable on the weathered 
 surface. The light grey, coarwr tuff has the texture and general np|)<>ar- 
 ance of a fine-grained ark()»>e and the quartz grains can be seen with the 
 naked eye; 8u))angular fragments of an intermediate glass were found at 
 rather wide intervals in certain layers. The finest black layers are dense 
 and homogeneous, break with conchoidal fracture, have all the character- 
 istics >f a normal argillite, and when schisted are distinctly slate-like. A 
 thin section of the coarser tuff examined under the microscope was found 
 to consist of quartz grains characterized by incurving edges, calcite, and 
 other obscure secondary minerals probably derived from feldspars. 
 
 In this outcrop, the tuff is intimately associated with an andesite lava 
 which in places shows the characteristic darker lava bands marking off 
 irregular ellipsoids. The chilled edge of the lava indicates its intrusive 
 relations. 
 
 MtUimor-phhm. In the <»outh(>rn part of this outcrop the finely bedded 
 tuffs are tightly folded an<l schist-d, and resemble closely folded', banded 
 rocks occurring elsewhere in the region, which would certainly have been 
 classed as clastic sediments in the absence of other evidence us to their 
 origin. A transition due to intense metamorphism can l>e followed in the 
 outcrops on Turgeon river fronj 2\ to 4 miles below Corset island. The 
 exposures to the south are like the banded tuffs just described, whereas 
 those to the north are banded mica schists which show numerous tiglit 
 folds. One of the tuff exposures on the left bank of Turge<in river, 3J miles 
 below Corset island, is cut by a rectangular network of quartz stringers, 
 a tiny fissure being observed in the middle of each stringer. These stringers 
 and the rock on either side stand out us ridges. The rock adjoining the 
 stringers has been recrystallized with the development of prisms of green 
 hornblende in a finely granular mass of chlorite quartz and fehlspar. A 
 small outcrop of intrusive granite occurs a short di.stance south. 
 
 Origin. The rocks are believed to be volcanic ash (h-posited under 
 water, the bedding being due to diffennt rates of settling of the fine and 
 coarse material, and their repetition corresponding to the successive periods 
 of explosive activity. 
 
26 
 
 Mm 
 
 W 
 
 Banded Mica Schist. 
 
 Dittribution. Banded micaceous achists were found in the foUowino 
 localities- on the nght bank of Harricanaw river just below the ES 
 4 ™n'«T Wa«^ago8ik river 4J miles above its mouth; on TurgLn ri^ 
 4 miles bdow Corset island, and 3§ miles above its junction wUh Theo 
 
 r«7L.f" ^''f^°t''^u'^T ^ ™'f« ^'^""^ *»'*' 6-mile portage; onXnorth^ 
 east shore of lake Abitibi on the point which projects toward KenoVha 
 island; 2 miles southeast of Rest lake; in the northeastern pirt of Ungue- 
 doc township at the 10-foot cascades on Makamik river and the hiU Tn 
 
 Chiko^ 'Tn']'""*. °^ ""T ^^'' ''\^^^ ^'^^ h'" 2 miles southwest of lake 
 Chikobi; and at several points which seem to form irregular east-west 
 bands Imile ami 3 miles respectively south of lake Chikobi. ' 
 
 Lithohgual Character. The rocks in these outcrops are by no means 
 fZtA- ''"^ f "'' characterized by highly developed fissility.^anessTnrial 
 composition of mica quartz, and feldspar, and a more or less distinct 
 colour-banding depending on the abundance of mica. The bands vTS 
 from dark grey and green to buff and light grey. The texture is usualK 
 fine-grained but may vary sli,;htly in thf different bands of the ^me oS 
 crop Lenticular quartz veins and rectangulariy intersecting veinlets of 
 quartz ure common in these schists (Plate VA) ""^^""B vemieis oi 
 
 of a mncT''*''?'*' examination shows that the biotite schists are composed 
 iLtTT^ '^"^'*^ and feldspar with marked parallel elongationVand 
 ♦.? f nf T ^'.°'^° *"/ ^u-''" *?'**H*^ ^'■y^**'^ ^I'^se longer axes also conform 
 to the direction of schistosity (Plate VB). The feldspar is chiefly orthT- 
 
 o.^ntftlV^f*'K/'i' •'•°*'i." f'-e^l^ently shows pleochroic haloes^ SSnor 
 quantities of chlorite, carbonate, pyrite, magnetite, sericite, epidote 
 zircon, and apatite were observed. ^ ' » " ' '>''"^^^^, epiaote, 
 
 «bir,^T*''™? °^ biotite schist from lot 58, range IX, Languedoc town- 
 ?nTU K*""' '!lT secondary orthorhombic crystals ^hich are believ^ 
 to have been andalusite but the schist is now composed of a dense felt^ 
 colourless mu-a and other obscure materials. Since the schisto^ bends 
 
 ffr hp H """^ **'"'" ?yf\'^? ■* '? concluded that the schist was compressS 
 after the development of this mineral. pi«-oocu 
 
 nliP Jonf "'^" T^\"''=a 8*=hi8t8 have been tightly folded and the minor 
 plications are we shown on the upper Okikodosik river. Here, the folds 
 
 so tiZ th.f tr'^'T' r"'^*f ' ^^'^ ^" amplitude of about 2 feet and are 
 so tight that the anticline of any particular bed corresponding to a svncline 
 seen in the outcrop could not be found, though the bed waVvislbTe for 7 
 teet. Ihe axes of the minor folds appear to be vertical and apparentlv 
 
 si^nTf^i- ''''" Pk'^'- ''"^"' r^P" ^'^^'^'^ °" ^^^ horizontal surface no 
 sign of folding can be seen in the banded schists. The tightness of the folds 
 in these rocks explains the fact that the bedding coincides so nearly wth 
 the schistosity that it is rarely possible to distinguish them in exposures 
 Tnd'Sin o7t*h: 'T^'fl''\^f- ^* '? •'^•^.«"* '^'^''^^ this locality Krike 
 r dip ^ffhJ m.:&mi?"^ '^"" *'^ ''^''^ ^"* ""* the^Hclination 
 
 ontcrlns 1n''fh!"«*l!i''^"^'' "u^uf ^^"'^'"'^ ^''^'^^^' '^ measured on horizontal 
 originaUeposH ' " ^'^ ^^^ enormously greater than that of the 
 
 Origin. The origin of the banded micaceous schists is not definitely 
 known, nor is it certain that they are all of the same origin. Rec^S 
 
27 
 
 iiiation has destroyed nearly all trace of original diagnostic structures 
 and textures. Since the schists are definitely stratified, it is evident that 
 they are waterlain deposits, but whether these deposits were normal 
 sediments of the shale-arkose type, or volcanic tuffs, is an open question. 
 Similar rocks, which are classed among the Pontiac schists in the Kewagama 
 region to the south, are regarded by M. E. Wilson' as being derived from 
 arkose and greywacke, on account of apparent conformity with and 
 transition into sedim»'ntary rocks of this character. The field evidence 
 collected in the Ho,:.':h)i3w basin, however, leads the writer to favour 
 the view that t' ■■ bandciJ niica'-eous schists are altered waterlain tuffs. 
 In the outcrop < i\ T>irgpon rivci ; i miles below its junction with Detour 
 river, undpubte ijr'.nded vclctt ac tuffs are intimately associated with 
 andesitic lavas. \ uoal inUnsi folding of these rocks has changed them 
 to banded mica ..clil-- On Turgeon river 3 to 4 miles below Corset 
 island a complete gradation is iound between banded tuffs and the typical 
 banded mica schist; in fact, scattered subangular fragments of volcanic 
 rock can still be seen in the coarser bands of the schisted tuff. The 
 elUpsoidal andesitic lava flows which compose a great part of the Abitibi 
 complex are believed to have been given off by submarine volcanoes; the 
 tuffaceous rocks produced during the explosive periods of these volcanoes 
 would naturally be stratified since they were deposited under water. The 
 high content of ferromagnesian mineral and of plagioclase which character- 
 izes the schists is in accord with the view that thay are recrystallized tuffs; 
 although these minerals would also be expected in case of recrystallized 
 shales and arkoses, they would not be produced from sandstone, and in 
 a medium and fine-grained siliceous sedimentary series of such prominence, 
 some sandstone at least would be expected. 
 
 A sedimentary series strongly resembling the rocks to the south of 
 Kewagama lake which are said to show a gradation into the handed schists, 
 also occurs in the Harricanaw-Turgeon basin, but in this region docs not 
 appear to be related to the banded mica schists. The irregularity of 
 distribution and the lack of continuity over long distances, of the banded 
 mica schists in the Harricanaw-Turgeon basin, suggests that they are 
 folded pyroclastics developed most strongly at irregularly spaced centres 
 of volcanic activity, rather than that they are folded sediments which 
 should show regularity and continuity of outcrop. 
 
 BHYOLITE AND QUARTZ POUPHYRY.- 
 
 In addition to the acidic differentiates of the ellipsoidal andesit«, 
 other fine-grained, acidic rocks in the district .occur in distinct masses, 
 and these are classed according to their texture, as rhyolite and quartz 
 porphyry. 
 
 Rhyolite. 
 
 Rhyolite outcrops were observed in the following localities: near the 
 right bank of Harricanaw river 3 miles below Amos; half a mile east of a 
 point on Wawagosik river, 7 miles above its mouth; on the left bank of 
 
 ■Geol. Sarv., Can , Mem. 3«, p 73 
 
 59813—3 
 
! 
 
 
 
 milea 
 
 
 jipiiiil! 
 
 'if ; 
 
 QtMirtz Porphyry. 
 Turgeon river; SonS^llf^iZk'Tlnrll "^""^ ^^"^ J"?''*'°° ^*h 
 
 -diameL,em\SinaleneiLmatrii^^^^^^^ about 1 mm. in 
 
 AUard portage on Harricanaw rl^r??^^ '^5"*' "*'''"" ^^ ™''«« below 
 constituent of tWs roJlT ' ^^^ ^""^^ ^PP*"^" *« ^e an original 
 
 phenocrysts of'S and grtn'^wE ^^''^'i *1?^ 
 
or 
 
 ACID PTB0CLA8TICS, BCLATSD ROCKB, AND IBON FOBIIATION. 
 
 Aeidie Agglomerate. 
 
 On- small outcrop of a peculiar acidic agglomerate was found on the 
 upper part of Leslie creek, ^ miles west of Chobodis house on Turgeon 
 river. A boulder composed of red chert fragments embedded in green schist 
 was observed on the upper end of the -BO-chain portage on Turgeon river. 
 
 The material found in the outcrop is a dark, greenish-grey rock, which 
 at first sight might be mistaken for one of the andesites so abundant 
 throughout the district. Close exanaination, however, reveals the presence 
 of rounded fragments of dark grey, chert-like material embedded in a 
 fine-grained, but not glassy, dark, greenish-grey material which is highly 
 
 siliceous. , , w . i ,-x 
 
 Under the microscope the chert-hke fragments are found to be rhyolite. 
 The smaller fragments are distihctly elongated in the same direction, 
 probably due to flowage in the lava, there being no indication of strain 
 or shearing. The matrix of the rock was probably a quartz porphyry; it 
 now consists of phenocrysts of quartz in a fine-rrained groundmass of 
 quartz, carbonate, chlorite, and epidote. Although fine-grained, it is 
 much coarser than the rhyolitic fragments. Small pyrite cubes occur in 
 both the fragments and enclosing material. 
 
 Banded Acidic Tuffs. 
 
 Distribution. Banded acidic tuffs were observed at the following 
 localities: on a hill a few chains west of the forks of Authier river; on 
 the islands and numerous points on the main peninsula and north shore 
 of lake Chikobi; on the left bank of Octave river one mile below the upper 
 10-chain portage; and on a ridge to the east of Harricanaw river 3 miles 
 below the village of Amos. 
 
 Litholon^'rr I Character. These rocks vary in general appearance from 
 types rer T the intermediate banded pyroclastics to a cherty type. 
 
 The . ufF on lake Chikobi is made up of thin beds of fine-grained 
 
 grey matt. . lich alternate with beds of pale grey ash showing small 
 fragments -i quartz porphyry and rhyolite in a fine-grained, siliceous 
 matrix. Under the microscope, the pale grey rock is seen to consist of 
 indistinct fragments of rock composed of quartz, albite, and orthoclase, 
 some uniformly fine-grained, but the majority porphyritic; these frag- 
 ments are embedded in a matrix of broken and irregular crystals of quartz, 
 albite, and a little orthoclase. The darker grey beds in this rock are much 
 finer in texture, but otherwise similar. _ 
 
 The occurrence near Authier river and on Octave river are similar to 
 the Chikobi tuff, except that the former is finer-textuied throughout and 
 the latter r coarser in texture. 
 
 The . criitic tuff, near Amos, is a banded, pale grey and white, 
 schisted rock in which small fragments of quartz porphyry and rhyolite 
 can be d'<t«rmined. The matrix of the rock has been largely altered to 
 sericite an quartz. The less schisted parts of this rock have a cherty 
 appearanc 
 
 59813— 3J . N 
 
IS 
 
 I : 
 
 
 
 
 
 % 
 
 30 
 
 infinJ?^T*?k"!r" "^^^ *^'*^'" pyroclastics have not been uniformly 
 
 out ??p ^S**'5*^r'l'°'' *'^ "> :^^''^ "PP^"" t« have operated throS^ 
 out the whole distnct in which they occur. The tuffs whichaoDcar to 
 
 ^ive^fri^rerandTJe ''^'^ .?'''°»'.'' P-^* ^" •'^^Sn^ Swee^^ 
 ra»8Bive vaneties and fassde sencite achista. In a 1 the outcrons whi^h 
 
 tTuctHeSsli^tr"-'^ metamorphis. the tendencytaTee^t 
 
 theSf^ir^^^^^^^^ 
 
 yertical, with the exception of the outcrop on Octave rh^I? There the 
 strike 18 north 5 degrees west, and the dip 85 degrees to the east t£ 
 outcrops on Chikob lake are intimately associated wHh a dac ie llva 
 and ellipsoidal andesite. The occurrence on Octave river shows a ^radl 
 
 St a firgi:iii:?s Th^i ?r«^ 'i^^ ^^"""^ frornVs^gSd 
 
 mil M) a nne-gramed tuff. The latter is characterized bv hanHa r,fuu,.v 
 
 ?-'rrtr J^'^/rPr^.>'««'^ of^chWite and f r u^no^^^^ cLboS' 
 dift.rver^d'^^ln ea'ch "^^f ^^H*" *^^ T'^ '« "^ ^''''''''' the "om^ct be'S 
 Xtir^iththlVdjtS roct P^™^"'«*"'« '^PP-'- t» be in conformabl^ 
 
 Carbonaceous Slate. 
 . , dfi^t^-""^ Character * black, carbonaceous, slate-like rock occur. 
 
 tain layers. A few small grains of rutile, zcisite, and sericite can be spp" 
 r^L^^"^"" 's. present in varying amount through the whole rock Th; 
 
SI 
 
 introduction or recryBtallisation of quarti at the Bides orihe pyrite nodulM. 
 The pyrite is in procees of weathering to limonite. 
 
 Field RehUiona. In the Octeve River outcrop the slate rock occurs 
 as lenses in "an acidic tuff. The elongation of these masses conforms to 
 an indistinct banding in the surrounding rocks, the strike of which is 
 north 5 degrees west, and the dip 8S degrees to the east. On Rest lake 
 the strike is west and the dip vertical, and in passmg across the strike 
 toward the north a fragmental phase is encountered, m which angular 
 chunks of ferruginous dolomite up to 2 inches in diameter are enclosed 
 in the black, slaty matrix. Beyond this, a slightly schisted, finely-granular 
 ferruginous dolomite occurs. Across the lake, on Vie west shore, a sencite- 
 carbonate schist occurs which in some measure resembles both the slate 
 rock and the ferruginous dolomite. It contains abundant spherical 
 concrelions of pvrite, some of which are 10 inches in diameter. These are 
 so closely packed that for a distance of 20 feet the pyrite makes up more 
 than 50 per cent of the rock. ... •* 
 
 Origin. This rock is believed to be a volcanic mud, a^id since it 
 occurs in intimate association with laminated tuff':, and in one ouicrop 
 shows an apparent bedding, it is believed to have been deposited under 
 water. The abundance of pyrite which was formed before schisting 
 took place leads to the conclusion that the waters in which the mud was 
 deposited were highly ferruginous, the whole deposit thereby acquiring a 
 unique character somewhat analogous to that of the slaty, banded, iron 
 formation, found on Michiwakenda lake in the West Shiningtree district,' 
 in the Onaman iron range,' and elsewhere. 
 
 Carbonate Rock. 
 
 Distribtdion. A carbonate rock composed largely of a -cerite or 
 ferruginous carbonate occurs on the left bank of Harricanav. river 14 
 miles in a straight line below Allard portage; on the northeast shore of 
 Rest lake; 15 miles east of this pJ.nt; a short distance south of Authier 
 river; and on the west shore of McKenzie lake. Two large boulders of 
 this rock were observed on the south shore of Chikobi lake 20 chains west 
 of its extreme east end. 
 
 Rest Lake Occurrence. The ferruginous dolomite is a pale grey, hnely- 
 crystalline, schisted rock containing disseminated pyrite cubes. Car- 
 bonate forms the greater part of it, butsericite is abundantly seen on the 
 cleavage surfaces. Green chrome mica was not observed in this rock. It 
 consists of carbonate in small rhombohedrons and irregular grains, mosaic 
 quartz, and abundant tiny sericite scales in parallel orientation Py"*]? 
 cubes measuring sometimes as much as 6 mm. on edge, are scattered 
 
 through the rock.- . ^ i •** j 
 
 The glaciated surface of the outcrop is rusty and minutely pitted, 
 
 and narrow veins of quartz and carbonate enclose irregular, ellipsoidal areas, 
 
 giving the rock an appearance similar to the ellipsoidal andesite. 
 
 The rocks exposed along this shore are all schistose and the schistositj 
 
 dip is vertical or nearly so. 
 
 ^lliii.,W. H, Geol. Surv.CM.Mem.M. p. 3». 
 
 tlloore. E. 8. Out. Bureau ol Mines. Ann. Kept , vol XVm, pt. 1, 1919. p. 234. 
 
 •ChrnnU mic i. wrnimonly found in the terniginous dolomite of the Kewa«Bina districl: Geol. Surv., CM., 
 Mem. 39, p. 64. 
 
"■- t 
 
 ; I 
 
 I' 
 
 iim 
 
 % 
 
 !^ i 
 
 ml 
 
 S3 
 
 outcrop and schistoeity strike °* ^ '"' *****''*' '^**' *»'«'• width of 
 
 SoUitOM dolomite 
 
 CcmUot obMnrad •tiikiM. , 
 
 nSft '^"'.'°"'' oont;i25, friiniciiU of d,Jo.nit.. 
 
 ?jW»totedoiomit<»'.'./.;.".' 
 
 Unit 
 
 BJjck lUty KKik'Withdi;rty Uiyei: ' ; ." 
 
 f^tatoie doJomiito..'. 
 
 iJrift 
 
 BUckiiity rook.; .■;;.' .';;;;; 
 
 iJTUl 
 
 fjeWf**!** dolomite. . '. ] .' .' .' 
 
 JJrtft 
 
 BiMk (Uty nidt'shoWiii beddiii'. ! . .' 
 
 s. «r w. 
 
