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Ontario Geological Survey
Report 187
Quaternary Geology
of the
Palmerston Area
Southern Ontario
By
W.R. Cowan
1979
Ministry Of Hon. James A.C. Auld * Minister Natural ^ , ^ n Dr. J. K. Reynolds Deputy Minister Ontario OMNR-OGS 1979 Printed in Canada
Publications of the Ontario Ministry of Natural Resources and price list are available through the Map Unit, Public Service Centre, Queen©s Park, Toronto, and the Ontario Government Bookstore, 880 Bay Street, Toronto. Orders for publications should be accompanied by cheque or money order, payable to the Treasurer of Ontario ISSN 0704-2582 ISBN 0-7743-3621-8
Parts of this publication may be quoted if credit is given. It is recommended that reference to this re port be made in the following form:
Cowan, W.R. 1979: Quaternary Geology of the Palmerston Area, Southern Ontario; Ontario Geological Sur vey Report 187, 64p. Accompanied by Maps 2383, 2384, scale 1:50 000.
1000-300-78-TP CONTENTS PAGE Abstract ...... v Introduction ...... l Present Geological Survey ...... l Acknowledgments ...... 2 Previous Work ...... 2 Physiography and Drainage ...... 2 Paleozoic Geology ...... 3 Silurian ...... 3 Devonian ...... 6 Economic Geology ...... 6 Bedrock Topography and Drift Thickness ...... 7 Quaternary Geology ...... 7 Till Stratigraphy ...... 7 Catfish Creek Till ...... 8 Stirton Till...... 9 Tavistock Till ...... 12 Mornington Till ...... 17 Elma Till ...... 18 Saugeen Kames Till ...... 21 Glacial Landforms ...... 21 End Moraines ...... 21 Ground Moraine ...... 22 Streamlined Drift Forms ...... 22 Glaciofluvial Features ...... 23 Meltwater Channels ...... 23 Outwash Deposits ...... 24 Ice-Contact Stratified Drift ...... 25 Eskers ...... 28 Lacustrine Sediments ...... 29 Bog and Swamp Deposits ...... 30 Alluvium ...... 30 Historical Geology ...... 31 Economic Geology ...... 34 Gravel and Sand ...... 34 Outwash Deposits ...... 35 James Murray Construction Ltd. (113) ...... 35 Ice-Contact Deposits ...... 36 Clay ...... 36 Engineering Geology ...... 37 Agricultural Soils ...... 38 Appendix A ...... 39 Appendix B ...... 45 Appendix C ...... 50 Appendix D ...... 57 Selected References ...... 59 Index ...... 63
Tables 1-Chemical analyses of Salina Formation ...... 5 2-Trace element analyses of Salina Formation ...... 6 3-Quaternary deposits and events ...... 8 4-Summary of till analyses ...... 10
Jii 5-Garnet content of major till units ...... 12 6-Pebble assemblages of principal glaciofluvial deposits ...... 26 7-Agricultural soils ...... 38
Figures 1-Key map showing location of Palmerston area ...... v 2-Paleozoic geology and drainage divides ...... 4 3-Textural diagram for tills ...... 11 4-Quaternary stratigraphy along Conestogo River ...... 14 5-Quaternary stratigraphy along South Saugeen River ...... 15 6-Chert distribution in Elma Till pebbles ...... 20 7-Time distance diagram for Late Wisconsinan substage ...... 32 8-Chert distribution in gravels ...... 34 9-Location of stratigraphic sections ...... 40
Photographs 1-Salina Formation, South Saugeen River ...... 5 2-Section on Conestoga River at Arthur ...... 13 3-Tavistock Till overlying stratified drift ...... 16 4-Section 383 on South Saugeen River ...... 17 5-Typical stony Elma Till ...... 19 6-Outwash sand and gravel west of Mount Forest ...... 25 7-Glaciofluvial ice-contact sand and gravel ...... 27 8-Faulted ice-contact gravels and silts near Clifford ...... 27 9-Riverstown esker north of Pike Lake ...... 28 10-Coarse alluvium developed on Catfish Creek Till ...... 31
Geological Maps (back pocket) Map 2383 (coloured )-Quaternary Geology of the Palmerston Area, Southern Ontario. Scale 1:50 000. Map 2384 (coloured )-Granular Resources of the Palmerston Area, Southern Ontario. Scale 1:50 000.
IV ABSTRACT Surficial materials are of Late Wisconsinan age and were deposited by ice sheets originating to the north or northwest. The oldest till, Catfish Creek Till, was deposited during the Nissouri Stadial and underlies the entire map-area. It is overlain by Stirton, Tavistock, Mornington, and Elma Tills which were deposited during the Port Bruce Stadial. Stirton and Mornington Tills are believed to
Figure 1-Key map showing location of Palmerston map-area. Scale 1 inch to 50 miles (1:3 168 000).
represent fluctuations of the Tavistock ice due to enhanced flow into proglacial lakes contained within the Conestogo basin. Tavistock Till represents a major advance and underlies the entire map- area. Elma Till represents a middle to late Port Bruce Stadial event and forms the Teeswater drum lin field. The Saugeen Kames are a recessional moraine related to retreat of the Elma ice; a local silt till is present within these morainic deposits. Gravel deposits of regional economic importance are limited to outwash associated with the Sau geen Kames. Devonian chert is common in gravels located southwest of Palmerston. Slope failures are common along the Conestogo River. These occur at the discontinuity at the base of the Tavistock Till.
Quaternary Geology of the Palmerston Area Southern Ontario
by W.R. Cowan1
INTRODUCTION
The objective of this report is to provide information on the distribution, properties, stratigraphy, and history of surficial geologic materials of the Palmer ston map-area for use in planning, engineering, hydrologic, pedologic, geologic, and environmental studies. The Palmerston map-area comprises about 1100 km2 (430 square miles) bounded by Latitudes 43045© to 44000©N and Longitudes 80030© to 81 000©W (Na tional Topographic System Map 40P/15). Most of the area is within Wellington County, however, small areas are located in Perth, Huron and Grey Counties. The towns of Harriston, Mount Forest, and Palmerston and the villages of Ar thur, Clifford, Drayton, and Moorefield are the principal commercial centres. Road access to the area is by Highways 6,9, and 23 which are supported by a close network of township and county roads. Both the Canadian Pacific Railway and Canadian National Railways serve the map-area though no passenger ser vice is available. Sand, gravel, and natural gas are geologic commodities presently being com mercially extracted from rocks within the map-area.
Present Geological Survey
The present reconnaisance survey began in 1972 and was completed in 1973. Field data were obtained through the examination of roadcuts, stream and river banks, excavations, and by test pitting or hand augering. Additional data were obtained from files of the Ministries of Natural Resources, Environment, and
Geologist, Ontario Geological Survey, Manuscript approved for publication by the Chief, Phanerozoic Geology Section, July 5, 1976. This report is published with the permission of E.G. Pye, Director, Ontario Geological Survey, Ministry of Natural Resources. Palmerston Area
Transportation and Communications. Aerial photographs were used extensively. A preliminary map of the area has been published (Cowan 1976b).
Acknowledgments
Competent field assistance was provided in 1972 by D.R. Sharpe (Senior), J. Clue, J. Carr, and R.A. Brinsmead, and in 1973 by A.J. Cooper (Senior), J. Clue and J.R. Hill. P.P. Karrow of the University of Waterloo and B.H. Feenstra and D.R. Sharpe of the Ontario Division of Mines provided much discussion and in formation on geologic topics related to this survey. Many private landowners kindly permitted access to their properties. Laboratory analyses were carried out by the Mineral Research Branch of the Ontario Division of Mines. The assistance given by each of the above is very much appreciated by the writer.
