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MKROCOrV MSOWTION TBT CNAUT 
 
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 1653 East Main Str^t 
 
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^ 
 
 
 CANADA 
 
 DEPARTMENT OF MINES 
 
 Hon. Martin Burrell, Minister; R. G. McConnell, Dcputy Minister. 
 
 GEOLOGICAL SURVEY 
 
 \VlLLI.\M McISNES, OlRECTIXr, f.EOLOCIST. 
 
 MEMOIR 113 
 
 No. 96, Geological Series 
 
 Geology and Mineral Deposits of a 
 
 Part of Amherst Township, 
 
 Quebec 
 
 BY 
 
 M. E. Wilson 
 
 OTTAWA 
 
 J. Di LABUOQUERIE TACUfi 
 
 PRINTER TO THE KINGS MOST EXCELLENT .MAJESTY 
 
 leig 
 
 No. 1745 
 
-' 
 
i 
 
 ''i^\ 
 
eisw 
 
CANADA 
 
 DEPARTMENT OF MINES 
 
 HOH, Mabtin BviBiix, MiMinu; R. G. McCommill, DtruTT Miniitb*. 
 
 GEOLOGICAL SURVEY 
 
 WiLUAM McInnbs. Dibbctino Geolcx^ist. 
 
 MEMOIR 113 
 
 No. 96. GEOLOCICAt. Sebibs 
 
 Geology and Mineral Deposits of a 
 
 Part of Amherst Township, 
 
 Quebec 
 
 BY 
 
 M. E. Wilaon 
 
 OTTAWA 
 
 J. Di LABROQUERIE TACB£ 
 
 riUNTER TO THE KINO'S MOST SXCEUGNT MAJESTY 
 
 1(19 
 
 No. 1 745 
 
 81SS0-1 
 
CONTENTS. 
 
 CHAITKK I. 
 
 Intrmlurtinn 
 
 Ocnor*! Mtalprntrnt nn<l nrknowlnlgmpnta. 
 
 Location ami mrana of acc.<M 
 
 Prcviouii work 
 
 HiblioKraphy 
 
 CHAPTER n. 
 
 Phyniography 
 
 (ipneral utateinent 
 
 Ht . Rpini Hat 
 
 liockway flat 
 
 Rocky upland* 
 
 Drift covered uplandii . 
 
 lAPTER III. 
 
 General geology 
 
 General Htatement 
 
 Table of fomiationa 
 
 Basal complex 
 
 GrenviUe terie* 
 
 Crystalline limmtone 
 
 Distribution 
 
 Lithological character. 
 
 Garnet gneiss 
 
 Distribution 
 
 Lithologieal character. 
 
 Quartsite 
 
 Distribution 
 
 Lithological character. 
 
 Structural relations 
 
 Origin 
 
 Buckingham series 
 
 General statement 
 
 Distribution 
 
 Lithological character 
 
 Pyroxene syenite 
 
 Pyroxene diorite 
 
 Gabbro 
 
 Pyroxenite 
 
 Other related type« 
 
 Structural relations 
 
 Internal 
 
 External 
 
 Correlation 
 
 Metamorphic pyroxenite 
 
 \ 
 i 
 I 
 3 
 3 
 
 4 
 4 
 
 4 
 4 
 S 
 S 
 
 « 
 
 « 
 8 
 7 
 7 
 7 
 7 
 7 
 7 
 •» 
 A 
 8 
 8 
 9 
 
 
 10 
 
 10 
 
 10 
 
 10 
 
 10 
 
 11 
 
 11 
 
 11 
 
 !? 
 
 12 
 
 12 
 
 12 
 
 13 
 
 13 
 
u 
 
 PAGE 
 
 Granite-eycnite gneim 14 
 
 General Btatement 14 
 
 Distribution 14 
 
 Lithological character 14 
 
 Structural relationships 15 
 
 Internal 15 
 
 External 15 
 
 Correlation 15 
 
 Late Pre-Cambrian intrusivcs 16 
 
 Diabase 16 
 
 Quaternary 16 
 
 Glacial 16 
 
 Marine clay and sand 17 
 
 CHAPTER IV. 
 
 Mineral deposits Ig 
 
 General statement 18 
 
 Kaolin, kaolinic quartzitc, and comish stone 18 
 
 History of development 18 
 
 Distribution 19 
 
 General character 19 
 
 Structural features 21 
 
 Faulting 21 
 
 Jointini;; 21 
 
 Granular fracturing 23 
 
 Replacement 23 
 
 Composition 23 
 
 Origin 25 
 
 Summary statement of hypotheses 26 
 
 Kaolin of superficial origin 26 
 
 Kaolin or kaolinizing agency of deep-seated origin 27 
 
 St. Remi deposits 29 
 
 Kaolin from a superficial source 29 
 
 Kaolin from a deep-seated source 30 
 
 Conclusion 30 
 
 Discoloration in kaolin 31 
 
 Extent of deposits 31 
 
 General statement 31 
 
 Kaolin ' 32 
 
 White kaolin 32 
 
 Discoloured kaolin 32 
 
 Kaolinic quartzite 33 
 
 Cornish stone 33 
 
 Kaolinized garnet gneiss 34 
 
 Uses of materials contained in deposit.<< 34 
 
 Kaolin 34 
 
 Kaolinic wall rock « 35 
 
 Equipment and mining methods 36 
 
 Production 30 
 
iii 
 
 Graphite 
 
 General statement 
 
 Hiatory of development . 
 Geological relationships. 
 Character of deposits. . . 
 
 Mineralogy 
 
 Paragenesis 
 
 Origin 
 
 Equipment 
 
 38 
 38 
 38 
 38 
 38 
 40 
 40 
 41 
 41 
 
 CHAPl'ER V. 
 
 Summary and conclusions . 
 
 42 
 
 Index. 
 
 51 
 
 II. 
 
 III. 
 
 IV. 
 
 Illustrations. 
 
 Map 1681. Portion of Amherst township, Quebec in pocket 
 
 1676. Diagram showing pits in kaolin deposits in lots 5 and 6, range VI, south, 
 
 Amherst township, Labelle county, Quebec in pocket 
 
 Plate I. Fragment from bed of kaolinic Grenvilte quartzite showing the vertical 
 linearity of the qiuirtz grains, lot 5, range VI, south Amherst 
 township, Quebec Frontispiece 
 
 A. fSt. Remi flat and village of St. Remi as seen from the Alsio ridge. . . 
 
 B. Washing plant, Canadian China Clay Company, lot V, range VI, 
 south, Amherst township, Quebec 
 
 A. Crumpled, variegated garnet gneiss member of the Grenville series, 
 lot 6, range VI, south, Amherst township, Quebec 
 
 B. Bande<l gametiferous gabbro, lot 1, range II, Amherst toivnship, 
 Quebec 
 
 Variegated surface of garnetiferous gabbro, lot 1, range II, Amherst 
 
 township, Quebec 
 
 V. A. Jointing in Grenville quartzite in fault zone, lot 5, range VI, south, 
 
 Amherst township, Quebec 
 
 B. Fluted and slickensided surface of Grenville quartzite along fault 
 zone, lot 5, range VI, south, Amherst township, Quebec .... 
 VI. A. I'itted surface of quartzite bed showing the solvent action of solu- 
 tions depositing the kaolin m the quartzite, lot 5, range VI, 
 
 south, Amherst township, Quebec 
 
 B. Specimen from kaolin deposit, lot 6, range VI, south, Amherst town- 
 ship, Quebec 
 
 VII. Aggregate of orthoclase, pyroxene, titanite, woUastonite, graphite, 
 
 and calcite associated with graphite deposit, lot 17, range 
 
 VI, Amherst township, Quebec 
 
 Figure 1. Index map showing position of area 
 
 2. Section of south face in pit in china clay deposit on lot 6, range VI, 
 
 south, Amherst township, Quebec 
 
 3, Diagram showing parts of lots 16 and 17, Amh»st towtiship, Quebec . , 
 
 618S»-2 
 
 45 
 
 45 
 
 46 
 
 46 
 
 47 
 
 48 
 
 48 
 
 49 
 
 49 
 
 50 
 2 
 
 22 
 
 37 
 
Geology and Mineral Deposits of 
 A Part of Amherst Township, Quebec. 
 
 CHAPTER I. 
 INTRODUCTION. 
 
 GENERAL STATEMENT AND ACKNOWLEDGMENTS. 
 
 Although deposits of the mineral kaolin, kaolinite, or china clay 
 are known to occur in numerous localities in Canada', most of these 
 occurrences are of small extent and hence of no commercial importance. 
 Furthermore, since kaoUn commonly occurs in such relationships fts to 
 indicate that it has been formed as a product of surface weathering and 
 throughout a large part of Canada, the products resulting from such altera- 
 tion have been, for the most part, removed by the erosive action of the conti- 
 nental glaciers, it is probable that deposits of kaoUn, on the whole, are less 
 abundant in Canada than in parts of the world where Pleistocene conti- 
 nental glaciation did not occur. The presence of extensive deposits of 
 kaolm near the village of St. Remi, in the southern part of Amherst town- 
 ship I^belle county, Quebec, a locaUty well within the glaciated uplands 
 of the Laurentian plateau, is, thereforcj not only of considerable geological 
 interest but of great importance to Canadian industries in which kaolin 
 is used. 
 
 The field investigations, upon which the following report is based, 
 with the exception of a re-examination of the kaolin deposits in July, 1918 
 were carried on in the latter part of the summer of 1916. This work in- 
 cluded a study of the deposits of kaolin, an examination of a number of 
 graphite occurrences on lots 15, 16, and 17, range VI, north, Amherst 
 township, and the preparation of a geological map of the district, 12 square 
 miles in area. 
 
 The writer wishes to express his indebtedness to Victor Dolmage 
 and L. P. Gouin, both of whom assisted in the field work necessar ' for 
 the preparation of the geological map which accompanies this report- 
 and to J. C. Broderick, Managing Director of the Canadian China Clay 
 Company, by whom every facility was afforded for the studv of the kaolin 
 
 uCDOSlt'S " 
 
 LOCATION AND MEANS OF ACCESS. 
 
 The St. Remi district, in which the kaolin deposits occur, is situated 
 in the province of Quebec, approximately 30 miles north of the Ottawa 
 nver and ahnost equidistant from Montreal and Ottawa. It lies at the 
 
 ..' ^f*; ^y- ^^'SP- 0* >'■■■»■ RMOunsn o( OaUiio, p. 70: Aaa. Bwt. Oat. Banau al Mi^ vol Tnil »t t 
 
 f. Ti^- *^" ^- °^ °' ^^- """■ "■ ""• '■ "•' Au. B5pt"Si!lES« rf 3i^?^™k!:*pi* 
 
 618SD-2} 
 
western terniiiiiiH of the Huberdeau branch of the Canadian Northern 
 railway and almost midway between St. Jovite on the Mont Laurier 
 branch, and Calumet on the North Shore Branch, of the Canadian Pacific 
 
 Figure 1. Index map showing position of area. 
 
 railway. It is, thus, most easily accessible by way of the Canadian 
 Northern railway from Montfort Junction, but can also be reached by 
 way of the Rouge River road from either Calumet or St. Jovite. 
 
 PREVIOUS WORK. 
 
 In ihe year 1862 Mr. James Low, assistant to Sir William Logan in 
 the Grenville district, examined the geology along Maskinonge river, the 
 principal western tributary of Rouge river, and in the course of this examina- 
 tion traversed the southwestern part of the territory afterwards surveyed 
 as Amherst township. 
 
 In 1895 Mr. J. Obalski, late Superintendent of Mines for Quebec, 
 visited the district for the purpose of examining a deposit of kaolin which 
 had been newly discovered at that time, and in his report for that year 
 stated that kaoUn containing a large proportion of quartz had been found 
 in the bottom of a well on lot 5, range VI, south, Amherst township. 
 
3 
 
 In 1911 the kaolin deposits of the district were visited for the GeoioKical 
 Survey by F. Ries and J. Keele and were described by Mr. Ries in the 
 Summary- Report of the Geological Survey for that year, and by Mr. 
 Keele in Memoir 64, " Preliminary report on the clay and shale deposits 
 of the province of Quebec." 
 
 BIBLIOGRAPHY. 
 
 Dawson, G. M.— Geol. Surv., Can., Ann. Rept., new ser., vol VII, 1894, pt. 
 A, p. 101; vol. IX, 1896, pt. A, p. 110. 
 
 Denis, T. C. — "Mining operations in the province of Quebec," Depart- 
 ment of Colonization, Mines, and Fisheries, Quebec, 1909, p. 23; 1910, 
 pp. 66 and 77; 1911, p. 32; 1912, pp. 34 and 44; 1913, pp. 57 and 60; 
 1914, pp. 77-82; 1915. pp. 39-42; 1917, 54-55; 1916, pp. 52-53. 
 
 Ells. R. >y.— "Report on the geology of Argenteuil, Ottawa, and part of 
 Pontiac counties, province of Quebec, and portions of Carleton, 
 Russell, and Prescott counties, province of Ontario," Geol. Surv., Can., 
 Ann. Rept.. new ser., vol. XII, 1899, pt. J, p. 135. 
 
 Hoffmann, G. C. — Report of the section of chemistry and mineralogy, 
 Geol. Surv., Can., Ann. Rept., new ser., vol. VIII, 1895, pt. R, p. 14. 
 
 Keele, J.— "Preliminary report on the clay and shale deposits of the 
 province of Quebec," Geol. Surv., Can., Mem. 64, 1915, pp. 2, 5, 
 138. 148, 171. • yy > • 
 
 Logan, W. E.— "Geology of Canada," Geol. Surv., Can., 1863, p. 837. 
 
 Obalski, J. — "Report of the Commissioner of Crown Lands for the pro- 
 vince of Quebec," 1895, pp. 61-62. 
 
 Ries, F.— "Kaolin .^ar Huberdeau, Quebec," Geol. Surv., Can., Sum, 
 Rept., 1911, pp. 229-231. 
 
 Selwyn, A. R. C— CJeol. Surv., Can., Rept. of Prog., 1870-71, p. 7. 
 
CHAPTER II. 
 
 PHYSIOGRAPHY. 
 
 GENERAL STATEMENT. 
 
 The St. Renii district lies close to the border zone between the great 
 Pre-Cambrian upland of northeastern Canada and the extensive lowJiod 
 which forms the central part of the lower St. Lawrence basin. Thus, 
 it exhibits most of the characteristic topographic features of the Laurentian 
 highlands, but is distinguished from other parts of the Laurentian upland 
 by greater dissection and by the presence of post-glacial marine clay and 
 sand deposited in the bottoms of its major depressions. 
 
 For the purpose of topographic description the district falls naturally 
 into four areas: (1) the St. Remi flat, (2) the Rockway flat, (3) the rocky 
 uplands, and (4) the drift covered uplands. 
 
 ST. REMI FLAT. 
 
 The St. Remi flat occupies the bottom of a deep valley which extends 
 in a southwesterly direction diagonally across range VI and adjacent 
 portions of ranges A and B in Amherst township, and is a northern continu- 
 ation of the wider flat which extends along Maskinonge river. It has 
 an elevation of 701 feet above sea-level' and is underlain by silt, clay, 
 and sand. The surface of the flat, or the whole, is uniform and plain- 
 like, but is interrupted here and there by knobs and ridges of bedrock and 
 glacial urift and by shallow basins occupied by marshy lakes (Plate 
 II A). With the exception of a small area in the southwestern part of the 
 district traversed by Maskinonge river, the drainage of the flat is 
 effected enti'.'ely by Pike creek, a stream of considerable size originating 
 in a series of lakes situated farther to the north outside the area examined. 
 A well developed terrace between 15 and 20 feet in height has been formed 
 on the east side of Pike creek in lots 1, 2, and 3, range VI, north and south, 
 Amherst township. 
 
 Although marine shells or other positive evidence of the marine origin 
 of the deposits underlying the St. Remi flat were not found in the district 
 examined, the presence of marine clay and sand in adjoining districts 
 at higher elevations* indicates tbnt they represent material la down 
 during the Cham plain marine submergence. 
 
 BOCKWAY FLAT. 
 
 The Rockway flat occupies an extensive area in the southeastern part 
 of Amherst township and adjacent parts of Ponsonby township. It is 
 similar in character to the St. Remi flat, but has a somewhat lower eleva- 
 tion (663 feet above sea-level at the village of Rockway)*. Only the north- 
 western part of the flat lies within the boundaries of the district described 
 in this I'eport 
 
 •White. Jam<M, "Altitudea !b Caaada," p. 212, Commiauon of Coiaervatioa,'CaBada, I»l». 
 
 '73.S i(wt above sea-ievel northwest of Laehule. 
 
 ' White, Jamea, "Altitudea ia Caaada," p. 212, CommiasioE of Coaaervation, Caaada, IMS 
 
ROCKY UPLANDS. 
 
 The rocky uplands include the elevated rocky parts of the district 
 and are characterized by a minutely rugged topography, numerous irregular 
 lakes, precipitous water courses, and other features typically developed 
 in the Canadian Laurentian highlands. In most localities these upland 
 districts correspond approximately in form to the batholithic masses of 
 granite or syenite which occur so abundantly in the Pre-Cambrian complex 
 of the region, but in places they are underlain by the garnet gneiss member 
 of the Grenville series or by pyroxenic gneiss belonging to the Buckingham 
 series. The maximum elevation of the upland areas in the St. Remi 
 district is approximately 1,300 feet above sea-level. 
 
 DRIFT COVERED t'PLANDS. 
 
 The drift covered uplands include those areas in the district — generally 
 intermediate in elevation between the rocky uplands and the marine 
 flats — in which the bedrock surface is almost completely covered by glacial 
 drift (Plate II A). The most extensive upland of this type occurs in the 
 vicinity of the china clay deposits of the Canadian China Clay Companv 
 in the southern part of range VI, Amherst township. The drift covered 
 area in this district has an average width of approximately half a mile and 
 a length from north to south of 3 miles. It has an elevation ranging from 
 800 to 900 feet above sea-level. 
 