 N. 8P W. 
 N. TOP W. 
 N. «• W. 
 
 N. es* w. 
 
 porph^r'* "*''™'' *" *'^ ""*•>• '''^'^ "^ -•« distant, is a schisted quartz 
 
 was o\tv3'aronV;K,intf L'indtS^^^^^^^ t 'r^^^^ '^"'-'te 
 a foot wide borderinrthe c^nTact Snt»il? ^^'''^' 1**^ "'^*'' fo^ about 
 of the dolomite up to 2 inches in diaZtPr T°^ jubangular fragments 
 to be seen in the slaty roik at tWs D^^nf Th ^-^ '°d'''?«on of bedding is 
 « parallel schistose plaZ in it l^L Lt . !.'"'''"1^*^ /'■*«'°«'"t« ''Pl^ar 
 conglomerate or an autocSstfcThpJh.w ?erta,n whether this rock is a 
 changes from south So degj^s w^tloTHW'^VA'^'''^'^'''''^^^^^'^i^^ 
 across the outcrop from northw^T to J^.fh f ^^J^^ ^««* '« Posing 
 tact appears to be thrsame JIthP «S T*" J^^ ^^'^^^ of the con! 
 65 degrees west. The Se of oont^Ji'^"''*^ ^* **>'» Poi"*- ic, north 
 dips 80 degre.. toward tKortheSf^'* '' ''"'*'"''' ^^^ *•>« schistosity 
 
 «trikLVn^'rtrforg!'e:8LTfnd%-' '''' t*>; ^'''^ ''^^'^-^ *« visible 
 west; this differs onfrsligS' f^ol t P'"'^.^ degrees toward the south: 
 67 degrees west and dips vertfcany ''*''«*''«'*y' ^^ich strikes north 
 
 it« ooma"tttK4yno^1,^,ot^^^^^ *'^ ^'^ ^^^ «t"»^« of the plane of 
 this point. The SK the tw IXto tf '*' V^t '^'.P ''"^ «*"^' «* 
 the 8 aty member stratigraphiS ov^rnL ♦». !.''?°*'^'^* P''"'^ «bow8 that 
 of dolomite in the slaty mSer are of tt Lm "^k'*""'**"- '^'^^ fragments 
 
 ttR a-dSo^i ^&ce£i^^^^^^^^^^^^ br *KrtSf 
 
 If. however, the fragmenrrX:!;? SL^ ^f of dXL^ ^^^^^^ 
 
interUyered with the slaty member and have been dismembered during 
 the schisting of the slate, then the chief significance to be attached to thesa 
 fragments is that they show that a rock of dolomitic composition was 
 present in the slate before it was schisted to its present extent. 
 
 The repetition of slate and dolomite in the outcrops micht equally 
 well be interpreted >as an interlayered seros which now stands on edge, 
 or as a truncated series of small folds composed of only two beds, one of 
 slate and one of dolomite. The latter view is favoured, since these rocks 
 were not encountered on land traverses or elsewhere in this vicinity, 
 except along the projection of their strike. If they represent a monoclinal 
 series it is highly probable that the other limb of the fold would have been 
 found either to the north or south. 
 
 Harricanaw River Occurrence. The ferruginous dolomite is a massive, 
 pale grey, fine-grained rock with dark mottlings and disseminated, tiny 
 crystals of pyrite. The weathered surface is rust-coated. The rock is 
 cut by a large number of quartz stringers. Some are tiny, irregular, and 
 discontinuous, and contain carbonate, and others, later in age, cut the 
 rock and the older stringers in two rectangularly intersecting sets and 
 occasionally in other directions. 
 
 A thin section of the dolomite rock was found to consist of very small, 
 interlocking, carbonate grains; small quartz grains and pyrite cubes occur 
 irregularly through the section. A small, irregular stringer of quartz and 
 carbonate was observed carrying small cubes of pyrite and one speck of 
 gold. This stringer fades into the rock material at its end by an increase 
 of carbonate. The quartz shows undulatory extinction, indicating that 
 it has been strained. 
 
 The exposure extends for 68 feet along the bank of Harricanaw river 
 and rises 6 feet or less above the water. At the northern end quartz 
 porphyry was found. This rock is .massive and consists of abundant 
 
 3uart2 phenocrysts from 1 to 2 mm. in diameter, scattered through a 
 ense, pale grey matrix which resembles chert in lustre and texture. 
 
 There appears to be a gradational contact between the quartz porphyry 
 and the ferruginous dolomite, since the contact comes in a band approx- 
 imately 2 inches wide which partakes of the character of both rocks, 
 but is somewhat different from either. Freshly fractured material 
 from this contact zone resembles pale grey chert and contains no quartz 
 phenocrysts; it weathers rusty, but contains only a small amount of 
 pyrite. 
 
 Since the material at the contact was not subjected to chemical or 
 microscopical examination, it is not certain whether there is a true grad- 
 ation of one rock into the other or whether the appearance of a grad- 
 ation is due to a cherty phase of the ferruginous carbonate occurring at 
 this point — this material bearing a close resemblance macroscopically to 
 the matrix of the adjoining quartz porphyry. No quartz veins were 
 observed in the quartz porphyry and no trace of quartz phenocrysts was 
 observed in the ferruginous dolomite, even adjoining the contact. 
 
 The contact between the quartz porphyry and the ferruginous car- 
 bonate trends northwest; its dip was not determined. The outcrop in 
 itself gives no clue to the attitude and geological structure of these rocks 
 at this place. 
 
ff I 
 
 tlh 
 
 About 6 miles farther down Harricanaw river in a northwerterlv 
 ^k ^wJ'?h'**^ exposure of quart, oorahyry wa. oIhi.,JJ3! Th2 
 I^„*j!3- ^i.-''* "^^ ."' """*"* ''•**' *^* ferruginous dolomite and is 
 mentioned in this connexion on account of the fact that under the micro- 
 scope it IS seen to contain tiny irregular quartx and carbonate strinsers 
 and also very small carbonate crystoTs within its matrix. The carbonate 
 mineral weathers rusty This rock has been slightly schisted a^ Snced 
 by the manner m which it cleaves when struck with the hai^i er. 
 .«~.-^*r ^^?^ Occurrence \ small outcrop of ferruginous dolomite 
 •^5^ I!.*^'?;i?^****' ■*"*'y ^"'* » »•'«'* distance south of Authier river 
 
 «K!„K ^IJ^'^^JP'** fiotiWer. A boulder of ferruginous dolomite was found 
 r»i wffh" h?i"'i*'"*"J'"* stratification. Thin beds of white chert alter- 
 SriLnatemaSl!" ^'"'•'^"»*^- Py"*« « disseminated through the 
 
 di«trS?fc- ^i^" ^'ir°' '." 'connexion w'th his study of the Larder Lake 
 rfnl^^u! •>*" »°!'^'^^ *''^ ^yidi^nce bearing on the origin of the ferruginous 
 dolomite of that region. He points out that the occurrence of Xht fer- 
 ISSrr^o, °°"u* '" ^''t^^ which can be traced for 5 miles, associated with 
 fif^H^K^ "k'^^'^ °°^ necessarily a nroof that they are also sedimentary ; 
 instead these bands might be regarcfcd equally well as metamorphosed 
 fo^r^nf nS '^'^'"""^ ',"*''« sedimentH exceptionally favoura.>ie conditions 
 isinti^Tn He concludes " that tlie ferruginous dolomite, which 
 
 18 intersected by quarts veinlets and contains chrome mica, has p^bablv 
 in every case originated by thermal replacement of aplite, quarts porphyry 
 
 KS^l^H^'f '°'^' *'^** ^^' "7«'"/' ^"^"^ which the dolomite^r^laS 
 had suifered deformation as a result of compressive stresses, and that the 
 
 contain ng carbon dioxide, silica chromium, boron, iron, sulphur S 
 Other elements percolated and thereby effected first the alteration and 
 ^vH?f Th* I'^I "T°'' '*^*' ^^ carbonate, sericite, chrome mica, S 
 aTo"?thSaires''"^'°^' '^"''^^ ^^•"'^*« "^^ '"^^ ^^P««*- °' ««- 
 Another hypothesis is that the ferruginous dolomite is a chemical 
 precipitate genetically related to the bandid iron formation ThircS^^ 
 ception presented itself to R. W. Brock when he studied the Larder Uke 
 district ,nl907. He states' tl .t on Pancake creek the rusty weathering 
 
 ♦Ko t'J^\^'^"?^il^ I" ^'•^/ePort on the Porcupine district states that in 
 luK*^ "^^''P* -^ ^f""^"" ^^^^ "^ ^"""^^ «f carbonate closely associated 
 
 being^coSpolSVpr^chX'^^^^^^ ^'^'"''" ^'^^' '^^'^ ''^ 
 
 northo"rn OntlH.^«i7A \""? reR?'-ding the ferruginous dolomite in 
 northern Ontario and Quebec to indicate that its origin presents one of 
 
 ■Geol. Surv., Cm., Mem. 3*. pp. 64-70 
 
 iaS:^ ^^ i M*^' ^"' 5^ • ™' ^ VI. pt. 1, 1907, p. 207. 
 
 JrS SS° i Jj!""' ^ 8^' • ™' XX.jp. 2. 1911,/ 12^ 
 
 ■»>« BonM of Mineo, Ann. R«pt , vol. XVlft, pt 1, 1801, pp 2S5, 259 
 
 III 
 
 Xm 
 
35 
 
 theae should be investigated. „„„.„,«. 
 
 !♦ i. not the Duroose of this report to discuss this matter compre- 
 l..n«ve V bit it Sv^ pointed out that the conditions observed in 
 i^Xrn^buebeJ aTonterK accord with those found in the Harncanaw 
 Strict l! th^^Ws^pin on the larger masses of ferruginous doom.te 
 fn Se Harriciwaw district^riginated as a chemical, sedment, genetically 
 .^uS-dt^^hrir^n formation; whereas the disseminations and dykelets 
 S^inl^ts* of ffe same material found in the a»ociated ac^ •«neou» ro^^^^^ 
 2^ b^UevJd to be composed for the most part of P^^r'S^^S^uS^viMe^) 
 
 S™raSJ^iaSgJe^us i^ks, and been given off into an overlymg body 
 
 **' '^The striniters of ferruginous dolomite material in the quartz por' hyry 
 are dykelfts Tv"in ets Since the same materials are found in segr gated 
 Jllh« and disseminations through the acid ign«.us rock mw^^^^ 
 ^rinirers occur and since the composition of the quarts P^'Pi^yy ,""" 
 reffi rocks preludes the possibility that this matenal wm derived from 
 Jh^TmXbv weathering, It is concluded that the ferruginous dolomite 
 rwJ^t^a^iff^^ntS'from the magma which gave rise to the quartz 
 r^rX?r The chemical composition is not to be regarded as a cntenon 
 - ^oriihTbut it mavbe pointed out that a similar origin has been deduced 
 tThrcinatTS^reri^ associated with the aplite in the quartz diabase 
 
 of the Gowganda district.* . , .. •„ ♦!.„ 
 
 Thp evidence that the larger masses of ferruginous dolomite in tht 
 Harricalaw £rict are a cheiSical precipitate is briefly stated as follows: 
 ftp nh^omena obsenTed at the contact of the ferruginous dolomite and 
 the beddTslaty rock on Rest lake suggest that they are conformable, 
 Edd^ deposited The boulder of ferruginous dolomite, «" ^h.kob. lake 
 Shows «trScation. This appears to be satisfactory evidence that the 
 dolomite here is some kind of a sedimentary deposit. indicated 
 
 That the ferruginous dolomite is not a normal sediment is indicated 
 bv its apparent ienetic relationship with certain quartz carbonate ve.n- 
 lete" wWdi occSr in it, and in the associated acidic igneous rocks. The 
 Smite otthe'wer Lake district -ntains chrome mica and th™era, 
 in not found in dolomites of the normal sedimentary type, ine nininy 
 fL^^ginZ comiTsi^ion of the dolomite di^stinguishes it from any dolomite 
 known to have orimnated as a normal sediment. • * i ;„ 
 
 Th^fSinous dolo°^it^ is frequently, if not always, associated in 
 the field wUh'quartz porphyry rhyolite, or rdated ••jj^-^J^^^^^'^^^'l 
 since these rocks contain a greater or less amount of the materials com 
 
 iiFoUia., W. H.. Geo!. S«'v , Cm.. Mem. 33, p. »7. 
 

 .iSL**^*. '•'!?«''">"• dolomite, in •irinnn and diMminatiom. it I 
 
 iron I!*™^T?°*?i!*lK°'^**i" *»>»7« "wciatwi in the field witli budec 
 18 found 600 feet eut of landed iron fonnmtton wlitch trends ewt »nd Wert 
 
 rfSffJnTf *'"' 'f.""po"" dolomite ia l>elieved to be a sedimentary depout 
 
 2 rSml whinM^'* '^^H-r"^ '"'"^" " "°"°»' »ediment,1S fo?S 
 SLsminTitil ? *''k '^""ditions were present wliici, favoured cliemic^ 
 sedimentation (as sliown by the banded iron formation), and sincethii 
 ^K !f. ■fS"!'!!!^,'"*^ genetically related to igneous ro^Citwoe^ 
 probable that the ferruginous dolomite formed afVchemkal LjdimfK 
 
 to hive^T SUDORS fn\l "** ^ *H banded iron formation is belieiS 
 Wbution ' the sSi^itKif Z"^" ?' deposition by direct volcanic con- 
 
 CAert fioc*. 
 
 A rock resembling chert was observed on the right bank of Patten 
 nver, one-sixth of a mile above its mouth; 14 chain7w«t of a Lint on 
 
 . n£KT-^ ""* ^"'^ ^ '^'^'"^ '™°» its northTnd ; ann; the 
 . -i^" «de of Hamcanaw nver about 3 miles below the village of Amos 
 
 ha« tS^rr"*"*^^ 7 P^""" "^« i" the only massive one. The mk 
 Joi *•>« »PP«"ance of a dense, white chert, through which a few rS- 
 coloured streaks run in discontinuous lines. ' 
 
 A thm section was found to consist of an extremely fine-irrained 
 S^^f^K^^T-"^'- ''"d feldspar and a considerable amS of ctJbJiate 
 distributed m irregular patches. Sparsely scattered through tWrfine 
 grained material are a few angular crystals of SclasT-afbite which 
 
 ^y&'''''Lf7\Hj. rVl^'r^!^'' "% "-hXtrthLnlhetht 
 irysiais. une of these crystals showed, under crossed nicols a division 
 into four quadrants which extinguished at different times the result 
 of combined twinning following the Manebach and GarTsbad laws A 
 
 cSsta"s tK nVc't- '•"''^.^ *\™1!?*^ ^\^ """"^^ these laSrfeZpa^ 
 crystals, /he .hin section when held to the ght shows alternate white 
 and colour es'. bands ranging in width from 1 mm. down to Se thrlads 
 This bedding cannot be detected in the hand specimen nor under the 
 microscope unless low power and reflected light aVe uTed This sumits 
 ouarf,"lhl'"i'''°"5\*^" '•""'^ '=«"*«'" ""'•« feldspar than the aheSe 
 KrStSp^its" ^*''°' ^"* ^''*« °" ''''-""* «^ theiryitrr 
 
 rnn+oTJ® ^^^^^ i^"^ '"^^ Ninemile portage and from Harricanaw river 
 contains a small amount of epidote which gives the rock TSertSie 
 
 ■Leith, C. K.. "Inm on, o( CmkU": Eooa. Col., vol III. „. jt»-mi. 
 
 iL... 
 
•7 
 
 Th. «:hi.t<-e portion, are ch.ntcteri«d by »n .bundant development of 
 
 to a chemical sediment. 
 
 /ron Formah'on. 
 
 strong magnetic attraction. Pr?^*»^/j;„J^eice of P amondon river. 
 „e.ttho junction of Tiirgeonund Patten nvei.. 
 
 of quart! grains and n"")"""', *J'"„n^" whit" band" The smaller 
 
 between them. , .u„.«= 
 
 Structure The outcrop, which is only a few yards «l"aj;e. «no*« 
 
 rtH<^.K9^»|r^i^Br£^^^^^^ 
 
 is beliTved IhatX outcrop lies near the trough of a synchnonum. 
 
 Fi,U ReUtions The iron formation is underlain by green chlont.o 
 
 Wa Which gave rise to the a_-sociated volcamc rocks. 
 
m 
 
 •WCCTCM or TUB awTIBI OMOF. 
 
 •littUon that the Abitibi .roun J i^CJLS k '^*''' '°.' *•>* '>«>«' Rene 
 and that the* fold, have Ke^edT^'tS" ^'* ""Nected to foTdSJ 
 8m;»^^ tight fold, can be aSly o^rJ^**^; 1"!"!, '^"JP'"" •'"?S 
 ttnSr*-^' '"'' ••^' ol^itffi-an' o^SiorofreWd; 
 
 eiap^dVlXfe tteS. SS: ttTS^i" /"'^ "'""^'^ ^''''^^ 
 to be ob^rv«| a. banded^^nj^^ itlX:"„^'r.StS^^^^^^^^^^^ - 
 
 -rie. a^dtt^rtrltSSjhTcalrS^^^^ ""•^""^ *"•• Harrioana, 
 the top of the Abitibi kSJ^ TW.TS th/"*""***.*" ^ "t orT" 
 iolT '"f*f"°" *" »t one time wWe"v d^rtrihlllL'""* -uppo-ing that 
 now the whole urouo ha. been tZZli^i,^^*^' ""e wou d exoeot 
 
 of the iron forma^ionVoSd b^ foS Jnlv"!!'""/*^' u**"** *»"• '^^^^^ 
 or, jf erosion had proceeded far enoLh^K *'"' *™"*'"' «' the synclineT 
 to. the main troughs of rynHinoriaS'Xri'''""*^^*""''' »^ conS 
 minor folds). This latter supSio™1ndI^inl? 7-^''^ "T '"P^'rimposed 
 Turgeon basin. Considering tKKrotkTn^H^h*'!!" "I *> """ioimtw. 
 occurrences and the points at whidi ^tm^^ l*''^'"'"*'^♦^ ''"^ formation 
 w "^ 't^fved a. all indicative of the n^S 7f' '?T''t''' attraction 
 we find that the distribution is verv liS of b d^ j^^^ formation, 
 P^'-'tf.two linear cours,>s ar" tra7j "hS *miv 't* "'^'" J"*"'"« the^ 
 approximate position of the main tSirhs^ of t J?.^ K consitjered as the 
 to the north of Mistawak batLlUh «..V * i''^"'"''"oria. One occurs 
 from the mouth of Patten river he o^rll^'^A ""'*'l. "^^ '^'•f'^ eL" 
 from a point near the north end ofVnemiiJ l^^f *""*'',*' ^^'^^ east 
 that Imes pro ected along these svnclinSr ^'^^- ? ""^y «>« noted 
 the west and diverge toward thpl.*".- toughs tend to meet toward 
 folds was toward the welt The ZlSrV^"' '^' F''"^ "^ the S 
 across the middle of the niaD-aLTf S ' f'' ™**" '"^s as measured 
 Kreat fold is 51 miles. ""P"*^" «t nght angles to the main axis of the 
 
 bat^'llira'^erS^fLteV^^^^^ -"^* "^ the Mistawak 
 
 Th.8 suggests that the plane of contact b^tw^^n";^ °' 'ts northern contact, 
 group plunges more steeply beneath th.tS *''^K™'"tf and the Abitibi 
 of the batholith than on the n^rth ^' "^^^ °" the south margin 
 
 Abiti^?;!^CJ.t fTutttlJlLtr^^^^ the deformation of the 
 
 in a number of outcrops, No ?Ze f^ i?i ? *^T''* ^''^^ ^^» observed 
 district; but, since the area h J n^f i!^i*'«*'^,*JLV'' '^''ognized in the 
 
 unsafe to say that faulting haHlayed a^ inSS '1 ^^'i** '' '* '^""'^ ^ 
 deformation. '^ pmyea an insignificant role in the regional 
 
 
 \41y s * 
 
AO«. 
 