Previous Work
Recent maps showing bedrock geology are those of Sanford (1969) and Lib erty and Caley (1969); the contacts on these two maps vary considerably and both should be consulted. Older maps include those of Caley (1941), Williams (1919), and Logan (1863). Subsurface stratigraphy and references are available from Beards (1967). A map of the bedrock topography was prepared by Davies and Mcclymont (1962). Early comments on the glacial geology of the map-area were made by Logan (1863) and Taylor (1909 et seq), but it was not until 1951 that a synthesis of the glacial history was available (Chapman and Putnam 1951) and much of this is relevant today. Since then detailed work has been carried out in the Conestogo area to the south (Karrow 1971; 1974; Feenstra 1975a) and in the Orangeville area to the east (Cowan 1976a). Much of the stratigraphy found in these areas continues through the Palmerston map-area. Soil survey reports are available for the entire map-area (Hoffman et al. 1952; Hoffman and Richards 1952; Gillespie and Richards 1954; and Hoffman et al. 1963).
Physiography and Drainage
The area is flat to gently rolling with elevations ranging from 490 m (1,600 feet) above sea level in the northeast to 360 m (1,175 feet) a.s.l. in the northwest and 340 m (1,125 feet) a.s.l. in the southwest. Local relief seldom exceeds 15 m (50 feet) and in general the topographic surface slopes from north to south in the eastern one third of the map-area and from east to west in the remainder. Physiographically the map-area consists of ground moraine broken by a few eskers, a series of northeast- to southwest-trending meltwater channels, drum- lins, and a belt of morainal topography located in the northwest part of the map- area. Chapman and Putnam (1951) mapped four physiographic regions in the map-area. The largest of these is the Dundalk till plain which occupies most of the map-area east of a line drawn between Mount Forest and Palmerston. This area consists of low rolling ground moraine broken by a few eskers and meltwa ter channels. The southeasternmost part of this map-area is part of Chapman and Putnam©s (1951) Stratford till plain which is essentially similar to the above. The third unit is the Teeswater drumlin field which occurs west of a line drawn between Palmerston and Drew Station. This area consists of drumlinized ground moraine having a low rolling surface. The fourth unit is a belt of rolling stratified drift located between Clifford and Mount Forest which Chapman and Putnam (1951) referred to as Saugeen kame-moraines and included it within their "Horseshoe Moraines" physiographic unit. Drainage of the map-area is to Lake Erie via the Grand River system and to Lake Huron via the Saugeen and Maitland River systems (Figure 2). Generally the northern quarter of the map-area drains northerly via Saugeen River, the western third of the map-area westerly via the Maitland system, and the re mainder southerly to the Grand system via Conestogo River. Rivers and streams are of low gradient, seldom exceeding 2.9 m/km (15 feet per mile), and become almost dry in late summer because they are in the headwater regions of their re spective drainage basins.
PALEOZOIC GEOLOGY
Regional bedrock maps including the map-area were available as early as 1863 (Logan 1863), however, recent maps are based on the mapping of Caley (1941). Contacts on the map prepared by Liberty and Caley (1969) (Figure 2) do not vary from Caley©s original. However, Sanford©s (1969) map does vary be cause of differing stratigraphic opinion. Information on the bedrock geology is available in Caley (1941), Liberty and Bolton (1971), and Beards (1967). Paleo zoic rocks within the map-area dip toward the southwest at a low angle.
Silurian
Dolostones of the Guelph Formation (Middle Silurian) underlie the north eastern part of the area but they do not outcrop. Within the area the Guelph ranges from 20 to 110 m (60 to 350 feet) in thickness. Overlying the Guelph rocks is the Salina Formation (Upper Silurian) which con sists of dolostone, shale, and some gypsum or anhydrite. These are the only rocks outcropping within the map-area; outcrops occur along the South Saugeen River about 10 km (6 miles) west of Mount Forest. These rocks are up to 60 m (200 feet) thick within the Palmerston map-area. o SI (A O U) ra ST CO en
ra O •o ra r" l LJ E o
ra o) ra o. ra E "wo
0) E ra Q. oO) w. sf O) .5 wo . ra
C\J 0) D O) OGS 9837
Photo 1-Salina Formation dolostone with interbedded shale on South Saugeen River.
TABLE 1 CHEMICAL ANALYSES OF SALINA FORMATION DOLOSTONE (2270) AND SHALE (2271).
Sample SiO2 AI 2 O 3 Fe 2 O 3 MgO CaO P 2 O S SO 3 LOI
73-2270 1.59* 0.48 0.37 21.0 29.5 0.04 0.01 46.8
73-2271 26.5 7.10 2.78 13.7 17.5 0.08 0.52 28.0
*in percent
Outcrops (Photo 1) located on lot 23, concession IV, Normanby Township, Grey County just north of the area were sampled in 1973 for chemical analysis (Table 1). Sample 73-2270 is from a 20 cm (8 inch) dolostone bed and 73-2271 from a 10 cm (4 inch) shale bed. Comparison of these data with those provided by Parks (1903) from Paris, Ontario shows the present shale unit is less siliceous and more dolomitic than at Paris. For comparison with data used in till studies the same samples were ana lysed using the Chittick procedure (Dreimanis 1962) with the following results: Sample 73-2270, 102 percent total carbonate 1 , calcite: dolomite 0.32; sample 73- 2271, 68 percent total carbonate, calcite:dolomite 0.26. Clearly tills derived from these rocks will have low calcite to dolomite ratios.
©This analytical technique is only accurate to a few percent. Palmerston Area
TABLE 2 TRACE ELEMENT ANALYSES OF ROCK SAMPLES FROM SALINA FORMATION. LOCATION AND DESCRIPTION OF SAMPLES IN TEXT. DATA IN PARTS PER MILLION (PPM).
Sample Mn Cu Pb Zn Ni Co Cr Ba Li
73-2270 130 6 50 8 < C5 6 40 O
73-2271 200 15 95 35 20 45 240 50
The samples were also analysed for trace element content for hydrologic and environmental control data. The results of this are given in Table 2. The shale sample has interesting amounts of manganese, lead, zinc, chromium, barium, and lithium. The copper, lead and zinc content in sample 73-2270 is similar to that reported by Warren and Delavault (1961) for carbonate rocks in southern Ontario excepting zinc in the Lockport Formation. The youngest Silurian unit in the map-area is the Bass Islands dolostone (Upper Silurian) which does not outcrop at the surface. It is about 30 to 45 m (100 to 150 feet) thick in this area.
Devonian
The oldest Devonian rock unit is the Bois Blanc Formation (Middle Devoni an) which consists of cherty limestone and dolostone easily distinguished from the underlying dolostone. It does not outcrop in the map-area and is about 45 m (150 feet) thick. These rocks are overlain in the southwesternmost corner of the map-area by the northern facies of the Detroit River Formation (Middle Devo nian) which does not outcrop at the surface. Within this limited area these rocks are probably not very thick.
Economic Geology
Dolostone of the Salina Formation was formerly burned locally to produce lime. At present the only commodity extracted from bedrock within the map- area (excluding water) is natural gas. This is obtained from the Arthur Gas Field located in Arthur Township. The gas is obtained from the Gull River (Middle Ordovician) and Shadow Lake (Cambrian) Formations at depth. The field was discovered in 1968 and about one half of the proven recoverable reserves remain. Production in 1972 was 51.5 MMcf which was less than one percent of Ontario production.