CHAPTER III. 
 
 GENERAL GEOLOGY. 
 
 GENERAL STATEMENT. 
 
 I,- ui^*^ ""^^^ abundant rocks in many localities throughout the Lauren tian 
 highlands of southeastern Ontario and Quebec belong to a group of highly 
 metamorphosed sediments: crystalline limestone, garnet gneiss, and quartz- 
 ite, constituting what is generally known as the Grenville series. This 
 region IS thus distinguished from other parts of the Canadian Pre-Cambrian 
 upland by the presence of this series of sediments, and for that reason has 
 been designated the Grenville Pre-Cambrian subprovince. The St. Remi 
 district in Amherst township, Quebec, lies in the midst of this subprovince, 
 and includes not only the rocks of the Grenville series but many of the 
 otLer rock types commonly represented in the Grenville belt. 
 
 TABLE OF FORMATIONS. . 
 
 The buccession of formations present in the district, arranged in 
 descending order, is as follows: 
 
 Quaternary ChamDlain Gravel, sand, and clay. 
 
 ?.!.„<-. u • Glacial Boulder clay, gravel, and sand. 
 
 Late Pre-Cambrian Diabase. •" "^ ' 
 
 Early Pre-Cambrian '.'.'..'. Granite^yenite gneiss. 
 
 Metamorphic pyroxenite. 
 Buckingham series: 
 Pyroxenite (igneous). 
 Ciabbro. 
 
 Pyroxene diorite. 
 Pyroxene syenite. 
 Grenville series: v 
 
 Quartzite. 
 Garnet-gneiss. 
 Crystalline limestone. 
 
 BASAL COMPLEX. 
 
 With the exception of the unconsolidated Quaternary deposits and a 
 single dyke of diabase, all the rocks observed in the district mapped belong 
 to those ancient Pre-Cambrian formations which because of their highly 
 deformed or otherwise metamorphosed condition are commonly grouped 
 together as the basal complex. The detailed succession of formations 
 withip this complex, as represented in eastern Ontario and the southern 
 Laurentians of Quebec, has not yet been completely worked out, but the 
 results of investigations in scattered localities seem to indicate that four 
 principal groups of rock are represented, as foliows: (1) a group of recrys- 
 talhzed marine sediments known as the Grenville series; (2) a group of 
 Igneous pyroxenic rocks— gabbro, anorthosite, pyroxene syenite, etc 
 intrusive into the Grenville series; (3) batholithic masses of granite and 
 
syenite intrusive into the rocks of groups 1 and 2; and (4) nmsscs of diop- 
 side, Bcapolite, and other lime-silicate minerals known as " nyroxenite ", 
 formed by the contact action of rocks of groups 2 and 3 on the limestone 
 member of the Grenville series. 
 
 ORKWILLE HERIEH. 
 
 The oldest rocks observed to be present in the St. Remi district, as 
 elsewhere throughout the Grenville Pre-Cainbrian subprovince, l>elong 
 to the Grenville scries. This series of rocks is believed to have Ijocii 
 originally laid down as alternating l)eds of shale, sandstone, and limestone 
 .nimilar in every respect to marine sedimentary formaticns laid dowt) in 
 later geological periods, but owing to the metamorphism to which they 
 have l)een subjected, the limestone has been transformed to crystalline lim«^- 
 stone, the shale to garnet gneiss, and the sandstone to vitreous quartzite. 
 
 Cryslalline Limestone. 
 
 Distribution. Crystalline limestone was observed in two localities 
 within the area included in the accompanying map, namel}': ^n the slope 
 of the upland area occurring at the cast end of lot 5, range V, .south, 
 Amherst township; and in the district adjacent to the graphite deposits 
 occurring in lots 15, 16, and 17, range VI, Amherst towrship. 
 
 Lithological Character. The Grenville limestone occurring in St. 
 Remi district, in its typical outcrops consists of fragments and crumpled 
 bands of rusty grey gneiss inclutled in a matrix of medium to coarse- 
 grained calcite in which grains of green pyroxene and tlakes of graphite 
 are abundantly disseminated. The rusty gneiss inclusions, when studied 
 in thin sections under the microscope, were found to vary considerably 
 in the different occurrences. In one thin section examined the rock con- 
 sisted of granular quartz, orthoclase, microcline, and plagiodase (having 
 the optical properties of Al)7 Anj), throughout which a few grains of pale 
 green pyroxene, titanite, and apatite were disseminated. In several 
 other thin sections, however, the principal constituents were orthoclase, 
 plagiodase, pyroxene, and scapolite; the le.sa common constituents we.t: 
 titanite, apatite, pyrrhotite, and graphite. The first rock type thus had 
 the composition of an aplite or pyroxene granite, whereas the other types 
 were scapolitic pyroxene syenite. All of the inclusions are fine-grainetl 
 but variable in texture, the individual mineral grains ranging from • 1 
 mm. to 2 mm. in diameter. The limestone matrix in which the fragments 
 and bands of pyroxene granite and syenite are enclosed was seen under 
 the microscope to consist chiefly of grains of pyroxene and scapolite enclosed 
 in a calcite matrix. The less common disseminated constituents were 
 pyrite and graphite. 
 
 Garnet Gneiss. 
 
 Distribution .' The garnet gneiss occurs partly in small lenses and bands, 
 intcrlaminated with quartzite and pyroxene gneiss, and partly in more 
 extensive masses, throughout which the other rocks of the basal complex 
 have been more or less intimately intermingled. Occurrences of the first 
 type are common in the areas indicated on the map in the central part 
 
 61858—3 
 
of lotB 4, 5, 6, and 7, range VI. south, and in IoIh 23, 24, and 25, ranRCH A 
 and B, AmherHt township. The areaH of the second type He alona the 
 western border of the area mapped. These include a brRc proportion 
 of pyroxenic gneiss and granite-syenite gneiss, as well as intermediate 
 types possibly the result of the interaction of these intrusions with nurnpt 
 gneiss. " 
 
 Lilhological Character. The outstanding characteristic of the garnet 
 gneiss as seen in the hand specimen or on the surface of its outcrops, is the 
 heterogeneous ar x>arance which it presents' (Plate IIIA). This heter- 
 ogeneity may a .« in part from variations in texture, and in part from 
 variations m composition, but chiefly from the occurrence of the individual 
 minerals in aggregates. The principal mineral constituents generallv 
 vi8it)le in the rock arc garnet, quartz, feldspar, mica, and pyrite, but the 
 proportions of these constituents is exceedingly variable. Thus in some 
 thin sections of the rock examined quartz was entirely absent and ortho- 
 clase or orthoclase and plagioclasf- were the sa'.ic constituents, whereas 
 in others orthoclase or plagioclase were subordinate in quantity and 
 quartz was abundant. The garnet contained in the rock occurs as numerous 
 large, irregular grains, traversed by numerous fractures. The orthoclase is 
 commonly filled with perthitic inclusions too minute for definite determina- 
 tion. Ihey have a refractive index higher than the orthoclase, and in 
 some sections are in the incipient stages of alteration, features which indicate 
 that they are probably plagioclase. Plagioclase when present in the rock 
 in individual grains usually exhibits the optical properties of andesino. 
 Ihe biotite is a light yellow to red brown variety and is generally abundant. 
 It usually occurs m aggregates, but in one thin section was observed to 
 lie in the interspaces between the feldspar grains. Sillimanite, which is 
 generally a common constituent of the garnet-gneiss, was observed in 
 only one of the thin sections prepared from specimens of garnet gneiss 
 collected in the St. Re- . district— namely that taken from the new shaft 
 on lot 5, range \ I, south, Amherst township. 
 
 QuarUite. 
 
 DMbutiun. The Grenvillr quortzite has its principal development 
 in a north-south zone extending through the western part of range VI, south 
 Amherst_ township. In this locality, excavations through the drift have 
 
 •j!^iP *"?t Informs a continuous mass, approximately one-half mile in 
 width and 3 miles in length. 
 
 Lilhological Character. In those localities where the quartzite has not 
 
 beo" granulated by deformation it presents a white, vitreous, massive 
 
 ai ance, very similar to vein quartz. Its bedded character is indicated 
 
 ! .ees by its interlamination with garnet gneiss and with beds containing 
 
 irger proportion of impurities than the normal quartzite. Under the 
 
 icroscope the rock is s^en to consist mainly or entirely of irregular grains 
 of quartz, averaging roximately three-quarters of a millimetre in 
 diameter. In some i actions a few flakes of pale yellow to red brown 
 biotite were observed; i.. Jthers, flakes of muscovite; and in one, plagioclase 
 having the optical properties of andesine. The biotite and muscovite 
 lie along the contacts of the quartz grains, a feature indicating that 
 
they have poiwibly been introduced into the quartz Heoonclarily. 
 a few aectionfl the quarts waH obitcrved to contain hair-liice incluHiouK. 
 far on wan obnerveil, th(>8e did not have any definite orientation. 
 
 Structural Helationn. 
 
 In 
 
 . The outMtnnding structural features exhibited by the rocks of the 
 Grenville fteries are the effects which narently rcHuit where aHsociated 
 rockn of varying competency undergo ...a-nne deformation under extreiii' 
 conditions of temperature and pressure. If a rock of low competency— 
 HU» h as limestone — into which dyUes of granite or other igneoas rocks have 
 been intrwied, or with which IkmIs of quartzite or garnet gneiss are inter- 
 stratified, were subjecte<l to deformation under conditions of high 
 temperature and pressure, it would seem probable that the associateil 
 dykes or beds of more competent rock wouhl break up into fragments and 
 l)ecome scattered through the limestone as inclusions. On the other hand, 
 if garnet gneiss or quartzite with which l>eds of limestone are interst ratified 
 at intervals were similarly deformed, it is apparent that the less competent 
 limestone member wouUf tend to flow to those points where the pressure 
 was leas* intense, and that a l)ed formerly uniformly continuous would 
 Income liroken up into detached masses. All of the preceding processes 
 were evidently in operation when the rocks of the fJrenville series were 
 deformed; foi tl.e crystalline hmestone is filled with inclusions of other 
 rocks, anti occurs everywhere in detached, irregular masses rather than in 
 continuous bands; and even the more competent quartzite and arnet 
 gneiss in many places exhibit a similar phenomenon, the ({jartzite occurring 
 as lenticular masses enclose<l in the gneiss. 
 
 The intrusive relationships of the rocks of the Buckingham series, 
 and the bathoUthic granite and syenite to the (Jrenville series is rather a 
 matter of inference than direct observation, for dykes of the latter definitely 
 intrusive into the (Jrenville series were not observed anywhere in the 
 St. Remi district. Since, however, these are clearly igmH>us rock types, 
 and the Grenville series is of sedimentary origin, it is inferred from the 
 occurrence of the gabbro, pyroxene syenite, pyroxene diorite, and granite- 
 syenite bands alternating with the Grenville sediments, from the mcta- 
 morphism they appear to have effected in places, and from their occurrence 
 as inclusions up to 50 feet or more in diameter in the limestone, that they 
 have been intruded as sills, dykes, or lit par lit injections into the Grenville 
 series, and that their intrusive relationships have since been obliterated 
 by deformation. 
 
 The relationships of the Grenville series to the rocks which precede 
 them, up to the present have not been observed anywhere within the 
 Grenville subprovince. It is obvious that a floor upon which these sedi- 
 ments were deposited was at one time present in the region, but observa- 
 tions would seem to indicate that it is either not now exposed or has been 
 obliterated by igneous intrusion and deformation. 
 
 Origin. 
 
 It is believed that the rocks of the Grenville series represent a group 
 of marine sediments originally laid down as alternating beds of shale, 
 sandstone, and limestone, and that as a consequence of the intense meta- 
 
 61880—3} 
 
10 
 
 inorphwin to which the ierien hu been iiubjected, the lime«tone hM \iera 
 Jran«tfonne<l to cryntalline limeiitone, the Mhale to (carnet RneJM, and the 
 ■amlHtonc to vitreouH quarti. The reaNonH for these eonrliMionH are: 
 (J) the aiwociation of the niekn of the wries ax iiiterst ratified \ml» nimilar 
 to the manner in which marine sedimentarv deponitH UNually occur, and 
 1 ' 9.""""'*' ""alyw of the garnet gneixH HhowH that thin rock in every 
 detail haw the chemical componition of a nhale. ho that the three rock typet> 
 garnet gneiiw, quartxite, and limentone have rexpertively the chemical 
 rompoKition of the three dominant memlien* of the normal marine Hcdi- 
 montary serien of the well M>rted Jypen. 
 
 BUCKI.VUHAM HEHIEM. 
 
 ^ti 
 
 I 
 
 General Statement. 
 
 In most localities throughout the eastern part of the (irenville hu\f 
 province, m .ses of gabbro, pyroxene-<liorite. pyroxene-«yenite, anorthosite, 
 and related rocks occur, which although varying in composition from 
 syenite or even granite to peridotite, have so many features in common as 
 to indicate that they are genetically related to one another. The rocks of 
 this group all have a granular texture, contain a pink to pale green niono- 
 chme pyroxene as their most abundant ferromagnesiai. constituent, and, as 
 far as their relationships have liecn observed, appear to l»e younger than 
 the Grenville series and older than the batliolithic intrusions of granite- 
 syenite gneiss. In consideration of the wide extent of these rocks, their 
 peculiar mineralogical composition, their evident genetic relationship to 
 one another, and their probable approximate contemporaneity in age 
 they have l«<>n grouped together as the Buckingham scries. In the St. 
 Remi district the Buckingham series is represented almost entirely by an 
 acidic gabbro. but outcrops of pyroxenite, pyroxene-fliorite, pyroxene 
 syenite, and p> loxene granite were also observed. 
 
 Distribvtion. 
 
 The rocks composing the Buckingham sfries are exposed in the 
 iSt. Hemi area partly in bolts interbanded with garnet gneis.s, and partly 
 as .scattered outcrops protruding through the marine flat that extends 
 along Pi! ^ '•reek and Maskinonge river. Occurrences of the first type 
 were ob.served in a northeasterly trending belt from 1,000 to 2,000 feet 
 wide, extending diagonally across the northwest corner of the area mapped, 
 and in the central part of the ridge of garnet gneiss outcropping at the south 
 end of lot 24, range A, ' mherst town.ship. The smalj scattered kno»)s 
 occur at the north end of lots 24 and 25, range A, at the west end of lot 7, 
 south, and lots 2 and 3, north, range V, and at the ea.st end of lot 3. range 
 IV. Amherst township. 
 
 Lithological Character. 
 
 Pyroxene Syenite. Rocks belonging to this class were observed in two 
 outcrop.*, one adjoining the south .side of the road leading west from 
 St. H.ini villagf on lot 3, range \', north, and the other adjoining Maskinonge 
 river at the west end of lot 7, south, in the same range. It consists of 
 
11 
 
 orthtM'laiir containing p«>rthitif ini'tuMionH of i>l»i^oclaM<. pink pyroxene 
 uimuMt romplpt<>ly altrre*! to olivi'-Rropn amphibolf, a fpw HcattoriHt flttln'w 
 «>f rrd-brown mini, and iliNHrminatrd Krainx of apatite and maKnetitc. 
 
 Pyroxene IhoriU. The name pyr«»xpn»' dioritr hax IwN'n appii«><i to 
 the rook eomtioHinR the knohn outeropping wittt of Pike en-ek on U»tH 2 
 and 3. ranRett IV and V, Amherxt townnhip. In the hand H|N>einien thin 
 roi'k reHenibleH the Ra>>l>ro memtierM of the Herien ol)Herve<l farther t»> the 
 ^outh, except that it contains a large proportion of feidxpar ami (■orreN|M>nii- 
 ingly iii«M pyroxene. A thin Hection of the rwk exumine<l under the 
 mieroHcop*' wu« wen to conxiKt chiefly of pah> green to pink pyroxene and 
 plagioclaM* (AI>,| An^,) hut titanite. apatite, and magnetite were also 
 present at* diHHeniinated crainw. 
 
 (inbbro. The i;at)hro meml)er of the Buckingham Heries repre!<ented 
 in the St. Remi area i.H a medium to ioanM'-graine<l, masHive to foliateii 
 rock, in which black pyroxene and a rt^xinoux l(Kjking feltlxpar are the nioMt 
 conxpicuouH conxtituents. When examined in thin xectionx, the rcM-k wax 
 found to contain the following conxtituentx: pyroxene, umphibole, plagio- 
 claxe, biotite, apatite, and magnetite. The pyroxene ix a red to pale green 
 variety, having an extinction angle in wctionx parallel the optic plane of 
 35 degreex. It ix generally more or lexx altered along the margin of the 
 individual cryxtalx to a compact, pale yellow to oliv«>-grcen umphibole. 
 The plagioclaxe poxxexxj'x the optical prop«'rtiex corres|)onding to the 
 i-ompoxition Abg4 .^nj*. and hence might be dexignated an amlexine- 
 labradorite. In xome thin xectionx the plagioclaxe wax o'.iserved to contain 
 a few perthitic incluxionx of a colourlexx mineral with conxidtrubly lower 
 refraction index, probably orthoclaxe. Biotite ^ not an abundant con- 
 stituent of the rock, but a few flakex an* generally prexent. These are 
 pale yellow to red brown in colour, and in xome xectionx were observed to 
 be embedded in the pyroxene. The magnetite occurs as numerous, 
 irregular grains scattered through the rock. It is pn>bable ♦hat this is n 
 titaniferous variety, similar in composition lo the larger inasses of this 
 mineral pn-sent in the gabbro in many districts. The texture of <he gabbro 
 ix seen under the microscope to vary in difTerent localities, for : some thin 
 sections the variou.s mineral grains appear to be approximately uniform in 
 size, whereas in others large crystals of pyroxene and feldspar occur 
 embeddefl in a matrix of fine, granular feldspar. Th'- e relationshijw 
 seem to indicate that the rock has been granulated in places. 
 
