Local causes influencing the course of glaciers. Lateral and terminal' moraines. drift. The striæ following the above courses may not have been all produced at the same time and by a continuous glacier. The ice-sheet would probably move in different courses in different parts, according to the general slope of the surface on which it rested, or according as it accumulated in one part and the resistance became relieved in another. When the maximum had passed, the more its mass diminished the more it would be influenced by the local form of the land. Finally, when it became divided into separate glaciers, these would follow the valleys or would be guided by their confining ridges. Hence in the bottoms of many valleys we find the striæ parallel to their general thread. There is reason to believe that the relative levels of some parts of this continent have changed considerably since the Drift period, and this circumstance must be taken into consideration in connection with the formation and the movements of the ice-sheets of glacial times. They Some The local or final glaciers of the period sometimes ploughed their way into the mass of till which had been left by the more general one. also left behind them lateral ridges or moraines of boulders and earth. fine examples of these are to be seen on either side of the southern part of Long lake, north of lake Superior, and along the upper parts of the valley of Steel river in the same region. In some cases the ancient glaciers also left terminal moraines, and these by damming up the waters have formed some of our smaller lakes in the north country. At any given locality the greater part of the materials of the drift Material of the usually consist of the debris of the rocks immediately underlying it, but it generally also contains a large amount of transported material, the percentage diminishing about in proportion to the distance from which it has been carried, the harder rocks surviving the wearing action the longest, and thus travelling the furthest. gravel strata. On the generally lower levels of the province, and in local depresClay, sand and sions elsewhere, we find stratified clay, sand and gravel resting upon the till. These sands and gravels are usually above the clay. It is supposed that the cause of this was a submergence of the land after the Glacial period, during which the clays were deposited, and as the land rose again the sands were spread over them, and that both deposits were worn into terraces during stationary intervals while the general elevation was going on. In the eastern and northern parts of the province some of the clays and Marine fossils in sands contain sea shells and other fossils, indicating a marine origin. In the districts of drift. valley of the St. Lawrence these are found as far west as Brockville, and along the Ottawa they extend about as far up as the junction of the Bonnechère river in clays and sands which constitute continuations of extensive deposits of the same character in the province of Quebec. But no marine fossils have as yet been found in any of the Post Tertiary deposits in the province west of these points and south of the watershed of Hudson bay. The writer has, however, discovered a variety of marine shells on the Albany, Kenogami, Missinaibi and Mattagami rivers up to heights of about 300 feet above the sea level and more than one hundred miles inland. West of the points above mentioned, south of the height-of-land, the marine deposits are replaced by others which appear to be in part, at Saugeen clays. least, of fresh water origin. One of the most important of these is an extensive blue clay deposit which we have called the Erie clay, and which The Erie and has as yet yielded no organic remains of any kind. It burns to white bricks, while the marine clays to the east burn red. The Erie clay is often very calcareous, and is seldom or never entirely free from pebbles and stones, more or less thickly disseminated through it. Indeed it often seems to merge into the underlying boulder clay. It covers the whole of the south-western part of the western peninsula, and is locally developed in many other parts of the province as far east as the line of railway from Brockville to Ottawa. Its greatest known depth is about 200 feet, but it is found at differences of levels amounting to 500 feet. When seen in fresh section it presents lines of stratification, and often a transversely jointed structure. In some localities its upper parts have been unevenly denuded before the deposition of the next higher formation, which consists of brownish clay yielding red bricks. unconformable formation is well developed in the valley of the Saugeen river, and hence it has received the name of the Saugeen clay. Its thickness appears to be less than that of the Erie clay, but it is found in broken areas in all parts of the province except the most easterly and northerly. When seen in fresh section it is usually found to be very distinctly stratified in thin layers, sometimes with partings of fine sand between them. Beds of sand and gravel are occasionally found between the Erie and Saugeen clays, and these are of importance as affording good wells of water. Fresh-water shells have been detected in a few instances in the Saugeen clay. The sand deposits overlying the Saugeen clay in the southern parts of Ontario are too irregular and varied in character to admit of classification Algoma sand, for the present. But in