Bedrock Topography and Drift Thickness
A contour map of the bedrock surface beneath the Quaternary drift was pre pared by Davies and Mcclymont (1962). Their map showed a generally south west-sloping surface with elevations of 460 to 475 m (1,500 to 1,550 feet) in the northeast, 380 m (1,250 feet) in the southeast, 335 m (1,100 feet) in the north west, and 350 m (1,150 feet) in the southwest. This was broken by a poorly defi ned northwest-trending bedrock valley in the vicinity of Pike Lake which has an elevation of about 335 m (1,100 feet). Karrow (1973) in his overview of bedrock topography of southwestern Ontario referred to this as the Walkerton Valley and suggested that it is a spur of a larger valley which links with the Buried Dundas Valley to the southeast. A bedrock valley was also hypothesized in the Conestogo Valley at Drayton as well as beneath its tributary at Moorefield. More recent data allows revision of the bedrock contours, however, the south- west sloping surface is the predominant feature. Drift thickness within the map-area, as reported by well drillers, ranges from 8 to 116 m (25 to 380 feet) though in the South Saugeen Valley outcrops are present. West of Rothsay the drift ranges from 12 to 30 m (40 to 100 feet) except in the vicinity of Pike Lake where it thickens to as much as 45 m (150 feet). Northeast of Kenilworth the drift also ranges from 12 to 30 m (40 to 100 feet) in thickness. South of Kenilworth and east of Rothsay drift is between 30 and 60 m (100 and 200 feet) thick except between Kenilworth and Farewell where it may be 60 to 90 m (200 to 300 feet) thick and between Rothsay and Bosworth where more than 90 m (300 feet) of drift has been reported.
QUATERNARY GEOLOGY
Till Stratigraphy
The Quaternary succession within the map-area is established from the identification and areal tracing of till sheets which represent deposition during glacier advance or fluctuation. Several till sheets have been identified and map ped, each a continuation of units mapped in adjoining areas (Karrow 1971; Cowan 1976a). All of these are believed to be of Late Wisconsinan age, the eldest being Catfish Creek Till. Pre-Catfish Creek Tills have been identified south of the map-area (Karrow 1971) and have been investigated in detail by A.J. Cooper (1975a). Field correlation is based on lateral continuity, stratigraphic position, tex ture, pebble lithology, and physical properties such as colour, degree of compac- Palmerston Area
TABLE 3 QUATERNARY DEPOSITS OF THE PALMERSTON AREA.
Deposit Materials Landforms 1- Z alluvium sand, silt, gravel modern floodplains, channel bars uu O Jij bog deposits peat, muck, marl filled depressions
ocal glacial lake sand. silt, clay veneer on ground moraine, and postglacial pond depression fill deposits
glaciofluvial outwash sand and gravel channel fill, terrace deposits, outwash plains
silt till in Saugeen Kames silt till kames, hummocky moraine Z LU Z ice-contact stratified drift sand, gravel, silt. kames. eskers, morainal landforms EISTOCEIV WISCONSI minor till
ELMA TILL sand silt to silt ground moraine, drumlinoid till forms
LU o. 1- MORNINGTON TILL silty clay till ground moraine -1 TAVISTOCK TILL silt till ground moraine plains
glaciolacustrine sediments silt and clay mainly buried
STIRTON TILL silty clay till buried
CATFISH CREEK TILL stoney, sandy. mainly buried silt till
tion, stoniness etc. These data are supported by laboratory analyses. Textural descriptions follow the scheme proposed by Elson (1961). Principal stratigraphic sections are given in Appendix A and individual till analyses in Ap pendix B. The stratigraphy and properties of the various tills are summarized in Tables 3 to 5.
CATFISH CREEK TILL
Catfish Creek Till (de Vries and Dreimanis 1960) has been traced northward from its type area at Lake Erie to the Palmerston map-area through regional mapping programs (Karrow 1963; 1968; 1971; 1977; Cowan 1972; 1975a; 1976a; and Dreimanis 1964). It has since been traced north of the area by Sharpe (1975). Most outcrops occur in deeply eroded sections along the Conestogo and South Saugeen Rivers though the till occurs close to the surface through much of the northeast part of the map-area. It occurs east of the area and its presence has been suggested west of the map-area (Cowan et al. 1975) though this is not 8 proven. It may be assumed to underlie the entire map-area though perhaps dis- continuously. Except in the southernmost part of the map-area it may be as sumed to rest on bedrock. Available outcrops are usually less than 3 m (10 feet) thick though up to 9 m (30 feet) was observed near Drayton; thicker occurrences probably prevail as the base of the till was only observed in the northern part of the map-area. As is characteristic in other areas, the till is a stony to bouldery (up to 15 percent clasts), extremely compact, sandy silt till (Figure 3). Unoxidized, it is grey to greyish brown (2.5Y5/2)1 and it oxidizes to yellowish brown (10YR5/4) or brownish yellow (10YR6/5). High dolomite in the pebble and silt-clay frac tions (Table 4) indicates derivation from Silurian dolostones occurring within and north of the map-area. Microscopic examination of six heavy mineral sam ples (Table 5) gives results which indicate the till has a distant source area within the western Grenville Province of the Precambrian Shield (Gwyn 1971). Four till fabrics from this till gave the following computed vector means ISO0 , 3100 , 3080 , and 2240 . Upper and lower contacts of Catfish Creek Till were generally sharp where observed. In the southern part of the map-area the till may be overlain by la custrine sediments, Stirton Till, or Tavistock Till. In the north it may be over lain by stratified drift or Tavistock Till. Through correlation with the type section at Lake Erie, Catfish Creek Till may be related to initial Late Wisconsinan glacier2 advances about 23,000 to 16,- 000 radiocarbon years ago (Nissouri Stadial of Dreimanis and Karrow 1972). The Palmerston area was probably overlain by ice throughout this stadial. Within the map-area it appears to occur as remnant ground moraine (largely buried). Dolomite content, heavy mineral content, and till fabrics indicate a northerly source area (Georgian Bay lobe).
STIRTON TILL
Stirton Till (Karrow 1974) was first identified south of the Palmerston area by P.F. Karrow (1971, till "B"). It takes its name from the hamlet of Stirton lo cated 3 km (2 miles) south of Drayton. Within the map-area it has only been ob served along the Conestogo valley between Arthur and Drayton and it has not been mapped at the surface. Its western limit is unknown and it has not been observed east of the Palmerston map-area by the writer. In the subsurface it is thought to be limited to the Conestogo basin area.
1 Munsell colour code 2A lens or inclusion of silt from Catfish Creek Till at Arthur was examined for pollen content by Christine Manville and J.H. McAndrews of the Royal Ontario Museum who reported the following: "The silt contains a small but significant amount of pollen, that is, 1095 pollen per gram. The follow ing number of grains were counted: Picea 36, Larix l, Juniperus l, Pinus 75, Quercus 3, Gramineae l, Ambrosia l, Tubuliflorae l, Dryopteris type l, Selaginella selaginoides l, and Cyperaceae 1." The data are consistent with those reported elsewhere for Middle Wisconsinan Interstadial pollen records. It is probable that the silts were incorporated into the till from underlying Middle Wisconsi nan lacustrine sediments. Palmerston Area "o CO O5 CO in O o 9 r ^ o w Tt CO CO r* co O5 o'CO Tt CO (3 d d d 6 d d d d d in T- oo o oo Tt in "!5 05 CO Tt CO p^ in V) Lil S CO Tt Tt CM P-. P-. CN 1- Tt Tt in Tt Tt CO in in z 0) o 3* o in CM t- o m I- K E 05 CO 00 o 00 o CO in CO Z t UJ S o Tt O5 O5 Tf in d CM CO O CO CN CO (N CN i- CN CM Tt CO OZ C* *7 T "? CM " o t d co d r- d o d UJ j W CO 'o CO T^ ^t 05 CO i— CN CN CN d CN p* d CM CO S s (3 CO CN - - o
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11 Palmerston Area
TABLE 5 GARNET CONTENT AND PURPLE TO RED GARNET RATIOS FOR HEAVY MINERALS CONTAINED IN THE THREE MAJOR TILL SHEETS OCCURRING WITHIN THE PALMERSTON AREA.