 Thp Ahitibi group minatltutrft the ulileat (iivMton at the Pr«*-( 'nmbrittn 
 roelu in the Harriransw-TurReun basin. Tht* ru<>kH in all thi- other ilivii«ion« 
 vii., Harriranaw ««>riM, granite bathnlithn, and pont-lmtholithir intruaivea, 
 are known to Im) younger than those members of the Abitibi group which 
 have been found at their rontarts. 
 
 The ages of all of the various rtKk types whteh make up the Abitibi 
 group, relative to each other, are not known, nor is it certain that all rocks 
 of the same type are of the same age. Nevertheless, a study of the general 
 field relations of the Abitibi grf)up suggests the following general inference 
 as to the relative age of its memlM'rs. The oldest rm-ks are th<> baxic and 
 intermediate volranic riM'ks together with the pyroclastic rocks of inter- 
 mediate composition. No attempt can l>e niacle, in the present state of 
 knowledge, to resolve this complex and it is presumed that it represents 
 a numlwr of succi-ssive volcanic ejections and outpourings which were not 
 separated by any great time interval. The basic volcanics and the pyn)- 
 clastic rt)ckB have liei'n alter«>ii to u greater extent by dynamic metamor- 
 phism than have the intermediate lavas, but since all appear to have taken 
 part in orogenic disturbances th*- degree of metumorphisni apitears to l)e 
 less of a criterion of age than a clue to the original strength or ccmipetence 
 of these rocks. 
 
 The rhy«>lite and quartz porphyry extrusives together with associated 
 acidic pyroclastic rocks are regarded os Ix'ing the products of a later p<'ri<Ml 
 of volcanic activity than that which gave rist? to the basic and intermediate 
 lavas. This conjectur** is based on the fact that rhyolitic material is 
 found as a kernel within the ellipsoids of the ellipsoidal andesite al a 
 number of localities and since this material is regarded as a residual differ- 
 entiate of the andesite it might l>e inferred that o similar process went on 
 in the parent magma and that the later ejections from it would be of the 
 acidic type. The relativ*- scarcity of these rocks and their general arrange- 
 ment in the field betwei-n the great granite batholiths suggests that their 
 stratigraphic position is above the more basic volcanic members. The 
 liedded deposits, banded iron formation, ferruginous dolomite, carbonaceous 
 slate and chert are regarded as the youngest members in the Abitibi group, 
 and on account nf inferred genetic affinities and their association in the 
 field th«-y an- supposed to be of approximately the same age. In one 
 locality it is known that the iron formation immediately underlies the 
 Harricanaw series. 
 
 HAimiCANAW SERIES. 
 General Character and Distribution. 
 
 The Harricanaw series consists of folded and highly metamorphosed 
 sedimentary rocks, the dominant member being conglomerate and the 
 accompanying beds arkose and greywacke schists. The rocks were found 
 in place in only one locality, a small hill 16 chains south of Authier river 
 and about 10 miles northwest of lake Chikobi. The previously described 
 clastic chert rock which occurs near the northern end of Ninemile portage 
 may lie related to the Harricanaw conftlomerate. hut no fleciaive field 
 
lUi 
 
 if 
 
 40 
 
 !2h?™-«! "" 'T"** ^ P">^« ■"•''» » correlation. A muOl exposun 
 sedimentoiy rocks is reported by Mr. J. A. Bancroft on aurioS^^ 
 a short distance above Allard portMe». namcanaw n 
 
 :. * Jit" "L"*^*"*! eamoBures on the amaU hill near Authier river wl 
 18, for the moet part, roil^wvered. Folding has been so intensf howe 
 that the geological interpretation as to thicknesTof b^ds" if rorture , 
 « folS^sT"*^"" " '"^'^'^ *° "^'°- "^^^ "«'«°° »* thuSSnt i^ii 
 
 Rook. TJiieka«ii«fMt. 
 
 cSSl'Sur*.'^'""''"'^^^* »+ 
 
 Limy grey waek* •eUii *•+ 
 
 Arkow 5* 
 
 ■ »± 
 
 Banded iron fonnatioo 
 
 Arkose. The arkose was not seen in actual contact with th«. ir 
 uT^Ti.^""^ ""^ separated from it by only a few SHf d^ft cov^ril 
 It 18 a light grey, medium-grained clastic which has been slightly mK 
 
 fragmente of quarti crystals, together with orthoclasa and albite the s 
 
 ^Lfn"^ ^'""J ""'^?'?°' "°"°^ *•»««« " «° interstitUdSling of veiy fin 
 
 grained quartz, sencite, and calcite which has been partJy recrSliw 
 
 Limy Greywacke. The schisted, limy wevwacke is a fin^!^in! 
 
 contact with the adjacent arkose below and the conelomerate ahni 
 Sn»i° k' *™°«'«?"«|- Microscopic examination reveaJsSwM Jf4 
 original character of the rock, since it has been thoroughly recrKite 
 to a drawn-out mass of sericite, quarts, and calcite. ^ ^crystallise 
 
 tongtomeraU. The conglomerate is a highly altered rock with 
 sencitic schist matrix. The rounded and subangular p^S ranie i 
 
 chertTd hl'^H -^ "°r'«M^ °^ ''V'''^' '^"^ «^«"««* for^he mosS S 
 chert and banded iron formation, other pebbles being of sliirhtlv schist*, 
 andes.tedac.te, and quarts porphyry, '^and granitf. The pebbTes S 
 abundant but are not closely packedf except in\ few small Hn^eargroum 
 The.r longer axes conform for the most part to the schistosUy wWch 
 nearly the same as the indistinct bedding; but a few notable excention 
 were found where the longer axis of the pebble stood at a coLidei?bl?and 
 rltit «f *''«*"«'*y '^"d the bedding. The stratification is sSesSd by th 
 relat.vely closer pack.ng of the pebbles along certain bands The matri 
 
 K:-ki /^5 i^'"^?"""'**'- ,J^^ ^'^nded light and dark grey greywackes are 
 highly folded sil.ceous, limy rocks, in which the bedding appS to ha"e 
 iin^ K.,f "''^ *' the schistosity; the dip could not be^a??urat"y dS 
 mined but appears at the conglomerate contact to be appSmaS 
 
 "it ;i 
 
41 
 
 vertical, whereM the schistoBity dip is about 80 degrees to the south. In thin 
 section, mieroacopic crenulations can be observed in the recrystaJlized, fine^ 
 grained materiaj, which is largely composed of quartz and sericite, with 
 a small amount of calcite and limonite. 
 
 Stnuture. 
 
 The Harricanaw sediments are believed to be a conformable series 
 which overlies the iron formation of the Abitibi complex unconformsbly. 
 They have been infolded with the rocks of the Abitibi complex, the whole 
 showing minor folds superimposed on a major fold. From an analysis of 
 the structural data obtained it appears that the rocks in the outcrop occur 
 in a major synclinorium a short distance south of the main trough. The 
 axes of the minor folds strike north 70 degrees west and pitch towards the 
 west at a low angle. Faulting was observed in the outcrop, but the 
 horizontal displacement was never greater than a foot. 
 
 Origin. 
 
 The Harricanaw sediments are believed to have been formed by the 
 erosion of an adjacent land area of the Abitibi complex. The iron forma- 
 tion which is stratigraphically just below the sediments supplied a majority 
 of the pebbles in the conglomerate. The pebbles are, for the most part, 
 well rounded, as if they were waterwom through either wave or river 
 action. The only feature noticeable in the conglomerate, which is not 
 characteristic of normal waterlain conglomerate, is that the majority of 
 the pebbles are not closely packed and contiguous but are separated by a 
 fine-grained matrix. The sharp contact between the conglomerate and 
 the overlyicg.fine-grained deposits shows that deposition of the conglomerate 
 gave way suddenly to deeper water deposits, thus suggesting sudden 
 subsidence. It.might be mentioned that the banded sediments overlying 
 the conglomerate have been intensely metamorphosed and resemble 
 banded schists which occur elsewhere in the region and which have been 
 previously described as altered stratified tuffs. The origin of these rocks 
 has been given on the basis of their association and stratigraphic position 
 in the field. 
 
 Age. 
 
 Harricanaw sediments are younger than the iron formation and other 
 rocks of the Abitibi complex, which occur as pebbles in the conglomerate. 
 These pebbles include greenstone volcanics and a granite which has not been 
 recognized in place in the district. No members of the Abitibi complex are 
 known to be younger than the Harricanaw sediments. Since the sedi- 
 ments are cut by large lenticular quartz veins such as are commonly found 
 in intruded rocks near the granite contact and have been infolded with the 
 Abitibi complex and since the folding is supposed to have taken place at or 
 before the time of the great batholithic intrusions of granite, it is concluded 
 that the sediments are older than the granitic batholiths. Thus their age 
 is given as being between that of the Abitibi complex and the granitic 
 batholiths. 
 
rW 'in: 
 
 'Si ' 'li' 
 
 
 42 
 GRANITE AND GNEISS. 
 
 r :Hl!; 
 
 (« 1 
 
 Distribution. 
 
 Approximately one-half of the mapped area in the Harricanavz-Turse 
 basm 18 underlain by granite and gneiaa. A larRe area ".xtends entin 
 acroM the central part of the sheet in an east-west direction, with an avera 
 width of about 20 mil«.. This, for convenience of reference, is called t 
 Mistawak bathohth. .South of this are the Abitibi batholith, the Roberts 
 lake bathohth, and the Davy River batholith of considerable dimensioi 
 and numeroMs small irtrusions. To the north of the Mistawak batholi 
 ' f ^® several small granitic outcrops, and one rather large mass on t 
 lower Turgeon nver at the junctions of the Theo and Wawagosik rive: 
 the northern boundary of which is not known. 
 
 Lithological Character. 
 
 The granitic rocka found in the batholiths of the district vary conside 
 ably in texture and composition, especially at the margins of the batholitl 
 and m the smaller intrusiona. The granite in the central parts of the larg 
 bathohth la typically coarae-grained with pink and white feldapara, biotit 
 a little hornblende, and quartz. A gneisaoid atructure ia rarely w( 
 developed except near the batholith margin. The typical granite is 
 coarse-grained, even textured rock consisting of quartz, orthoclase, albit 
 and biotite with small amounts of hornblende. The plagioclaae ia occi 
 sionally zonally banded, the core being albite-oligoclaae and the outer layei 
 albite. The central part of such crystals is usually partly decomposed 1 
 a mass of sencite, calcite^and epidote; the other feldspars are not so muc 
 altered. The biotite crystals sometimes contain fine needles of rutil 
 regularly oriented in three directions parallel to the edges of the basj 
 pinacoid; zircon inclusions surrounded by pleoehroic haloes were ala 
 observed. Apatite and magnetite occur as accessory minerals. 
 
 Many of the granite outcrops show a complex of different rocks whic 
 vary m texturr composition, and foliation. Thus, on the hill to the eag 
 of Pajegasque river, 8 miles above its mouth, a medium-grained, pini 
 biotite gneiss is cut by a coarse, grey biotite gneiss of more basic composi 
 tion, and also by pink aplite dykes. 
 
 Near the contact with the older rocks a great variety of granitic type 
 is encountered. For example, the granite on Harricanaw river 5 mile 
 above the confluence of Octave river is a dark biotite gneiss with a porphy 
 ritic development of pink and white feldspar and allanite crystals. On th( 
 northwest shore of Otter lake a coarse, fresh-looking hornblende granit( 
 occurs near an acidic biotite granite which in places contains phenocrysti 
 of biotite and nearby becomes finer-grained but with phenoerysta of feld 
 spar. In the biotite granite, rounded inclusions less than 2 feet in diametei 
 were found, composed of a fine-grained biotite granite-porphyry with wel 
 developed phenoerysta of bluish-quartz a half-inch in diameter. In the 
 northeast corner of Languedoc townahip, pink hornblende svenite of various 
 textures occurs along with very coarse-grained pegmatites. In some of which 
 the feldspar crystals have a diameter of over 1 foot. 
 
 A hornblende syenite-porphyry occurs at the headwaters of the north 
 fork of Authier river, and abundant hornblende phenocryats averaging 
 
48 
 
 one-quarter iuoh in diameter are embedded in a fine-grained matrix of 
 hornblende and 'pink feldspar. The rock at the western contact of the 
 bstholith on lower Turgeon river is a very coarse-grained hombjende 
 granite, whereas near the contact farther east there is a fine-grained biotite 
 gneiss. 
 
 Microscopic examination of these granites which occur near the green- 
 stone contact shows that they differ from the normal type in that microcline 
 is the most abundant feldspar present. These rocks range from granite* 
 to granodiorites and syenites. There are other much more basic phases, 
 but all these appeareo to be partly asrimilated blocks of greenstone which 
 had been engulfed by the granite. In general, it might be pointed out that 
 the' granitic rocks which occur near the margins of the batholiths have a 
 greater range in composition than those occupying the central parts, and 
 that in the more basic varieties there is a tendency toward a porphyritic 
 texture which occasionally becomes strongly developed. The phenocrysts 
 may be either quartz, feldspar, hornblende, or biotite. 
 
 (Structure. 
 
 The granite and gneiss areas are believed to be truncated batholiths, 
 their upper parts and the overlying rocks having been removed by erosion. 
 The size and abundance of the granite intrusions and the occurrence of 
 granite and pegmatite dykes between these suggest that the whole region 
 may be underlain by an enormous granite mass, of which the outcrops at 
 the surface represent only the higher prominences. 
 
 The granitic rocks have not been folic d by metamorphic agencies. 
 In places where a gneissoid structure is developed, this appears to be due 
 to movements in the magma which arranged the minerals in lines, but these 
 minerals do not show a parallel orientation of their longer axes. 
 
 The batholiths evidently intruded into their present position, at least 
 partly, by a process of stoping; the overlying greenstones having been 
 shattered by differential heating or other means and engulfed and assimi- 
 lated by the magma. All stages in this process can be traced in the present 
 contact zones. 
 
 That the granitic batholiths also forced their way through the old«r 
 rocks and compressed them into folds is shown by the contact phenomena 
 on the east shore of Wawagosik lake. Here, the strike of the schist is 
 parallel to the line of contact with the granite ; and dykes of granite are 
 infolded with the hornblende schists and are cut by uncontorted dykes of 
 similar granite arising from the same intrusive; i. c. there is an intimate 
 relation in time between the intrusion of granite and folding of the Ahitibi 
 volcanics. 
 
 Contact Metamorphism. 
 
 At all points where the relationship couid be studied, the granite or 
 gneiss was found to be intrusive into the rocks of the Abitibi complex; the 
 greenstones near the contact are intruded by abundant dykes of granite, 
 aplite, and pegmatite and are characteristically altered to black, glistening 
 amphibolites and hornblende schists and less frequently to sericite and 
 chlorite schists. The schistosity, when present, usually parallels the line 
 
 59813—4 
 
«t I 
 
 44 
 
 Jh.*'!!^" ^ **°i* c*«e8 no definite Une of contact can be drawn, since 
 
 the granite permeates a shatter tone of greenstone blocks, which may b< 
 
 . either polygonal or plate-like (Plates vfl and VIII). GreenrtoiSYrai 
 
 ments m the ^|amte mass are always homblendic rocks: they decreaaeiE 
 
 fragments have sharp boundanes, but several cases were observed whew 
 the block was either drawn put or rounded and passed transitionally into 
 
 timi^S. L*? •'"''"T °'.<»'^» ""d [eW»?«; in fact there are wme- 
 times bands and irregular areas of hornblende-rich granite in the more 
 acid oanite which may represent assimilated fragments. It is in such 
 tocahties where evidences of greenstone assimilation are found, that the 
 SS7."?^!„f*f •*'" r^ '" £l««*<^ri»«d by variations in common 
 ^it^^fT^i^Z"^ ,* P"Pl>ynti« te'rture. In other places. aTat the 
 contact of the Mistawak batholith in the eastern part of the sheet the 
 gramte shows few inclusions and is neither fine-grained nor porphyritic. 
 «,.™ "Tl 'o^fi'tie" t^e greenstone schists have been intruded by 
 
 XZfv^J^'''PT'**'**'?P"**'' *?^ granite, which either parallel tS 
 schistosity, or may cut across it at various angles. In these dvkes and in 
 
 Setl^r ntC°"^lf-?^* schists, certain miners are founTwSh s^ „S 
 met under other conditions, and it is in such localities that mineral deposits 
 
 mnWhH?nf*°*'^^ ^/^ "^^ ^ "J^**^' ^he minerals refe^ tHS 
 molybdemte, garnet, vesuvianite, tourmaline, and allanite. The irreeDK 
 
 5l^T„."l'^'"^*'°}r °e'y '^^'^ '«' « '«^ i^'^hes away from the%SSte 
 S?5?„«:S """^'y ^^^ metamorphic effects extend back a consiSbk 
 JSf 1^ *i? ^"ft^'^^y pronounced in the neighbourhood of pegmatite 
 h. SL,,?i1,*'**"*r- P'^"''* ?f th« greenstone is remarkablVrimUM 
 L™«^^f T^'^'''^ " ™.??*^'"° °' fine-grained hornblende schist or 
 amphibolite which has been silicified and mineraUzed with pyrite 
 
 «..„!?°^ t """^^ «iope of Oditan hill a "red rock" lens is enclosed by 
 granite dykes. This rock is a fine-grained syenite porphyry comwised 
 almost entirely of pink orthoclase and microcline phenoc^rstsin^ matrix 
 throu'^hTthr^^f •'^*'' «mall crystals of green hornblende scaTteS 
 on ^enstone " Presumably the product of interaction of granite 
 
 Origin. 
 
 The granite and gneiss of the Harricanaw-Turgeon basin are believed 
 to represent immense, deep-seated batholiths which intruded into the 
 Abitibi complex after the deposition of the Harricanaw sed^nte m a^ 
 accompaniment of folding and faulting on a large scale. IMffereic^s b 
 
 trnS^?i/°"°1- ° '\'^'' ^^ °^ **»« «™°*^«- eei^ain gneisses and 
 the pegmatite, aplite, and granite dykes, are believed to have oriirinated 
 through a process of differen ation by crystallization whereas certain 
 otW local variations near the contact, chamcterized by TunTnt fSi- 
 magnesian minerals and sometimes also by a porphyritic texture, originated 
 iLnV. r'''^K**^*V°° «"><! P-^rtial assimilation of blocks of o°de? mk 
 which were broken loose and engulfed by the magma at the contact. 
 