 Pyroxenile. Throughout the northern part of the zone of pyroxene 
 gneiss, extending diagonally across the northwest-rn part of the area 
 mapped, numerous scattered masses of .oarse pyroxenite up to .iO feet or 
 more in diameter are included in gabbro and constitute from 25 to 50 p<»r 
 cent of the whok. These are not sharply defined inclusions, but fade into 
 the adjoining rock by a gradual decrea.'^e in the proportion of pyroxene 
 present. In one locality, however, small dykes of gabbro were observed 
 to intersect and to connect across the pyroxenite ma.ss. Lithologically, 
 the pyroxenite consists of closely compacted, coarse crystals of pyroxene 
 up to 2 inches in diametir, the interspaces between which are filled with 
 plagioclase. The rock thus is mineralogically similar to the gabbro, and 
 differs from it merely in the relative abundance of the constituent mineral 
 present. It seems ivideat, therefore, that the pyroxenite member of the 
 
12 
 
 HuckinRhum series is genetically related to the gahhro member, and has 
 been segregated froni it by differentiation. 
 
 Other Related TypcH. In several localities a number of rocks contain- 
 ing pyroxene were observed, which are jwssibly either phases of the 
 Riickingham series, or are intermediat»! tyjM's resulting; from the interaction 
 of the rocks of the Buckingham series with the garnetiferous member of 
 the (Irenville series. A fine grey gneiss in which garnets are sparsely 
 disseminated is exposed on the face of the escarpment adjoining the west 
 shore of Lavigne lake. When examined under the microscope, this rock 
 was found to consist of numerous, angular grains of quartz, orthodase, 
 pale green to i)ink pyroxene similar to that contained in the gabbro of the 
 Huckingham series, and a few di.sseminated grains of red garnet. • 
 
 According to its mineralogical composition this rock is a garnetiferous 
 pyroxene granite, and hence; may represent another member of the 
 Buckingham series. It might be possible, however, that it is merely the 
 garnet gnei.ss member of the Grenville series, into which emanations 
 derived from the gabbro of the Buckingham series have penetrated. 
 
 Another peculiar rock related to the Buckingham series occurs on the 
 ridge of banded garnet gneiss (Plates IIIB and IV') that outcrops on the 
 north shore of I.iavigne lake. This rock under the microscope is seen to 
 consist of pink jjyroxene partly altered to olive green amphibole, red brown 
 mica, labradorite, and numerous large, angular grains of red garnet. It 
 thus differs from the normal gabbro of the Buckingham .series merely in 
 the presence of the garnet, and in the greater abundance of the mica 
 present. It is possible that this garnetiferous type has been formed by 
 the interaction of the gabbro member of the Buckingham series with 
 garnet gneiss, but if sucli were the case, it might be presumed that the 
 resulting rock type could l)e more acidic in compo.sition than the normal 
 gabbro. It is, therefore, more probable that it is merely a garnetiferous 
 phase of the galibro. 
 
 Structural Helations. 
 
 Internal. The most common internal structural feature exhibited by 
 the rocks of the Buckingham series is the occurrence of the ferromagnesian 
 antl feldspathic constituents in aggregates so that the rocks present a 
 heterogeneous ai)pearance. This phenomenon is strikingly illu.strattnl by 
 the mas.ses of pyroxenite included in gabbro observed in the northwestern 
 part of the area mapped. 
 
 The other members of the .series, gabbro, pyroxene syenite, and 
 ))yroxene diorite occur in separate outcrops, so that their relationship to 
 one another was not ol)served, but it is probable that they belong in part 
 at least to .neparate masses intruded into garnet gneiss belonging to the 
 (Irenville .series. 
 
 In these cases, therefore, it is probable that the differentiation of the 
 syenite and gabbro from the original magma occurred before the ma.s-ses 
 were intruded. 
 
 External. It was inferred in the discussion of the structural relation- 
 ships of the (irenville series that the rocks of the Buckingham series had 
 been intruded into the (Irenville series, l)ut that the direct evidence of 
 intrusions had l>een largely oljliterated l)y deformation. They occur most 
 
13 
 
 commonly as liands interlaminated with the rocks of the (Jrenvillc scries 
 and apparently conform in the main to the stratification in these rocks. 
 It is probable, therefore, that they were intruded as sills. 
 
 Correlation. 
 
 After completing the examination of the St. Hemi areas, the writer 
 made a short reconnaissance between Montfort on the Huberdeau branch 
 of the Canadian Northern railway, and Piedmont on the Mont Laurier 
 branch of the Canadian Pacific railway, for the purpo.se of comparing the 
 rocks of the Buckingham series with tho.se mapped as anorthosite i)y Sir 
 William Logan.' 
 
 It was found that the area indicated as anorthosite in this secti<m, in 
 reality consisted of zones of pyroxen*; diorite, pyroxene-quartz monzonite, 
 and anorthosite interbanded with and intruded by granite gneiss. It 
 would seem evident, therefore, that in places at least, the anorthosite of 
 Logan included a large proportion of other pyroxenic rocks, and that the 
 Buckingham series and the rock clas.sed as anorthosite in this locality by 
 the early geologists, have the same geological relationships and are probably 
 equivalent in age. 
 
 METAMORPHIC PYROXENITE. 
 
 Throughout the Grenville belt, masses of rock consisting of diopside. 
 scapolite, woUastonite, titanite, tourmaline, and other minerals^of the lime 
 silicate or pegmatitic class, to which the name pyroxenite has been generally 
 applied, are commonly associated with the limestone member of the 
 Ctrenville series. Since th»'se masses, however, are believed to have been 
 formed by the interaction of siliceous solutions with the limestone member 
 of the Grenville .series, the name metamorphic pyroxenite is used by the 
 writer. 
 
 Rocks of this class were observed in the St. Remi area in as.sociation 
 with the graphite deposits on lots 15, 16, and 17, range VI, Amherst town- 
 ship (Plate VII), and in a cut on the Canadian Northern railway at the 
 point where the railway line intersects the northern edge of a granite ridge 
 on lot 15, range VII, south, Amherst township. 
 
 The rock associated with tin- graphite deposits cons'sts predominantly 
 of woUastilnite with pyroxene, scapolite, orthoclase, titanite, and graphite 
 as less abundant constituents. In the occurrence on lot 15, range VII, 
 south, on the other hand, the dominant mineral is a green diopside, with 
 which scapolite is intergrown in places. The other minisrals ol)served to 
 be present were calcite, titanite, tourmaline, and pyrite. 
 
 In some localities within the Cirenville belt, the relationships of the 
 metamorphic pyroxenite are such as to indicate that the solutions by 
 which the rock was formed emanated from the intrusives of the Bucking- 
 ham series. In other localities, however, similar rocks are present which 
 are evidently related to the later batholithic intrusions of granite and 
 syenite. The woUastonite rock, in which the graphite on the property of 
 (Jraphite, Limited, lots 15, 16, and 17, range VI, Amherst township, is found, 
 
 ■ Map in atlaa acoompsnying the Geology of Caiuda, 1803, ahowiag the diatributioB of {.aurentian rocks in 
 parts of the counties ' * Ottawa, Tenvbonne, .\ricenteuil, aad Two Mountains. 
 
14 
 
 occurs as contact zones bordering masses of pyroxene granite which, 
 probably, represent a phase of the pyroxenic gneisses, so that the meta- 
 morphism in this case is evidently related to the Buckingham series rather 
 than to the later batholithic intrusives. The mass of pyroxenite exposed 
 in the cut on the Canadian Northern railway, on the other hand, adjoins 
 the younger porphyritic quartz syenite belonging to the batholithic group 
 and passes transitionally into it by a gradual decrease in the proportions of 
 pyroxene present, a relationship which might result from the interaction 
 of the igneous rock with the limestone. It is possible, therefore, that this 
 nnass of pyroxenite may be related in origin to the later batholithic intru- 
 sives. It has, nevertheless, been placed in the legend of the accompanying 
 map as older than these rocks, because in most localities in the eastern 
 part of the Grenville belt the pyroxenite is known to occupy this strati- 
 graphical position. 
 
 GRANITE-SYENITE GNEISS. 
 
 General Statenii '4. 
 
 The granite-syenite gneiss member of the basal complex is widely 
 represented throughout the Grenville subprovince in batholithic masses, 
 basses, and dykes intruding the rocks of the Grenville and Buckingham 
 series which preceded them. In most districts the rocks of this class are 
 represented by two phases— a coarse porphyritic type and a fine aplite-like 
 variety; but in the St. Remi district, only the former was observed. 
 
 Distribution. 
 
 Within the area mapped, the batholithic intrusions occur in two 
 principal areas, the eastern and northeastern part of the district and the 
 southern part of range \\, Amherst township. A few detached masses 
 also outcrop close to the southea> rn border of the area. These, however, 
 may possil)ly be connected with the larger masses beneath the overlying 
 drift. 
 
 Lithological Character. 
 
 The granite-syenite member of the basal complex in tha St. Remi 
 district is generally a coarse porphyritic rock consisting of phenocrysts of 
 orthoclase up to an inch or more in length, embedded in a matrix of fe' ' par 
 or feldspar and quartz and small quantities of ferromagne.sian minerals. 
 A thin section prepared from a specimen of a porphyritic granite that 
 outcrops in a cut on the Canadian Northern railway, on lot 12, range 
 VII, south, Amherst township, was found under the microscope to consist 
 of orthoclase, containing small perthitic inclusions, plagioclase, quartz 
 biotite, amphibole, titanite, apatite, and iron oxide. The plagioclase 
 present in the rock is easily distinguishetl from the associated quartz and 
 orthoclase by its slightly decomposed condition. It has the optical pro- 
 perties of andesinc. The quartz is very abundant in the rock, occurring in 
 large, irregular grains in which numerous hair-like inclusions are dissemi- 
 nated. As far as was observed, these have no definite orientation with 
 respect to the crystallographic directions of the quartz. The biotite is u 
 
15 
 
 pale yellow to red brown variety occurring either in association with the 
 amphibole or in minute flakes disHeminated through small areas of granular 
 quartz and feldspar. The amphibole occurs in large, irregular grains up 
 to 1 mm. in diameter. It is pale yellow to light green and is generally 
 more or less decomposed. 
 
 Structural Relationships. 
 
 Internal. The porphyritic granite and syenite occurring in the St. 
 Remi district is a comparatively ma.ssive type in which the foliation is 
 scarcely discernible except in a few local areas, as for example, in the rock 
 mass exposed on the Canadian Northern railway, on lot 13, range VII, 
 south, where a typical augen structure has been developed. The trend of 
 the foliation conforms in general to the local trend of the different parts 
 of the batholithic ma.ss. Thus in the region adjoining the western border 
 of the quartzite belt in range VI, south, the t.end of fohation is north- 
 westerly, whereas in areas adjoining the valley of Pike creek in the 
 north n part of the district it is northeasterly. 
 
 External. The study of the structural relationships of the batholiths 
 of granite and syenite gneiss in other parts of the Grenville subprovince 
 has shown that these masses are distributed in norths ^terly trending zones 
 and have made room for themselves partly by thrusting aside the older 
 rocks and partly by lit par lit injection along the planes of bedding and 
 foliation in the older rocks. In the St. Remi district it may be observed 
 from an examination of the accompanying map that the foliation in the 
 batholithic masses of granite and syenite parallels the structural trend of 
 the adjoining rocks of the Grenville and Buckingham series and that the 
 older rocks apparently dip under the batholiths along their eastern border 
 as if the granite and syenite had been intruded in the form of huge sills. 
 It is more probable, however, that these relationships are in reality the 
 result of deformation; for the batholiths occurring in the St. Remi district 
 are merely parts of a huge massif which it is believed was intruded into the 
 rocks of the Grenville and Buckingham series as an accompaniment of a 
 mountain building crustal movement, and under such > ;iditions, the 
 offshoot batholithic masses after their intrusion would be subjected to the 
 same deformation as the intruded rocks and might thus be forced into a 
 conformable attitude. In the St. Remi district the rocks of the basal 
 coniplex apparently lie on the southeastern limb of a northeasterly trending 
 anticline, the strike being generally northeasterly and the dip southeast -^rly, 
 but the belt of Grenville quartzite in which the kaolin is found apparently 
 became detached from the main mass of the Grenville series and assumed 
 a north-northwesterly structural trend. 
 
 Correlation. 
 
 The bathoUthic granite and syenite occurring in the St. Remi district 
 forms a part of the complex originally classed as Laurentian by Sir William 
 Logan and probably belongs to the Laurentian as this term has been defined 
 by the Geological Survey in eastern Ontario and southern Quebec, but in 
 recent years an attempt has been made to classify all the Pre-Cambrian 
 granitic rocks of the St, Lawrence basin as belonging to two and onlv two, 
 
 61859-4 
 
16 
 
 periods of intrusion, Laurentian and Algoman, an assumption theoretically 
 improbable, and proved by observations in the field to be untrue.' The 
 use of the term Laurentian in this report might, therefore, imply a corre- 
 lation with similar rocks in other parts of the Pre-Cambrian complexes of 
 the St. Lawrence basin that is unwarranted. 
 
 LATE PRE-CAHBRIAN IJfTBUSIVES. 
 
 Diabase. 
 
 Along the southern border of the Laurentian highlands adjoining the 
 lower Ottawa and lower St. Lawrence rivers a remarkably uniform system 
 of diabase dykes extends continuously for nearly 200 miles. Although 
 the individual dykes belonging to this system are generally not more than 
 200 or 300 feet wide, yet some of the dykes are known to continue without 
 interruption for at least 100 miles. In the St. Remi district, as far as was 
 observed, only one dyke of this class is represented. This intersects the 
 south end of the gabbro ridge outcropping on lot 24, range A, Amhe-^t 
 township. It is approximately 40 feet in width, outcrops for 600 feet 
 along the strike, and has the usual east-west trend and lithological character 
 of the dykes of the system to which it belongs. 
 
 gUATERNARl". 
 
 Gktcial 
 
 In common with the Laurentian highlands generally, the bedrock 
 surface in this region is overlaid by an irregular mantle of glacial debris. 
 This consists chiefly of boulder clay, sand, and gravel distributed partly in 
 well-defined esker-like ridges, but mainly in thick, irregular masses. The 
 most extensive area of this material occurs in the drift covered upland 
 lying in the western part of range VI, Amherst township; the most striking 
 of the esker-Uke ridges is that indicated on Map 1681 as extending diagon- 
 ally across lots 1, 2, and 3, range V, south, Amherst township. 
 
 The direction of glacial movement in the St. Remi district, as indicated 
 by the glacial striae, was approximately from north to south. The presence 
 of the kaolin deposits possibly affords a very definite estimate of the 
 amount of material eroded from the surface of the Laurentian plateau by 
 the continental ice-sheets in this locaUty, for it is possible that these deposits 
 have been formed by the residual downward concentration of kaolin 
 resulting from surface weathering, and if the deposits have orginated in 
 this manner, then the erosive action of the continental glaciers was scarcely 
 more than sufficient to remove the weathered debris from the bedrock 
 surface. It is pointed out in Chapter IV, however, that it is also possible 
 that the kaolin contained in the St. Remi deposits has been brought up 
 from a deep-seated source by thermal waters ascending along the zone of 
 faulting and fracture in which the kaolin occurs. 
 
 Bomemlature in the St. Uwrence bmiii,' Jour. Geol., vol. XXVI, 1918, pp. 32}-333. ™-oau.uruui 
 
17 
 
 Marine Clay and Sand. 
 
 Throughout the lower part of the St. Lawrence basin generally, the 
 glacial and older formations are overlain by stratified clay and santl which 
 contains marine shells and which forms extensive flats in depressions 
 within the Laurentian highlands up to points over 100 miles from its 
 southern border. The maximum elevation at which these deposits are 
 known to occur in the Ottawa valley is approximately 735 feet. Within 
 the district described in this report, two flats of this class underlain l)y 
 gravel, sand, siit, and clay occur, the upper of which, the St. Remi, has an 
 elevation of 701 feet, and the lower, the Rockaway, an elevation of <)63 
 feet above sea-level. Marine shells or other positive evidence of nuirine 
 origin were not obtained within the deposits themselves, but they are 
 classed as marine because they are uniformly stratifietl deposits lying in 
 depressions opening towards the main St. Lawrence lowland depression 
 to the southward in which the marine deposits occur and lying below the 
 maximum elevation to which these deposits are known to occur. 
 
 6185»-4) 
 
18 
 
 CHAPTER IV. 
 MINERAL DEPOSITS. 
 
 GENERAL STATEMENT. 
 
 The principal rninoial materials of commercial value so far discovered 
 in the St. Remi district arc kaolin, kaolinic quartzite, cornish atone, 
 graphite, phlogopite (amiwr mica), and dolomite. Of these, only the 
 kaolin, kaolinic quartzite, cornish stone, and graphite are known to occur 
 within the area included in the accompanying map. 
 
 KAOLIN, KAOLINIC QUARTZITE, AND CORNISH STONE. 
 
 HISTORY OF DEVELOPMENT. 
 
 In the summer of 1894, Milion Thomas, while digging a well on the 
 farm of Philibert Tasse, encountered kaolin at a depth of 15 feet and sent 
 a small quantity of the material to Richard Lanigan of Calumet, who 
 identified the sample as kaolin and purchased the right to mine the material 
 from the owner of the property. No attempt was made to determine the 
 extent of the deposits at that time, however, and it was not until 1911 that 
 actual development work on the deposits was commenced. 
 