Till Sample Size Garnet Content "/o Purple/Red Range Mean Range Mean
Elma 10 5-14 10 .13-.43 .26
Tavi stock 9 8-28 16 .17-.45 .32
Catfish Creek 6 635 14 .20-.33 .26
Within the map-area Stirton Till is a dolomitic, silt to silty clay till which is very dark grey (10YR3/1) to greyish brown (10YR5/2) in colour. Observed thicknesses range from l to 3 m (3 to 10 feet). It is lithologically very similar to the younger Tavistock Till (Table 4) though it is usually finer grained. Pebble and cobble content is usually less than one percent and the till is very stiff. Li thologic data presented are similar to those for Stirton Till to the south (Karrow 1974a; Feenstra 1975a) though more dolomitic due to a lesser influence of Devo nian limestone. Where the lower contact is exposed the till may directly overlie Catfish Creek Till or intervening lacustrine sediments which account for its fine grained texture. It is usually overlain by lacustrine sediments then Tavistock Till (Photo 2). In several multiple till sections along the Conestogo River, Stirton Till was found to be absent (Figure 4). The dolomitic lithology of Stirton Till indicates a Silurian source area in the north. The computed vector mean for one till fabric (Sample site 22) was 168 de grees and striations measured on the upper surface of an included cobble at the same site were oriented at 3100 to 3300 . It is probable then that Stirton Till was deposited from the northwest (Georgian Bay lobe) which concurs with the origin suggested by Feenstra (1975a) and Karrow (1974). Based on stratigraphic position Karrow (1974) assigned Stirton Till to the Port Bruce Stadial (circa 15,000 years B.P.). Compared to the Tavistock Till, Stirton Till represents a minor advance which probably occurred as a fluctuation during advance of Tavistock ice. Within the Palmerston map-area the restricted occurrence and relationship to lacustrine sediments of Stirton Till leads to the conclusion that this fluctuation was the result of enhanced flow rates in a lacust rine environment (e.g. Wright 1973). Karrow (1974) has suggested that Stirton Till may correlate with the Mary- hill Till of the Ontario lobe to the east.
TAVISTOCK TILL
Tavistock Till (Karrow 1974a) has been traced into the Palmerston map- area from the south (Karrow 1971, till "C") and from the east (Cowan 1976a). It occurs as ground moraine over much of the eastern part of the map-area and has 12 OGS 9838
Photo 2-Section 22 (see Appendix A) on Conestogo River at Arthur: A - Weathered gravel; B - Ta- vistock Till; C - stratified sediments; D - Stirton Till. been observed in the subsurface along the South Saugeen River, near Listowell, at Palmerston, and possibly at Newbridge. In addition it has been traced north of the map-area by D.R. Sharpe (1975) and has been tentatively identified as far west as Wingham by the writer (Cowan et al. 1975). It is therefore believed to be present throughout the entire Palmerston map-area. Observed thicknesses range from l to 9 m (3 to 30 feet). Texturally this till is a silt to clayey silt till containing about two percent pebbles and cobbles; it overlaps the siltier phases of Elma Till and may be difficult to separate from it locally (Figure 3). It is stiff to very stiff and is usually oxidized to a brown or yellowish brown colour (10YR5/3-10YR5/4) though deep sections show it to be dark grey or dark greyish brown (10YR4/1-10YR4/2) when unoxidized. Lithologically the till contains high dolomite in the pebble and silt-clay frac tions (Table 4) indicating that it was primarily derived from Silurian dolostones, i.e. from the north or northwest. Garnet ratios in the heavy mineral fraction (Ta ble 5) imply a distant source in the western Grenville Province of the Precam brian Shield to the north (Gwyn 1971). Lithologic data are similar to those of the Orangeville map-area to the east (Cowan 1976a) however more limestone associ ated material occurs in this till south of the area (Karrow 1974; Feenstra 1975a) due to the greater influence of Devonian limestones. 13 Palmerston Area
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OGS 9839
Photo 3-Tavistock Till overlying sand and gravel 3.2 km (2 miles) southeast of Mount Forest.
In the southern part of the map-area Tavistock Till may overlie Catfish Creek Till directly or it may overlie lacustrine silts and clays and then Stirton Till (Figure 4). To the north it is frequently observed overlying glaciofluvial sands or gravels (Photo 3), thin lacustrine sediments, or Catfish Creek Till. In the vicinity of Drayton it is overlain by thin lacustrine sediments then Morning ton Till; throughout much of the remaining area it is overlain by Elma Till though up to 2 m (6 feet) of sand may intervene. At a few sites thin lenses or beds of silt were found within this till, and near Mount Forest (Section 383 Appendix A, Photo 4) 1.2 m (4 feet) of gravel and sand was observed between two units of Tavistock Till. In the same vicinity the north end of the Mountview Esker is locally overlain by Tavistock Till. These occurrences lead the writer to suggest that a minor fluctuation occurred in the northern part of the map-area during retreat of Tavistock ice, probably over a distance of less than 1.5 km (l mile). It is not known whether this event has any relationship to the Maple Lane Moraine (Sharpe 1975) which extends to the northeast. Dolomite content, garnet ratios, esker orientation, and surface flutings (120- 140 degrees) indicate that Tavistock Till was deposited by ice moving from northwest to southeast (Georgian Bay lobe). Stratigraphic evidence presented here and elsewhere (Cowan 1976a; Karrow 1974; Terasmae et al. 1972) shows this till to be of similar age to the Port Stanley Till of the Ontario-Erie lobe (de 16 Photo 4-Section 383 (see Appendix A) on South Saugeen River east of Mount Forest: A - mainly Tavistock Till; B - gravel and sand; C - Tavistock Till (?) with Catfish Creek Till at base; D - sand; E - silt with few clay bands.
Vries and Dreimanis 1960; Karrow 1974) and it is therefore of Port Bruce Stadial age (Dreimanis and Karrow 1972).
MORNINGTON TILL
Mornington Till (Karrow 1974; 1971, till "D") takes its name from Morning ton Township south of the Palmerston map-area. Within the map-area it out crops over a small area near Drayton. Here it is usually less than l m (3 feet) thick and auger sampling may penetrate the entire thickness to reveal underly ing lacustrine sand, silt, and clay. It is closely related to an overlying gritty la custrine clay from which it is difficult to distinguish. Mornington Till is a dark grey to grey, frequently mottled, clay till with rare pebbles. Though no samples were obtained, it is very similar texturally and li- thologically to both Tavistock and Stirton Tills (Feenstra 1975a). For this reason it may outcrop over a slightly larger area shown on Map 2383 (back pocket). Data presented by Karrow (1974) and Feenstra (1975a) indicate that this till was deposited from the northwest (Georgian Bay lobe); flutings on this till ori ented at ISO0 to 1600 are continuous with flutings on the younger Elma Till and may represent later overriding rather than the flow direction of Mornington ice. 17 Palmerston Area
The limited outcrop area of this till suggests that it represents a readvance dur ing retreat of the Tavistock ice, largely into a shallow proglacial lake. This latter condition perhaps explains its limited northerly extent, i.e. it is postulated that Mornington Till represents an areally restricted advance with flow rates en hanced by the proglacial lacustrine environment (e.g. Wright 1973). The ad vance was limited to the north by the lake margin and may be a time equivalent of the fluctuation in deposition of Tavistock Till described above. Auger sampling near Moorefield showed Mornington Till to be overlain by Elma Till. Due to its stratigraphic position Mornington Till has been assigned to the Port Bruce Stadial (Karrow 1974).