 Age Relations, 
 
 ^ Jmtn^J*"'** *?*^ *°/'^ m' this region occur to the north and west of 
 an immense complex of similar acid plutonics, which extends along the 
 
 ;-il 
 
 -if I 
 
45 
 
 whole of the southern part of the Laurentian plateau from the gulf of St. 
 Lawrence to Georgian bay. Since these rocks constitute the bulk of the 
 Laurentide plateau the name Laurentian was given to them by Sir William 
 Logan in 1853. But the recognition of two granites of different ages in 
 the Lake Superior region suggests the possibility that elsewhere the granites 
 may be a complex of batholiths of different ages, and consequently it is 
 considered advisable to drop the term Laurentian in this district, since the 
 granites are not known to be of the age to which this name has been assigned 
 in recent classifications, i.e., younger than the volcanic greenstones and 
 older than the pre-Huronian sediments. In the Harricanaw-Turgeon 
 basin there is a granite older than the Abitibi pyroclastics and the Harrica- 
 naw conglomerate, pebbles of it being found in these rocks; but no masses 
 of it being recognized in place. The large granitic batholiths of the region 
 are younger than any of the rocks of the Abitibi complex with which they 
 come in contact, and are probably also younger than the Harricanaw sedi- 
 ments, but they are older than the diabase which is believed to be Kewee- 
 nawan in age. Their age relative to Huronian sediments is unknown 
 since these rocks do not occur in the region. 
 
 POST-BATHOLITHIC INTRUSIVES. 
 
 IiAMPBOFHYRS. 
 
 On the east shore of Rest lake, 32 chains north of the outlet, an 8-foot 
 dyke of biotite lamprophyre cuts the Abitibi quartz porphyry schist. 
 The rock is black and massive with abundant smwl biotite crystals visible 
 in a dull black matrix. Small quartz veins occur near the contact between 
 the dyke and schist and cut both rocks. One of these veins carries small 
 crystals of galena. Microscopic examination shows the dyke rock to be 
 a minette. It is porphyritic, with dominant phenocrysts of brown biotite 
 in a matrix of fine-grained biotite and mosaic quartz, together with small 
 amounts of plagioclase, orthoclase, sericite, pyrite, and iron oxide. The 
 biotite phenocrysts show numerous bands of secondary penninite parallel 
 to the cleavage; and where this mineral has formed the crystals are slightly 
 twisted and contorted. Alteration of the feldspar has given rise to calcite. 
 
 The minette has not suffered dynamic metamorphism as has the 
 surrounding quartz porphyry; the biotite shows no trace of a parallel 
 arrangement as in a schist and the deformation of the crystals is due to 
 chemical alterations within the rock itself. 
 
 Age. 
 
 If the schisting of the rocks of this region occurred at the time of the 
 granitic intrusions it is probable that this rock is younger than the granite 
 batholiths. 
 
 Minette was found only in this one outcrop in the Hamcanaw-Turgeon 
 basin, but two other occurrences are recorded 33 and 41 miles, respectively, 
 south from this occurrence, on lakes Dufresnoy and Dufault.' Mr. Wilson 
 includes these dyke rocks in the Abitibi group. 
 
 •Gaol. Surv., Caa., Mem. 3«, p. 4t. 
 
 59813— 4J 
 
m 
 
 KBWUNAWAN (?) DIABASE. 
 
 Diatribution. 
 
 The youngest coiwolidated rocks observed in the Harricanaw-Tunteon 
 basm are diabase dykes. An outcrop on Rifted hill and the two exposures 
 west of Beauchamp lake are of ohvi ae diabasn; the other seventeen observed 
 outcrops are either normal diabase or quarts diabase. A majority of the 
 dykes «« lew than 100 feet in width, though the one cutting Rifted hill is 
 
 ^Ii J^^t^lu **>^:,efP«"i"' on PluR W"" i» of even greater extent. 
 Ihe lengths of these dykes could not be determined on account of the 
 abundant drift covering. 
 
 LUhological Character. 
 
 The diabase is always fresh-looking and massive. A considerable 
 rtnge m both texture and composition is found, due to the different condi- 
 tions under which the rock soUdified and to magmatic differentiation In 
 the smaller dykes and along the chilled edges of the larger masses the rock 
 IS blMk and aphamtic, but elsewhere it is green or rusty brown and either 
 medium or coarse-grained, with a distinct ophitic structure. In the 
 
 S*^I! "^1^1^^"^ *^"."' °" 'o* ^^' ™"K« "• La Reine township, on the 
 TJS *k or\"5K«>n nver one mile above the junction of Garneau river, 
 and on the right bank of Turgeon river 3 miles below the junction of 
 IJfitour nver, a remarkable porphyritic texture was observed, phenocrvsts 
 fifeS^" plagioclase (labradorite) over half an inch in diameter being 
 embedded ma black matnx of fine-grained diabase. In the last mentioned 
 occurrence the phenocrysts are in greatest abundance near the central part 
 of the dyke and do not occur in the marginal zones for a distance of 3 or 4 
 inches from the contact. 
 
 A thin section of the coarse quartz diabase from Oditan hill was found 
 to consist of abundant laths of labradorite, augite, and a micrographic 
 mtergrowth of quartz and feldspar; accessory minerals are orthoclase 
 brown biotite, magnetite, and apatite. The rock is quite fresh-looking' 
 though some of the feldspar crystals are clouded by incipient alteration 
 The micrographic mtergrowth of quartz and feldspar was not observed 
 in shdes of finer-gramed quartz diabase, though in all other particulars 
 these thin sections conform to the above description 
 f .K^°'"*' Z^ the oli vine-free diabase appears to be lithologically similar 
 to the quartz diabase, but quartz is either lacking or so scant that it can 
 only be regarded as an accessory mineral. 
 
 The olivine diabase which occurs on the summit of Rifted hill is a 
 medium-gramed, greyish green rock locally characterized by nodular 
 prominences on the weathered surface. The nodules appear to be of the 
 same texture as the rest of the rock, but contain a greater number of 
 plagioclase crystals. Microscopic examination of this rock shows that the 
 first essential mineral to crystallize was olivine, this beinR followed bv 
 plagioclase, augite, and hypersthene successively. The olivine is in 
 irregular and roughly six-sided crystals, and is only slightly altered along 
 Its boundaries and fracture hnes to magnetite and serpentine. It is not 
 uniformly distributed, but is abundant in certain small areas. The laths 
 of labradorite are fresh and unaltered and terminate abruptly at the 
 
47 
 
 Buirgms of the olivine crystab. Augite »nd hyf^"*^'*"* J" ♦'jfj^Sl^P^ 
 ^^n the other cryttals. Accewory minerals are apatite, ilmenrte, and 
 
 auart?Md orthoclase, and orthoclaw and plagioclaae, through which run 
 uSwfkrcrvBSs of gi^een hornblende and fibrous bunches of epidote. 
 
 An ap^te of somewhat different type occurs <» dykes in the diabase 
 of Plu J hills It has the appearance of a coarse-grained gnuiite, consist ing 
 oqK white feldspar, 'hornblende, and a P«''-«-^"tX. llrt. ' 
 varies^considerably from place to place, as does also the quart.. 
 
 Structure. 
 
 All but one of the diabase outcrops appear to be dykes cutting eit! r 
 the rocks of the Abitibi complex, the rfarricanaw sediments, or the p-«na. ?. 
 In the caS of the diabase forming Plug hil s, the ^t''^™"^^"^^^ fe^I 
 comoosed of diabase and rises as somewhat conical masses for 200 feet 
 Tv^^e muskeg plain with.no known ^\--'^\r''^l^^^J^^'j^^T^ 
 that thev are eroded and glaciated volcanic necks. The trend ol the oyKes 
 diffen. in SfferS parts of the region and no general parallelism is to be 
 oS"^. Where fhe diabase intrudes ^o^f^t^d ™f ^^Ts^ ^ras S 
 the schistosity and sometimes cuts across it. The dykes, so far as couia 
 be observed, were always nearly vertical. 
 
 Metamorphism. 
 
 The diabase, as seen in the field, appears fresh and unaltered That 
 found at the contact with the older rocks is fine-grained, dense, and black 
 but so far as known its composition is not greatly different from that of 
 the ^ L a whole. The coJitact effects on the intruded rocks are usually 
 8HKht^ i^ tlTe case of intruded granite nil. The greenstone m contact 
 S the Sabase on lot 55, range VIII, Languedoc township •« altered to 
 Tdense fine-grained, black amphibolite for about an inch bordering the 
 conSc^i farther away it passes gradually into normal hornblende schist. 
 
 Origin. 
 
 The numerous small dykes of diabase of similar ^-^^f^" ^"^^'^^ 
 scattered through this and the adjoining regions suggests that these were 
 Sy the upSmost tongues from some huge deep-seated magma of basic 
 composition. 
 
 Age. 
 
 The diabase dykes are younger than any of S^^^.^^Xwrer'^tCr 
 rocks found in this region, so they are post-bathol thic. However, tneir 
 KoSc sinSarity to the Keweenawan diabase of lake Superior and the 
 abuSnt oc^urre/ee at numerous intervening points, of rocks of the same 
 
Ii 
 
 ^: ' 
 
 '. i 
 
 1 
 
 ■ 
 
 .i 
 
 48 
 
 dUbMe could beXtlnJ^hS t aie f™5:%!?«'?. ' ^^^^ »»>« diJine 
 Montmd River di8trici%SJre SnSr Si •.,»* "^Li^P!?' ^."* '» *•»« 
 diabase » younger than the Wt^dEbSS." ^ "^^"^ *''« ""^"^ 
 
 PLEISTOCENE AND RECENT. 
 
 OLAaAL. 
 
 extend cUring^o?bJul;""^^^^^^^ T, ^^^^ocene time, an 
 
 m*gularly on tfe smoSthS' Kl^^en' fl"oJr^of 'pL"^^ 
 The evidence of glaciation are plainly tisibl^Lfh'S!""''"*" ~<''"- 
 distri'it. The hills viewed fw»« 1 !? * "^''''^ >« *"« rocky parts of the 
 
 Wgher prominenS T^mu nti^fan7'.r.r°°*'''?L ^"°^«1- ^K 
 than on their northern sIodcb ffkLf ^i^"*^^'" °" **'«'• «>"*»» «de8 
 and stria, are well preSi^Xn all jKd^^n^fcJ'^l f k^ F'''"'" «^^^ 
 several feet above the present hi«rh »!*l!S i .,: ?o*-hole8 were found 
 river 14 miles belol tff ^tS^^^^^^ "ght bank of Tui^eon 
 
 ««.th W dSL"'eK« Xr^'r,' '{? ^'^^ '^'•'*"''*- 8*"« tending 
 Turgeon rivers near thShinS^nH «♦%'' °''^'°^ "» Harricanaw an! 
 river 10 miles beWii^ySa wHh P^tlTnT* "*^^ 
 mentioned locality the stri* ari 1.1^ Plamondon nver. In the last 
 heterogeneous p^MSs Jnd bolere hive" ll^"'***' J"?^ '° ^'>*<''' "^e 
 positions and evenly planatS (Plate mR^V^*^'^ '5^ contiguous 
 degrees east, occur abundantly in Si niii 2f ^Stris trending south 30 
 viously mentioned outcrop tK Sril^ / ^^a ^"l"*^* 1° 8o°>« ?«- 
 trending south 80 dS^ast THp T.» ^'°""'' J° ^ '»*«' **»an those 
 west appears to be tKfe ^ ch hw had thJtf '/'^'"«"°^'» ^0 degrees 
 topographic features of the districr n».?». *7***l* ^^!?* °" **»« ^n^r 
 south were found on the w»ste™ shorP i Ak fV""^ l'"^"*^'!?^ *'™o«t d«e 
 Wee; in both localities they cro^ the^d^r Srlt f '^.-^ *"•* °J» Makamik 
 east. ' ""^ '^°® °'a»' stnffi trendmg south 30 degrees 
 
 Boulder Clay. 
 
 all o?L'Sct°'thfdiSuS"o^^ "°^ "*''*''» '^°-" Pr-tieally 
 cannot be deterndned. The .Se/ ilVJ^PT *J??« -"^ '^^^ ^eposite 
 beleved to be boulde; day though n^t^-^ ***^ •*"'* '° **»« '^^n is 
 which possess all the nSl cEctPri«f in« T .?"*"?P« ^«« observed 
 The boulder clay arounneauchamp Takris^of f^^^^^ "^'^'^ "**"'*• 
 which occurs so abundantly in i^nthtlt* ^^*"® ^"^ *yP« «« that 
 pebbles of granite and grSstone^ i^^^™ ^.?**"°- ^""'d^"' ""d 
 yards down to a fraction ^fn^n!^*!, *^°*^ "" diameter from several 
 
49 
 
 •ubugular blocks of foamliferous limeBtone, some of Z^,t*^vi!M^ 
 in dSSeter Fowilfl from these boulders were submitted to Dr. Kindte 
 who JSSted as foUows. " The fossils present in the coUection we referred 
 to the following species: 
 
 8tr«malapora *p. 
 FatotiUt rf. ntagartntu. 
 Diamttopora tp- .. 
 
 Camantotckia e(. wAOtt. 
 Ptntamtru* cf . iMongui. 
 
 These fossils reoresent a horizon of Silurian age." 
 Throcr^nS^suggests that an outlier "^Sil^nan hmeston^^^^^ 
 found within the sheet in a northwesteriy direction from this point. The 
 outJrop of boulder clay at Pavement camp on Hamcanaw "vct, 9 mi^s 
 below its junction with Plamondon river, is remarkable in that »t shows 
 eSdence of having been overridden by an ice-sheet. Pebbles and boulders 
 yvaigSl^gnei««e8, and greenstones are closely Pa«ked and evenly 
 «i«n«i«r Wii* dav occuDies the small nterstitial spaces. In a gravel 
 S Un tot'll rLi VIL ff sLre township, boulder clay 5 feet in thickness 
 ^l^{^d\^^ngnt^ii&'^ lake clays, the contact being imguUr 
 Th^ Btratified clavs unconformably overlie a kame-like deposit of stratified 
 ^STd SSveh TlSrexposure Is of particular interest since it indicates 
 Kvtrietv of conditions which obtained at this point during successive 
 
 "*'^?n"thhln'trtf'and northern parts of the sheet the drift, is chiefly 
 unstratified Sue clay, through which boulders are sparsely and "regulariy 
 mattered This tyi of boSlder clay is such as would be formed by the 
 oIoSm UDWid reworking, by an overriding glacier, of deposits like 
 £TK5 Kke clays wSich^occur »« the south Parjcd^^^^ 
 pxnosures of this material were seen on the west shore of MistawaK laice. 
 •^A Kder clay which is believed to be of a different origin from the 
 norimilt?Se is abundantly exposed on cliff faces on Turgeon nver between 
 fheTnS of NinemileVi^e and Burnt^^^^^^ 
 
 ridge and Wawagosik rivers above their junction. A matrix of blue 
 cla? contains abundant pebbles, the ma ority of which are less than 1 
 S in diameter; about half are rounded and half angular. A suggestion 
 of sirina wTfoind in the various horizons of each exposure, explaining 
 tLaSlara^ce of stratification when viewing the deposit from a distance 
 cK Samfnation, however, shows no distinct bedding and occasional 
 uS? bouldere are found in various horizons all through the deposits, 
 m oebb eswe, for the most part, separated from each other by clay, 
 and thoS wWch are flat or elongated have their longer axes inclined at 
 various angT^anHot horizontal. This type of boulder clay is beheved 
 Shave Sn deposited in water from melting ice blocks which rafted 
 the glacial debris from the ice front. 
 
 Moraines. 
 
 A lanre moraine occurs near the north boundary of the sheet extending 
 aloneffi^n river from its junction with Harricanaw nver. approxi- 
 matelvS 80 degrees west, to Grand Bend, a distance of 22 miles. 
 HarrcaS river h^7ut through this moraine; and the large boulders. 
 
m 
 
 ■ " t. 
 
 Ml 
 
 Manyof there are overWnbrcl.vH«IwL* ?'?"°" <>' *»>« dirtrict 
 
 Fluvioglacial Depotitt. 
 
 U Sam and in Trw^tJn to^Sw'nT 'i^"*''!.'"'^ •'?t*n«ons in wwtera 
 An extensive outwaah niain «* ---^ j ^"^ ""d Trecesson townahina 
 
 /or several miles, oie from cSkob' like thiotn'/* *° .*''" ""^heK * 
 of Authier river. This deoorit iii pK ♦ • j t' '""» **»e headwaters 
 pitted with numeroiM ketKolSi m""**7'^u>?: ^ P'»'n-«ke »uK 
 '^'i*^ I", the southwestern Mrt ofTL ♦ '''"T """u**^" clear-watSJ 
 ff^ "»d free from bouldeS^^Here St,?*?r'''P' *''« 5»"'J " 8"^ 
 a forest fire has removed the v^etetl^k -n!i * ^""f* «« found where 
 w«d. The dunes are now en?f^ii£/"i {^^ *^? "."^»«' *« th^ 
 "d several dead trunks are to be see^tenfe^^^^^^^^^ 
 
 lacustrine DeposUa. 
 
 riyer^lS^tl™SS'l5fcTdS °" ■^''^ ^-''» «' Tun^eon 
 tnne deposit was found north of ConrlS^n''"" ,"''^?- ^o other W 
 ^'•y^.^^'^ observed at nuCrous locSraW th 1^™*'^,^ ^''"l^ ''"d 
 on lakes Makamik, Chikobi, and Obakki f„ 7 *''*' 1'"^ «' the railway 
 nvers and Concretion cr«ek An of 1; "I* '^ "" ^"**''" ''^d Octav^^^ 
 
 S """■" rf *"*1 ''^"'d not h« traced lati' ' T'* ''"^ ^akaJk 
 distance. In fact, the lack of contiS t ''" ""^^ considerable 
 
 in areas which show no siirn of in^Tn^ I "' stratified clay deoosita 
 
 biity in thickness of thS"de ' sUsTtrot?"^^ ' ' ''"'T"' ''"d^the S 
 a^I l«d down at the same tiSl^^ one hu/e^at:'*r*. I''** ^^^y ^^re not 
 of lakes more or less completely s^n!«t5 \ ' *»"* ^ej^an in a number 
 unmelted remnants of the Xfer Ek ''•°™, «'«<•»' other by the stfll 
 proceeded. The lake clay of ih. Za- .P"''»«Wy coalesced as meltini 
 pjibway clay, follow.^ the conceptSTii^^''**r*« ^as been TamS 
 •n a huge glacial lake, which hL^n^^^rl-.^^'P^^'* *«« 'aid down 
 ?„Th*' °' *•*>" Harricanaw re£n conS^J ?^l^T^), 7^^ 'acustrine 
 in beds rangmg from one-third of «n^^k. "'t'rf'anded sit and clav 
 thicker beds biing characSe of fh ^^ *° °?^ '"*^^ '« thickS the 
 «ejth.- pale grey'^or baS ght l^Lv *^"''"^*'^.- ^he^oloSr 
 ■A-- ....o.t.iWu,.«i«. ,«, „ Tp ^ '^'^^- ^" occasional boulder 
 
 iHS 
 
SI 
 
 of gnuiite or greenstone can be found in these deposit*. lim^ conrre- 
 tions of fantMtie shapes ocrur in all the stratified clay deposits in the 
 region, except the occurrence on the lower Turgeon river. The concrp- 
 tions are often broad and Bat, conforming to the stratification, and either 
 diseoidal or irregular in outline. The projections on the irregular varieties 
 and the growth lines frequently show a bilateral symmetry. Rosette 
 and ring-shaped forms were also found. A number of linear markings 
 occur irregularly or in Yadiating groups on the concretions of Concretion 
 creek (Plate IX). 
 