 In the autumn of 1909, Mr. F. R. Lanigan, of Montreal, acquired 
 from the government the mining rights to parts of lots 4, 5, 6, 7, and 8, 
 range VI, south, Amherst township, and in 1911, having leased these rights 
 to Mr. J. C. Broderick of Montreal, formed the St. Remi Kaohn Company, 
 to take over the ownership of the property. In 1911, some development 
 work was performed and the construction of a washing plant begun by 
 Mr. Broderick, and in 1912 the Canadian C^hina Clay Company was 
 organized to continue mining operations under the terms of Mr. Broderick's 
 lease. In 1913 the Canadian China Clay Company purchased the mining 
 rights to parts of lots 4 to 8, range VI, south, Amherst township, from the 
 St. Remi Kaolin Company; the mining rights to parts of lots 2 and 3 
 and additional parts of lots 2 to 8, range VI, south, Amherst township, 
 from the government; and the surface rights to all these lots, from the 
 local owners. Since that time the washing plant on the property has 
 been enlarged, some trenching, stripping, and drilling for the purpose of 
 developing the deposits completed, and several thousand tons of kaolin 
 produced. Prior to 1916 the washed product had to be transported by 
 wagon to Huberdeau, the terminus of the Huberdeau branch of the 
 Canadian Northern railway, but in that year the railway was extended to 
 the china clay deposits so that the cost of transportation from the mine 
 has been greatly reduced. 
 
 The only known deposit of kaolin in the district, outside the area 
 owned l)y the Canadian China Clay Company, occurs near Pike creek, 
 
10 
 
 on lot ,8, range 4, Amherst township, and is owned by Mr. A. Lanigan of 
 Calumet. This deposit, which had l)een known to Mr. Lanigan for a 
 numl)cr of years, was staked by him in December, 1911. 
 
 DISTKIBUTION. 
 
 Deposits of kaolin have Ijeen discovered in the St. Renii clistrict in 
 two localities up to the present time, the j)rincipnl occurrences in a zone 
 approximately 1,000 feet in width extending in a north-northwest ilirection 
 from lot 8 to lot 2, range VI, south, Amherst township, and a single deposit 
 occurring near Pike creek on lot 8, range IV, Amherst township. The 
 latter deposit occupies a position almost directly on the continuation of 
 the principal zone of deposits farther to the south and may be another 
 outcrop on the same zone, but whether or not a connexion exists has not 
 been determined since there are no rock exposures in the intervening 
 distance. 
 
 (iESERAL CHARACTER. 
 
 Lots 2 to 8, Range VI, South, Amherst Township. In the western 
 part of range VI, south, Amherst township, there is a north-south trending 
 drift-covered ridge about one-half mile in width, which intervenes between 
 rocky ridges of granite-syenite gneiss, and from which it is separated by 
 well marked depressions. An examination of the bedrock surface expo.sed 
 in outcrops and in the bottom of trenches, railway cuttings, and other 
 excavations, shows that this ridge throughout nearly its whole extent is 
 composed of vertical or nearly vertical lieds of Grenville quartzite and 
 garnet gneiss, which trend in a north-northwest direction, and that, 
 whereas on the eastern slope of the ridge the quartzite is exceedingly 
 massive and unbroken, on the western slope, throughout a zone approxi- 
 mately 1,000 feet in width, it has been shattered almost everywhere to a 
 friable condition. Within this shattered zone kaolin occurs, finely 
 disseminated between the quartz grains, in veins following the planes of 
 fracture and movement and in more extensive deposits up to 100 feet ii; 
 width and several hundred feet in length. Owing to the presence of the 
 thick overburden of glacial drift which nearly everywhere covers the 
 ridge, the whole extent of the shattered zone in which the kaolin is found 
 has not yet been determined, but sufficient information has been obtained 
 by means of trenches, test pits, and stripping, to indicate that the zone 
 extends in a unoction north 20 degrees west, parallel to the structural 
 trend of the quartzite, and is continuous for approximately 7,000 feet. 
 
 The most extensive deposits of kaolin so far discovered in this 
 shattered zone are lots 5 and 6, where an almost continuous lead of kaolin, 
 ranging from a few feet to 100 feet in width, has been laid bare by stripping 
 and test pits for a distance of 1,400 feet. Bore-holes on this deposit show 
 that it persists to a considerable depth beneath the surface, a depth of 
 150 feet in kaoUn having been attained at one point. Although the kaolin 
 leads everywhere contain considerable quartzite either in the form of 
 fragments or finely disseminated grains, the determination of the amount 
 of kaolin contained in average samples shows that the kaolin content in 
 the masses of kaolin as a whole is not less than 35 per cent. 
 
20 
 
 Lo< 'J 
 
 Ijot 5, roDt of main drpcwit 
 wpHt of main depo«it . 
 Lot« 
 Ixjt 7. 
 
 Irf)( 8. 
 
 ThroUKhout other parts of the Hhntteretl zone numerous kaolin leads 
 ranging from a fraction of an inch up to 65 feet in width have been 
 discovered at several points where the drift cover has lieen removed from 
 the bedrock surface. The deposits of this character so far discovered on 
 the various lots are the following: 
 
 LradH 65 and 12 feet wide in trenrhes. 
 
 Leads 5, 21, and 1 foot wide in test pitH. 
 
 Numerous leadi) from i inch to 4 feet in width. 
 
 Lead in excavation for xpring. 
 
 Lead of kaolin ) iueh in width in broken kaolinicqitartzite 
 
 expcded in cutting on Canadian Northern railway. 
 Half ipch leads of kaolin, in broken kaolinic quartzitc 
 
 exposed in cutting on (Canadian Northern railway. 
 
 At the time the kaolin deposits were examined by the writer in 
 September, 1916, a trench for a pipe-Une had been excavated from the maixi 
 pit to the washing plant of the Canadian China Clay Company, the 
 lH)ttoni of which intersected fractured, kaolinic quartzite for a distance 
 of 133 feet from the wall of the main pit southward. Continuous average 
 samples were taken at intervals of 10 feet along the bottom of the trench 
 and the percentage of kaolin in each sample determined by the loss in 
 weight on removing the kaolin from the crushed material by decantation. 
 The description of the .samples and the percentage of kaoliii contained in 
 each was as follows: 
 
 Feet. 
 
 Description of sample 
 
 
 
 Per cent of 
 kaolin 
 
 Ito 10 
 
 tt leads 1 to i inch wide. 
 4, J-inch leads. 
 
 
 
 141 
 10 
 
 10 to 20 
 
 
 
 20 to 30 
 
 3, }-inch; 1, 2-inch; 1, 4-inch; and 1, 6-inch lead. 
 
 
 16 
 
 30 to 40 
 
 1, (i-ineh and 1, 2-inch lead. 
 
 
 
 11 
 
 40 to 50 
 
 1, (V-inch lead. 
 
 
 
 15! 
 
 50 to 60 
 
 1, 2-inch and 1, S-inch lead. 
 
 
 
 tiOto 70 
 
 I, 4-inch lead. 
 
 
 
 11 
 
 70 to 80 
 
 2, i-inch and 1, 7-inch lead. 
 
 
 
 13 
 
 80 to 90 
 
 1, 2-inch lead and 3§ feet of exceedingly 
 
 quartzite. 
 1, J-inch and 1, 3-foot lead. 
 
 friable 
 
 kaolinic 
 
 15 
 
 90 to 100 
 
 
 
 17 
 
 100 to 110 
 
 \o leads. 
 
 
 
 2 
 
 110 to 120 
 
 Exceedingly friable but no lead.>i. 
 
 
 
 10 
 
 120 to i:jo 
 
 1, 2-inch lead. 
 
 
 
 a 
 
 130 to 133 
 
 No leads. 
 
 
 
 2 J 
 
 .\verage kaolin content for whole section equals 11 J jicr cent. 
 
 Lot 8, Range IV, Amherst Township. At the ea.st end of lot 8, range 
 IV, Amherst township, kaolin is expo.sed in the bottom of a few small pits 
 excavated 011 the bank of Pike creek. The material composing these 
 deposits consists of grains of quartz, aggregates of kaolin, and rusty zones 
 containing (iis.seminated flakes of muscovite. The distribution of these 
 cojistitueiits i.x rciiiarkal)iy similar to that of the constituents composing 
 
21 
 
 the Kr&nitc-KncMB of the reKion, the quartz grains occurring disseminated 
 in a manner similar to quartz grains of the granite, the kaolin similar to 
 the feldspar, and the rusty zones similar to the forroniagnesian constituents. 
 It seems probable, therefore, that this deposit has l)een formed by the alt»>r- 
 ation of granite-gneiss. 
 
 8TUUCTURAL FEATURKS. 
 
 The outstanding structural feature of the kaolin deposits is their very 
 evident as.sociation with a zone of deformation throughout which the 
 Grenville quartzite has i)een faulted, fractured, and minutely shatteretl 
 to a friable condition. 
 
 Faulting. 
 
 Owing to the poorly exposed condition of the tone of deformation it 
 has not yet Ijeen positively determined whether it is associated with u 
 single fault of considerable displacement or with a series of small faults. 
 It is sif^nificant, however, that the only localities where positive evidence 
 of faultmg can be observed are all associated with the principal deposit of 
 kaolin on lots 5 and 6, range VI, south, Amherst township. 
 
 The locality at which the evidence of faulting in association with the 
 principal kaolin deposit was most apparent at the time the deposit was 
 examined by the writer was on the south face rf No. 2 pit of the Canadian 
 China Clay Company on lot 6 (Figure 2). At this point the quartzite Iwds 
 adjoining the foot-wall of the fault have lieen dragged downward from a 
 vertical to a recumbent or overturned attitude, a feature which indicates 
 that the movement along the fault plane was considerable. Indications 
 of faulting can also be seen on the west face of No. 1 pit on lot 6 (Plate V'B). 
 Here the surface of the quartzite beds exhibits the gently curving and vertic- 
 ally ridged appearance commonly present on rock faces along which dis- 
 placement has occurred. The fault plane with which the principal kaolin 
 deposit is associated parallels the structural trend of the quartzite in 
 which it occurs, and trends in a direction 20 degrees west of north. 
 
 Jointing. 
 
 The second structural feature indicating that the kaolin deposits are 
 associated with a zone of deformation in the Clrenville quartzite is the 
 jointed character of the quartzite wherever the kaolin is found. It is 
 possible that when the drift cover is removed from the zone of deformation 
 it will be found that the planes of jointing fall into definite systems, but, 
 in the present unexposed condition of the deposits, the data upon which 
 such generalizations could be based are not yet available. At some points 
 two well developed intersecting systems of joints were observed to strike 
 almost at right angles to the strike of the quartzite beds (north 70 degrees 
 cast), and to dip approximately at 45 degrees; at other points the quartzite 
 .shows a tendency to break horizontally (Plate V A) ; but in ost localities 
 the conspicuous joint planes occur in systems which intersect the quartzite 
 l)eds obliquely on the strike and vertically on the dip, with the result that 
 the quartzite tends to break into columnar blocks. 
 
23 
 
I 
 
 
 23 
 
 (imnular Fracturing, 
 
 Tht« thini (IrforinatiMiml offoct cxhilateil by the lono in which kaolin 
 ot'curs in the remarkable manner in which Kraniilar fracturinK han occurred 
 in the quartzite. ThrouKhout nearly the whole of the fracture lone the 
 quartzitehaHbi>en broken to a more or leHMfriuble condition unci in places hnM 
 Ijeen cruHhinl to dust. 
 
 REPLACEMENT. 
 
 The evident aHHociation of the kaolin deposits <»f the St. Heini district 
 with 11 zone of fnultinK and fractvire and the occurrence of niawM's of kaolin 
 in the depowts, forniinx a nmtrix encl«)sinK broken niaHw's* of ((uartzite, 
 would »iH»m to indicate that the kaolin deposits had lK>en formed entirely 
 by the deposition of kaolin in o|H>i:<n((s resulting from the d>-formation of 
 the (Jrenville quartzite; but there is also much evidence to indicate that 
 large masses of kaolin have l.cen deposited by replao-menf, that is the 
 quartzite adjoining the planes of faulting and fracture has been carried 
 away in solution by circulating waters and kaolin depoxited in its place. 
 The principal observations on which this conclusion is lws«'d are: (!) that 
 the surfaces of the quartzite be<ls adjoining the pianos of iM'dding are 
 channeled and pitted with caverns (Plate VIA) in which the kaolin has been 
 deposited; (2) that l)ed8 of quartzite remain in their original vertical 
 attitude here and there within the kaolin deposits (Figure 2); (3) that the 
 bedded structure of the quartzite is preserved in the kaolin deposits in 
 places; (4) that the quartz grains contained in the quartzite have u markecj 
 vertical elongation and this elongation is preserved by the quartz grains 
 contained in the kaolin even where the kaolin constitutes 7.5 jht cent of 
 the deposit. The photog ^^.hs of specimens shown in Plates I und VI B 
 have been inserted to illustrate this feature. In Plate I a specimen of 
 quartzite exhibiting the vertically linear structure of the quartz grains is 
 shown; in Plate VI B the residual quartz contained in the kaolin retains 
 the same linear arrangement.' 
 
 C0MP081TI0.V. 
 
 In the northern part of the fracture zone, the kaolin deposits con.sist 
 almost entirely of white to cream white kaolin and quartz, other constitu- 
 ents being either uncommon or only local in their occurrence; in the south- 
 ern part of the zone, on the other hand, the greater part of the outcrop so 
 far disclosed by stripping operations is coloured in various shades of red, 
 brown, and yellow from the presence of disseminated hydrous iron oxide, 
 but whether this is merely a superficial discoloration or persists in the ileposits 
 at depth has not yet been determined. The uncommon impurities 
 observed in the kaolin deposits are fine flakes of muscovite, aggregates of 
 tourmaline, and disseminated flakes and aggregates of graphite. 
 
 That the normal white to cream white kaolin contained in the St. 
 Remi deposits is remarkably free from impurities is indicated l)y the 
 
 • Hayes, C. A., Ball. G«»l ."tec Am . vol. Vlfl, 1S»7, pp. "IS-3W. 
 
34 
 
 «„uly«* of the wMh«! product, included in clunum I and II of the follow- 
 init tatilc. 
 
 An,,lyne,of Kaolin from Aniher»tTown^hip,CimparfduntkAnaly»e»of Kaolin 
 " ^ from Other Countnen. 
 
 HilioH 
 
 Alumina 
 
 Fwrir iion 
 
 Kerroiii! iron 
 
 Ijmc 
 
 Mogni'xiit 
 
 Potiuth 
 
 Soda 
 
 TiOi 
 
 IxMW cm ignition 
 
 Moixturo 
 
 Totttl 
 
 72 
 
 none 
 
 none 
 0'2fl 
 U'OO 
 
 13 Rl 
 
 10040 
 
 II 
 
 44 4:) 
 
 40 '4H 
 
 0'0:)0 
 
 0-24 
 0'3« 
 
 14 40 
 
 III 
 
 100 01 
 
 40- 17 
 
 43 
 
 00 
 04 
 
 2 77 
 
 12 01 
 
 IV 
 
 9003 
 
 47 10 
 
 30-42 
 
 2:i 
 
 31 
 24 
 10 
 OH 
 13 
 12 24 
 
 99 91 
 
 45 7H 
 MW 
 
 2H 
 
 SO 
 OM 
 
 25 
 
 13 40 
 2 05 
 
 98'K4 
 
 C'oniDunv. <'an. Min. Jour., vol. 3J, 191^, ?•?*'• . „ , ., .j^.i „ c,-, 
 
 'Xorth (Carolina, OpoI. Surv., BuU. 13, 1897. 
 
 The analysen of typical kaolin from localties in EnRlancl and United 
 States haveffinserted in columns III to V for the purpose of coirr.an • ^ 
 
 The chemical composition of the discoloured kaohn. according to an 
 analysis by A. C. Spencer, is as follows: 
 
 1. 
 II. 
 
 III. 
 
 IV. 
 
 V. 
 
 Silica 
 
 Alumina . . . 
 Iron oxide 
 
 Lime 
 
 Magnenia. . 
 Loss on ignition. 
 
 Per cent. 
 M 24 
 34-24 
 2-04 
 2 54 
 0-40 
 0-87 
 
 Teslhi' Lar,onvtori^",'MonTreal": with the fdlowinR result 
 
 Silica ■ 
 
 Alumina 
 
 Potash 
 
 Lime 
 
 Magnesia 
 
 Iron 
 
 Water 
 
 A spec-imcn of this icck, sent the writer by Mr. 
 CanucUan China (May Company, c-ould be seen with 
 
 Per cent . 
 72 06 
 17-30 
 11 41 
 1-50 
 tio 
 10 
 110 
 
 Broderick, 
 the naked 
 
 cjf the 
 eve to 
 
25 
 
 coniiiiit of iHiin<>n)U8 Kraiiii* of quartz and HrattcriHl flak«-it of niuwoviti> 
 (•inl>f>(l(lt<<i in fclilNpar. An fxaminntion >f a thin M>ctiou of thi- riM-k iinilVr 
 the inicromH>|M> tthownl that the fcldhjathic ronittitut>nt nn>iM-nt wan a 
 plaKio<;laM> having the optieal proper*' •< of andeMine (Ah^ An»»), in which 
 a kaoliniziMl fclilnpar, premimahly onnoelatK-, wan p«'rthitically incliKled. 
 That the rwk had U-en subjeeted to coniiiderahle <leformatioii wan indi- 
 cated \>y the iindulatory extinction of the quartz and the broken an I JM-nt 
 condition of the feldnpar. Both the quartz and the feldHpar contained 
 numerous hair-like inclumouM of a mineral having a high refringi nee anil 
 birefrinnence and paraih'l extinction— jHrnHibiy rutile. Then- htul appar- 
 ently no definite orientation with rcHpect to the cryntallonraohic direction 
 of the mineral enclomnK them. 
 
 At the time the writer vinited the dintrict hint (July 1!»18). » nhaft 
 waw being mmk on the prop«'rty of the Canadian China Cluv Company, 
 at a point approximately T'l feet to the cant of the wanhinK plant, aiid 
 hence on the western lM)rder of the fracture zone in which the kaolin 
 (M'curx. The rock encountered in thin shaft ix a heteroKene<ius, coarse, 
 garnet gneiss in varioua stages of kaolinization. In its least altered phases 
 it consists of orthoclase in the incipient stages of kaolinization. a few grains 
 of quartz, broken aggregates of red garnet, fibrous sillimanite. re<l brown 
 mica, scattered flakes of muscovite, and small grains of a dark brown, 
 highly refractive, mineral, probably rutile; in its more highly altered 
 phases it retains its original texture, but is stained yellow with iron oxide 
 and has In'en kaolinized to a friable condition. 
 