ELMA TILL
Elma Till (Karrow 1974; Karrow 1971, till "N") takes its name from Elma Township south of the map-area. It is the till of the Teeswater drumlin field and as such was referred to informally as "Teeswater till" by Chapman and Putnam (1943b) who described it as stony loam containing locally derived rock frag ments. This till mantles much of the western two-thirds of the Palmerston map- area and has its eastern margin within the map-area. The outer margin is not marked by an end moraine but by numerous ice-marginal meltwater channels and an attenuated drift border. The thin discontinuous nature of the latter means that shallow or areally small outliers of the till have not been mapped, es pecially in that area between Wagram and Kenilworth where the till is only identifiable as 50 cm (IVz feet) of weathered loam. Elma ice locally flowed beyond its mapped drift border fluting the subjacent materials. A similar occurrence has been described by Feenstra (1975a) who demonstrated that some flutings on Mornington Till were actually the product of Elma ice. Elma Till occurs as ground moraine or drumlinized ground moraine within the map-area. Observed thicknesses range up to 9 m (30 feet) though greater thicknesses may be expected, especially in drumlins. It is a stony (five to seven percent; Photo 5), sandy silt to silt till ranging from soft at the surface to very stiff at depth. Most exposures are oxidized and the predominant colour is yellowish brown (10YR5/4) though it ranges to brown or light yellowish brown. Texturally Elma Till is more sandy in the west and northwest and finer grained to the east and southeast. In the Trecastle-Moorefield area a clayey phase exists (samples 358, 359, 360, 361; Appendix B) which is believed to result from massive incorporation of older fine grained till, principally Tavistock Till; some of these samples also have calcite:dolomite ratios more akin to Tavistock Till. The textural overlap of Tavistock and Elma Tills (Figure 3) in the eastern outcrop area presented some problems in field separation. At depth the sandy Elma Till is physically very similar to Catfish Creek Till; greater clast rounding and the absence of flaggy clasts in Catfish Creek Till may usually be used to re solve this problem. Pebble lithologies strongly reflect the underlying bedrock. Most of the till contains high percentages of Silurian dolostone and less than five percent chert, however, in the subcrop area of the Bois Blanc Formation, chert content in- 18 OGS 9841
Photo 5-Typical stony Elma Till in northern part of map-area.
creases to as much as 17 percent (Figure 6). Garnet ratios (Table 5) are similar to Tavistock and Catfish Creek Tills and imply a western Grenville Province source for far-travelled material (Gwyn 1971). Jasper conglomerate pebbles of probable Huronian Provenance (Lorrain Formation) occur within the till but very rarely. D.R. Sharpe (Ontario Division of Mines, personal communication 1975) has noted limonite erratics in both Elma and Tavistock Tills. Throughout most of its outcrop area Elma Till overlies Tavistock Till or associated stratified drift, however east of Moorefield hand auger sampling shows Mornington Till to be the underlying material. Where overlying materials are present they usually consist of outwash sands, lacustrine sands, or bog de posits. Elma Till was deposited by a major advance from northwest to southeast (Georgian Bay lobe) as determined by, 1) orientation of the Teeswater drumlins (1200-1550 ), 2) low chert content except in the southwest, 3) the very high do lomite content, and 4) garnet ratios. Ice moving from a more westerly direction would have resulted in a broader distribution of chert (Figure 6). The age of Elma Till is known from its relationship to other tills. From data presented here and by Karrow (1974) it is known to overlie Tavistock Till or Mornington Till, where it is present, which are known to represent the early part of the Port Bruce Stadial. To the west, Elma Till is known to be overlain by till of the Mitchell Moraine (Cowan 1974; Cowan et al. 1975; Cooper 1975b) and by till of the Wawanosh Moraine (Cowan 1974) which are known to be pre-Port 19 Palmerston Area
11
o i) 2 w -Q c l |-8 l l!
*- *- JO tb *o fe s .s -S l l l 8: S^
0
20 Huron Stadial and therefore late Port Bruce Stadial in age. To the north Elma Till is known to be overlain by silt till of the Walkerton moraine1 (Cowan 1975b) which is believed to be of Port Huron Stadial age (Chapman and Putnam 1966). Therefore in its peripheral outcrop areas, Elma Till is of middle Port Bruce Sta dial age (circa 14,300 years B.P.) and to the north of the map-area it also spans much of the latter part of the Port Bruce Stadial.
SAUGEEN KAMES TILL
Silt till occurring very locally within the Saugeen Kames is referred to here as Saugeen Kames till. It is brown silt till associated with the ice-contact stra tified drift and is probably derived from lacustrine sediments of similar texture and colour. It is lithologically similar to Elma Till and has been observed overly ing Elma Till at one site. This till was apparently deposited during a very minor readvance at the time of construction of the Saugeen Kames. Elma Till is the surface till north and south of these deposits which places this till as middle to late Port Bruce Stadial age.
Glacial Landforms
END MORAINES
Though the glacial advances, associated with the deposition of Elma and Mornington Tills (and perhaps Stirton Till), had their easterly termini within the Palmerston map-area, no end moraines mark these positions. Sediments marking possible recessional positions are present for Catfish Creek, Tavistock, and Elma Tills. Buried glaciofluvial sediments located northwest of Riverstown are believed to be stagnation deposits related to Catfish Creek Till. It is thought that these represent a stillstand during retreat of this ice sheet. The oldest morainic deposits occurring at the surface are located 3 to 5 km (2 to 3 miles) south of Arthur. Here kames and associated hummocky till represent a recessional position of Tavistock ice. These may be a westerly extension of the Orangeville Moraine, but if so, they do not mark the terminal position of the Ta vistock advance, as does the Orangeville Moraine much further to the east. Ice-contact deposits located southeast of Brotherston mark a retreat posi tion for the Elma ice though no well defined ridge is present. These deposits are associated with outwash in the valley of the Little Maitland River and with the termini of several eskers.
'Since this report was written the Walkerton moraine has been reinterpreted as being pre-Port Huron Stadial in age. 21 Palmerston Area
A large belt of morainic materials located between Clifford and Mount For est was identified as the Saugeen kame-moraines by Chapman and Putnam (1951) who had previously suggested a possible linkage between these deposits, the Seaforth Moraine, and kames located in the Durham area to the north (near Holstein) and in the Markdale area near Flesherton (Chapman and Putnam 1949). These deposits are referred to herein as the Saugeen Kames. The relation ship of these deposits to the Seaforth Moraine has not been proved or disproved at this time. However, recent work by Feenstra (1975b) and Sharpe (1975) in tracing moraines to the north has led to renaming of the northerly materials as the Singhampton Moraine; thus the westerly extension of the Singhampton Mo raine to Walkerton as described by Chapman and Putnam (1951; 1966) becomes the Gibraltar Moraine. The relationship between the Saugeen Kames of the Palmerston map-area and the Singhampton Moraine at Flesherton was mapped by Taylor (1913) though in Taylor (1939, p.379) he interpreted the Seaforth Mo raine as having a more northerly course. The area occupied by the Saugeen Kames in this study consists of belts of ice-contact stratified drift and proglacial outwash suggesting two or three ice marginal positions. Included brown silts in the ice-contact deposits indicated the presence of small pondings and the localized brown silt till described in the pre vious section indicates a minor advance at the time of moraine building. Elma Till is the surface till both north and south of the morainic belt implying that the moraine is a recessional feature constructed during retreat of the Elma ice.