 A small, chitinous sponae spicule wa4 found in a sample of the stratified 
 clay from Concretion creek which was examined under the micn)srope. 
 Lacustrine sand deposits are intimately associated with the stratified 
 clay on Obalski lake and Octave river. The deposits consist of alternate 
 layers of nit and fine sand ranging in thickness from 1 inch to 2 inches. 
 They overlie the clay conformably in both occurrences. In all the lacus- 
 trine deposits which were examined the beds appeared to bo slightly 
 warped. This may he due to the irregularities of the surface upon which 
 they were deposited. 
 
 RBCKNT. 
 
 The solid rinks «)f the district have been only slightly eroded wnce 
 Glacial time. The most marked effect was seen on certain soft, micaceous 
 schists where about one inch of the rook has been ennled around the 
 upstanding ridges of quarts veins whose edges show glacial polish (Plate 
 VA). On the more resistant rocks and all those which have been protected 
 from weathering until recently, by the soil, the glacial markinRS are still 
 
 C reserved. The streams have cut through 40 feet of drift in some places, 
 ut usually the erosion valley is much less. It ie only where prominences 
 in the rock floor are encountered that the streiims have cut through to 
 bedrock. River deposits have built the banks of many stretches of the 
 various streams higher than the country inland. These deposits are 
 formed during the spring floods when the waters overflow their banks 
 and drop part of their load among the marginal bushes and trees. 
 

 ■ff 
 
 j" ft 
 
 I 
 
 r 
 
 i 
 
 CHAPTER V. 
 ECONOMIC GIOLOGY. 
 
 GENERAL STATEMENT. 
 
 inth .rt.,e,.. „ ...e «hertu'1^!ii!i I^^ '«»n?e interstream area 
 it in . . wi . ,, , .ecupfed b?mJki^'..? """^ H'>»"«rinK field, since 
 
 pected occur a! .., the n>Sr» and no atte»nT^''' t^""" ""*. »^" P'"- 
 
 Betw. u th. ra.nvav ind Jhe Mis a±^^ "'"•" promising, 
 
 the ruck floor is coinDosed o/ th« ^^^ batho ith the greater part of 
 hills supply a Jd frt^^ro^Utor wS K^ht n'l^h"""''??^ *'"« 
 
 map-l?eTarp;Serbr!h?7:?t^ttd 'Xe^tv'""*' - *^« 
 
 galena are known to occur wamniTthp.v;^ IT' ^'^"'copyrite, and 
 will reveal other deposits!"^?bn^o*Sr»:Sri^^^^^ 
 
 oou>. 
 
 pegm°a«t1c'q";art/ve[rw'hiS.?rL3 ^'''-"* l^P*- (^ 
 
 contact and are apparently connected with the ^^}^T,l''^" *^^ «r»nit« 
 
 a fei%ui;hS-be°ariSg%'e"„Vrwri 'a^l^lf '^fr'^'"^ '° *»>^ ^^'^ ^-^ 
 Of these, thequartz veinr/rom thH nth »^ f^^ •''°"**'"* "P^" «««ay. 
 lake, showed a trace of goldThe vein fr^^tL"' ^*'" P^insula, Chiboki 
 portage on Harricanaw'riv^r^mrrnera^hX^Tace"'!^^^^ 
 I'loX^lfi^l^-T^^ W^y. 3 mrnSe'asro'f to^rr^; 
 is found in schis ed Kute tuff S^d'^J Th?*'??"^ occurrence th;7ein 
 altered andesites-in each cL the «ant/?nnf*^*L^•*^'' ^^^ ^*''"« <^"t 
 
The topognphlo eonditiona in the HarricMiaw-Turgeon bMin are 
 pcrticularly favourable to the proipector in learch of cold depoaitt of 
 the KienawMk type. Numeroua bare hilla rise fr^m the drift-covered 
 plain in the interatream areas in the louthem half of the sheet. A majority 
 of these hills are composed either of granite near the greenstone contact, 
 or of greenstone near the granite contact. Pegmatitic quarts veins are 
 abundant in the marginal sone of the intruded areenstone— a strikin| 
 example of this being st-vn on the hills to the south and west of Chibou 
 
 l»ke. ., . .... 
 
 On the west bank of Harrieanaw nver, 14 miles in » straight line 
 below AUard portage, a rusty-weathering, grey, ferruginous dolomite was 
 found to carry fine gold and abundant fine crystals of pyrite. The whole 
 exposure is cut by a meshwork of tiny quartz veins. A sample of this 
 rock assayed .*> 86 ounces of gold to the ton, and smaller samples of the 
 same rock which did not include the quarts veinlets yielded 10, 10 
 and a trace, respectively, per ton. Chemical teste of this material revealed 
 the presence of tellurium. 
 
 The ferruginous tlolomite is an unschisted, finely crystalline rock 
 which appears io pass Krsdationally on the northern part of the outcrop, 
 into a massive quartz p«i»rphyry. The latter rock shows numerous pheno- 
 rrysts of colouriesM quartz about 1 mm. in diameter, together with a few 
 ffldspar crystals of similar dimensions scattered through a pale grey, 
 translucent matrix which -iimewhat resembles chert. A few tmy grains 
 of a substance which had the appeu.-ance of gold were seen in the matrix 
 of this rock but no gold was found when the rock was assayed. The 
 Ri Id in the ferruginous dolomite is believed to have been derived from 
 the magma which gave rise to the quartz porphyry. 
 
 The outcrop, at the time of the writer's visit, extended iS feet along 
 tilt river bank and sloped back for a height of 5 feet, aljove which it was 
 drift-covered. The trend is probably north 52 degrees west, or approxi- 
 mately the same as that of the river. No extension of the ferruuinoua 
 dolomite was found upstream, the Mietawak granitic batholith < iming 
 in at from 2 to 5 miles above the gold occurrence in a drift-covered wm tion. 
 
 On the south shore of Chikobi lake, 20 chains west of the extreme 
 east end, a large boulder was fouu'l composed of pale grey, 8ili> tfied, 
 ferruginous dolomite, through which were scattered numerous small scales 
 of bright green mica, probably fuchsite. The rij( k was rut by numerous 
 ititersecting veinlets of quarts. The surfat ■' of the l«nlder was entirely 
 coated with rust. Glacial strise near this poiir tren luth 3.5 degrees 
 east. A sample of this rock assayed a trace of )i>\d. 
 
 The ferruginous .iolomite in this reci-m is !ithoii>eically similar 
 to the rock in which gold occurs in the Lar ; r Laki Hstrii * and its asso- 
 ciation with quartz porphyry indicates that the geologital relationships 
 are similar in both localities. ReRarding the origin of he gold, Mr. 
 Wilson' says: " In the Larder Lal« dis* ct and vicinity, gold was found 
 in quartz veinlets in aplite on the k)! King claim, and in quartz por- 
 phyry on the property of the Pon lac .ind Abitihi Mining Company to 
 the northeast of lake Opasatika. G>.u\ selluride has been found associated 
 with the gold in the latter. I ^, ther. fore, possible that the gold in these 
 3t,'^kwork deposit,"* of the Ijird^r Lake district is genetically related t-o 
 
 >0«>l. SVT., Cu., Hoi. 17E. ini, ». B. 
 
54 
 
 the graniticrock. of^e^eSJ?^ ^ indirectly reUted to 
 
 thefStKX\^iSf„ot'?jStetd;S^^^ '"'^^/J "<» 
 teruticaUy found on tS bich hSk th. ^f^J2^ .P**^''^ '^ °o* charac- 
 
 of the Larder iJe tn^rSlifv S^™?!±i' '^'*^^. ^ gold deposit* 
 viously mentioned locSitv !^«K* '*'?'; ^° .*ddition to the pre- 
 found^on Authier ri^*[6 SS nS^^'f.Srf^KrK-'^f'r'** ^"^ 
 northeast shore of Rest lake" Inrf nn Vk- JTT *^'"'i*''»> hike; on the 
 Quarts porphyry, litKK«kaUv8fmiU^n^K'^***K?\^^ °' McKenxie lake, 
 river 14 and 19^l^V^Ll^/Zi^J^^ ^^'''^ °*'""? "" Harricanaw 
 river 3 and 5 miles rMSvplv"„»^^*' ^" observed on Harricanaw 
 on Burntbush riv^'l aSr? mL »^ *■ *** J""'^°'' ^'**' burgeon river; 
 of the east shorroTRU like a^d 2 «Z'l^ r"*,**!"" **•* '«"'t''«™ P^ 
 iake. No gold was fo"*nit 'anj'of SS Scrot ' '"^ *°' °' "^""^ 
 
 SILVER. 
 
 >n pegmatites and quarts veins which rnttlT-u ,'i?''' A^ "«»y»ng, 
 near their contact ^th graS 'mwS ~'''' °' **** ^'*'*'»'' «5'o«P 
 
 ship, cuTCe'^rn'tLrCne^aXl*^^ ?' ?°'^ J".'' ^ R«i°« town- 
 batholith. The Serai aL^oUfi^n' T>'* "^'^^ **>« ^Wtibi granitic 
 and fluorite. An^y onM^'Z^^'t^Z^'^''^' «Pt'Jj«rite, "Jyrite! 
 ton; go dO: lead 0-46 n^rppnt-rk-- 7^^^°^' "'ver 202 ounces per 
 Feria|d and grvifcripoSi^^rh^ 
 
 shore of Main peninsXinlJeChZbi^ftl''^ middle of the southern 
 portage on Harricanaw river and in the T-iti"^^ "'..*''^ ««^hain 
 
 from Amos. ' '" *°^ Tremblay vein 3 miles northeast 
 
 and Jt'^^uVhilirrmllS tuTS\t''fc^''''-*^^J-'^«t- - clykes. 
 probably in the form of volcanic neckl ThllTT-^ vU'*^? Junction- 
 
 COPPER. 
 
S8 
 
 intruded rock, striking east and west and dipping 30 degrees to the north, 
 parallel to the dyke. The veins carry fibrous green hornblende, pyrite, 
 and a small amount of chalcopjrrite. An assay of the vein yielded 0-60 
 per cent copper and a trace of gold. On lot 54, range VIII, Languedoc 
 township, several pegmatite dykes intrude the Abitibi green schists. At 
 the edge of one of these dykes a small amount of caleite was found carrying 
 a few grains of chalcopyrite. A small amount of chalcopyrite was observed 
 in the ellipsoidal andesite on a projecting point on the east shore of Obalski 
 lake, 1 mile northeast trqm the inlet. None of these occurrences appear 
 to have any commercial significance. 
 
 Tremblay Claim. 
 
 In August, 1915, Mr. Joseph Tremblay discovered chalcopyrite on lot 
 42, range II, Dalquier township, 3 miles northeast of the village of Amos. 
 The writer visited the claim in September of that year. This part of the 
 district is chiefly muskeg with occasioned rock hills or ridges, burnt bare, 
 rising above the general level. The claim embraces one of these ridges, 
 the trend of which is north 66 degrees west, and the copper deposit occurs 
 on its southern slope. The rock composing the ridge is a pale grey sericite 
 schist, in places finely banded with darker grey, micaceous and also siliceous 
 phases. Occasionally the appearance of an original clastic structure can 
 be seen in the rock, though fragmental and interfragmental materials 
 seem to be of the same composition. The rock is believed to be a schisted 
 rhyolite tuff, and possibly also schisted rhyolite, of the Abitibi group. 
 In the neighbourhood d! the deposit the schistosity strike of the rock is 
 north 65 degrees west; the dip approximates 90 degrees, but fluctuates 
 from north to south, indicating deformation since foliation was developed. 
 A thin section of the schist was found to consist of abundant quartz and 
 sericite and smaller atiiounts of orthoclase, albite, chlorite, a carbonate 
 (probably dolomite), and pyrite. The quarts occurs as small phenoCi j'.sts, 
 and around such crystals a mosaic of tinv quartz grains either radiates or 
 tails off in the direction of schistosity. Some of the small orthoclase 
 and albite crystals are angular. The greater part of the rock is composed 
 of an extremely fine-grained mass of quartz and sericite, the latter occur- 
 ring in radiating fibres and parallel plates. Certain areas are marked off 
 by more abundant sericite around their borders; this is the only indication, 
 observed under the microscope, of a cla.stip structure. 
 
 On the south side of the ridge three Hmall, irregular, lenticular veins 
 occur close together, all striking north 63 degrees west, and each off.set 
 to the south by a few inches, from the continuation of the neighbouring 
 vein on the ea.st. The total length of the three veins is 20 feet and their 
 maximum width is 2 feet. In the 8-foot pit which had been sunk, the 
 veins were found to pinch out at a depth of 4 feet, but another vein of 
 similar shape and dimensions to those at the surface was observed coming 
 in on the south side of the pit at a depth of 3 feet, and pitching toward 
 the north at a high angle. Running part of the distance across the west 
 wall of the pit a small fault plane filled with gouge was seen in a horizontal 
 position; the deformation in the schist indicates that the rock below the 
 fault plane moved relatively south a short di.stance. The veins and the 
 adjacent schist carry abundant chalcopyrite. The mineralized zone has 
 a maximum width of 8 feet and pinches out at the ends of the veins, giving 
 
decrem wMt TK« <!;i; *• P*** ^o- ^i » 1* leet wide und trends south 20 
 S^!^ Tk • • '°'»a*'on »° the rock was found to bend south on the welt 
 
 M* nf ♦?! T ^*'.'" canying the mineral deposit. Eeaardina the 
 
 LEAD. 
 
 in th?HSS,°'lw:n S' ?°™°"°«' inportmce m known to occur 
 
 secondary ealcite is pre^n!^'l^n^^^i;ie^Z^o::J:''^''''' '*'^' '™" "''''*«' 
 
 Tu Jon' bS T/T^lT"^'^ '"^ n «*^^^ '"'^'^''ty i» th« Harricanaw- 
 
 sSs whiS it intJuSs^' "*° °°'^ '^ "^^^^ ''^ '»*«■• ^^'^ *»»« Abitibi 
 
 Similar dykes of minette are reported to occur in the Kewagama 
 
57 
 
 sheet, 33 and 41 miles south from this occurrence,' on the peninsula which 
 projects into lake Dufresnoy and on the southwest shore of lake Dufault 
 about 100 yards north of the entrance to the lai^ west bay. 
 
 IBOK. 
 
 The possibility of iron or^ being found in the district is indicated by 
 the observed occurrence of banded iron formation, and the abundant 
 deposit of pyrite in a carbonaceous volcanic slate of the district. 
 
 Banded iron formation occurs on the south side of Authier river 
 about 10 miles northwest of lake Chikobi. The rock is composed of 
 alternate bands of magnetite and chert, the latter predominating. The 
 rock has been closely folded, the axes of the folds trending east and west. 
 Although the rock exposed at this outcrop is too lean to be of economic 
 importance, it is possible that the iron formation elsewhere in the district 
 may be of value. Localities with abnormal magnetic variations and 
 outcrops of chert which resemble the non-ferruginous part of the iron 
 formation suggest that it occurs in two narrow bands across the district, 
 one north and the other south of the Mistawak batholith. 
 
 The carbonaceous slate rock which occurs on the west shore of Rest 
 lake about 1 mile north of the outlet, carries abundant spherical or augen- 
 like masses of pyrite, partly altered to Umonite. Some of these have a 
 diameter of 10 inches, and for a width of 20 feet pyrite makes up over 50 
 per cent of the rock. 
 
 A similar rock also containing spherical nodules of pyrite, though 
 not in such large amount, occurs on the left bank of Octave river 1 mile 
 below the upper 10-chain portage. 
 
 MOLYBDENITE. 
 
 Molybdenite was observed in only one locality in the Harricanaw- 
 Turgeon basin, namely, on the southern slope of PLamondon hill. A few 
 scales of the mineral were found in a small pegmatite dyke which cuts the 
 hornblende schist of the Abitibi group, a few hundred yards north from 
 the granite contact. 
 
 Workable deposits of molybdenite occur in the vicinity of Kewagama 
 lake, a few miles to the south of the map-area. The mineral is found 
 irregularly distributed through pegmatite veins near the contact of granite 
 batholiths or apophyses with the older rock. 
 
 ASBESTOS. 
 
 Small veins of stiff-fibred asbestos occur in the greenstones on the 
 shores of lake Obalski. On a projecting point on the east shore, 50 chains 
 northeast of the entrance of Harricanaw river, asbestos was observed in 
 fibres less than half an inch long; a similar occurrence was found in the 
 ellipsoidal andesite on the west she re about 1 mile north of the entrance 
 of Harricanaw river. The rock in which the asbestos was observed is 
 not a peridotite. 
 
 Mr. Bancroft's report' refers to other occurrences in this neighbour- 
 
 iwibM, M. E.. Gcol. Sanr., Cka., Hem. 3*. p. 4t. 
 
 '"Miaiai opemtiow ia the proTiae* ol Quabee", 19I>, pp. lM-157. 
 
M «o,rt& ^5" P?™*?**** ''«• obnerved to be pr«wnt within the 
 £kf «?^^*'^T\i°' ^^* "**: <^ *^« eastern shore of ObdiSd 
 Ijto at a point about H mi es north of the entrance of the Harriomaw 
 ^tinkyZT^"^^ of peridotite i. traversed by a few in*guUr veK 
 2^'iSrl w***^ Z^ °°. economic value, possessing a mSrimum "dS 
 1 W *^ JJ"^^**' ^° "^P**"* "^ similw^k is rep^ M S 
 on a hill a short distaBce north of the railway line 7 miles eMtTtheSl- 
 
 SuX"J?nSiriSSh"5'^'^ ^^--^ °' "^- nottfe^d^' 
 
 been «IlirlS fn*^'?? °- *•** ^^*'»''' ^« '^"t™* »° Peridotites have 
 
 liE?v7C^v l^iS^T"*^"^'*?*"" *^'°' *°'* '* « °o* considered 
 iiKeiy that any deposits of asbestos of economic importance will be found 
 
 CXAT. 
 
 H-~J?.f government railway crones an extensive clay aone. The chiv 
 deposits constitute the most valuable as well as the most immXte^v 
 JSid'bv'lhe^^ilw **■* Harriraw district. The landdSg StJ^iS 
 Sf^ZU J" "7^ " 'J^'^^y ^"^ *»•'«» "P 'or farms Tn accountof 
 The Zw S advantages of transportation facilities and natural draina^ 
 
 take, and the valleys of La Sarre and Okikodosik rivers near the railwav 
 are composed of clay land suitable for farming, as also are the natuS 
 drained lands .a;ound Makamik and Robertson lak« Bouffir da J 
 occurs m the vicinity of Beauchamp lake, where Spirit LkkelnteramerA 
 ^^IrffnH^*?"'**^^'^''** much work is nefesiiry in the remoS of bSiweS 
 
 rj^eKa^ftSLteai?^ ''' ^* agriculturalt^dsTSh'-wS: 
 tk.i.^lf-'' *?»"" '!' «!'« H«iTlci.iuiw.Tuijeoi, bwin, in addition to 
 
 The stratified clays of the district represent boulder clay which has 
 ^n transported bv streams or currents and deposited in a huge lake w 
 
 Tf holLS''f'''""ii."°7''^ **^« '^°° ^^ *^« t™« of the retrfat of one 
 of the ice-sheets. The clay now exposed on the northern oart of Tunrpnn 
 river often contains pebbles of boufder clay and smdlS^Snte oMW 
 stone and other rocks. This clay is unsuitable for comSaf purpo"^ 
 a.s the hme pebbles burn to quickUme. In many of the stratified cU^ 
 concretions of claystone are abundant. Such deposits are of nTcommeroUi 
 use under present conditions, since the concretionrnecessitat^ either 
 screening or crushing. Some of the stratified cUys contarrch tery tw' 
 Seir shrink^:* *'"' ''°"'' °"*^ *" "^^^ '' "^^'"^ with "sand t^dut 
 
 railway IL^^^riof^iLra^^^^^^^^^^ 
 
 " " Smerr '■ ''"'^' %\Y r^'r ^^^^^' -^Ss'jrolCf""^'- 
 Spec men from range VII, U Sarre township U miles west of fh» 
 La Sarre nyer and f of a mile north of the railway. Brownfehnii 
 calcareous clay, evidently from the surface of deposit.^as it ap^aw to £ 
 
WMtthered and leached. It is smooth and exceedingly plastic wh«tt wet. 
 It bums to a*deep red colour and dense hard body. 
 