 OKKilN'. 
 
 It has been pointed out. in the sections of the re|)ort in which the 
 structural features of the kaolin deposits and the eviile'ices of replacement 
 which they exhibit were <liHcus.sed, that the kaolin leads occur in associ- 
 ation with a wide zone of faulting and fracture ♦rav<'rsing (irenville quartz- 
 ite and have been formed partly by the deposition of kaolin along the 
 planes of fracture and faulting and partly by replacement of the friable 
 quartzite wall rock. The association of the kaolin deposits witli a zone 
 of fracture and faulting is of considerable economic imixirtance, since the 
 horizontal extent of the deposits is directly related to the extent of the 
 zone or zones of deformation. It is equally important, however, from a 
 commercial standpoint, that the source froni which the kaolin was derived 
 be determined: for, if the kaolin has l)een carried down into the zone of 
 deformation from a superficial source, the deposits may disappear before 
 the depth to which mining operations might be carriecl On is reached; on 
 the other hand, if the kaolin has been derived from a deep-seated source, 
 it is rea.sonal)ly certain that the deposits p«'rsist to depths beneath the limit 
 to which the kaolin could be profitably mined. 
 
 The discussion which follows of the origin of the kaolin deposits has 
 been divided into three parts: (1) a summary statement of the various 
 ways in which kaolin deposits found in other parts of the world are believed 
 to have originated; (2) a discussion of the evidence indicating the manner 
 in which the St. Uemi deposits have originated, and (3) a concluding 
 section in which the conclusions with regard ti> the origin of tlH> St. liemi 
 deposits are inferred from the evideni e cited in sections 1 and 2. 
 
26 
 
 ' I 
 
 >r ii}<\i-:i dtemenl of Hypotheneit. 
 
 The hvpotlu-sps which have been suKH<'*^ti'(l to explain the origin of 
 kaolin, althouRh varied and numerous, all fall into one or other of two 
 classes, acpordinR to whether the source of the kaolinizinR an<'ney has been 
 superficial or deep seated. 
 
 Kaolin of Superjicial Origin.^ There are two groups of hypotheses 
 belongiuK to this class: in one the importance of certain mmerals from 
 which the kaolin is believed to have been derived is emphasized, and in 
 the other the particular agency by which the kaoUnization is effected is 
 regarded as important. 
 
 The oldest and most g(>nerally accepted hypothesis to account for 
 the origin of kaolin has been that it is formed as a product of the processes 
 of mechanical disintegration and chemical decomposition to which rocks 
 exposed at the earth's surface are subjected in weathering. The fornaation 
 of kaolin in this manner has been called in question by some geologists in 
 recent years; nevertheh'ss, it is still believed by others to be the only 
 reasonable explanation of the origin of many deposits. Occurrences of 
 kaolin that have beeii described in recent years as having originated by 
 kaoUnization in the zone of weathering are found in the island of Bornholm^, 
 at .Josingsfjord, I'-kersund-Soggendal, Norway', at M<'issen and Halle in 
 Saxony*, and in numerous localities in United States*. 
 
 It has been generally assumed that the principal source from which 
 kaolin is derived in weathering is the feldspars, the chemical reaction by 
 which this change is effected in the case of orthodase being as follows: 
 
 K,0, Alj(>3, 6Si02+2H2() + C()2 = Alo()3, 2810,. 2H2() + K2('03+4Si()j. 
 
 The formation of kaolin by the weathering of muscovite, an hypothesis 
 originally suggested bv Schmid«, has been advocated in recent years by 
 Selle' for the kaolin deposits at Halle in Saxony, and by Hickling for the 
 Cornwall kaolin deposits. Sini-e both ScUe and Hickling regard the mus- 
 covite as merely an intermediate stage in the transformation of feldspar 
 into kaolin, this is merelv a modification of the prevailing theory of kaoUn- 
 ization of feldspar. The kaolinization of scapolite by weathering has mIso 
 been advocated by Fuchs and by CJummel" to account for the formation 
 of deposits of kaolin occurring in the vicinity of Passau in Bavaria. With 
 
 ' ExoKi-nc kaolin. Stahl AKred. Dip VcrbreiluBg iKt Kiiolinlugoralatten in Deutwhlanil, Archiv. (ur I.agtr- 
 statten-Fonichuttg in DeutschlamlB, Heft 12, 1912, p. lOH. 
 
 •Winkel. H. K., Kaolin.ilemnuTiet. Rabekke([aard paa Bornhnlm, Denmark, 2 Tav. Kjobenhavn, Tckn. 
 Forenings TidMkrilt, 188.5. 
 
 • Vogt. J. H. L, " The geneBis o( ore-deposita," 2nd e<l., 1W12, pp. 661-685. 
 
 •Darnitike, J. E., Ulier das Vorkommcn der Poriellanerde liei .Meiaaen and Halle a.S., Zeitschr. lur prakt 
 
 *"° ' Wont,''!'., Die EntatehuBg der Kflolinerden der Gegend von Halle a.S., Zeit-whr. fur prakt. geol., 1907. i.p 
 19-23 
 
 ' Ilie«, H., Mil. Geol. Surv., vol. 6, 1904. 
 North Carolina Geol. Surv., Bull. 13, 1897. 
 r S. Geol. .Surv., Prof. Paper No. 11, 19()3 
 " ClayB, their occurrence, propertien, and uses, 1908 
 
 Trana. Am. Ceramic Soc, vol. 13, 1911, pp. 52-74. , .. , i r ,o,u 
 
 Rie«, H.. Kummcl, H. B.. and Knapp, G. N., Geol. Surv. of New Jemey, vol. 6, 1904. 
 Watte, A. 8.. US. Bur. Mines, Bull. 92, 1915. 
 « Srhmid, E. E., Die Kaoline de« thuringiachen BundaandBteina, Zeitachr. deatach geol. Gaa, vol. 28, 1876, 
 p. 110. 
 
 ' Helh, v., I'ber Verwittening und Kaolinbildung Halleanher, Quariporphyre, ZeitBchr. fur, NaUrw. Halle, 
 
 Hickliag, U, Trans. Inst. Min. Eng., vol. 35, 1908-09. p 10 
 ' See H. Riiler, neoea Jahrback fur Mia. Geol. und Pal., vol. 18, 1902, pp. 28«-26«. 
 
27 
 
 sonu' citKcs, at least, 
 by the oxidation of 
 
 these few excoptions, however, geologists are gen<Tall.v agreed that in so 
 far as kaolin has been formed by weathering, it has been derived in the 
 main from feldspar. 
 
 The agencies which are believed by va.rious writers to have been 
 especially effective in briniri' , pbout superficial kaolinization include 
 carbon dioxide, waters d -iviil fMnii --'vamps, hydrolysis, and sulphuric 
 acid formed by the oxic itioii of siili)iii m <. That carbon dioxide con- 
 tained in percolating wa' r;- has been a Most potent agency in bringing 
 about the decomposition »f ;, Urates vva.- long ago proved exi)erimentally 
 by Bishof, Mueller, Daul.' Mil uthe.s,'- and the probable importance 
 
 of the role it plays in kaolinization lu.: been generally recognized. The 
 common occurrence of many kaolin deposits in Cicrmany, associated with 
 feldspathic igneous rocks at points where they underlie coal beds, has led 
 many Cierman geologists to conclude that the kaolinization in the case of 
 these deposits has been brought about i)y percolating swamp waters. It has 
 been pointed out by Cameron and Bell' that many minerals are soluble 
 in water alone and that kaolinization might, therefore, occur without the 
 presence of carbon dioxid(> or other dissolved material. The kaolinization 
 is assumed to take place by hydrolysis, the reaction in the case of ortho- 
 clase being as follows: 
 
 KAlSi308+ HOH = HAlSijO, + K()H 
 HAlSiOjOs - 2Si()2 = HAlSiO^ 
 
 Kaolin is also believed to have been formed in 
 through kaolinization by sulphate solutions formed 
 the sulphides contained in ore deposits.* One of the most evident exami)les 
 of kaolinization by sulphate solutions formed in the oxidized zone occurs 
 at the Helen iron mine at Michipicoten, Ontario. In this locality a dia- 
 base dyke has been kaolinized at the point where it intersects the ore 
 mass which consists of hematite and goethite and which is believed to 
 have been formed by the oxidation of pyritic siderite with which the iron 
 ore is associated. The diabase dyke, although wholly unaltered where it 
 intersects the adjoining iron formation, has been completely kaolinized 
 where it crosses the ore-body, and is said by Parsons to be less unalt<'r(>d 
 in the lower workings where the alteration of the siderite and pyrite is 
 less complete.''' 
 
 Kaolin or Kaolinizing Atjency of Deep-Seated Origin. The hypotheses 
 of thi.s class usually have reference to deposits which have been formed 
 in nitu by the alteration of pegmatite, granite, and related rocks, and it 
 is the agency by which the kaolinization has been effected rather than the 
 kaolin that is regarded as deep seated in its origin. In the St. Uenii 
 deposits, however, the kaohn has not been developed in situ, and if it is 
 of deep seated origin it must have been carried up from below. 
 
 > Bishof, O. C. Ijehrburh der chem. und phvuikaUM^hen Geoloftie, Bonn. IHiS. 
 Mueller, H., Tachemi. Min. Mittheil, vol. 7. 1877, pp. 30-48. 
 Diiubree, A., Ktudon fi.vnthetiquofl de (ceokHcie eiperimentale, 1879, pp. 268-273. 
 
 * Merrill, G. P., " llorkn, roek weatherinK, and nod," Macmillan Company, New York, 1807: Van Hiwe, C.R , 
 V. S. Geol. .Snrv., Mon. 47, 1904, pp. 473. 483; and Clarke. F. W., U. 8. Geol.'Surv., Bull. 491, 1911, p. 349. 
 
 : Camemn, F. K., und Bell, B.. IS. Dept. Agr., Bur. of Soils, Bull. 30, 1905. 
 
 * I-indnren, W., Keon. Geol., vol. 2, 1907, p. 120. 
 
 RMUome, F. 1.., Econ. Geol., vol. 2, 1907, p. «89; I". S. Geol. Surv., Prol. Paper M, 1909. 
 Jacquet, J. B., Geology of the Broken Hill lode and Barren Ranites tninrral field, Xew .South Wales, 1894, 
 p. S9. 
 
 ' Parsons. A. I.., Onl. Bureau of .Mines, Ann Uept., vol. 24, pt. 1, 1915, pp. 18S-215. 
 Bvttofi, I-. I;., tjrrsottal commutticntion. 
 
28 
 
 The kaolinization of granite aiul other igneous roeks at Carlsbad and 
 other localities through the agency of cold springs charged with carbon 
 dioxide has been noted by Stremme' ^ Gagel,' and drupe,' but with these 
 exceptions the hypotheses of this class all assume that the kaolinization 
 has been effected by ascending thermal waters or gasses. The origin of 
 kaolin by pneumatolytic processes was suggested as early as 1824 by 
 von Buch, who noted the presence of fluorspar in the kaolin deposits of 
 Halle, in Saxony, and concluded that the kaolinization had been brought 
 abotit by hydrofluoric acid vapours. Since von Buch made his original 
 suggestion the pneumatolytic theory has liecn advocated by numerous 
 writers, including Collins,* and Butler* for the Cornwall kaolin deposits; 
 Daubree, DeLauny*, and Mallard for certain occurrences of kaolin in France; 
 Forshhammer and Eichstadt for Scandinavian deposits, and Roslei« and 
 Stutzer' for German kaolin deposits. 
 
 The principal data upon which those who favour the pneumatolytic 
 theory base their conclusions are the following: (1) the common a.ssociation 
 of kaolin with tourmaline, fluorspar, topaz, pyrite, and other minerals of 
 pneumatolytic origin; (2) that kaolin deposits are commoidy as.sociated 
 with faults and fissures which afford channels along which the kaoUnizing 
 vapours could ascend; (3) that the normal weathering of granite does not 
 result in a pure white kaolin; (4) that the first stage in the weathering of 
 a granite is mechanical disintegration, whereas in kaolin deposits original 
 textures are conunonly preserved (Plates I and VI B); (5) kaolin deposits 
 extend to greater depths than could possibly result from surface weathering; 
 (6) sericite is abundant in kaolins though this mineral is not a product of 
 weathering. 
 
 It is contended by Rosier that kaolin deposits are not only formed by 
 ascending agencies, i)Ut that the kaolinizing agency is aqua-gaseous. 
 Lindgren, on the other hand, as a residt of < .servations in ore vein fleposits, 
 concluded that kaolin is not found in the deep vein zone, and, therefore, 
 cannot be of pneumatolytic origin. 
 
 The evidence bearing on the various ways in which kaolin may have 
 originated has recently been discussed at considerable length by Stahl, 
 Ries, and Howe. Stahl concludes, from a study of the German kaolin 
 deposits, that the formation of kaolin is easily effected by weak acids and 
 .1 the ca.se of German kaolin deposits only through the agency of carbon 
 dioxide in aqueous solution, and that the kaoUnizing agency penetrates the 
 rock, in some cases from above (exogenous kaolins), partly as percolating 
 atmospheric water, more commonly as swamp water, and less commonly 
 as surface waters derived from graphite deposits, and in other cases from 
 l)elow (endogenous kaolins) in the form of cold acid waters or niore rarely 
 as thermal waters.' Ries, who is especially familiar with American kaoUn 
 deposits, likewise concludes that " a careful sifting of the evidence would 
 seem to indicate that kaolin might be formed according to any one of the 
 three important processes, viz., weathering, volcanic waters, and vapours 
 
 > Oa«el. C, and Stremme. V., C«iitralblst. fur. Min. uiiw., 1»0«. 
 ' Stremme. V.. and Grape, O., Mooaube'', der Deutach. geol. gesel., 191(1. 
 ' Collins. I. H., Min. Mag., vol. 7. 1886-7. pp. 205-214. 
 • Butler. F. H.. Min. Mag., vol. 19. 1908. 
 ' DeLauny, L.. Bull. Soe. Geol.. France. 1888, vol. 16. 
 
 'See Roeler. H . \eura Jahrbuch fur Min. Geol. und Pal., vol. 15, 1002, p. 390. 
 ' Stutier. O., Zutachr. fur prakt, geol., vol. 13. 1905. pp. 333-337. 
 
 'Stahl. A., Die vcrbrrilmig dfr Ksoli!a»rtit9tt«l in n«jtwhlhihl, .Airhiv. fur TAjer=t«tt4-n.ForKhuni Ht^ft 
 12. 1912. 
 
29 
 
 or acidulated waters from coal beds and swamps That kaolin 
 
 may be formed by post-volcanic vapours or water is no doubt true, as shown 
 by the formation of this mineral below ground water level in the wall rock 
 of many veins, and the turquoise deposits of New Mexico," but whether 
 any commercially valuable deposits have thus originated remains to be 
 proved'." Howe, on the other hand, in common with most geologists who 
 have siudied the Cornwall kaolin deposits, attaches somewhat greater 
 importance to pneumatolysis. He concludes as follows: " It may Im; 
 permissible, therefore, to regard carbon flioxide as most prol)ably the 
 principal accessory agent in kaolinization in all its varied modes of occur- 
 rence, though in no single case has the sequence of steps in tht, process been 
 absolutely proved. It is clear there are many occurrences of kaolin whicli 
 cannot be referred to pneumatolysis while there arc others in which some 
 form of igneous activity is the most obvious prime cause of kaolinization. 
 In short, as F. W. Clarke has said, kaolin, like many other substances, 
 may be formed by any of the several processes in all of which vater, hot or 
 cold, and carbonic acid take part. No one interpretation can fit all its 
 occurrences."' 
 
 The conclusions of Stahl, Ries, and Howe indicate the present status 
 of our knowledge with regard to the origin of kaolin. The (ierman geolo- 
 gists, on the whole, with the exception of Rosier, regard surface alteration, 
 and especially alteratioti effected through the agency of swamp waters, as 
 the most important. Similarly, the geologists of United States, for the 
 most part, regard kaolinization by weathering as the principal source of 
 kaolin; the English geologists, on the other hand, who are familiar with the 
 kaolin deposits of Cornwall attach greater importance to the pneumatolytic 
 theory. All are agreed, however, that kaolin may be formed in many ways 
 and the various conclusions of the different writers have reference mainly 
 to the relative importance of the proces.ses advocated. 
 
 M. Remi Deposits. 
 
 The kaolin deposi oi St. Remi district are peculiar in that the most 
 extensive leads do not occur in association with highly feldspathic rocks 
 but with quartzite, so that the kaolin in these occurrences has been trans- 
 ported along the planes of fracture and faulting from an extraneous .source 
 either above or below the present local ' n of the deposits. 
 
 Kaolin From a Superficial Source. There are two possible superficial 
 sources from which the kaolin may have been derived. These are the 
 quartzite-garnet gnei.ss belt in which the kaolin deposits are found, and the 
 batholithic mas.ses of granite and syenite gneiss which adjoin (he quartzite- 
 garnet gneiss belt. 
 
 The Grenville quartzit. ..ith which the kaolin deposits are a.ssociated 
 generally contains sparsely disseminated feldspar, is intruded in places by 
 dykes of granite or syenite, and includes beds of garnet gneiss; and since 
 granite, syenite, and garnet gneiss all contain an abundance of oi'hoclase, 
 it is p ossible that the kaolin deposits have l>een formed from feldspar by 
 
 > Zalinski, E. K., " Turquoise in Heiioo," Eeog. Geol., vol. 2, t90<, p. 464. 
 ' Rina, H.. Tnuu. Am. Ceramic Soc., vol. 13. 1011. 
 
 ' Howe, J. Allen, ".K handbook to the collection of kaolin, china-clay, anil china-eune in the iiiuMum ol prac- 
 tical leoloiy, London, 1914. 
 