the district of Algoma and between the great lakes and the Ottawa river a yellowish sand, to which the name of the Algoma sand has been given, is extensively distributed in the more level areas, while on the higher grounds are found considerable accumulations of gravel, stones and boulders, which have been already referred to. Deposits of clay resting on sand with clay again beneath are found over large areas in the extensive and comparatively level tracts beyond the height-of-land. These regions have been explored and reported upon for the provincial government by Mr. E. B. Borron, who has paid much attention to their surface geology. In the western peninsula there is a remarkable and very extensive accumulation of gravel above or west of the Niagara escarpment, which Artemesia extends from near Owen Sound to Brantford. It has been called the Artemesia gravel. gravel, after the township of that name, and consists principally of the debris of the Niagara and Guelph formations, with some pebbles and boulders of Laurentian origin. The gravel, which has a considerable depth, is well rounded, often washed clean of finer material, and is extensively used for road metal. the Drift. From an economic point of view the superficial deposits are important in relation to water supply, the nature of the soils which they afford, etc., and Economics of many of the clays have a direct value for the manufacture of bricks and drain tiles. The shell-marls and peat among the recent deposits also belong to this part of our subject. Lignite, associated with clay and sand, is found on the Actinolite in Goulais river, and indications of it have also been met with on Rainy river and the southern part of Lake-of-the-Woods. North of the height-of-land the writer has found beds of this substance associated with the till and the overlying deposits in several places on the Missinaibi river, and also on the Kenogami. Extracts from the evidence of witnesses examined by the Commission bearing on the geology of the province are appended to this section, in accordance with the general plan of the Report. EASTERN ONTARIO REGION. Charles Taylor-We get actinolite within a distance of two and a half to four miles from Bridgewater; there is some in the 2nd concession of Hungerford, and Hungerford and there is some on lot 7 in the 2nd concession of Elzevir. I know where there is Elzevir, plenty of it, but the greatest deposits are in those places; it is in pockets in a magnesian rock associated with dolomite. It appears in forms like veins, which run crosswise of the country rock. We find it at the surface, but have never been successful in following it to any depth; it appears to be in pockets and runs out. "Occurrences of magnetic iron go in Bedford. Joseph Bawden-The magnetite in Bedford is found against crystalline limestone, with hornblende on one side and hornblende or granite on the other. In one occurrence the hornblende is on the north and the crystalline limestone on the south. At Black lake we have the granite on the north side, and I think crystalline ore and plumba limestone on the south side, but I cannot speak positively as to that as it is under water. The granite in Bedford is, I think, mostly on the north side. The course of the iron deposits is north-east and south-west. Some years ago a shaft was sunk 30 feet, and a drift of 30 feet was opened on lot 2 in the 6th, and about 100 barrels of plumbago were taken out and shipped to the United States, since which time no work has been done and no plumbago has been mined for export. The plumbago occurs kidney shaped, and in round nodules in crystalline limestone in a well defined vein fully three-quarters of a mile in length and 10 feet wide; the walls are limestone. The gangue is crystalline cales par occuring in crystalline limestone. The vein is defined by a little band of hematite, a gossan streak on each side of the vein; it is just like a ribbon. I take it to be a true fissure vein. The limestone in the vein is coarser, and it is plumbaginous, the plumbago being diffused through the vein as mentioned. The nodules are from a quarter of a pound to five pounds weight. The plumbago is of very good quality. Michael Grady-The iron deposits of the Kingston and Pembroke region are Iron ore in the usually found in belts the general run of which is north-east and south-west, about the same as the ordinary run of the rock. The associated rock is granite, and where we find limestone coming in contact with it we always consider the indications favorable for iron. The largest deposits I found were where the limestone and granite came in contact. We have found some soapstone on the surface, but as a general thing it is down deep. I have found some connected with diorite. It is difficult to account for its occurrence when hardly any two experts will agree; each seems to have his own idea. I never noticed any ranges of greenstone rock. The rock in this country varies very much. In building the railway in a cutting of two or three hundred feet four or five different kinds of rock would be found, such as limestone, red granite and black granite. Kingston and Pembroke district. Iron ore in Iron ores in the Haliburton district. At William Rattle-There is no question but they have the true formation for ore-bearing rocks in Darling. We found specular ore in several places on the range. In one place we were shown a vein of magnetite 35 feet in width. another place we saw hematite at