 " Specimen from left bank of Octave river 4 miles above the junction 
 <rf Concretion creek. - 
 
 " Light grey, silty, calcareous clay, stratified and laminated with 
 whitish silt films. It is granular in texture and fairly plastic when wet. 
 It burns to a porous light red coloured body, suitable for common bricks. 
 The shrinkages are low. 
 
 " Specimen from east shore of Obalski lake 1| miles southeast of the 
 outlet, lower beds. 
 
 " Stratified grey clay, interlaminated with thin layers of silt, the clay 
 bands being about twice the thickness of the silt layers. It is slightly 
 calcareous. This material is very plastic and smooth, but works easily, 
 not being too stiff when wet. It burns to a light red, fairly hard body. 
 
 " Specimen from the upper beds of the deposit on lake Obalski, same 
 locality as the above. 
 
 " Light grey, non-calcareous, stratified clay, very plastic and smooth 
 when wet. It burns to a good red colour and dense, hard body, but the 
 shrinkages are a little too great. 
 
 " This clay and the lower part of it (the previously mentioned speci- 
 men) are suitable for the manufacture of common building-brick and 
 field drain tile. The addition of some sand, say 20 per cent, would lower 
 the shrinkage and improve the working and drying qualities." 
 
 59813-^ 
 
 •ikia^b 
 
APPENDIX. 
 
 KIENAWISIK GOLD DISTRICT. 
 
 QKNCKAL STATCMUrr. 
 
 same year numeroua cam^ were locIiJSin th?-' v" • •? *'»«»"*'"»'» of the 
 tion direrted toward the ^nZ^^n^e^on "^^ "** «*"*'^ •"•'°- 
 
 P««" 2. O^toUd .ketch mw of Ki^^ridk gobl di 
 
 diatrict. 
 
ei 
 
 Toward the oIom <rf the field aeawm of 1915 the writer spent • week in 
 enmining the rocks along the uppw Harricanaw river and certain cokl 
 claims m the vicinity of De Montigny lake, in the hope of being able to 
 direct the attention of proepectors to particular areas in the Harricanaw- 
 lurgeon sheet where similar geological conditions might be encountered. 
 The excellent report of Mr, J. A. Bancroft, which appears in the "Report 
 on imnmg operations in Quebec for 1912" is summarised and given here, 
 together with observations on the progress which has been made since 1912. 
 A geolopcal sketch map has been made from notes taken by the writer 
 (rigure 2). 
 
 LOCATION AND TRANSPORTATION. 
 
 The upper Harricanaw river is a quiet stretch of navigable water, with 
 several lake expansions, which extends 42 miles south of the National 
 iranscontmental Railway crossing, 141 mUes east of Cochrane. This part 
 of northwestern Quebec has been subdivided and the townships through 
 which the waters flow are Desroberts, Dubuisson, Varsan, Malartie, La 
 Motte, and Figuery. All the gold discoveries are located in the township 
 of Dubuisson near the shores of Lemoine and De Montigny lakes. 
 
 Transportation facilities are exceptionally good. The whole distance 
 from the railway to the head of lake Mourier, about 60 miles by water, is 
 navigable by gasohne launch. The town of Amos, situated on the railway 
 at the Hamcaiww River crossing, has grown very rapidly in the past few 
 dS" t '"''P "^y ^ obtained there by parties wishing to visit the 
 
 GENERAL GEOLOOT. 
 
 General Statement. 
 
 „ . ^' *^« district along Harricanaw river between the railway and the 
 Height of Land is underpin by Pre-Cambrian rocks. The majority belong 
 to the Abitibi comp ex. Through these appear intrusive masses of granitic 
 rocKs, the larger isolated masses occurring in the vicinity of lake Okikeska. 
 n? «ranite near the Height of Land is part of an enormous granitic complex 
 which extends far to the south. 
 
 Table of Formations. 
 
 In the following table of formations the rocks of the district are arranged 
 m order of age, the youngest first. * 
 
 Quatenuuy 
 
 Oreat wteotrformilif 
 Keweeiuiwan (?) diabase. 
 
 Intrurive eontaet 
 Laurentian (?) (Batholithic intrusions of granite gneiss). 
 _ IiUrutive contact 
 
 Abitibi iptmp (Volcanic complex). 
 
 (finded schist complex). 
 
 Banded Schist Complex. 
 
 K ik!Pl.*^^M'' °f "^^ ^^^'^^ ^'^ *^° designated by the name Pontiac 
 by M. E. Wilson' outcrops continuously for 11 miles along Lemoine lake 
 and for 3 miles below lake Okikeska. -a »* uuie imb 
 
 ■Osol. Burr., Om.. Sam. Rapt.. If II, p. Vt. 
 
 69813—6 
 
09 
 
 I- jI^^***^ "",'•'"* •!??P'*f " l^'^^y compoMd of qiMTti-biotite schiatR 
 In difltinct bands from 3 feet in thickness down to a fraction of an inch, 
 m Mine places the Unding appears to be due to a slight change in texture 
 n the biotite schists, but more frequently it is due to a iMerence in mineralo- 
 logica composition, the darker bands havinc more biotite (and sometimes 
 Hornblende) whereas the lighter bands contain more quarts. Thin sections 
 are composed chiefly of quarts, biotite, and hornblende, with a few small 
 pains of magnetite and pyrite. Biotite is much more abundant than 
 Hornblende, very often being present to the exclusion of the latter, Pleo- 
 chroic haloes are commonly seen in the biotite sections. Some of the 
 bands contain grains of plagioclase and orthoclase. In all the specimens 
 examined the grams of quarts, and feldspar crystals if present, are of about 
 the same sue, forming a mosaic within which the biotite and hornblende 
 crystals are arranged with their longer dimensions parallel to each other, 
 in one of the beds on the northwest shore of Lemoine lake, about 2\ miles 
 below Its inlet, a stronK development of characteristically twinned stauro- 
 nte crjrBtiUs occurs in the biotite schist. 
 
 On Fire Rangers point, on the southeast shore of Lemoine lake a few 
 disconnected lenies of pale biotite schist were observed in the darker biotite 
 Bcbist. These lenses were not in exact alignment with each other and their 
 longer axes made a small angle with the schistosity. 
 
 All of the rocks in the banded schist complex are highly metamorphosed 
 recrystallization being their characteristic feature. 
 
 The schistosity strike of the banded schists on Lemoine lake varies 
 from south 30 degrees east to east and west. The schistosity dip varies 
 from 25 degrees to 80 degrees northeast. The banding conforms to the 
 schistosity. Dykes and small irregular masses of granite, granodiorite. 
 and diorite intrude the schists in many localities and quarts veins and 
 stringers are particulariy abundant. At several localities the quarts 
 stringers were observed to be contorted as if tightly folded, the amplitude 
 being only a fer- inches in a fold several feet long. 
 
 The contact of the banded schists with the granite shows that the 
 granite IS intrusive, and from the coarser grain of the schissts near the con- 
 tact it 18 evident that intrusion caused or assisted the recrystallization of 
 * *k Vu^ ?chi8ts. The contact of the banded schists with the volcanics 
 of the Abitibi complex is exposed on the narrows between Lemoine and 
 Ue Montigny lakes, opposite the mouth of Thompson river. Here the 
 rocks of the schist complex are beautifully banded, but the normal biotite 
 schist only occurs in a few bands, the material bet\,een being a dense black 
 rock in which no minerals can be determined. Approaching the green- 
 stone the dark bands become wider and wider and one of the bands was 
 Identified as ,• normal andesitic lava. Beyond this point, passing to the 
 north, the rocks are volcanics in which no banding occurs. 
 
 In Dr. Bancroft's report, t! ese- ba«ded schists are referred to as 
 altered sediments— conglomerates and arkoses. He also notes certain 
 amphibolite bands which may represent altered volcanic tuffs. His 
 evidences of sedimentary origin found on the upper Ha anaw are the 
 banding of the rocks and the presence of staurolite crysta. one locality 
 also when the contact between the greenstones and the ists is traced 
 toward the northwest, i.e., along the strike of the banded s^uists, a series 
 of highly metamorphosed but undoubted sediments are encountered and 
 
6S 
 
 when these sediments are followed acroM their strike toward the granite on 
 the Houth, there appears to be a gradational change into the bunded srhiatM. 
 tu *", "P'**" o' '•>«»*' '»c*". the writer is not convinced that the wide \>eh 
 of banded schwts which appear on lake Lemoine is for the miwt part altered 
 sediments. Lithologically similar rocks in the Harricanaw-Turgeon basin 
 appear to »)e metamorphosed waterlain tuff* (see page 27). 
 
 The assumption that the banded mica schists and the associated nor- 
 mal sediments belong to the same series (Pontiac) presents a baffling 
 structural problem. The banded mica schists dip toward the north, and 
 apparently underlie the greenstone, whereas, the normal sediments, which 
 occur south of lake Kewagama and in line with the strike of the banded 
 schists, stratigraphically overlie the greenstones, as mav l)e inferred from 
 the variety of greenstone pebbles in the conglomerate member. This 
 suggests to the writer that the mica schists and the normal sediments are 
 two distinct series of quite different age. The normal sediments are 
 regarded as a series younger than the Abitibi volcanics; and the banded 
 mica schists are regarded as a series older than the Abitibi volcanics under 
 which they appear to dip, and consequently much older than the associated 
 normal sediments. On the geological map' it is to be ol)8erved that the 
 Fontiac sediments occupy a narrow belt between the banded mica schists 
 and the Abitibi volcanics. By following the structural trend of these 
 toward the west one encounters the Cobalt series, which, for several miles, 
 also occupies a narrow belt between the banded mica schists and the 
 Abitibi volcanics. By following the structural trend of the Pontiac sedi- 
 ments toward the east, a point north of Lemoine lake is reached where 
 banded mica schists lie adjacent to the Abitibi volcanics, an<l in this 
 lm;ality there is no conglomerate nor recognisable normal sediment. To 
 the writer this evidence does not imply a correlation iMween the latter 
 two fecries any more than it does between the Pontiac sediment.s and the 
 Cobalt series. The lithological character and the data regarding age are 
 distinct and different between the mica schists and the Pontiac sediments 
 just as they are between the Pontiac sediments and the Cobalt series, and 
 there is no reason for regarding either of the three as other than a distinct 
 series of different geological age from the others. Hence, the a.ssociation 
 of the younger Pontiac sediments with the banded mica schists does not 
 influence in any way conjectures as to the origin of the latter. 
 
 The banding of these rocks is of no diagnostic significance, because the 
 tuffs, if deposited under water, would be in layers similar to sediments. 
 
 tuffs of the adjacent district to the north are characteristically banded. 
 
 The abundance of ferromagnesian minerals and feldspars in the schists 
 accords mineralogically with what would be expected in the recrystallization 
 of tuffs. The same composition might also be obtained by the recrystalliza- 
 tion of arkose and slate rocks, but certainly not from well-assorted siliceous 
 sediments. 
 
 The presence of staurolite in the micaceous schist is taken by some 
 geologists to indicate the original sedimentary character of the rock. But 
 there is no reason why staurolite might not be formed by the recrystalli- 
 zation of an Igneous or pyroclastic rock if its chemical composition were 
 suitab le. Staurolite has been reported in a metamorphosed igneous rock.* 
 
 ■Knraauna. Geo!. Sarv., Cm., Mas W A 
 'US. Or>I. Surv., Bttll. Ml, IIM, p. H. 
 
 59813— «} 
 
64 
 
 The itrot^rat doubt aa to the Mduuentary origin <rf thaw banded 
 
 ""^^ ^fr^ '" *•»• '"'•^ <^ *•»• *•'**«' •'y *•»* ««trirt«d diatribution of • 
 •eriet wWch, aceordinf to M. E. Wilson, ha« a thicknew of 37,000 feet.' 
 A seriea of such dimenaions, folded, with east and wett axes, if it had the 
 noraial uniformity of thickness of sediments should be found in the area 
 to the north ot the railway, i^ereas only one small outcrop of undoubted 
 ■edunentary rocks is found there and this may very well correspond to the 
 Mrrow band of undoubted sedimentary rockH found just south of bke 
 Kewagama. If, on the other hand, these rocks represent tuffs counter- 
 parts mteht be found in the Harricanaw-Turgeon basin, but in no such 
 well-marked broad band. A difference in continuity of area and diHtribu- 
 tion might well be expected between sediments and waterlain tuffs, even (rf 
 the same texture, as sediments are supplied in the upper portions of the 
 water body whereas the debris from submarine volcanoes is supplied from 
 the floor. In the case of sediments, they are spread out from a shore-line 
 and subjected to the distributing influence of waves and currents which are 
 at a maximum at the surface, whereaa the submarine volcanic ejects may 
 be given out at such a depth as to escape this distributing action and may 
 eyen be piled up in a conical manner. 
 
 rwL- J*i'' ''*'''*^*** **>** *he Pontiac schists on Lemoine lake and below lake 
 Okikeska represent a series of highly altered volcanic tuffs and some lava 
 Hows in which younger infolded sediments may occur (but which were not 
 observed), the tuffs being older than the volcanic complex to the north, 
 but belonging to the same great period of igneous activity. 
 
 Abitibi Voleanic Complex. 
 
 The greenstones of the Abitibi Volcanic complex are the most abundant 
 rocks in the upper Harricanaw basin and underlie the whole area north from 
 lake Lemome to the railway except for thr belt of banded mica schists 
 * *Jjf. granite batholith in the neighbourhood of lake Okikeska. 
 
 This group, which has been referred to as the Keewatin by Bancroft, 
 consists of numerous types of extrusive and intrusive rocks all more or less 
 metamorphosed. The most abundant type is an ellipsoidal andesite. 
 Other lavas occur having various compositions ranging from rhyolites to 
 basalts. These rocks have been altered in some localities to sericite, chlo- 
 rite, and hornblende schists. Intrusions of peridotites, hornblendites, 
 diabase, diorite, porphyrites, and quarts porphyry have cut the lavas. 
 
 Near the granite contacts, the Abitibi volcanics are usually altered into 
 a hornblende or chlorite schist, but where the granite mass is small, very 
 little change appears to have taken place in the greenstones. 
 
 The whole of the Abitibi complex appears to be highly folded, but in 
 most of the exposures no information as to the amount of deformation can 
 be gleaned. At the contact between the greenstones and the Pontiac 
 schists at the north end of Lemoine lake, certain layers of greenstone appear 
 conformably interlayered with the micaceous schist, the dip being about 
 86 degrees to the north. 
 
 Aside from the conclusion that the abundant ellipsoidal andesites in the 
 distnct represent the outpouring of ancient submarine volcanoes, little is 
 known as to conditions under which the volcanic complex originated. The 
 
 'Ibid. p. 7*. 
 
 SSH 
 
66 
 
 Mquence of extruaion of the various rock typn htm not be«n worked out 
 Mtbfactorily u yet. The writer luut observed that in general the baaic 
 rockf are more hiphly altered than the acidic volcanim, but, upon ron- 
 flidering their r<>lative reaistanee to Dtetamorphic influences, would hesitate 
 to use this fact as a criterion of age. 
 
 (iranite and Gfuiu. 
 
 Batholithic masses uf granite and gneiss, together with their different- 
 iates and assimilation produrts, are irregularly distributed in the upper 
 Harricanaw basin in masses of variable site, the largest orourring on lake 
 Mourier at the extreme south of the district and around lake Okikeska. 
 
 The rocks are chiefly biotite granites. Near the bordnrM uf the intru- 
 sions, hornblende granite, granodiorites, diorites, and hornblendites are 
 common, together with pegmatitic phases of the granite. 
 
 Keweenawan (?) Diabane, 
 
 Small dykes of diabase are said to occur at the following localities: on 
 a small island three-quarters of a mile north of La Motte lake, crossing the 
 southern boundary of lot 45, range VI, La Motte township; about 200 
 yards west from the discovery post on Smith's vein (property of Ed. 
 Carriere) southeast of De Montigny lake, also on the adjoining claim to 
 the east; and on range VI, Dubuisson township, just west of Lemoine lake. 
 The diabase has not been dynamically metamorphosed and haa not been 
 weathered to nearly the same e](tent as the rocks of the Abitibi complex. 
 So far as knowti it is the youngest consolidated rock found in the upper 
 Harricanaw basin. 
 
 No veins or minerals of economic importance have been reported in 
 connexion with these diabase dykes. 
 
 Quaternary. 
 
 Unconsolidated glacial deposits form a mantle of variable thicknesa, 
 over the irregular, scoured rock surface. These deposits consist of boulder 
 clay, sand, boulders, and bedded lake clays, the lutter being the most 
 prominent of the series. 
 
 ECONOMIC OEOLOGT. 
 
 Gold. 
 
 General Character of Deposits. Native gold occurs in a restricted area 
 in the central part of Dubuisson township, and since the majority of the 
 claims are close to lake De Montigny (previously called Kienawisik) the 
 camp is known as the Kienawisik Gold camp. 
 