80 
 
 downward concentration along the planes of faulting and fracture as the 
 upper parts of the zone of deformation weathered away. As far as known 
 at present, however, the proportion of feldspar contained in the quartzite 
 and garnet gneiss, including all its modes of occurrence, is small, and. 
 unless the proportion erntained in the unexposed portions of the belt is 
 larger than the exposed portion, the concentration of the kaolin deposits 
 would require the weathering away of an enormous thickness of rock. Thus, 
 if the quart zitD-garnet gneiss belt contains an aveiage of 5 per cent of 
 orthoclase, and the zone of fracture and faultmg, in which the kaolin occurs, 
 contains an average of 20 per cent of kaolin to a depth of only 100 feet, the 
 concentration of this kaoUn by downward enrichment would involve the 
 weathering away of nearly 800 feet of rock and 8 tons of silica and other 
 impurities would have to be carried away in solution for every ton of 
 kaoUn produced. 
 
 It is probable that prior to the glacial epoch the surface of the batho- 
 lithic granitic rocks of the Amherst area, like the unglaciated regions of 
 North America at the present time, was covered with a thick mantle of 
 weathered material, and that, as at the present time, the areas underlain 
 by these rocks stood at a higher elevation than the belt of quartzite u\ 
 which the kaolin is found. It is possible, therefore, that the kaolin i-- 
 the St. Remi deposits may have been derived from the weathering product 
 overlying the feldspathic rocks of the district, but this would involve the 
 horizontal transportation of the kaolin for at least several hundred feet 
 and it is doubtful whether the kaolin contained in the St. Remi deposits 
 would have remained so remarkably pure if it had l)een transported this 
 distance. 
 
 Kaolin From a Deep-sealed Source. Since the quartzite garnet gneiss 
 belt, in which the St. Rei ' kaolin deposits are found, lies between batho- 
 lithic masses of granite and ..yenite gneiss, and these are merely parts of a 
 huge massif extensively developed in this part of the Laurentian highlands, 
 it is probable that the zone of fracture and faulting along which the kaolin 
 is found intersects granite or syenite at depth. It is possible, therefore, 
 that thermal solutions ascending along the fault plane might kaolinize the 
 feldspar of the granite or syenite and then transport the resulting alteration 
 product upward, redepositing it in the quartzite above. The principal 
 evidence observed in the study of the kaolin deposits, that might have a 
 bearing on this hypothesis, was the presence of sericite and aggregates of 
 black tourmaline in the kaolin and in the quartzite wall rock. Where 
 tourmaline crystals occur in the quartzite, it was observed that these 
 generally seemed to lie on the surface of bedding planes or other openings 
 where circulating waters had penetrated, and in no case extended very far 
 into the solid rock (See upper part of Plate VI A). It seems apparent, 
 therefore, that the tourmaline was deposited after the quartzite was 
 fractured and faulted, and that highly heated aqueous or gaseous solutions 
 at some time circulated through the fracture zone. 
 
 Conclnsion. From the preceding discussion it io concluded that, as 
 far as the writer was able to observe, evidence from which a definite 
 conclusion with regard to the origin of the St. Remi kaolin deposits may 
 be inffi->d, is not yet available. Nevertheless, there are certain features 
 exhibit bv the deoosits that have definite bearing on the problem. These 
 that the kflolin occurs in a zone of fractix and faulting traversing 
 
 are: 
 
31 
 
 Grenville quartzitc and garnet gneiss; that the principal kaolin leads so 
 far discovered occur in quartzite and hence the kaolin lias not l)een 
 developed in situ but has been transported into its present position; antl 
 that the relationships of the kaolin in places show that it has been deposited 
 in part by the replacement of the quartzite wall rock. Whether the 
 kaolin originated by superficial weathering and was carried down into the 
 fracture zone, or was brought up from below by thermal waters, the writer 
 is unable to decide. The presence of crystals of tourmalir", a mineral 
 formed at high temperatures, indicating that thermal waters at some time 
 circulated through the fault zone, might seem very positive evidence in 
 favour of the deep-seated origin of the kaolin; on the other hand, the 
 occurrence of oxidized and kaolinized garnet gneiss at a depth of 85 feet 
 in the shaft recently sunk on the property of the Canadian China Clay 
 Company is possibly equally positive evidence favouring the derivation oi' 
 the deposits from a superficial source. 
 
 DISCOLORATION IN KAOLIN. 
 
 It has been previously noted (page 23) that a considerable part of 
 the surface outcrops of the kaolin deposits on lots .5 and 6, range VI, south, 
 Amherst town.ship, are discoloured with iron oxide, so that the kaolin at 
 such points is valueless for most of the purposes for which kaolin is used. 
 The depth to which this discoloration descends is, therefore, of importance 
 in estunating the extent and value of the kaolin deposits. 
 
 The process by which the discoloration of the kaolin is brought about is 
 presumably either the infiltration of hydrous iron oxide derived from the 
 overlying glacial drift or the oxidation in situ of the pyrite -ind other 
 ferruginous impurities contained in the quartzite or garnet gneiss. The 
 depth to which the discoloration descends in the deposits is limited by 
 the depth of the ground water level, but, as far as known to the writer, 
 no data is available from which the maximum depth of this point through- 
 out the fracture zone might be inferred. The occurrence of oxidized 
 material in the new shaft on the property of the Canadian China Clay 
 Company indicates, however, that oxidation may descend, in parts of the 
 zone at least, to a considerable depth. 
 
 EXTENT OF DEPOSITS. 
 
 General Statement. 
 
 As is indicated on the accompanying map. No. 1681, the l)elt of quartz- 
 ite and garnet gneiss, with which the kaolin is associated, is almost entirely 
 hid.''^n beneath glacial drift and, along the continuation of the fracture 
 zor.. in which the kaolin occurs, there are outcrops of rock beyond 
 the known occurrences of kaolin for over 1,000 feet on the south and 5,000 
 feet on the north. Furthermore, at the time the writer last visited the St. 
 Remi district (July, 1918), the shaft on the property of the Canadian 
 China Clay Conpamy, from which it is proposed to develop the deposits 
 underground, was not yet completed, so that all that is known with regard 
 to the extent of the kaolin deposits, is the information obtained from 
 
32 
 
 trenehing and stripping opt'rations in scattered localities and from a few 
 drill holes sunk on lots 5 and 6, range VI, south, Amherst township. For 
 the foregoing reasons, the ainounts of kaolin and associated materials 
 known tv- he present in the district are small compared with the amounts 
 that development work may eventually prove to he present. The follow- 
 ing account of the extent of the deposits is, therefore, to a large degree, a 
 statement of prospective possibilities rather than an estimate of amounts 
 positively determined to exist. 
 
 The materials so far shown by development work to occur in the 
 fracture zone traversing the Ixjlt of quartzitc and garnet gneiss, are the 
 following: white kaolin, discoloured kaolin, kaolinic quartzite, kaolinized 
 granite (cornish stone), and kaolinized garnet gneiss. 
 
 Kaolin. 
 
 Kaolin leads ranging from a fraction of an inch up to 100 feet in 
 width are known to \w present iu iiumerous localities throughout the frae- 
 ti.re zone, but it is only on lots 5 and (>, range VI, south, Amherst township, 
 that the superficial extent of the deposits has been determined by stripping 
 operations. On these h)ts, kaolin has been shown to occur almost con- 
 tinuously in a zone of leads ranging from a few feet to 100 feet in width 
 for u distance of over 1,400 feet. With the exception of the mass of kaoUn 
 adjacent to No. 1 pit at the north end of this zone (Map 1676), however, 
 the outcrop of the kaolin in this locality is nearly everywhere highly 
 discoloured and hence cannot be used as a filler in paper or for other 
 purposes for which kaolin is most valuable, but is being employed as a 
 fire-clay in the manufacture of fire-brick. 
 
 White KaoUn. On lot 5, range V'l, .south, Amherst township, on the 
 property of the Canadian China ('lay Company, there is a lead of white 
 kaolin approximately 300 feet in length and from 1.5 to 40 feet in width 
 that has been shown by a boring to descend to a depth of at least 150 feet. 
 If it is assumed that this mass n.aintaiiis its superficial dimensions at 
 depth, there was originally present at this point approximately 10,000 
 tons of kaolin for every 50 feet to which tiie deposit descends. The data 
 on which this estimate is based are the following: 
 
 Approximate length of (ieposit 300 feet 
 
 Approximate average width of deixwit 2.5 feet 
 
 Average percentage of kaolin present 35 per cent 
 
 Depth of deposit 50 feet 
 
 Number of cubic feet of kaolin in 1 ton 13 
 
 The amount of kaolin above 50 feet now present in this deposit is, 
 therefore, 10,000 tons less the amount removed by mining operations. 
 This would include all the kaolin produced from the property (5,176 tons 
 up to the end of 1917) and in addition the kaolin contained in the quartzite 
 dumps from the washing plant. 
 
 It is possible that the discoloration in the outcrop of the southern part 
 of the zone of kaolin leads on lots 5 and 6 disappears at depth and that 
 white kaolin underlies the discoloured material. If development work 
 should prove this to be the case and the zone maintains its superficial 
 
33 
 
 dimensions at depth, thort' would be present appioximatelv 7r>,(K)<) tons of 
 white ka()lin for every 50 feet of depth in tiiis urea. The (iiita on which this 
 estimate is based are the followinn: 
 
 Approximate length of zone 1,10() feet 
 
 Approximate average width of zone (M) feet 
 
 AcMumed depth of deposit 50 f,,.t 
 
 Average |H>rcentage of kaolin present ;{U i>er rent 
 
 Number of eubic feet of kaolin in 1 ton |;j 
 
 Discoloured Kaolin. As fur as known at present, the discoloration in 
 the kaolin occurs in only the southern part of the zone of deposits outcrop- 
 ping on lots o and (5, range VI, souxh, Amherst townsiiip, but it is possible 
 thai, here and there throunhout the fracture zone, other masses of this 
 character may be foimd as development work is continued. 
 
 It has been discovered that this discoloured kaolin, along with the 
 <iuartzite grains and fragments which it contains, can be used as a fire-clay 
 for the manufacture of {ire-l)rick and information with regard to the amount 
 ( ' this material present in the district is, therefore, woithy of note. If the 
 zone of discoloured kaolin exposed on lots .5 and (5 continues to a depth of 
 
 00 feet there would be present, on the basis of the data given above 
 approximately 2.jO,0(K) tons of this material. If the discoloration con- 
 tinues to a greater depth than 50 feet the <iuantity of fire-clav present 
 woidd be proportionately increased, but the amount of white kaolin 
 underlying the discoloured material would be correspondingly decreased. 
 
 Kaolinic Qiiartzite. It has already been pointed out that the zone of 
 shattered quartzite in which the kaolin is found has a width of 1,0(K) feet 
 anil a length of approximately 7,000 feet, and that a sample taken conlinu- 
 ously across a section of 133 feet through this shatte.ed material contained 
 on the average II per cent of kaolin. It is possible that there are con- 
 siderable masses of quartzite in the shattered zone which are more or less 
 unbroken and in which the kaolin content is much less than 11 pei cent, 
 nevertheless the areas of broken and granulated (juartzite already known 
 to be present in the fracture zoih' indicate that an enormous quantity of the 
 highly kaolinic quartzite is present. Thus, in the area lying to the west of No. 
 
 1 pit on lot 5, range VI, south, Amherst township, sufficient development 
 work has been performed to show that a mass of kaolinic qtiartzite at least 
 400 feet long by 200 feet wide is present, so that if this niasb continues to a 
 depth of only 50 feet, it contains over 300,000 tons of quartzite, and, if it 
 continues to a depth of 150 feet— as the i)resence of kaolin to that ilepth 
 beneath No. 1 pit would indicate— it contains 900,000 tons of quartzite. 
 Furthermore, wherever the surface of the fracture zone has been laid bare 
 by trenching or stripping operations the quartzite has been fotnid to be 
 broken in a manner similar to the mass adjacent to the No. 1 pit, and it is, 
 therefore, reasonably certain that a consiilerable part of the fracture zone 
 7.000 feet long by 1,000 feet wide is underlain by this material. 
 
 Cornish Stone, m a small pit near the eastern margin of the fracture 
 zone an altered granite having the chemical composition of cornish stone 
 has been found. The bottom of this pit was filled with caved in material 
 at the time the district was examined, and the cornish stone was, therefore, 
 not observed in place l>y the writer. The extent of the deposit is wholly 
 unknown, however. 
 
34 
 
 Kaolinized darnel (Sneim. Up to the present time kaolinized fcarnet 
 uncitis has been encountered in only one locality within the lone of fracture 
 and fuultinit traversinj? the belt of quartzite and garnet gneiss, namely, in 
 the shaft now being sunk on the property of the Canadian China Clay 
 Company; but the presj-nce of numerous outcrops of garnet gneiss in the 
 eastern half of lots o and 0, range VI, south, Amherst township, to the 
 eastward of the fracture zone, indicates that kaolinized garnet gneiss zones 
 that are unexposed may be present in the fracture zone. It is possible that 
 the completely kaolinized parts of this material would serve as a fire-<'lay 
 in the same manner that the discoloured kaolin and quartzite are being 
 used. 
 
 VseK of Materiah Contained in the Depositn. 
 
 Kaolin. Kaolin has long been the most important of the raw material^ 
 used in the ceramic industries and its use for this purpose is by far it 
 principal industrial applicatipn. It is mixed with feldspar, china stone' 
 quartz, bone ash, ball clay, swla, chalk, and other ingrefftents in varjing 
 proportions to form both the body and glazing of chinaware, porcelain, 
 wall antl floor tile, electrical insulators, enamelware, stoneware, etc. The 
 other industrial uses to which it is applied include the following: as filler in 
 the manufacture of paper, cotton, and other textiles; as a constituent of 
 certain plasters, paints, and colouring agents; as face powder, as polishing 
 powder, and as an ingredient in certain medicinal preparations. 
 
 Tests of the physical character of the china clay, made by J. Keele of 
 the Mines Branch, are described by Mr. Keele as follows: " The washed 
 kaolin requires 4.5 per cent of water for tempering. It has a fair amount 
 of plasticity, but like all kaolin it works rather short and crumbly. The 
 shrinkage on drying is 7 per cent. 
 
 Cone. 
 
 Fire 
 shrinkage. 
 
 Absorption. 
 
 010 
 
 Per cent. 
 30 
 3 6 
 4-.-. 
 9-3 
 11-3 
 
 Softens. 
 
 Per cent. 
 34-3 
 
 Ofi 
 
 :m-3 
 
 1 
 
 32 
 
 a 
 
 20 
 
 9 
 
 17() 
 
 34 
 
 
 
 
 This material has greater plasticity and higher shrinkages than most 
 of the standard brands of washed kaolin or china clay. The samples for 
 testing were taken from near the surface, but at deeper levels it is possible 
 that the kaolin will not be so plastic and not shrink so much on drying or 
 burning.' 
 
 Experiments made by Mr. Keele have shown that the mixture of 
 white kaolin and quartzite composing the kaolin deposits can be mixed 
 with the ordinary Pleistocene marine clay of St. Remi district to make 
 fire-brick. These experiments are described by Mr. Keele as follows: 
 
 " The crude kaolin is highly refractory and when moulded into brick 
 shapes and burned at the ordinary temperatures of burning fire-brick the 
 
 '"Preliminary report on the clay and shale deponits o( the province of Quebec," Oeol. Sorv., Can 
 o{ Jiinee, Mem. 64, 1915, pp. 4 and 5. 
 
 Dept. 
 
n-«ultinK ».nrk an' rather mift ami porous, with (•hprlc.d „r crac-kod Hurfac-s 
 
 wnnU." I "...*""''*,"'•* ;''*'"V* ♦••»">«P"rtation W..11, h.^i.h-s the l.rick 
 «oul.l he stmetural y weak. It, therefore, seeme.I neeessarv to introduce 
 
 the ■vallej of Rouge nver. whieh eontaina a high pereentage of fluxinit 
 impurities ami m eonsequently rather easily fusihie. i"'xmjt 
 
 1 ^ *".' ™w^"o,? "*""'' '" ''"^ *'"^^ eonsisted of 10 to 20 per e.'nt of marine 
 day and (K) to 80 per eent o erude kaohn. Brieks made from this m7xt" e 
 r o . wT'' '" ^J?*" fi'-«'-l"-i<k kilns at St. Johns, (Juehee, at a temperature 
 ..f 2,4(K) degrees F. The resulting hriek had all the appearance of m i ,^ - 
 eommereial hre-hriek, heiny. d.nsc and strong. • 
 
 A small portion of one ,.f tlie brieks was placed in an electrie kiln and 
 raised to a temperature <.f 3,(KX) .legre.'s F. without L.-ing sinter..<l " 
 
 Ihe crude, dmcoloure<l kaolin, owing to the impurities which it con- 
 tain.s (see analysis, page 24) is less r.'fractory than the white kaolin and 
 can, therefore, he used as a fire-el.iy without the addition of Pleistoc-n.' 
 Clay as a Hux. Kxpenments made with this material hv Mr. Keele showed 
 that It remained intact in a carbon resistance furnaV, at cone 2.5 but 
 that It was rather short-grained and inclined to be weak ip the raw state 
 and shrank excessively when burned in a kiln.' 
 
 Kaolinic Wall Rock: The easily crushed kaolinic <|uartiite wall rock 
 associated with the kaolin deposits may possibly be of great.'r commercial 
 value than the kaolin deposits themselves, for this material can be used 
 tor the manufacture of silica brick of the ganist.-r tvpe, and when freed 
 rom the kao in content is suitabl. for use in the manufacture of lime 
 Domled sihca brick, gla.ss carborundum, and as a steel foundrv sand 
 
 .An experiment made with the kaolinic wall rock to determine its 
 suitability for the manufacture of silica brick of the canister tvoe is 
 described by Mr. Keele in the following statement: 
 
 '' The material was cru.shed to pass a 10-mesh screen and milled with 
 a little water until it became somewhat cohesive. At this stage it could 
 De moulded into brick shapes by hand, and re-pressed bv machinery when 
 partly dry. The bricklets were burned in a gas kiln to 1,300 degrees C 
 and afterwards in an electrie i istanee furnace to ^.^JSO degrees C . a small 
 portion of one of the bricklet> being finally raised to 1,6.50 degrees {' 
 Ihe bricklets bur.ie.l to l,.i30 degrees were hard and dense, and showed 
 that a fused bond between the kaolin and quartz grains was effected. 
 