GROUND MORAINE
Ground moraine (till plains of some writers) comprises the surface of much of the map-area. The oldest and most featureless ground moraine is the area of flat ground underlain by Tavistock Till in the eastern part of the map-area; it in cludes the small area of Mornington Till mapped near Drayton. The Conestogo River and associated streams are the principal features breaking this monoto nous surface. It includes parts of the Dundalk and Stratford till plains described by Chapman and Putnam (1951; 1966). A second large area of ground moraine includes much of the area mapped as Elma Till. This is cut by numerous meltwater channels and is in part drumlin- ized; these features provide this area with much greater relief and better drain age than is present to the east.
STREAMLINED DRIFT FORMS
Streamlined landforms indicating the direction of ice flow within the Palm erston map-area occur as drumlins and glacial flutings; the former occur as positive features rising above the surrounding ground moraine while the latter are negative linear features. The most extensive area of drumlins occurs northwest of Palmerston where the southwesterly extension of the Teeswater drumlin field (Putnam and Chap- 22 man 1943; Chapman and Putnam 1951) enters the map-area. These drumlins are not as well formed as in the Wingham area, however their orientation, 1200 to 1550 , serves to indicate the direction of ice flow during formation. These drumlins range up to 1.5 km (l mile) in length though most are about 0.5 km (V* mile) long; they range up to 15 m (50 feet) in height. Only Elma Till has been observed in these drumlins though no good cross-sections were located during the field survey. Flutings associated with these drumlins have a similar orientation, 1350 to 1600 . These range up to 1.5 km (l mile) in length and are best identified on air- photos. When observed in the field they may have up to 2 m (6 feet) of relief. As discussed previously Elma ice advanced beyond the mapped sediment in places and flutings of similar orientation occur on adjacent but older sediments. Such cases exist near Drayton and east of Mount Forest. In the former instance Mornington Till is fluted at 1500 to 1600 west of Drayton. These may have been formed by Elma ice; Feenstra (1975a) demonstrated that flutings on Morning ton Till near Conestogo Dam to the south were due to overriding Elma ice and that the Mornington Till was deposited by ice moving from a more westerly di rection. East of Mount Forest flutings on stratified drift are related to the Elma ice. A few flutings on Tavistock Till occur in the eastern part of the map-area. These indicate the flow direction at the time of formation, about 1200 to 1400 .
Glaciofluvial Features
MELTWATER CHANNELS
The surface of the Palmerston map-area was strongly modified by glacial melt waters which left scores of channel segments as their legacy. These channels are almost entirely related to the retreating Elma ice and indicate successive ice- marginal positions during withdrawal. The major systems are listed here from oldest to youngest: 1) Conestogo River south of Highway 9 is undoubtedly the principal in dicator of the outer limit of the Elma advance. Its northern extension is not as well defined, however it is probably that channel which extends northward through Kenilworth. 2) A channel system extending from Moorefield, through Rothsay, to east of Riverstown. 3) A system trending northward through Trecastle, and Teviotdale and extending southward to Middle Maitland River and then westward through Listowel (located south of the map-area on Highway 23). 4) A major system trending northeasterly along Little Maitland River through Palmerston to east of Mount Forest. This channel is associated with the termini of several eskers and appears to mark a prominent re cessional position. 5) The Maitland River from Newbridge through Harriston to its head waters north of Melgund. A continuing network of channels links up 23 Palmerston Area
with the northeasterly trending segment of the South Saugeen River at Mount Forest. These channels are not mutually exclusive and numerous interconnecting linkages exist. The channels are primarily erosional with but little original out wash, though the northward continuation of the sequence is marked by sheets of outwash gravel associated with the Saugeen Kames. The pattern of the major channel systems described indicates that as the ice retreated meltwater drainage shifted from north-south to northeast-southwest, to east-west. This is the result of the northward retreat of the ice and the loca tion within the area of the topographic divide between Lake Erie and Lake Hu ron drainage.
OUTWASH DEPOSITS
Most outwash deposits within the map-area are associated with the retreat ing Elma ice; very little outwash occurs within the terrain east of the Elma Till boundary. Outwash occurs as channel fills, terrace deposits along meltwater channels, as sheet sands near Harriston, and as gravelly braided outwash be tween ridges of ice-contact deposits within the Saugeen Kames. The channel fills are not well exposed, however in most instances these are l to 3 m (3 to 10 feet) thick and consist of gravel and pebbly sand. Because much of this lies within wet depressions the upper part of these deposits is frequently strongly weathered and gleyed. They may also be overlain by muck, alluvium, or lacustrine sediments. Terrace deposits flanking the channels are not extensive. They commonly are worked for granular aggregates and l to 5 m (3 to 15 feet) of medium gravel and gravelly sand are exposed in pit faces. Coarse pebble and cobble gravel is un common. Sheet sands of mixed outwash and lacustrine origin overlie broad areas in the vicinity of Harriston. The sands here are fine to medium textured and are locally coarse and pebbly. One to five metres (3 to 15 feet) of sand may be pres ent. These sands occupy an area of low relief adjacent to the Maitland-South Saugeen meltwater channel. The most extensive deposits of outwash gravel occur within the Saugeen Kames as belts of braided outwash between ridges of morainic deposits. Most ex posures observed were less than 6 m (20 feet) thick, however, up to 15 m (50 feet) may occur locally. Flow directions within these deposits were parallel to the mapped belts (generally east to west) or toward the south or southeast where drainage was through breaches in the moraine and parallel to the secondary meltwater system (Photo 6). These gravels are generally medium to coarse peb ble gravels and coarse cobble gravels are uncommon. Pebble lithologies (Table 6) are primarily dolostone and are similar to the associated Saugeen Kames. Data on the composition of many of these deposits are given in Appendix C.
24 OGS 9842
Photo 6-Outwash at Murray Construction Pit southwest of Mount Forest. Foresets in pebbly sand dip toward southeast.
ICE-CONTACT STRATIFIED DRIFT
Materials mapped as ice-contact stratified drift consist primarily of glaciofluvial sediments but contain lacustrine sediments and till locally. They are characterized by great variability, collapse features, and hummocky topogra phy. Within the map-area these deposits occur in three principal settings: 1) buried glaciofluvial sands and gravels, including some outwash; 2) morainic de posits; and 3) eskers. Buried glaciofluvial sands and gravelly sands underlie Tavistock Till south- east of Mount Forest (Photo 3). These are thought to be mainly stagnation de posits related to Catfish Creek Till though some of it may be advance outwash associated with Tavistock Till. Buried sands and gravels underlying Tavistock Till along the Conestogo Valley north of Drayton occupy a similar stratigraphic position to those described above; however, they do not bear the same affinity to Catfish Creek Till and are probably younger. Ice-contact sands underlying Elma Till occur over several hundred hectares about 1.5 km (l mile) southeast of Kurtzville. It is not known whether these were deposited in conjunction with the Tavistock Till or the Elma Till. Ice-contact deposits occurring as morainic features are found in three princi pal locations. The oldest deposits comprise a group of sand and gravel kames sit- 25 Palmerston Area
TABLE 6 PEBBLE ASSEMBLAGES FOR PRINCIPAL GLACIOFLUVIAL DE POSITS.