 The gold occurs in quartz and pegmatite veins which in places contain 
 tourmaline, pyrite, chalcopyrite, calcite, galena, and sphalerite; tourmaline 
 is by far the most abundant and widespread. The veins are narrow and 
 lenticular as a rule, and occur either individually, or as stockworks. They 
 occur in the metanaorphosed volcanics of the Abitibi complex, and in an 
 intrusive granodiorite or granodiorite porphyry representing an apophysial 
 
l^'?!*??.'""" *!l- ff*"?*'' »>«tJK>Ihb to the MMith. When" the vehu .re 
 not m the gmnodwrite intrusive, thin rock occtim newby (loW T^^^i 
 
 rtr^^"iis!r •" *'• '"^ ^"^ °' "> "^^^ whSr.'2:iocift;"ve!S 
 
 »-j«ft!IS^* "^^f** ^*^- . ^"*" *•>• aiModBtion of the quarti urn] neniAtite 
 jS^S?i t^oi™ u"^ P^' *!i'' *'^ Kr»«odiorite intJiSon. aiffSTtK 
 prwence of tourmaline in the vein* a mineral charaeteriHticBlly iL»ocbt«I 
 
 Si£SrSl?e;"15^i''S;^'* ^ ^onrluded that the vHn. we/e^'ZS b? 
 ^JS^!«.T!!!!li*'r?.^ ''""; *•" jp-anodiorite intnuiive*. That thei^* 
 
 fa "t*r. Kr Ji* i'SIn* *'"ir ': '^L'l*^*-'^^ ''y *»'- '-"^ that ZlJ 
 IL. If 'Li «««• Bet, as Men on the Le B anr property. Pro»)ablv both 
 net* of veinH oriKimited from the same masma The winTtiow «vn««!^ 
 
 •uperrtructure which at one time overlay the plutS^ intru"iv« hIvrM 
 
 t^EVcSn'of^E&v uw^Tk'"'* '''^''^ ^^ in"U";Eo!;ic:'r; 
 
 th. S*i„ i^.^ Montifny lake there appear to »>e m«ire quartz veins in 
 
 irth'r:iX:?ii?o;!te Eiss^^V^^^ 
 
 mapM%7Abitr':i*i'irlt"" ?•' '^^ ^ ^^«"»'«"y »«ke have »,een 
 I!!, ^r u II ' ^o'<^"n>c8, the only exposure of Kranite beinir Mhown 
 
 U wlw j"J'I!l" fTf^'^y-. if thi. area were niappS^Cn a Ur^r S 
 U would be seen tha xranite is much more widesprekd than exKa inam 
 would indicate, for it occurs on all the propertiw which we^e«m?3 
 
 ^tttnVitldt'dfcr%t^" thCt Slppingof a ZV^ luZ^ 
 c?ay L ^rXral in fhf £;j The overburden of glacial clay and boulder 
 
 of J^^ Tf ?• * ''^^•'••Ption of properties exami^ in 7he autumn 
 work h»H ii!!''"i'°" '^'^ especially given to those on which develop n«,t 
 work had lieen done since Mr. Bancroft's visit in 1912. "«-^i •«?"»«'« 
 
 Protpeets. 
 
 Th« i"/*V'*k"°''" ^^'"^ "^ '°<^**<^<' on a 'ow, rocky hill near the shore 
 
 Thil^^ f'"''*!?^ " ™'""«' drift-covered land, heavily foi^sted 
 irregSr ^L?Krn'» T 'T"*'1'T*^ '^'''••'' ''"''"^" BeverSTenS and 
 AWtS? vSJScs ^?v^Zf '"''"'* •:?P'^.«-nting fragments of the older, 
 
due to the pmenetf of plaipui-laae pheiMxryata, i* quite common. - A 
 gneiwoid ^trurtuR* can be dwtinKuishcd iti a few localitiea on this pro|M>rty, 
 being ntuMt pronounced ne«r the hornbt«>nde schist iuclusionii towuti the 
 south. 
 
 In the hand spmimen, the ra«k appears to h«> weathered. The 
 felcbpar crystals and qiiarti, when present, are the onl^v easily recognisable 
 crystals, theniaterial Itetween these being a greenish-grey complex of 
 secondary minerala. Tnder the microscope the rock is seen to consist 
 chiefly of plagioclase, chlorite, tremolttc, and calcite, with smaller amounts 
 of orthoclase, quarts, sericite. and a few grains of magnetite, sircon, and 
 apatite; of thetie, chbrite, treinoiite. calcite, and sericite are secondary. 
 The fcUspar crystals, although still n'cognizable as albite-oligoclase, have 
 f)een largely altered to a felt of sericite crystals. Mr. Bancroft mentions 
 the presence of sphene in the typical granodiorite, but this mineral waa 
 not observed in thin sections of rock from the Rullivan property. 
 
 Numerous faults were observed in connexion with the veins, the 
 direction of rock movement lieing recorded in striations on the slicken- 
 Hide*i rock material and in fructuro cleavage. In the northern and central 
 parts of the outcrop it was olwerved that the southern part of the rock 
 mass moved upward ami to the east relative to the northern pvt. 
 
 In the sheare<i gnmodiorite near the vein containing the original 
 discovery of gold and if the granodinrite ndjsicent to the central part 
 of the vein No. 4, hugt cuIm - of pvritc occur m-s iw'condary replacements, 
 sometimes enclosing u con*.!., ruble Hinouiit <jf the rock material. The 
 largest culw observed moatdircd 2 inthcn on tlio edge. Mr. Bancroft 
 reports that two such cryxtiilo IVoiii this lorality assayed S33 per ton in 
 gold. The writer examineti oti<' cube in tbiii neVtion and observed small 
 amounts of native gold iU/B few cleiivagc cracks m the pyritc and at the 
 contact lietween an irreguUr inclusion of feldspar and the enclosing 
 pyrite. 
 
 Ten veins are now uncovered on this property, and in all of thene 
 gold has been found. There are also numerous, small, irregular itringer^ 
 of quartz. All of the viins are lenticular, though some are drawn .1 • 
 to a greater extent than others. It is commonly found that after . •\<;-^ 
 has pinched out another occurs along its strike. Thus the vein :" w^ ! 
 the original discovery was made is a lens with a length of ab< .. ;i ■ ' 
 only, but similar lenses occur beyond more or less continuously . .• 7\»^ 
 feet. Three such veins can be trace<i for over 300 feet; the uti.i;- u- 
 either covered by drift or arc too irregular to follow over any cousidi 1 nl !e 
 distance. The width of the veins usually ranges from 2 feet to more 
 stringers, though vein No. 4 in one place is slightly over 3 feet. 
 
 The main veins strike slightly north of east; the smaller veins and 
 stringers of quarts strike in various directions, though the majority trend 
 northeast and southwest. In a majority the dip varies from vertical 
 to a steep inclination to the south, though at the original discovery the 
 dip is toward the north. Faulting has taken place along some of the 
 veins and in vein No. 4 a pegmatite has been brecciated, the interstices 
 between the fragments being filled with quartz and tourmaline. A fault 
 not marked by vein material was observed on the side of the hill cutting 
 across vein No. 1, but no evidence of lateral displacement was ubsi-rvcd. 
 
vSn.^h«^?i i Abtibi volcaniM are more abundant near the main 
 hS^J. ^k!^*'!*'^ " *i*" B^nod'orite- It u mippowd that the horn- 
 
 ^1 Si°° °'f P«T8» >° ^hich the vein material Wlld L de^SS 
 u X . .,^®*?* "^ 'o' *••« ™o»t part composed of white alamv omH. 
 but locally the presence of large fSdspar c^b shows thS^lS'c 
 nature. Tourmaline in black fibrous bunch^ is common btEWti^ 
 
 SthT ''tor/" *?? •^'^Ti* °' ^T No- 4. the vein^aj;,riil iJffik' 
 r fKi; .f^^ of native gold occur both in the pure white quarts and 
 m that carrymg abundant tourmaline. The veins .also include pyrite 
 
 S^^^er-J^ifi'Su'nl^ ""' -^^^y^^-^^' •" except Ihe ^ 
 
 1 noJrth!!*'"* °* ?°].^ ^"""'^ '" *" *^*™8e 8»™Ple taken across vein No. 
 L^^n AnT"*' '^^^'T^' ««" '<""><« by Mr. Bancroft to be $15& 
 Sf t£ ;hln^L*'^*!;'^.^'^P'*/S''?" ^*'° No. 4 and even including some 
 nf 2L. "^ 'i^n-' "^y^ ^-.^2 ounces of «old to the ton and I trace 
 of silver. Mr. Sulbvan states that the average value of goldin all the 
 Z^XZ S' P'oP^rty was apprexmiately $33 per ton. 'coun^rj rojk 
 near vein No. 1, assayed by Mr. Bancroft, did not yield a trace of ioldL 
 
 hnA^Llr"* P^Pf^y the gold-bearing veins appear in the granodiorite 
 body near its contact with greenstone. It is e^dent that thiy are near 
 
 S^. ^^^"^ *"1'* .'•" *>"i*« ?''»'?*"« *•"** *»>« values indicates iTthS^ 
 ^S hSrri„t"v'"''"'**i.°V' '''^"*- " i° ^ ^^'P**'*^' *t 8«»ter depth in til 
 Jropertf ™ "*'''"'■ "* **** "'*""**^ ^*''*'''' "^'"» in adjoining 
 
 the if.th «^ ^IV^'aJ^^- ^ ,®l*"? property includes the_peninsuU at 
 .? fn^ th» ™1* ^^°"u*"y. 'ake just west of the inlet. The peninsuU 
 ?«.„ j« fii""'*!^*'^ *"?*• ?"•* '^•e'cy, but the overburden of clayTso 
 J^'^h^in'^n' ^f^P* the north face, that comparatively little rock 
 can be seen. Development has consisted in folloWSg back a multSe 
 
 2S5?r pirt" ^'''^ °" "°'^'' '*** """^ •" "^^^^ *^-'«°* «h»ft o"?S 
 
 t« thl'^AK^K; " •"'bu'ted andesite, both simple and elUpeoidal, belonging 
 fVitn 7n i^P**'^;u ^^ 8fhi8t08ity strike is north 36 decrees *^t, 
 the dip 70 degrees to the southwest. A dyke of granodiorite Dornhwv 
 amilar to the mtrusive on the SulUvan projsrty, with awidth oWfi' 
 cute the schist about 60 feet southwest of the vein. This dyke was o3y 
 
 STnTrir ••'" ^^1 ?••*"*• ''"* •* » ""PPO*^ to parallel the^w hS5>ri?/ 
 No quarts veins or stringers were observed in it, but since the gold-b^Sne 
 rSpntIf ^''.'^ the southwest, it probably piUses into the '^nSS 
 at depth. It was also observed that the quarts vein on being follow^ 
 
 tLt ft n°!iJr'- ^'K* ^''T'^ *?« west after leaving the shore, fuS^tTS 
 that it might join the dyke under the lake. »M««wug 
 
 to J^o JZiS composite. On the north face of the peninsula it is seen 
 1?™^* ^T^ "^ numerous nearly parallel quarts stringers, making an 
 almost solid mass of quarts for a width of 15 feet. These veins we rf 
 
 tllfEioX' v°- *^? ''^^^^yot the greenstone flows „ound some rf 
 the lenticular veins indicating that some of the deformation took place 
 sISt andTh^ Tf Present while later quart, veim. cut across bJthJhe 
 rfTLn^ln» , k'J """T "1 r *"u*"«l«»- There are several small blocks 
 of greenbione schist enclosed by the vein material, giving the appearance 
 
0» 
 
 of a breccia in some places. To the southeast, the vein is irregularly 
 lenticular, pinching out, then widening again. At a point where it is 
 about 3 feet wide, a 7*foot pit has been sunk. Specimens of free gold have 
 been collected in the quarts in this locality. No evidence was gathered 
 indicating whether the gold occurs in both or only in the «. ^er set (A veins; 
 but both appear to be rather pure quarts veins. Near the shaft only one 
 vein was observed; this evidently belonged to the older series. 
 
 The mineral association in the Le Blanc veins is very simple, so far 
 as known; pyrite is the only metallic mineral which occurs along with the 
 gold. A sample veighing two pounds 4 ounces, taken by the writer 
 across the vein at the bottom of the pit, assayed 0*80 ounces of gold to 
 the ton. Other assays made by the owner in the wider composite vein 
 are said to have yielded higher values. 
 
 Gale Claim. This claim, previou<)ly known as the Callinan property, 
 is situated on the east side of Harricanaw river one mile south of De 
 Montigny lake. The rock surface here is low-lying with many small 
 irregularities. Except for a few rocky prominences, the whole claim was 
 drift-covered. A considerable amount of work has been done in stripping 
 and several veins have been exposed. 
 
 An ellipsoidal andesite, with abundant amygdules at the borders of 
 the ellipses, is intruded by two dykes of porphyritic granodiorite. The 
 ellipsoidal andesite in this locality is remarkable in that it has not suffered 
 dynamic or contact metamorphism except for a distance of a few inches 
 from the actual contact of the granodiorite. The ellipsoids are composed 
 of a light, greenish ^;rey rock containing quarti amygdules; a dark material 
 composed of chlorite, calcite, and quarts fills the interspaces. The dykes 
 are composed of a massive dark porphyritic granodiorite with rounded or 
 subangular phenocrysts of white plagioclase in a dark matrix of very fine- 
 grained hornblende, plagioclase, and quarts. The contact of one dyke 
 with the greenstone runs north 70 degrees west; the other, to the south, 
 is south 52 d^rees west, sun<»ting that they intersect at an acute angle 
 toward the east. Stripping nas not exposed this supposed junction point, 
 nor the total width of either dyke. The lack of metamorphic phenomena 
 in the greenstone suggests that the dykes are narrow. The dyke to the 
 north appears to have intruded vertically and the one to the south dips 
 83 d^ees to the northwest. 
 
 liie principal quarts vein consists of a series of long, narrow lenses in 
 a narrow band of greenstone schist bordering the north dyke of granodio- 
 rite. Maximum widths range from 1 tu 6 inches. The vein was observed 
 almost continuously along the contact for 3 chains. Spectacular showings 
 of gold were found in this vein. At one point, it is joined by an 8-inch 
 quarts vein running west into the greenstone; near the junction pockets 
 were observed into which numerous small prisms of quartz projected 
 fn ?■} One pocket was partly filled with calcite. Fine gold wa.s observed 
 er c I in and also lying on the surface of some of the quarts crystals 
 BL. . Jvoding these pockets. 
 
 Going south across the greenstone outcrop four other veins were 
 observed similar to the one at the contact and running parallel to it. These 
 were spaced at distances of from 20 to 30 feet. Small showings of gold 
 were observed in all of them. 
 
 Farther to the south, the second dyke is encountered and here also a 
 narrow, gold-beariug quartz vein occurs at the granodiorite-greenstone 
 
70 
 
 contact. The trend of this vein differs by 68 degrees from that of the 
 others, but stripping has not shown whether they intersect or not. 
 
 Pyrite is abundant in the veins and the neighbouring greenstone. 
 No other metallic mineral was observed associated with the gold. 
 
 The veins on this property appear to be as well mineralised as those 
 on the Sullivan property, but they are very narrow. 
 
 Clowea, AiOhier, and Le Clair Clainu. Clowes' pioperty is situated 
 2 miles east of the extreme north end of Lemoine lake, Authier's claim is 
 on the eastern shore at the extreme north end, and the Le Clair property 
 is 1 J miles west of the Authier property. All are situated near the contact 
 .of the Pontiac schists and the Abitibi greenstone, and in each case the 
 veins are lenticular masses of smoky or dark-coloured quarts. 
 
 Very little development work has been done on the Authier or Le 
 Clair property since Mr. Bancroft's visit in 1911. At that time assays 
 showed no trace of gold in the quartz veins. 
 
 Clowes' claim was not visited, but Mr. Clark, who was in charge of 
 development work, stated that a 26-foot shaft had been sunk on a vein of 
 smoky quartz and that gold had bee" found in place. No assay returns 
 were available. 
 
 Carriere Claim. This claim of 135 acres was one of the most promising 
 in the district five years ago when its principal vein was discovered by 
 S. G. Smith. Since that time the property has been restaked more than 
 once, the gold showings have been removed, and no further development 
 IS taking place. It is situated one-third of a mile south of the first bay 
 east of the inlet of De Montigny lake. The vein is situated on la bare, 
 rocky hill. 
 
 The geological relationships found on this claim are quite similar to 
 thcwe on the Le Blanc property. The rock is Abitibi green schist. The 
 schistosity strikes north 85 degrees west; and dip from vertical to 80 
 degrees south. A massive, porphyritic diorite dyke similar to the intrusive 
 on the Le Blanc property cuts the schists on the northet-n face of the hill. 
 This dyke is 35 feet wide and striLes north 40 degrees west. On the 
 eastern part of the outcrop a 2i-foot dyke comes off to the south from 
 the larger one. A small exposure of Keweenawan (?) diabase occurs on 
 the trail in low land 2 chains northwest of the hill; its presence does not 
 appear to have any relation to the mineral deposit. 
 
 The quartz vein in which the gold occurs is on the rocky hill and 
 extends in a direction north 60 degrees west from the smaller dyke of 
 pwphyritic diorite. The vein dips toward the south at angles of from 
 35 degrees to 55 degrees. It consists of a succession of long lenses, from 3 
 mches to 14 inches wide; which can be followed continuously for 73 feet 
 to the west of the diorite dyke. It there becomes drift-covered, but 
 beyond along the projection of the strike another quartz vein is said to 
 occur. 
 
 The quartz is in places glassy, in other places sugary. It is colourles-s 
 or v'hite except where stained by iron in the neighbourhood of pyrite 
 crystals. One cavity was observed lined with large, projecting quartz 
 crystals. 
 
 The mineral association in the' quartz vein is pyrite, chalcopyrite, 
 gold, black tourmaline, calcite, and epidote. 
 
 Mr. Bancroft mentions a spectacular displav of gold in a fragment 
 taken from the upper part of this vein. At the time of the writer's visit 
 
71 
 
 no gold was to be seen even in the place where it was said to be best mineral- 
 ised. Mr. Bancroft's average sample of this vein yielded oiily 20 cents 
 per ton in gold whereas that collected near the gold showings yielded Sl.iO 
 per ton in gold. 
 
 Catndy Claim. The Cassidy property lies south of De Montigny 
 lake and adjoins the Carriere claim on the west. Several low, rocky hills 
 occur in this locality with swampy, drift-covered country lying between. 
 
 Gold is reported from a vein on one of these hills about one-quarter 
 mile southwest of the Smith vein. The rock on this hill is an andesite 
 schist striking north 60 degrees west and dipping vertically. It is intruded 
 by a porphyritic granodiorite dyke. One side of this dyke was observed 
 in contact with the andesite, the trend following the schistosity strike; the 
 other side of the dyke was drift-covered beyond the base of the hill. A 
 short distance to the north of this hill, a dyke of Keweenawan (?) diabase 
 outcrops in the lower ground. This is probably part of the dyke observed 
 on the Carriere property. 
 
 The quartz vein occurs in the granodiorite a few feet in from the 
 schist contact. Its trend is north 55 degrees west. Toward the north- 
 west face of the hill the vein is 5 feet wide, a few blocks of country rock 
 being included in the quartz. It was followed 80 feet to the southea.st 
 where it divides into several veins; one of these, 3^ feet in width, curves 
 to the east for a short distance then resumes its former direction before 
 being lost under the drift covering. 
 
 The quartz in the vein is white. Pyrite grains and radiating bunches 
 of black tourmaline are common in it. Visible gold was reported, but 
 none could be found in place at -the time of the writer's visit. 
 
 Sisco Claim. The Sisco claim is located on the west side of the largest 
 island in De Montigny lake. Here, as in the case of the above-mentioned 
 property, a small quartz vein cuts a granodiorite dyke which is intrusive 
 in green schists. Specimens collected from this vein by the owner con- 
 tained several small pieces of gold. 
 
 Benard Claim. The Benard claim is located on the northeast shore 
 of De Montigny lake on the peninsula which is closest to the largest island. 
 At the end of this peninsula is a low, drift-covered hill, which projects to 
 the south. Where the waves have removed the drift on the west side 
 the rock is seen to be Abitibi greenstone. On the east shore of this small 
 peninsula at the south end and 60 feet north of this, the Benard veins 
 are exposed. Very little development work has been done on this pro- 
 perty. 
 
 The oldest rock on the peninsula is an Abitibi chlorite schist. The 
 schistosity strike is due west, the dip vertical. This rock is intruded by 
 a dyke of granite about 54 feet wide. Another 8-foot dyke carrying 
 several small veins occurs 60 feet south of this. The main dyke is cut 
 by a stockwork of veins, so abundant that at first glance the whole exposure 
 appears to lie vein material. The veins are for the most part less than 
 10 inches wide and trend in an east-west direction, sometimes dividing 
 and joining again, making a pattern like a drawn out net. Small inclusions 
 of dyke material are abundant in the veins, the feldspathic minerals being 
 arranged in lines giving the vein a gneissic appearance. 
 