least 15 feet in width, and in length we traced it 200 feet. I should judge from appearance that it was a very good quality of ore; it had no appearance of sulphur or titanium. That was at Playfairville. The course of those veins is north-east and south-west, dipping about 75° to the south-east. C. J. Pusey-The course of iron deposits in the Haliburton region is northeast and south-west. I have carefully observed the shores on the north and south sides of Burnt river, and they differ essentially. On the south side it is an open, granular ore of the hematite or specular kind, while that on the north side is a magnetic ore of close grain and smooth fracture. A number of specimens analysed by Professor Chapman, taken from various locations on the north side of the river over a distance of fifty miles, were so uniform in their character that they were supposed by the analyst to be taken from one location. Ores have been discovered at eight or ten different points between the north-east corner of the township of Glamorgan and the village of Bancroft, in the township of Dungannon, & distance of nearly forty miles. George Richardson-In the Kingston district the phosphate occurs in limestone Phosphate of veins in granite, the phosphate occurring in irregular masses in it. I have noticed lime." phosphate at Haley's, and it is about the same formation. Mr. Smith's mines are irregular; the work is done the same as in a quarry, there being enough phosphate between the layers of granite to make it pay. In Loughborough a great deal of the phosphate is found in connection with pyroxene rock; the pyroxene sometimes mixes with the phosphate and makes it valueless. Sometimes crystalline limestone is mixed with the phosphate in the same way. width of Perth district... Robert Adams-The apatite in the Perth district occurs more in regular seams than in the Ottawa district of Quebec, where it occurs in bunches through the Length and gangue rock. We have traced many distinct veins as much as a mile. They are, phosphate I think, mostly across the line of the stratification. Most of them run in a north- veins in the west and south-east direction, but there is a good deal of irregularity about them. The country rock is uniform, and consists largely of pyroxene. There is also a great deal of quartz in that country, and pink calcspar. In some cases we find veins in the line of the stratification, and we have struck phosphate veins running at right angles. The width of the veins varies from a few inches to six and seven feet. The greatest depth we have gone there is 100 feet. We find that as we go down the width varies, being in and out all the way down. We see no difference as far as we have observed between the workings at a depth and at the surface. James Foxton-At the surface where we found the phosphate on lot thirteen in the tenth concession of Loughborough, it was about two and a half feet wide. Occurrence of phosphate of It is enclosed in a kind of a hard black rock. On the surface we have stripped the lime in vein about twenty feet, and we have made openings along the course of the vein, Loughborough.. which runs across the whole lot. The tendency of the vein was to widen as we went down. At the top it was two and a half feet, at ten feet it was about five feet, then it ran about the same down to about forty or fifty feet, and at that depth it was about ten feet wide. Then it began to narrow till it got to be about four feet; after that it began to widen again, and continued to widen till we came upon a horse." After passing that it continued to increase in width till at the depth of 115 feet it is fifteen feet. The shaft is about perpendicular; a bucket will go down without touching anything. Sometimes we come on pieces of hornblende, some of them as large as two by four feet; the phosphate is all around them and they come out as clean as possible. The phosphate as it comes up is nixed with hornblende and the wall rock, and that is where we have the labor of cobbing it. lime in the James Bell-In the Perth district we find that generally where there is a Mica and mixture of mica, very fine and almost like salt, it is an indication that phosphate is phosphate of there. It is pretty certain to lead to a vein. There is any quantity of this dark Perth district. mica, but it is in distinct veins; it occurs on the same lot as the phosphate and within 400 or 500 feet of it. The mica occurs in veins of different widths from about three feet up to nine and ten feet. There are any number of these mica veins, the whole surface being covered with them. Marmora and William Kelly-My lithographic property is in the township of Marmora, Lithograpli being lots nine and ten in the third concession. I think the quarry extends over stone in 100 acres ; it crops up at the surface, and we have sunk about seven or eight feet Madoc. upon it. I do not know the depth below that. It is on the east side of Marmora lake. The layers are from six to twenty-four inches thick, and as they go down the thicknesses are greater; it would require to be sawed for the market. It is a pure lithographic stone. It has been tested and pronounced by experts to be equal to the best German. The property is convenient for shipping. D. E. K. Stewart-I am interested in a lithographic stone property on lot 7 in the 5th concession of Madoc. It is laminated and there are very large quantities of it. The layers of stone are from two to four and five inches