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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 \o. t73S ^<J 2Ed2^Sy^ J i } ¥ U 'si ■&I '>s f c 5UKt:i 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/.