Deposit Sample Lithology Size
VJ k- •o O) o u oj o in CO E 05 CO ~oj o .c CO .C CD OJ i3 Q U w C/5 c/) LL ^ ^ 9 1 Mount View 84 0 0 0 0 2 4 0 Esker 10 (2-15) 2 (79-93) (0-1) (0-1) (1-4) (0-8) (0-2)
Riverstown 8 82 1 0 1 0 2 3 2 Esker 4 (7-11) (76-87) (0-3) (0-2) (0-3) - (0-6) (2-4) (0-7)
Riverbank 13 76 0 0 1 0 4 5 0 Esker 6 (10-18) (76-79) (0-1) (0-1) (0-2) - (2-6) (3-7) (0-1)
Esker north 9 79 2 0 0 0 5 3 2 of Palmerston 4 (8-10) (77-82) (0-6) - (0-1) - (3-7) (0-5) (0-3)
Esker north 7 81 2 0 0 0 4 4 2 of Dryden 6 (3-10) (77-89) (0-3) - (0-1) - (1-10) (0-7) (0-3)
Newbridge 12 77 4 0 0 0 5 2 1 Esker 5 (10-16) (75-82) (1-8) (0-9) (0-3) (0-1)
Saugeen 8 83 1 0 .5 0 4 3 .5 Kames 11 (4-12) (79-87) (0-2) (0-1) (0-3) (0-9) (0-5) (0-3)
Outwash associated 10 80 2 1 0 1 5 1 1 with Saugeen Kames 5 (5-15) (65-88) (0-9) (0-2) - (0-4) (1-8) (0-3) (0-3)
-range uated 3 km (2 miles) south of Arthur. These deposits are part of a recessional moraine deposited by the Tavistock ice. Up to 9 m (30 feet) or more of material is exposed here. Deposits mapped southeast of Brotherston are related to a halt of the retreating Elma ice near the Little Maitland River; these sediments are mainly sand but include some till. The majority of ice-contact sediments present in the map-area comprise the Saugeen Kames located between Clifford and Mount Forest. These deposits have characteristic hummocky topography and consist mainly of sand and gravel (Photo 7) though a lacustrine brown silt is fre quently encountered and a brown silt till, probably derived from the lacustrine silts, occurs locally. Faulting (Photo 8) and slumping are very common within these materials. Up to 24 m (80 feet) of sand has been reported by well-drillers, however most of these deposits range from 6 to 15 m (20 to 50 feet) in thickness. Pebble lithologies (Table 6) for these morainic deposits are similar to associated outwash and consist primarily of carbonate rocks.
26 OGS 9843
Photo 7-Glaciofluvial ice-contact gravel and sand.
OGS 9844
Photo 8-Faulted gravel and silt in ice-contact deposits between Clifford and Mount Forest.
27 Palmerston Area
OGS 9845
Photo 9-Esker located 0.8 km (Vi mile) north of Pike Lake.
Eskers
Taylor (1910; 1912) reported several eskers that are present within the Palmerston area including one described previously by Logan (1863); these in cluded the esker which terminates at Riverstown, the one passing through Der- rynane, and the one located in the northeasternmost part of the map-area. The two oldest eskers occur in the northeast part of the map-area. These are the Egerton Esker (Chapman and Putnam 1951) and the Mount View Esker (Cowan 1976a). The former only crosses the corner of the map-area and ends in Luther1 Marsh to the east; the Mount View Esker originates north of the map- area and ends southeast of Mount View in the Orangeville area. Mount View Esker exceeds 24 km (15 miles) in length. Both of these eskers consist of disconti nuous ridges of gravel and gravelly sand flanked by sand and contain mainly do lostone clasts (Table 6; Cowan 1976a). Locally they may exceed 8 m (25 feet) in height. They are oriented northwest to southeast and were laid down as Tavis- tock ice retreated in that direction. At one location, just east of Mount Forest, Tavistock Till overlies the Mount View Esker. The remaining eskers were laid down by Elma ice as it too retreated toward the northwest. Two of these, ending at Riverstown and Riverbank, have their termini at about the outer limit of the Elma Till. The Riverstown Esker (Photo 9) originates north of Pike Lake and extends southeasterly more than 16 km (10 28 miles) to Riverstown. It is double-ridged over much of its length and locally con tains masses or beds of Elma Till. This esker is up to 12 m (40 feet) high in sev eral places, consists largely of sand and gravel, and contains mainly dolostone pebbles and cobbles. Riverbank Esker is up to 9 m (30 feet) high and it consists mainly of sand and gravelly sand; pebbles are mainly dolostone (Table 6). Several short esker segments were mapped south and east of Palmerston. These consist only of worked out gravel pits in some instances. Elma Till overlies some of these, which could imply that they are associated with older tills, that they were deposited subglacially and subsequently had till deposited on their upper surface, or that they were deposited and then overridden by Elma ice. The second suggestion is preferred by the writer. Northwest of Palmerston several eskers terminate at the Little Maitland River meltwater channel. These accentuate the stillstand position at this river by the retreating Elma ice but also may indicate greater ablation rates from this position northward. These eskers are discontinuous ridges of gravel and sand which may exceed 8 m (25 feet) in height locally. Several extend northward into the Saugeen Kames. Table 6 indicates that more chert is present in these eskers overlying the Bois Blanc Formation (Figure 2) than is present to the east. All eskers within the map-area are believed to have a subglacial origin. They are locally important sources of aggregate though many of the smaller ones are nearly depleted.
Lacustrine Sediments
Lacustrine sediments within the map-area result from sedimentation in proglacial lakes during glacial episodes and in local surface pondings during gla cial retreat and during the postglacial. Subsurface occurrences of such sediments occur in three stratigraphic positions along the Conestogo River; the oldest occur sporadically between Catfish Creek and Stirton Tills; the next oldest between Stirton and Tavistock Tills; and the youngest between Tavistock and Morning ton Tills. All of these imply that the Conestogo basin was dammed south of the map-area by ice or that the lakes are mainly very localized in extent. Those sedi ments occurring above Catfish Creek Till and perhaps those between Stirton and Tavistock Tills are of probable Erie Interstadial age (Dreimanis and Karrow 1972) and of r. similar age to the Wildwood Silts described by P.F. Karrow in the St. Marys area to the south (Karrow 1977). Those sediments occurring between Tavistock and Stirton Tills are the most widespread and thickest. They range from varved sands and clays to massive or very finely laminated, plastic clay. Analysis of one sample of lacustrine silt from Section 327 (Appendix A) (Sample 327a, Appendix B) contained 52 percent car bonates having a calcite to dolomite ratio of 0.4, i.e. very similar to associated tills, particularly the overlying Tavistock Till. Numerous slope failures along the Conestogo Valley appear to be geologically related to the presence of these sedi ments. Sediments occurring between Mornington and Tavistock Tills, in the vicin ity of Drayton, are thin (0.5 to 2 m; 2 to 5 feet) and consist of varved to lami nated sands, silts and clays. Sediments related to and overlying Mornington Till 29 Palmerston Area consist of sand, silt, or nearly massive gritty clay, and are usually less than l m (3 feet) thick. Along the South Saugeen River most lacustrine sediments occur between Catfish Creek Till and Tavistock Till and result from blockage of northward drainage. These consist mainly of weakly laminated sands but vary to varved silt and clay. Some of the lacustrine sediments appear to have interbeddded Catfish Creek Till within them. These sediments are also comparable in age with those of the Erie Interstadial. Brown massive to weakly laminated silts within the ice-contact deposits of the Saugeen Kames represent local pondings within a zone of stagnant ice. Surficial lacustrine sediments occur throughout the map-area. These are pri marily silty fine sands l to 2 m (3 to 5 feet) thick and most are associated with the retreating Elma ice; some of these may be deltas formed in larger pondings as with those southeast of Rothsay. Molluscs were noted in a few localities and are presumed to occur in local non-glacial pondings or in postglacial sediments overlying glaciolacustrine sediments.