 The dyke rock on this property is quite different in appearance from 
 that on the other claims, but it is believed to be derived from the same 
 magma. In the hand specimen, it is fresh-looking, medium-grained. 
 
n 
 
 Bmaitic roek in whkh auarti and pale green and white feljhjwyw are 
 OBterminaUe, with abundant small tube* ol pyrite uniformly dirtrmtrted 
 through it — a pjrritifarous binary granite. In thin aeetion, it » aeen to 
 eonaiat ot albite, quarti, and mrnte, with email amounts of rutile, lireon, 
 and iqtatite, and tne secoAdary minerals ealdte and serieite. Tlie quarts 
 contains num«rous. tiny liquid indurions and in places is micrographically 
 inter g r o wn with tne fddsiwr. Minute rutile prions occur individually 
 in the feldspar crystals and also in diamondHshaped intersecting aggregates. 
 Mr. Bancroft states that the fresh pyritiferous dyke material assays tl .40 
 to the ton in gold.* 
 
 The quarts veins, which cut the dyke, contain abundant needles of 
 black tourmaline and a few specks ol chalcopyrite. Finely panular, 
 iron-bearing carbonate, feldspar, and pyrite occur in streaks near dyke 
 rock inclunons. A sample cS van material collected across the entire 
 width d the exposed network assayed merely a trace of both gold and 
 silver. No visible gold has been reported. 
 
 >"Iliaii« (•mtioM ii Um fnriM* of OmDw". MM, pp. at, m. 
 
Plate II. 
 
 A. TonbcH rapids on Harricanaw river at northrm limit of this exploration. 
 
 (Pane .V).) 
 
 B. View from Rifted hill to eastward, NhowinK Obalski lake and typieal i-ven 
 skvlino. (Pane *<■) 
 59813—7 
 
74 
 
 Plati III. 
 
 Upper part of the long Merieii of casradM on Harricanaw rivef>22 miles north 
 of Amos, at low water. The most promiainii sourer of water-power in the 
 district. (Page 16.) 
 
 P. (lliiciati'il IxMildcr pnvenient on 2.'>-<'hain porfage, 
 Harricanaw rivor, Vi inilox below junction with 
 Plaranndon river. (PaRe 48.) 
 
75 
 
 Platb IV. 
 
 A. BouMer clay at Spirit Lake Intenunent camp. (Page 48.) 
 
 B. Elli|iBoidal andesitc, Harrlranuw river, 7 mile* above junction with 
 Turgpon river. (Page 22.) 
 
70 
 
 PunV. 
 
 B*nd«l mint «chiiit (altRrmi watrrlttin tuff) cut by quarts vj-inn and 
 MmwinK liiffiTi-ntial wcuthiTinn, Turgeon river, 4 miles below Corset ialand. 
 (I'uges 26 and 01.) 
 
 ^ v., r-.- < . 
 
 .'* -V.V •.■•-•'.. 
 
 B. I'hi.totnicroKruiih of micH Hrhist (ull.re«l tuff), Turni-.m 
 riyiT, \ uulfH Im'Iiiw Corwt iKiuml. MuKisilicl _•(' 
 iliuaii'terH. (I'u«l' 20.) 
 
ItATB VI. 
 
 Curbonun«)U8 iilatc rock, containtn« liiNwininuUil ttiiil u<> iiilur pvrilr, Octuvc rivpr, 
 1 mile Ix'low th«> up|M>r 10-rhaiii iiorliiKi'. IIh- iiuixununi width of tin- larapr 
 H|)cciiiirn wan inchc-i<. (Page JO.) ' 
 
7S 
 
 Vtjmt VII. 
 
 A. Urc<-cuil<H) umphibotitp imprcKnatni wilh icninit<< mnith shiw of Jiip 
 lakp, at hfwiwatm of Pnttpn rivpr. The maxinmni wi<llh »a» «} 
 inrhn). (PaKc 44.) 
 
 It 
 
 I-nrgp flat hliirkM of hciriiblt'mlr si-hint iiiciii led in coarse Kraiiitr, Turg«>on 
 rivpr, .J niilpd uImivp junrtion with Thro rivpr. Th^ '■■.-((<■ plato-likp inclu- 
 sions stund nearly parallel to each other and hnv. ■ jt been cornided by 
 the Kranite. (Pokp 44.) 
 
79 
 
 s 
 
 lllll 
 
 
 :? s i - 
 
M wwcow moumoN tkt chact 
 
 (ANSI and ISO TEST CHA*T ho. 2) 
 
 A 
 
 /1PPLIED HVHGE Inc 
 
 1653 Cost Main StrMt 
 
 RochMar. Nm rwk UecK usa 
 
 (716) «2 - 0300 - Ptwn. 
 
 (716) 268 - JM9 - fo. 
 
80 
 
 Plate IX. 
 
 Conorolions from stratififnl oliiy. The sixH-itnon with npttcnl surface of <iark linear 
 inarkinRs is from Concretion <reek, the others are from the north shore of 
 ('hikobi lake. The niaxiniiim diameter of the larKest specimen was 4Vc 
 inches. (Page 51.) 
 
81 
 
 INDEX. 
 
 Abitibi bttholith 
 
 " group 
 
 " •V • 
 
 " " itnicture of 
 
 " volcanic eomiilex. 
 
 Acknowledgmenta 
 
 Agglomnate, scidie 
 
 Ag^omentes 
 
 Aforitdlture 
 
 AUard portage 
 
 •«, 
 
 PAOB 
 
 42 
 
 16,18 
 
 39 
 
 m 
 p, 
 
 I 
 
 29 
 
 24 
 
 -. 12 
 
 ;;;;;;;;;;; 28 
 
 '.".'.'.'.'.'.'.'.'.'.'.".'.'.'.'.'.'.'..'.'.'.'.'.'. 28 
 
 1 
 
 40 
 
 57 
 
 72 
 
 71 
 
 rdportai 
 A'Jen, R. C. 
 
 Andeaite. 
 Angle river. 
 
 Aim 
 
 ArkoK. 
 
 Aabeatoa 
 
 Anay, gold, Benard claim. . . 
 
 " " Carriere claim . . 
 
 " " Le Blanc claim. 
 
 " " Sullivan claim.. 
 
 " TrembUy claim 
 
 Authier claim 
 
 " H 
 
 nver 
 
 " occurrence of carbonate rock. 
 
 .29, 31, 37, 
 
 56 
 70 
 60 
 54,57 
 34 
 
 B. 
 
 Bancroft, J. A. 
 Basalt. 
 
 .40, 
 
 Basic volcanics. . 
 Beauchamp lake. 
 BeU,R. 
 
 Benard claim — 
 Biblk)gn4>hy — 
 Brock, R.W.... 
 Bumtbuah river. 
 Burrows, A. G... 
 
 .24, 
 
 67,61 
 19 
 19 
 12 
 3 
 71 
 4 
 34 
 
 28,54 
 34 
 
 Callinan property 
 
 Carbonaceous slate 
 
 Carbonate rock 
 
 Camochan, R. K 
 
 Carrier claun 
 
 Caasidy claim 
 
 Chalcopyrite 
 
 ChikoW take.'.' .■.'.■.'.'.'.'.'..'.....'. ..•■••• 10, 2, 28, 52, 
 
 " carbonate rock boulder 
 
 Chobodis house 
 
 Clay 
 
 Clay, bouUer 
 
 Clergutf, F. H 
 
 Clermont, L 
 
 Climate 
 
 Ckywes claim 
 
 Cochrane^ A. 8 
 
 Conununication 
 
 Conglomerate 
 
 Copper • • • 
 
 Corset island 
 
 30 
 
 31 
 
 1 
 
 70 
 
 71 
 
 7,52 
 
 36 
 
 53,54 
 
 34 
 
 29 
 
 58 
 
 <8 
 
 3 
 
 1 
 
 11 
 
 70 
 
 3 
 
 1 
 
 40 
 
 54 
 
 21,23 
 
Daeite «Q 
 
 Dalquier t«wn§hip fV 
 
 Davy River batholith . i? 
 
 Dawson, C. B *J 
 
 De Montigny lake lo m 
 
 Dwbaw f2 
 
 Drainage g 
 
 Dubuisaon townohip ai 
 
 Dunes : jo 
 
 E. 
 
 Elevations '. .• g 
 
 F. 
 
 Faulting oa 
 
 Fauna '.'.'.'.'.'.'. 13 
 
 Ferland, Joseph j^ 
 
 Fire Rangers point ■ . 
 
 Flora ....■.;.■.■.■.■."."■.'.■.■ 13 
 
 Fluvioglacial deposits vi 
 
 Fossils ■■.'.'.'.'.'.'.'.'.'.'.'.'.'.'.'.'.'.'.'.'.[[[[['.'.:'.::'. w 
 
 G. 
 
 Gabbro U^ 
 
 Gale claim aq 
 
 Galena Y 52 5« 
 
 Gameau river • ' 24* 46 
 
 Geology, economic '^^'^^^''^':::::::::::::::::::7, 52; 65 
 
 Glacial ^r:"::::: v:::::::::::::::::::. «• ^«' «) 
 
 Glaciaticm a 17 ab 
 
 «"«« ■.■.•.•.•.■.•.■.•.•.•..■.•.•.• ■:::::::::::::^: II: m 
 
 ''"''Benardciaim.assay;::.;.;.;.-.;.-.;. .•.•..;.•.•.■.•.■.•. .•.;.•.•. . '':'^''' ^' «»• '°' I2 
 
 " Carriere claim, assay 71 
 
 " genesis of aa 
 
 " Le Blanc claim, assay gg 
 
 " Sullivan claim, assay ga 
 
 Granite j.9 «s 
 
 " batholith ' V2 
 
 Greywacke, banded «» 
 
 " ""ny ;.:::;::::::;:::::::;::;;;:: « 
 
 H. 
 
 Hanson, G . 
 
 Harricanaw river ■.'.'.".'.■.'.'.■.'.■.■.'.'.'.■.■.■. .'.14, 22,' 27,' 3r,'36, 52, 54 
 
 occurrence of carbonate rock 33 
 
 " series « <<> oq 
 
 Hebert hiU^ o, 10, J» 
 
 History 2 
 
 I. 
 
 Intermediate volcanics in 
 
 Iron ..".'.'.'.'.'.'..'.'.'.' 7 57 
 
 " formation ' 29* 37 
 
 K. 
 
 Keele, J u 
 
 Keweenawan (?) diabase 40 gij 
 
 Kienawisik gold district on' ak 
 
 Kindle, E.M .'.'.'.'.■.■.■.'.■.'.'.■.'.■.'.■.■.■.■.".'.'.'.■.■.■.'.■.■ 49 
 
83 
 
 Liunutrine depoeitx. 
 
 Laket*. 
 
 LaMoUpUke 
 
 Lamprophyre 
 
 LanKiuMoc township. 
 La Reine township . . . 
 
 LaHarre. 
 
 La Sarre river 
 
 Lead 
 
 \je Blanc property 
 
 Ijc Clair claim 
 
 Leith, C. K. 
 
 rAOB 
 AO 
 10 
 l» 
 45 
 
 28,ftS 
 4ft 
 12 
 
 10,14 
 56 
 
 66,68 
 70 
 37 
 20 
 
 Leslie creek 1, 61 
 
 Location 
 
 Lois lake 
 
 Lumber trade . 
 
 M. 
 
 McKeniie lake 
 
 Makami 
 
 " lake 
 
 " river 
 
 Main peninsula 
 
 Menard river 
 
 Metamorphism, contact. 
 Mica sc/iists, banded. . . . 
 
 Mining prospectJi 
 
 Mistawak batholith 
 
 " junction 
 
 " lake 
 
 Molyb<lenite 
 
 Moraines 
 
 Mourier lake 
 
 Nptional Transcontinental railway 
 
 N. 
 
 railway crossing . 
 
 Ne''. kalak^.. .• 
 Ninemile poriagc . 
 Kissing hills 
 
 14 
 13 
 
 31,54 
 
 2 
 
 10,14 
 
 26 
 
 54 
 
 48 
 
 43 
 
 . 24,26 
 
 66 
 
 38,42 
 
 24 
 
 49 
 
 . 7,57 
 
 49 
 
 65 
 
 . 1,52 
 
 61 
 
 10 
 
 36 
 
 9 
 
 O. 
 
 Obalski lake '22 
 
 Octave river. . 
 Oditanhill... 
 Oiibway clay . 
 Okikeska lake 
 Okiko. 
 
 Okikodosik river. 
 Otter lake 
 
 22,57 
 ,29,30 
 9,46 
 50 
 65 
 12 
 14,26 
 10 
 
 ... '• 49 
 
 Partnuge river 21, 36, 52, 54 
 
 Patten river 3 
 
 " T.J :::;:: 48 
 
 Pavement camp 6, 9, 57 
 
 Plamondon hill ' \q 
 
 " river 4g 
 
 scene ] 1 ! ! 47, 54 
 
 . .* hills.. 64 
 
 Pontiac schists 17 45 
 
 Post-batholithic intrusives 6 16, 61 
 
 Pre-Cambrian. ' 29 
 
 Pyroclastics, acid 24 
 
 " intermediate 
 
M 
 
 SS^'^::::::::/:::;::;::::;:;:::::::;::;;:;;:;:;::- 
 
 R. 
 
 R#C€nt , 4A . « 
 
 BdueT •■••••••■ "•'"i. "!;!■!!!":::::::;::;:;;;; '" 
 
 ^^ ",. iccun^ci' > -nrtwiikte^ckV.'. ■.;■.■.■.;■.; 26, 28, 31, 45, M 
 
 Rhvolite 31 
 
 Ri/tedhiU 27 
 
 RobertMm Lake bathoUth 1g 
 
 8. 
 
 Schiat complex, banded „, 
 
 Section, Harricanaw series 2™ 
 
 Siturian Hmeatone ™ 
 
 Silver V .n J? 
 
 SIkso claim 7,52,84 
 
 Smith, 8. O 71 
 
 Smith's vein JV 
 
 *rw»t , T. B * » 
 
 Spirit Lake detention camp , . . ,„ 
 
 8tri« *: ^ J2 
 
 " claims ^'"'22 
 
 Ob 
 
 T. 
 
 Table of formations m «• 
 
 TanbeU rapids "- SJ 
 
 Teljuride, goW » 
 
 TeUurium °3 
 
 Theo river ,, ^ 
 
 Ti mis ka min g and Northern Ontario railway.'.'.'. ' o 
 
 3>o«n*hy ' -l 
 
 TranqMHtatitm "' * 
 
 Treeeaaon township r* 
 
 Tremblay daim .„ S" 
 
 ^ u J o£, Ao 
 
 " vein ^ 
 
 TulTs, banded acidic! '.'.'.'.'.''.'.'.'.'. SS 
 
 " stratified ~ 
 
 Turgeon river iV o«" ok S 
 
 Twining creek ••....■..'.'.'.■.'.'.■.'.'.'.'.■;;;;;;;;;;.•.•;;.•.•;;"; ^^i ^' ^ 
 
 V. 
 
 VaUeys 
 
 Ai 
 
 w. 
 
 Wa]ker,L.I ..* , 
 
 Water-poweis "■ ,} 
 
 Jl^lll^s'^" ■••••■:"::::::::::::::::::::::::::i6;u; 22.27.19 
 
 Mi^iw:^'.'.'.':::;;:;::;::;;;;;;:;;;:;:;:::: 1,23.27.34,61 
 
 Woman river „J 
 
 mii mk^i^mm.'. 
 
^m 
 
Hfpwtmnit irf jHlws 
 
 Ho^. M»«TiN Bh«-. MiN.STrn. R,G.M'C.ONNiu,DiPiiTvM,N,»t[f. 
 
 OeOLOOICAL SURVCY 
 
 Wi., ,*v MMnsEs. Di,^t>.,r,Nr, G(oi.oc 
 
 78'i!%' 
 
 
wp 
 
 B^partmmt afiRims 
 
 ocoLooiCAL tunvtv 
 
 'William M'-nnu. Di,^ti.r;NG Gloi.o., sr 
 
 TB'm 
 
 THW 
 
 Trw 
 
Ta'M' 
 
 »«f^ 
 
 4 ••»•<' 
 
 £«w kmJ rimf 
 
 -a- 
 
 -|ter« 
 
 > I 
 
 i^r4"*lf * 
 
LKfiEND 
 
 Bmmm* intrufivvi 
 
 « XaJfMT . uUi^ iHrnifM* 
 
 H£iiUtlur iutr 
 
 Z 
 < 
 
 K 
 
 a 
 
 < 
 u 
 u 
 
 K 
 
 a. 
 
 Arifl hHUiiilitlur iutniam** 
 
 f*>ittit%tpm ittjirntrj tk\ Ifvmi^t fAm* j 
 
 iliurii'ajiaw m^nm* 
 Ahitibi ^mtp 
 
 Tuft 
 
 irwt fvrtniitton 
 CArrt rw*t4c 
 
 Hyzubolfi 
 
 '.iHolu^t'iil IhiuuiIhtt 
 
 
 (UuriH] Striv 
 
 Stj-ike Hud <tip 
 of KrhiNtdiiirT' 
 
 \'fTtiriJ nrhiiitaifitT 
 
 
^UU^^U^£l^^fli^ywik 
 
CO-Spd^hI . frroifrapMtT and Cki^t^' DrnuahtMtruu* 
 
 
 Scmir. 2S0 MIU, u I l,uk 
 
 Tti arromtfmnr Mfmnir 6v TTZ. Tmuun 
 
MAF 183 A 
 
 HAK RICA:VA\\^ TITRGEOiV BASIJV 
 
 ABITIBI.TIMISKAMING, AND PONTIAC 
 yiTiBEC 
 
 Srnle, sSi.Mo 
 
 MOea 
 
 KUoaftl 
 
 Soiiri'PH ol' lufor 
 
 <,V.../.../.«i t';,„ "Mnp or r^l 
 ^IbfariKi^'iit nr L^m1« »ind Fot^ 
 Mi^ Ml A Kf-wa JuW, Gfalof 
 
 'W' " ■"•rvmi/K Ay T.I,T«I 
 
 .gU fr...» "Mnp 93 A'. liwoUf 
 
 =^ .* 
 
 4 MILES TO I INCH 
 
MAP 183 A 
 
 ,BITIBI,TIMISKAMING, AND PONTIAC 
 Ql-EBEC 
 
 ScRle, 253,44b 
 
 KilAflwtrea 
 
 4 MILES TO I INCH 
 
PttUicftlicu Hf 1630 
 
 Soiircea «rf* iufomiBtiou 
 
 O^oirrnphy from "Umj^ sf thm AbittU R«^«£ 
 Dt^mrtmmt tt( LvmU and. Fa—to , Q— fc ac .1911 ', 
 'tUp n.1 A'KvwagamW, 0«Mklogieal » iw. MIS. 
 tfnf/ /^m 'u/^r' Ay TX.TiiaUa,m4,in&* 
 
 i,H»logY /^m murvpa ^ TL-TuttOK . 104,1815. 
 (iju/ />oiK "Map 93 A", G«al*gieal Ssvvv/.