 Haising the temperature to l,().iO degrees changed the character of 
 the material only slightly, there being no indication of failure through 
 sottening. and it would probal)|y titand a temperature of 1,700 decree-. 
 J U.St as eflfectively. 
 
 These results seem promising for such uses as puddling, malleable, 
 cupola, and crucible furnaces, or for convertor linings and glass makinir 
 furnaces. ' '^ 
 
 A quantity of the crude, kaolinic wall rock was washed in the labor- 
 atory of the Mines Branch by Heber Cole, and a silica sand of the follow- 
 ing composition was obtained: 
 
 SiOj 99-2.5 per cent, FejO, 0-69 per cent, ALSO, 006 per cent. 
 
 A Set •'■''('inont '^^ +Vii\ 1. nit . . .f I.: . ..,. 1 ... X . I! t .1 
 
 Mr. Cole is as follows 
 
 I'Xp 
 
 supplied the writer l)y 
 
 I Mines Branch. Dept. nl .Mines, Sum. itept.. I()l«. pp. 106-7. 
 
" The m«'th<Ml of prepariiiji this wimpU- wiw to vrwh iniitt'rial in i» 
 drv pan no that it all pasw-d throiinh a ltt-m«-Hh scmn. It wan th.n 
 viwhwl in a runninK »tn-am of water and the material paamng through 
 lOO-mesh wa« i-ollected wpnrat.'ly. Thi« fine material .'ontamed finely 
 .livide<l siliea and the kaolin preHent in the ermle rock. The ana ym« 
 uiven above was of the material retain.'d on the l(M)-me«*h. A sample of 
 this latter was submitted to one of the earl)onind«m companies, who 
 tested it and found it satisfartorv for the manufacture of carborundum. 
 In a proper commercial plant consistiiiK of crushers, grinders washers, 
 hydraulic classifiers, and dryers, silica sand runninn well (.v<'r W per cent 
 silica should be easily produced economically and a product put on the 
 market suitable for all the uses in which a hinh-class silwa santl is refiuircd. 
 
 Equipment and Mining Mtlhtxls. 
 The mininu method .-mployed on the property of the Canadian C"hiim 
 ('lav Company orininallv ccmsisted in n'moving the overburden and wail 
 rock by m«"ans of an aerial hoist and conveyinn the kaolin and associated 
 f.-.rtzite to thewa-shiuK plant in a ti-inch syphon. I)urin(t the winter of 
 . , , a stram shovel was employed in stripping the overburden from an area 
 over 1 300 feet long and from 30 to 100 feet wide on lots 5 and (>, range \ 1, 
 \mherst township, and at the time the writer visited the property in July, 
 i«»18 the discoloured kaolin from this area was being loaded into cars and 
 shipped to Laprairi.- for the manufacture of fire-brick. A shaft was also being 
 sunk at the west side of fracture zone on lot ", through which it was 
 proposed to mine the k* >• and kaolinic ((aart/ite from underground 
 
 workiniEH 
 
 The e<iuii)ment on the property of the Canadian China Clay Company 
 includes a washing plant (Plate II B) for the separation of the kaolin 
 from the associated (juartzite, an aerial hoist, compressor, drills, ami «)ther 
 i'tpiipment necessary for mining operations; and the camp buildings 
 required to accommodate the employees of the company. , , ,. 
 
 The process used in the washing plant consists m passing the kaolin 
 and its included quartzite through an agitator, then through a revolving 
 screen and finallv through troughs from which the kaolin is conveyed to 
 settling tanks. After the kaolin has settled the supernatant water is 
 drained off, and the kaolin pumped into filter presses From tin- filter 
 the cakes of kaolin are conveyed on cars to drying sheds in the summer 
 
 and to a kiln in winter. . ., . , ... n i 
 
 A plant for crushing, washing, and classifying the (juartzite wall rock 
 
 was also being constructed on the property. 
 
 Production. 
 The production of china clay from the property of the Canadian 
 
 China Clay Company has been as follows: =— ==. 
 
 Year 
 
 1912 
 
 19!3 
 
 1914 
 
 1915 
 
 1916 
 
 1917 
 
 Value. 
 
 520 00 
 4,354 00 
 9,000 00 
 13,000 00 
 17,500 00 
 11,144 00 
 
87 
 
 ^ i s s 
 
 '? 
 
 ^ 
 
 a 
 
 J|Li 
 
 I 
 
 ■■«>. 
 
 I 
 
 <i—ij»)i^ yij^mt^ 1^ 
 
 wwm. 
 
 liiiSli 
 
flRAPHITK. 
 
 LotH l.'>. l«, luul 17. runnf VI. Amhcrxt townxhip. 
 (iVncTd/ Sliitemenl. 
 
 Thr..uith.)Ut .•aHt.-rn Ontario ami the wmtlu-rii Laun-ntiuim of Qu.-lu.,-, 
 ..um.-roii.. .lop<"*it« of Kraphif (from whi.-h Kraphit.- hu« h.-.-n m»m\ .on- 
 timiouslv or at iiifrvaln for many yean*) oc-ur in a,s«o..atu»n with th.- 
 ■rv^tallin.' lim.'.tonc. m.-mb.-r of th. (Jn-nyill.. H.ru.s. Th.-m. •'••ix'^'t; "^;- 
 nmihir in most r.-npo-ts aiul hav. prol.al.ly onKinat.-.l ... th. «"".• wa> 
 » ,t th.. Kraphit.. <'omposi..K th.-m o(T„rs, partly .n <''!';"""""^": . 'V!" • 
 nartiv i.. v.- i.... and partlv in aKKn-K..t..s, a...l th.. ,U.p..s,ts a .;, th''"-'";'. 
 
 nSra..il a^ L.-lonitinK to .iiff.r.-nt .■hi.m.H a......r. ...k to th.. nart...uh,r f..rm. 
 
 i" whi.'h tl... Ki-aphif. ...... ..rs. I)..p.,mt8 ..f th.. .li««..mina ...1 an.l v.-m typ..H 
 
 r. th.. .•..mm..n'^m...leH ..f ......urr..n.... of ^raphit... h.,th in .u.nt.rn On .m., 
 
 an.i in Qu..Ih.c. Dt.|)o8its of th.. awri-nat.. var...ty, ..n th.. ot u-r han . 
 hav.. h...... ..».«..rv...l hy th.. writ..r in ..nly tw.. Un-a iti.'s <•" 'I't" J> '"'• 0, 
 
 rang.. V, (Jr.'nvilU- t..wnship (K«.yst.)n.. nun..), an.l ..n l..tw la. 1(». an.l i/. 
 rand<> VI. Amh..rst township, .hwrilu-.l in this r..port. 
 
 HiMory of Dcnlopmenl. 
 
 Att.>nti..n wai^ first <lir..<te.l to th.. Rraphit.- .l..poKits in Amherst town- 
 ship in 1007, wh..n tw.) pr..8p.Htors. M<.ssrs. P. l..tr.;ault ami H. il.)y, a<- 
 n iml th.. mininjj rights t.. l..ts 1.5 an.i Itt. rang.. VI. Amh..r8t t.>wnship. 
 ?n^ the Provi..eial (u.vernment of Queh...-. In IIM 9 a company w.is 
 ,riani^...l in Montr..al u.uI.t the title " (Iraphite I. im.te.l." to take ..ver 
 the property, an.l .levelopnu-nt work was l).>gun an.l was .-ontinu.'.l until 
 1912 DuriiiK this time nnm..ro.is prosp.-ct pits an.l irvwhi-n v/vn- exea- 
 vat..<l, an.l N... 1 shaft was snnk to a .lepth .,f 105 f<>'-t....7»'«'/'"Vf """*,"'" 
 of a mill was .•oinmenc...l in 1912 an.l e.miplet...! in 191S In D...eml...r 
 of that vear the eompany went into li.pndation. 
 
 In the autumn of 1916 an English (Multipar) syn.l.eat.. t.K.k :«<> opji"" 
 on the property an.l opene.l a pit near the north h..un<lary of lot K.; I>ut. 
 after a few wt.eks' op.'ratL.n. the option was .lr.)ppe(l. 
 
 (leologicnl Relationships. 
 
 On the east si.le of the northeasterly tren.liiiK Hat whi.-h extends 
 alonir Pike .reek on lots If). 10, and 17, range VI, Amherst township, the... 
 IS exp.)S.>.l a l.)w, .Irift overeil ri.lge un.l..rlain by eryslalline litnest..ne. 
 In eonimon with the Cirenvillc limestone generally, this inelu.les numero.is 
 masses of pyroxene granite, pyroxene syenite, and otlu'r rocks wli.-l. 
 nresumahly were originally intruded int.) the him.stoiie as .lykcs, hut w.-re 
 subsequently broken up by tlcformation into fragments. In places the 
 limestone also contains masses of orth.)clase, svoUastoiute, pyrox.-n.., ami 
 oth..r silicate minerals with which graphit." in excc-diiigly coarse Hake> is 
 ass.)ciate.l, ami these masses constitute th.- graphite .leposits. 
 
 Chanwlcr of Dcpo.nt^. 
 At the time the writer made his examination of the property the main 
 pit was fiUo.i with water, so that the ..haracter of the .leposits m the un.ier- 
 
3ft 
 
 ground workinnH was not ol)«.rvc«l. Thr followinn •loscription is, therefore. 
 bMwt mainly on obwrvatioriH ut the Kurfacc in f hrw localiticH, th<- oix-ninM 
 
 fk l"iPi *''*,' """", ^"*' •'"' P'* "f^""*"'' ''y '»"' >I"ltip«r «vndi.at.. noar 
 thp north »)ounilar.v of lot IH. and two small prowpoct pitx Hituatd a few 
 hi'.ndrpd feet north of the dotith line of lot 17. 
 
 Thp niain pit in sitiiato.! a fi'w foot from No. 1 shaft and is conni'ctp.l 
 t\u u ;"»"„"> Inp/'i'lTlcronnd workinRs. Tho oxravation at the top 
 of the «haft w 60 feet long hy 30 feet wido. and the .leep part of the oiKiiioK 
 w 30 feet long hy 15 feet wi.le. The roek ex|X)8ed is pyroxenic limestone 
 eontauung numerous erumpled inelusions of fin*' grev pvro.xene-granitc 
 and pyroxene-Byenite. It wa^^ ol.serve<l that at the soiith end of the pit a 
 zone of graphitu- wollastonite had In^en developed along the contaet of an 
 mcluded Igneous mass and that the east face of the pit a few feet farther 
 to the north consisted of granite, from whieh the graphitic material had 
 l)een mine« away. At the north end of the pit a number of other inclusions 
 surrounded by similar graphitic contact zones were also present. 
 
 The Multipar pit at the time the writer made his examination of the 
 property was 120 feet long. .50 feet wide, and from 10 to 20 feet (iwp. ( )m 
 the west fac-e of the opening a mass of rock approximately 10 feet wi(h' 
 and 5 feet high was exposed, consisting of syenite and wollastonite inter- 
 vening between vertical leads or aggregates of graphite 31 and 2 feet 
 wide, respectively. The south face of the pit consisted muinlv of rustv 
 crystalline limestone striking north 70 degrees east (magnetic) and dipping 
 50 degrees to the southeast, but included dvkes and mas.ses of pyroxene 
 syenite of considerable size in places. One of these at the west end of the 
 face was traverse^! by irregular zones of graphitic wollastonite from a few 
 inches to a foot m diameter. The rock exposed on the east face of the pit 
 beneath the covering of boulder clay included a considerable proportion 
 of graphitic wollastonite, but the ore rock was most irregular and the pro- 
 portion of graphite contained in the ore rock exceedinglv variable The 
 largest and richest continuous mass of the material exposed diagonally 
 across the south end of the face, was 20 feet long and from 2 to 10 feet 
 wide, and contained approximately 50 per cent of graphite. The central 
 part of the face, except for a few narrow, irregular vein-like leads of graphite 
 was barren, consisting of an elongated mass of pyroxene granite above and of 
 a hne-graincd grey rock which, under the microscope, was found to consist 
 of scapoUte, wollastonite, an<l garnet beneath. The north face of the 
 excavation was in Iwuldery drift entirely. 
 
 The pits on lot 17 are small prosix-ct openings in the (henville lime- 
 stone which at that point strikes north 35 degrees east (magnetic), and 
 dins 7o degrees to the southeast. The rock exposed in the faces of the pits 
 IS mainly limestone with the usual inclu.sions and zones or masses of 
 graphitic silicates (Plate VII) developed in places on the margins of the 
 inclusions The largest single mass of graphite ore observed was 3 feet 
 long by IJ feet wide. 
 
 It would seem evident from the preceding observations that the 
 graphite occurring m the St. Remi district is associated with masses and 
 zones of lime silicate minerals developed as a result of the silication of 
 Orenville limestone, and that the quantity of graphite in the deposits is 
 approximately proportional to the amount of this material present It is 
 not possible to definitely estimate the proportions of graphite present in 
 deposits of such irregularity, but it is certain that hi the total area of 
 exposed rock surface, at the top of the main pit. and in the pits on lot 17 
 
40 
 
 the percentage of graphite present is much less than that contained in the 
 lowest grade of ore that could possibly be profitably mined under present 
 conditions of operation. It is probable, on the other hand, that the 
 percentage of graphite contained in the exposed faces of the Multipar pit 
 at the time this opening was examined, averaged 5 or even 10 per cent, 
 and hence constituted an ore of workable grade, provided this average 
 maintained itself throughout a rock mass of workable dimensions; but 
 much additional development work is required before this can be estab- 
 lished. 
 
 Mineralogy. 
 
 The character and relationships of the principal minerals comprising 
 the St. Remi graphite deposits are as follows: 
 
 Graphite (Carbon). The graphite contained in the deposits occurs m 
 part as minute hexagonal plates disseminated in calcite, but more abund- 
 antly in lamellar aggregates up to 2 or 3 inches in diameter distributed 
 along zones of granulation and fracture in the woUastonite and other 
 minerals of the deposit. 
 
 WoUastonite (CaOSiO., Lime 48-3, Silica 51 • 7 per cent) . Wollastomte 
 is the dominant mineral of the deposits. It occurs in pale, green-white, 
 unifol-mly fibrous crystals from 1 inch to 10 inches in length, the inter- 
 spaces between which are filled with calcite, pyroxene, orthoclase, and 
 titanite. The crystals are commonly traversed by irregular fracture zones 
 filled with calcite and graphite. 
 
 Diopside (CaMg(SiOs)j, Lime 25-9, Magnesia 18-5, Silica 55-6 per 
 cent). The diopside is a glossy green variety occurring in short, thick, 
 prismatic crystals from one-quarter inch to 2 inches in diameter. These 
 exhibit a prominent cleavage parallel 001. 
 
 Titanite (CaO TiO, SiOj, Lime 28-6, Titanium Dioxide 40-8, Silica 30-6 
 per cent). Titanite is a common constituent embedded in the calcite 
 which fills the interspaces between the woUastonite crystals. It occurs in 
 flat, wedge-shaped, resinous brown crystals up to 3 inches in diameter. 
 In some of the large crystals a fine, uniform cleavage is well developed. 
 
 Orthoclase (KjO, AljO, 6Si0s, Potash 16-9, Alumina 18-4, Silica 64-7). 
 Orthoclase occurs chiefly as tabular crystals scattered through the material 
 filling the interstices between the woUastonite masses. At one point a 
 crystal was observed embedded in the diopside. In the specimen shown 
 in Plate VII a number of these tabular crystals are conspicuously developed. 
 
 Scapolite (a Calcium, Sodium, C'hlor., Aluminium SiUcate). The 
 scapolite associated with the graphite deposits is a peculiar opaque grey 
 vitreous variety. It occurs as rounded crystals up to an inch or more in 
 diameter, completely enclosed by the woUastonite. 
 
 Calcite (CaCOj, Lime 56-0, Carbon Dioxide 44-0). The calcite is a 
 pale yellow green variety which fiUs the int«rspaces between the other 
 minerals of the deposits. 
 
 Quartz (SiOj). Quartz is not a common or conspicuous constituent of 
 the deposits. It was observed in association with orthoclase, fiUing the 
 interspaces between the woUastonite crystals. 
 
 Paragenesis. 
 
 The manner in which the minerals composing the St. Remi graphite 
 deposits are intorgrown with one another is similar in every respect to the 
 relationships exhibited by the mineral constituents of igneous rocks, so 
 
41 
 
 that from these relationships the approximate order in which the various 
 mmeralB completed their crystallization can be determined. Thus the 
 occurrence of the scapolite as inclusions in the woUastonite indicates that 
 this mmeral completed its development before the woUastonite, whereas 
 the occurrence of orthoclase, titanite, and other minerals in the interspaces 
 between the woUastonite crystals indicates that these followed the wol- 
 lastonite in their development. Similarly the occurrence of the graphite 
 and calcite as a inatrix around other minerals, and filling the fractures 
 traversmg the woUastonite, indicates that these minerals were among the 
 last to be deposited. The approximated order in which the various 
 minerals composing the deposits completed their development was, there- 
 fore, as follows: scapolite, woUastonite, orthoclase, titanite, diooside 
 graphite, and calcite. ' ^ ' 
 
 Origin. 
 
 In a previous pu!)lication it has been pointed out that there are three 
 hypotheses which have been suggested to account for the origin of the 
 graphite occiirring in southeastern Ontario and the southern Laurentians 
 of Quebec: that they are recrystallized, carbonaceous material contained 
 in the GrenviUe limestone; that they have been derived from igneous rocks 
 intruded into the limestone; and that they have been formed from the 
 carbon dioxide of the limestone by reduction.' 
 