thick. We can get blocks of it of almost any size; I have taken out some 48 by 36 inches. There is upwards of 20 acres covered with this stone, and it is so situated that it would not be expensive to work. W. J. Morris-Barytes occurs in Bathurst, North Burgess and North Crosby, Barytes. In Oso I have seen a perfectly pure vein three feet wide. I have seen it also in good workable veins in North Crosby. Fire clay at Salt boring at Salt boring at Tecumseh well International well. Attrill's well. Boring at Mitchell. Dublin. Brussels. J. D. Dewar-Very good fire clay has been found near Toronto, and there is any amount to be found on any of the creeks. An analysis by Mr. Sperry gave silica 63.05, aluminum 21.06, ferric-oxide, 5.02, water .63. One analysis from the surface showed 2 per cent. of lime, but I think that was owing to fossils. There are hundreds of acres of it past the Humber; the river runs over it. It resembles a blue clay and they call it shale here. What I am using I find to be very good. WESTERN ONTARIO REGION. At Dr. Timothy Coleman-Our well at Seaforth is about 1,120 feet deep. The first 100 feet was through a loose kind of limestone, hard, with soft streaks. At 350 feet we struck a strong flow of fresh water which rushed up to within six or seven feet of the surface. After going to about 450 feet the Guelph limestone is struck. At 800 feet there is a kind of rotten stone of a clay color; there is about fifty or sixty feet, but about midway is a layer of very hard stone intervening. 880 feet there is a bed of clay, and after that it is limestone down to the salt, at 1,020 feet. There is a bed of salt at that depth of seven or eight feet. We continued on 101 feet and stopped, as we were in the rock salt and had all we wanted. After coming to the first bed of salt there is a layer of three or four feet of porous rock. Peter McEwan-The first well I drilled in this part of the country (Goderich) was in 1868, called the Tecumseh. It was in the town, and the depth was 1,130 feet. The depth of the surface material or drift on the high land is 120 feet, and in the valley 30 or 35 feet. There the surface material is marl, while on the hill it is different. The first 30 feet of the Tecumseh well was quicksand, and below that it was blue clay down to the rock. There was a streak of gravel on the rock below the clay, and a little clay mixed with the gravel. It was a sort of hard pan like cement, varying from 5 to 10 feet thick. The only difference in the wells here is before striking the rock; after that all are the same. The International well was drilled in the winter of 1873-4. There was no quicksand there; it was clay down about 110 feet. Below that there was a streak of hard-pan about 10 feet, and then a grey limestone rock. The first 50 or 100 feet of the limestone is hard; after that it becomes softer and more broken, and is full of water. After getting through the broken rock the limestone becomes more solid again, and there are nodules of flint in it. At 750 feet we reach blue shale with streaks of blue clay, which continues down about 1,030 feet, where the salt is struck. We suppose that the first bed of salt is about 16 feet in thickness. Below that we have 30 feet of light brown limestone of very fine grain; then a bed of salt about 30 feet, then 4 feet of blue shale, then another bed of salt about 22 feet, below which we found a brown limestone similar to the first. We did not go much more than 15 or 20 feet further, and I think the limestone does not go below that. Before we struck the salt rock itself the shale became salty, no doubt with small streaks of salt. The first salt we struck had small streaks of shale in it, and there are small streaks of gypsum at the bottom of the shale. The purest salt of all is in the lowest bed. In Attrill's well they went down further than we did, and struck two or three small beds below ours; they were very thin beds. At the greatest depth of all they struck a red shale. In 1871 we sank a well in Mitchell 2,000 feet and did not get salt. The material passed through was pretty much the same as here, but there was not such a thickness of limestone. About the depth at which we expected to get salt we got saline water. We got about as much white clay as we get salt here. The surface is about the same as here, but there is about 100 feet of limestone less than here. When down about where the salt should be we met shale the same as here, but softer than ours. There it is more like slate. In Seaforth there is about 200 feet like clay, and in both Mitchell and Dublin where we should have struck the salt we came on the substance like pipe-clay. There was about the same thickness of it as we get of the salt,rock here. It was very like the blue clay, only there was the difference in color. I do not think any experiments were made with it. At about 1,200 or 1,400 feet we struck a red or light brown shale which continued to the bottom, 2,000 feet; there would be about 600 or 700 feet of it. That is the deepest well in this part of Canada, that I know of. The salt appears to play out between Seaforth and Dublin. I drilled a well one and a quarter miles east of Seaforth and got salt, but not in large quantity. At Dublin we did not get any salt; there was salt water, but nothing that could be called rock salt. In 1872 at Brussels we went through similar strata, and we got salt water and pumped for three weeks; there was some salt made there, but it was con |