 The character and relationships of the St. Remi graphite deposits 
 indicate that the minerals associated with the graphite are the prwluct 
 resulting from the metamorphism of the Grenville limestone and that 
 this metamorphism was eflfected by emanations derived from the granite 
 and syenite, included in the limestone. This association of the graphite 
 with a contact metamorphic deposit would seem to support the hypothesis ■ 
 that the graphite had been formed from the carbon of carbon dioxide for 
 large quantities of carbon dioxide would be set free at the points where 
 the sihcations of the limestone occurred. It is likewise probable, however 
 if the graphite were derived from the igneous intrusives that it would be 
 evolved in company with other emanations, and might be concentrated 
 at the points where these emanations were most abundant, and hence where 
 sihcation had occurred. On the other hand, if the graphite were d. rived 
 from carbonaceous material deposited with the limestone, there is no 
 apparent reason why it should be associated with contact metamorphic 
 deposits. On the whole, therefore, the evidence afforded by the St. Remi 
 deposits seems to be most favourable to its derivation from carbon dioxide 
 and least favourable to the sedimentarv hvpothesis. ' 
 
 Equipment. 
 
 The equipment on the property includes a compressor, boiler, hoists, 
 and other machinerj- necessary for the mining of the ore, and a dry con- 
 centrating mill having a ccnacity of 100 tons per day. 
 
 The buildings on the property in addition to the mill include a board- 
 ing house having accommodation for seventy-five men, a manager's house, 
 »■ sh aft house, boiler house, barn, and storehouse. ' 
 
 • Tru*. Cu. Hia. Int.. vol. !•, IRI«, pp. 3«>-MS. 
 
42 
 
 CHAPTER V. 
 
 SUMMARY AND CONCLUSIONS. 
 
 The most important data with regani to the geology and mineral 
 deposits of the St. llemi district, stated in summary form, are as follows: 
 
 PHYSIOGRAPHY. 
 
 The district lies within the dissected southern border of the great 
 Laurentian plateau, which occupies the greater part of northeastern Canada 
 and in the main is characterized by the minutely rugged topography of 
 that great upland, but is distinguished from the normal plateau topography 
 by the presence of flats of post-glacial marine clay and sand deposited in 
 the bottoms of its major depressions up to elevations of over 700 feet above 
 sea-level. 
 
 GEOLOGY. 
 
 With the exception of a single dyke of diabase of late Pre-Cambrian 
 age and the unconsolidated Quaternary deposits, the rocks occurring in 
 the St. Remi district belong to a basal Pre-Cambrian complex composed 
 of three separate subdivisions, which, named in order of age from oldest 
 to youngest, are as follows : 
 
 " (1) A series of highly metamorphosed marine setlinients, crystalline 
 limestone, garnet-gneiss, and quartzite — the Grenville series. 
 
 (2) A group of igneous intrusives — gabbro, pyroxene syenite, anortho- 
 site, etc. — the Buckingham series. 
 
 (3) Batholithic masses of porphyritic granite and syenite gneiss. 
 
 MINERAL DEPOSITS. 
 
 The materials of commercial value known to occur in the region are 
 kaolin, discoloured kaolin, kaolinic quartzite, and graphite. 
 
 Kaolin and Kaolinic Quartzite. 
 
 In the southern part of range VI, Amherst township, a belt of Gren- 
 ville quartzite occurs, which is traversed by a north-northwesterly trending 
 zone of fracture and faulting approximately 1,000 feet wide, in which 
 deposits of kaolin occur in zones up to KK) feet in width and over 1.400 
 feet in length. 
 
 The kaolin occurs within the fracture zone, partly as narrow leads 
 following the planes of fracture and jointing, partly as the matrix enclosing 
 broken fragments of quartzite, and partly as replacement deposits, large 
 quantities of the quartzite having been carried away in solution and the 
 kaolin deposited in its place, so that the original structures of the 
 quartzite are preserved. 
 
43 
 
 The occurrenee of the kaolin in a fiaiture zone in which feklspar or 
 other aluminous sihcates are almost entirely absent, indicates that the 
 mmcral has not been developed in situ, but has been carried into the 
 fracture zone from an extraneous source. 
 
 Conclusive evidence from which the origin of the kaolin deposits 
 could be mferied was not obtained, some of the features observed pointing 
 to a superficial origin and others indicating a derivation from a doep- 
 seated source. If the deposits have })een derived from a superficial source 
 they presumably have been formed by the residual downward concentra- 
 tion of kaolin derived from either the dykes of granite and bands of garnet- 
 gneiss associated with the quartzite, or from the adjoining granitic batho- 
 hths, or from both of these sources. On the other hand, if the deposits 
 have been derived from a deep seated source they have presumably Ijeen 
 formed by the alteration of feldspar contained in granite or syenite occurring 
 along the lower parts of the fracture zone and have been carried upward 
 ^"d*^. " '»<* upper parts of the zone by ascending thermal waters. 
 
 '•'• .aartzite-garnet gneiss belt in which the fracture zone 
 
 °f*^" u '; ' *'''^' ^''^^^" beneath a mantle of boulder clay, the quantities 
 of whue kaohn, discoloured kaohn, and kaolinic quartzite present in 
 association with the zone of fracture and faulting, is not even approximately 
 known, but the wide extent of the zone, and the enormous size and abund- 
 ance of the kaolin leads exposed in those parts of the outcrop of the zone 
 TO far laid bare by trenching and stripping operations indica (see page 
 6S) that there are good prospective possibilities for the discovery of 
 enormous masses of these materials. 
 
 (iraphite. 
 
 At the eastern end of lots 15, 16, antl 17, range VI, Amherst town- 
 ship, a ridge of Clrenville limestone occurs throughout which masses of 
 pegmatite, pyroxene granite, and pyroxene syenite are included. Within 
 the hmestone adjacent to these included rock masses aggregates of wollas- 
 tonite, diopside, seapolite, and other lime silicate minerals are developed; 
 and throughout these aggregates graphite occurs abundantlv in coar.se 
 flakes up to 2 inches in diameter. 
 
 The occurrence of these deposits in association with inclusions of 
 Igneous rock in the limestone and in some cases following the margin of the 
 inclusions seems to indicate that they have been developed by the inter- 
 action of emanations from the igneous inclusions and the limestone. 
 
 The underground workings on the property were filled with water at 
 the time the writer made his examination of the district and such evidence 
 as was obtained with regard to the extent of the deposits was limited entirely 
 to the surface openings. Although the proportion of graphite contained 
 in small masses exposed in these excavations was as much as 50 per cent 
 in places, the deposits for the most part were too irregular and discontinuous 
 to be profitably mined. 
 
45 
 
 Plate II. 
 
 A. St. Heini flat and village of .St. Reini, as seen from the .\l«io riilge. (Pago 4.) 
 
 B. Washing plant, Canadian China Clay Company, lot V, range VI, south, Amherst 
 township, Quebec. (Page 36.) 
 
 61859-8 
 
46 
 
 Plate III. 
 
 A. Cnmiplo!!, vnrit'(tiitp<l pirnot (siicixs iiunibcr of Ihp (Irenvillc soricji, lot 6, 
 rangr VI, south, Amherst township, Qui-bcc. (Page S.) 
 
 B. Banded gametiferouR gabbro, lot 1, range II, Amherst township, Quebec. (Page 12.) 
 
47 
 
 . 
 
 J 
 
 ^^H^/■ 
 
 
 ^^^:: 
 
 
 
 
 
 /. .-^A 
 
 
 I; 
 ■g 
 
 a 
 IS 
 
 S 
 
 2 
 
 
 ■%XM.. '^fe 
 
 to 
 
 m 
 
 3 
 
 e 
 
 e 
 
 s 
 
48 
 
 Plate V. 
 
 A. Jointing in GrenviUe quaHxite in fault .one, lot 5, range VI, south, Amherst 
 township, Quebec. (Page il.) 
 
 B. Fluted and slickemnded suHace of GrenviUe qu«f^ »»^g fault lone, lot 6, 
 range VI, south, Amherst township, Quebec. (Page ll.) 
 
49 
 
 PtATE VI. 
 
 Pitted surface of quartiite bed showing the solvent action of solutiong 
 depositing the kaoUn in the quartzite, lot 5, range VI, south, Ambci-st 
 township, Quebfec. (Page 23.) 
 
 «18JW-« 
 
 B. Specimen from kaolin deposit, lot 6, range VI, south, 
 Amherst township, Quriiec. (Page 23.) 
 
M 
 
 Plate VII. 
 
 Agp-ogatp of orthtM'laBo. pyroxene, titanitr, wolbslonite. Kraphilc, and oalcitp iissociated 
 with graphite dep<«-it, lot 1" range VI, Amherst township, Quebt'O. (F:ige 13.) 
 O, orthoolase; P, py me; W, wollastonito; C, graphite; (', e:'!;ite. 
 
•1 
 
 INDEX. 
 
 Accen, meaiu of paoi. 
 
 ■\J8nnuui * 
 
 Amhent townahip ** 
 
 Aiuihraii, cornwh jitone, by A. G. Spencer. .'...'.'..'.'. oi 
 
 kaolin... . fj 
 
 " by A. G.' Spencer! '.'.'.'.'.'.'.'.'.['.'.'.". S 
 
 " kaolinic wall rock J? 
 
 Baaal eonplex. 
 BeU, B. 
 
 Bib'.oaaphy. 
 BiihoToC.. 
 
 Bricks.. 
 Broderick, J. C 
 
 Buckingham ttrin A" 
 
 Butler.^.H *• 
 
 6 
 
 27 
 
 3 
 
 27 
 
 35 
 
 18, 24 
 
 11, 42 
 
 28 
 
 Calcite ^. 
 
 Cameron, F. K *; 
 
 Canadian China Clay Comply.. i',' "s,' IS,' M, '21V 24, 24, sV, 32. 34 
 
 „ ,, ,, equipment and nuning methods ag 
 
 „ ^ . production •» 
 
 Northern railway o"ii"iA Ti 
 
 " „ . " " Hubcrdeau branch...: ] ' "' \Z' JS 
 
 II Pacific '< .......'.['.'. ' 2 
 
 „ _, " " Mont Lauricr branch \1 
 
 TestmK Laboratorien, Montreal ' ii 
 
 Carbon dioxide f? 
 
 Carlsbad ^ 
 
 China cUy, tests of f° 
 
 Clarke, F; W 34 
 
 Chy, marine 7? 
 
 Cole, Heber H 
 
 Collins, J. H ^ 
 
 Conclusions ^ 
 
 Cornish stone iaoA Jl 
 
 n " „," ,.«°»'y»«.o'.»'y A. G.Spencer ....:;:::.:::::::.■■; "*■ ■'*• ^ 
 
 Cornwall kaohn deposiu S 
 
 D. 
 
 Daubree, A „_ 
 
 DeUuny, L ^' ^ 
 
 Diabase ~ 
 
 Diopeide ]° 
 
 Dolmage, V *? 
 
 t I 
 
 E. 
 
 Eichstadt „ 
 
Fuikb« 
 
 Fin-brick 
 
 " -ctay 
 
 Pofahhanuner 
 
 Fracturinc, gnutulttr.... 
 Fuclu 
 
 Paos. 
 
 21 
 33 
 33 
 
 » 
 
 n 
 
 Gitbbro 
 
 Oagcl.C 
 
 Oamct gneiw 
 
 " " kaoliniscd 
 
 Gtotogy 
 
 " IHienl 
 
 Okekl 
 
 GottiB, L. P 
 
 OrHUt*«yenite gneiM 
 
 Onphite 
 
 <* (cMboa) 
 
 " limited 
 
 " origiii 
 
 " jmnteatmi 
 
 Grenville limMtoM 
 
 " Pn-Cmmbriui subprovincp 
 
 I, 87, 
 
 .:i3, 
 
 6, 7, 9, 
 
 Grape, O. 
 Gummel... 
 
 " oricin 
 
 H. 
 
 11 
 
 » 
 
 7 
 
 34 
 
 e 
 i« 
 
 1 
 u 
 
 43 
 40 
 88 
 
 41 
 40 
 
 a 
 
 • 
 
 43 
 
 9 
 
 28 
 
 as 
 
 VT 
 
 HelcB iron mine ofi 
 
 Hicklio^T, O 38 • 29 
 
 Howe, J. A ■.•••.•.■ •'. la' ta 
 
 HubeideftU branch, Canadimn Northern railway la, »o 
 
 Jointing. 
 
 21 
 
 K. 
 
 Kaolin. 
 
 1, 2, 18, 32, 
 
 Ai^errt" townrfiip, mnaiy»i» of, compared with analyses of kaolin from 
 other countries 
 
 " analysis of, by A. O. Spenoer 
 
 " denosit 
 
 " deposit*, extent of 
 
 " description and percentage 
 
 " discoloured 
 
 " from a deep seated source 
 
 " " supwficial source 
 
 " hypothnis of origin 
 
 " discobration in 
 
 " leads 
 
 " of superficial origin • ■• 
 
 " or luwlinizing agency of deep-seated origin 
 
 " uses 
 
 " white 
 
 Kaolinic quartiite 
 
 " wall rock i"tA 
 
 Keele.J ^' ^' 
 
 .18, 33, 
 
 42 
 
 24 
 24 
 19 
 31 
 20 
 33 
 30 
 29 
 26 
 31 
 20 
 26 
 27 
 34 
 32 
 42 
 35 
 35 
 
 ^O^HSSii^tHBi^ 
 
. 
 
 Unjpn.A. 
 
 " R 
 lAurtdtliin.. 
 
 Paiib. 
 
 W 
 IS 
 M 
 
 iJmatoae, aysuiUm. '.'..'". '| 
 
 l.indicrra, W J 
 
 lioraiiitn. 
 
 ■» 
 
 i:^."''.''v-:;:;;;;;;i:i;;:i:i;:;:i::iiii:i:::i;i-:;::::;;;;^^ 
 
 M. 
 
 Mallard. 
 
 Marine ahelii 
 
 MaaluBonae rirer 
 
 MrtMDorphie pyroxenite 
 
 Mil arml depoalu 
 
 Mineralogy 
 
 «"?i*i ^^'^ branch, Canadian Pacific' railway.'. '.'..'.'.'.'.'.'.'. 2 
 
 MuMler, R 
 
 Multipar pit 
 
 " ayndicate .....'.'.'..'.'.'.'.'.. 
 
 IS, 
 
 IT 
 3 
 13 
 43 
 40 
 13 
 27 
 » 
 39 
 
 K. 
 
 North Shore branch, Canadian Pacific railway. 
 
 Obalaki, J. 
 Orthoclaae. 
 
 3 
 40 
 
 Physiography . 
 
 Pleistocene marine clay 
 
 Pneumatoljrtic theory 
 
 Ponsonby township 
 
 Pre-Cambrian complex 
 
 " formation /, 
 
 " granitic rocks 
 
 " mtnisives, late 
 
 Previous work 
 
 Pyroxene dioritc '..'.'.'.'....... 
 
 " syenite 
 
 Pyroxenite 
 
 42 
 4 
 
 34 
 2S 
 
 4 
 42 
 42 
 15 
 16 
 
 2 
 11 
 10 
 11 
 
 Quarts.. 
 
 Quartsite. 
 
 Grenville.. 
 
 40 
 
 " kaoimiT:::;;;;:: "^^ 2»- 23. 29 
 
 Quaternary '2 
 
 deposits '.'.'.'.'.'.'.'.'.'.'.'.]'.'.'.'.[[['.['..['. IS 
 
 42 
 
i4 
 
 Paob. 
 23 
 
 ggf^«"' ::.:::.:::::::::::::::.::::::'.'.'.3,'7».io 
 
 Rouse river 
 
 8. 
 
 St. Bemi 09 
 
 " deposits , *J 
 
 " district *• ; 
 
 " flat ,2 
 
 " Kaolin Company |° 
 
 Sand.. 40 
 
 Soapolite 20 
 
 Sehinid. E. E na 
 
 Selle, V. ^ 
 
 8p«mcer, A. G l ' '. '. l ! ] ] '. ! ! ! ! ! /iS, 20 
 
 otanl, A 28 
 
 Stremme, V g 
 
 Structural relations 00 
 
 Stutxer, O ^ 
 
 Summary 
 
 T. 
 
 Table of formations ib 
 
 Tasse, PhiUbert '.'.'.[['.'.'. 4 
 
 Terrace 
 
 Thomas, Milion ^ 
 
 Titanite *" 
 
 U. 
 
 Uplands, drift-covered g 
 
 " rocky 
 
 V. 
 
 Von Buch 
 
 W. 
 
 Wollastonite ^ 
 
 I 
 
t^^ 
 
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Hon. Martin HunHtii 
 
 WiLLIAN 
 
 l^EGEND 
 
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 GLACIAL 
 
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 ORCNVILLE '< 
 
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 CiTstdUiM laaaati 
 
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Department of iEtms 
 
 M HuHHiLL, Minister; R.G.M'CoMNELL.Df.PuTy Ministir 
 
 OeOLOOICAL tURVEY 
 
 William M'^Innfs Dihectinu Geologist 
 
 tomi*<l I9HI 
 
 OUTLINE MAP 
 
 LEGEND 
 
 9li vela ^romdm mt^ ViHlitiniin 
 
 -_j 
 
 not wdl Aaftofld 
 
 Bmitymy 
 
 ft'opoaad raObrn- 
 
 Aerial «r— iiaj 
 
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 ■t»d 
 
 ORCNVILL-C 
 
 fyfimtmM 
 
 H^mmmuml 
 
 9yva.hokm 
 
 <i«nlggiral boundari* 
 
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 KT^ 
 
 aiy and atrika 
 
 
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 PORTION OF AMHERST TO> 
 
 •*>'M.B.WU4B. 
 
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 tttifnmir. a^UiuUtmt. U'M Wimt 
 
 FulAicatiaa. jr> Un 
 
 TOWNSHIP. LABELLE COUNTY, QUEBEC 
 
 Seal*" of Peet 
 
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