Bog and Swamp Deposits
Organic sediments consisting of muck, marl, and peat occur throughout the area as depression fills. Typical thicknesses are l to 2 m (2 to 5 feet) and com monly an upper unit of muck overlies a lower unit of marl, but peat is rare. These deposits are present in former glacial meltwater channels which now con tain underfit streams, in shallow depressions which formerly contained small glacial pondings, and in kettle holes. The latter are concentrated within the Sau geen Kames and are in part the result of high water tables. In these kettle holes the organic materials may be thicker than elsewhere.
Alluvium
Alluvium occurs along most major stream courses as gravelly channel bars or on the floodplains as silt and sand. Shifting channel conditions frequently give rise to a sequence consisting of bar gravels and sands overlain by floodplain silts. Composition of the alluvium varies with that of the materials being eroded. As much of the map-area is underlain by silty tills, the alluvium is predominantly silt and fine sand. However, coarse gravel occurs in bars where Catfish Creek Till is being eroded (Photo 10), mainly along the Conestogo and South Saugeen Riv ers where deep erosion has taken place. Included organic debris serves to charac terize these sediments as postglacial in age. Most alluvial deposits range from l to 2 m (2 to 5 feet) in thickness however up to 3 m (10 feet) may be present along the South Saugeen or Conestogo Riv ers.
30 OGS 9846
Photo 10-Coarse alluvium (A) developed on Catfish Creek Till (B) along Conestogo River.
HISTORICAL GEOLOGY
Knowledge of the glacial history of the Palmerston map-area is restricted to the Late Wisconsinan Substage though older sediments exist immediately to the south (Karrow 1971; Cooper 1975a). Figure 7 illustrates the glacial history as in terpreted from the present survey; it concerns only the Georgian Bay lobe dur ing the Late Wisconsinan and the figure is drawn along a northwest to southeast axis, i.e., parallel to most ice movement. Late Wisconsinan ice first advanced across the map-area from the north or northwest at the beginning of the Nissouri Stadial about 24,000 years ago. This ice continuously covered the map-area until about 16,000 years ago when the ice retreated north of the area. Catfish Creek Till was deposited throughout the area during this episode; buried glaciofluvial sediments northeast of Riverstown ap pear to be stagnation deposits related to the ensuing retreat. The Palmerston map-area was probably ice-free for a short period of time about 15,000 to 16,000 years ago; the time of the Erie Interstadial to the south (Dreimanis and Karrow 1972). A major southeasterly readvance then took place to initiate the Port Bruce Stadial. This blocked drainage in the South Saugeen Valley forming proglacial lakes; similar lakes also formed in the Conestogo Valley though blockage here 31 osg .5
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o cu c E .2 F ra
^ o. g E 5 c o o 51 E ® ra s S"2ra "- c ra ^, ra2 g .2^t •o D ra d, w ^ .tP raC T3c H c ra must have been to the south of the map-area. Fine grained sediments deposited in these lakes were later incorporated by the glacier and then redeposited as a se ries of fine grained tills. Though the major thrust of this advance was eastward to the Orangeville Moraine with concurrent deposition of Tavistock Till, minor fluctuations within the Conestogo River area during advance and retreat led to the deposition of areally restricted tills both older and younger than the main till body. The oldest of these, Stirton Till, represents a limited advance closely asso ciated with lakes in the river valley area. It may be that this fluctuation was pre conditioned by the presence of a shallow lake which gave enhanced flow rates due to excessive basal moisture (e.g. Wright 1973). This fluctuation was followed by minor retreat then advance to the Orangeville Interlobate Moraine and depo sition of the Tavistock Till. The Ontario lobe counterpart of this advance re sulted in deposition of Port Stanley Till to the east (Cowan 1976a). Retreat of Tavistock ice was accompanied by formation of eskers and glacio lacustrine deposition into local pondings. However, in the vicinity of Mount Forest a local fluctuation of the ice margin apparently occurred as two units of Tavistock Till are present at Section 383 (Appendix A) and evidence exists for overriding of the northern part of the Mount View Esker. Well to the south a re advance also took place. Near Drayton a younger till, Mornington Till, was de posited over a restricted area in conjunction with a proglacial lake, as indicated by underlying and overlying glaciolacustrine sediments. This fluctuation was perhaps also preconditioned by the ice marginal waters. It is suggested that the fluctuations in both the north and the south were concurrent but that the for mation of the new till was restricted to the area of the proglacial lake in the southern part of the Conestogo Valley. Tavistock ice then continued its northward retreat to a position north of the Palmerston map-area. Readvance of the Georgian Bay lobe again took place toward the southeast covering the Palmerston map-area to a position lying approximately along a line drawn between Moorefield, Kenilworth, and Conn. The sandy to silty Elma Till was deposited and the Teeswater drumlin field formed; no end moraine marks the outer limit of this major advance. Retreat commenced, numerous meltwater channels were cut and several eskers formed, including the large Riverstown Esker. When the ice reached a re treat position between Clifford and Mount Forest a stillstand or fluctuation oc curred and a major end moraine system constructed the Saugeen Kames (Sin- ghampton Moraine). A locally occurring silt till was deposited within the moraine area at this time. Retreat then continued northward and the ice moved beyond the area for the last time about 13,500 years ago. Subsequent geological activity includes the formation of soil profiles, the incision of modern streams and deposition of alluvium, and the infilling of boglands with organic sediments.
33 Palmerston Area
Figure 8-Distribution of chert content (percent) for gravels in west half of Palmerston map-area.
ECONOMIC GEOLOGY Gravel and Sand Excepting the northwest part of the map-area, sand and gravel resources are inadequate even for present needs. Consequently these resources must be re served for future use within the present and adjoining areas. Those townships lo cated within the County of Wellington are designated under the Pits and Quar ries Control Act, 1971, and at the time of writing 16 pits were licensed. Though there are more than 150 pits within the map-area only one pit was operating on 34 a full time basis at the time of the survey; that of James Murray Construction Limited, near Mount Forest. This pit is described below; information on other pits visited is given in Appendix C. Map 2384 (back pocket) portrays the distri bution of the gravel resources which may have potential for extraction; sufficient sand is available from gravel units so that areas mapped as outwash sand are not included. Well drillers' reports of gravelly materials near the surface are also giv en, but some of these appear to be stony tills. Analyses of pebble lithology are given in Appendix C and a few sieve analyses of sands are given in Appendix D. Lithology of gravels in the northeast half of the map-area does not restrict their use for most products. However, in the southwest part of the map-area chert derived from the underlying Bois Blanc Formation may comprise up to 25 percent of the pebble grade (Figure 8) which restricts these gravels for some uses. The distribution of the chert in the gravels is similar to that for Elma Till (Fig ure 6) as would be expected. Siltstone and shale derived from the Salina Forma tion may be restrictive locally.
OUTWASH DEPOSITS
Outwash gravels associated with the Saugeen Kames are the most impor tant aggregate resources within the map-area. These gravels range from 2 to 6 m (6 to 20 feet) for the most part though more than 15 m (50 feet) has been re ported locally. The gravels contain 25 to 60 percent stone and most of this is me dium to very coarse pebble gravel with some cobble gravel; boulders are rare throughout. Chert content averages two percent though one sample contained nine percent (Table 6). These gravels provide the only prospect for development of large extractive operations within the map-area; at the time of the survey the only full time operation was located in these deposits.
James Murray Construction Ltd. (113)1
This property, known as the Murphy Pit, is located on lot 4, concession XIII, Minto Township, Wellington County and is licensed under the Pits and Quarries Control Act, 1971. The deposit is considered to be an outwash fan flanking a small esker; foresets (Photo 6) indicate southeasterly flow though cross laminations imply a variability. The deposit may also include modified ice- contact materials at depth. Overburden consists of l to 2 m (3 to 5 feet) of fine sand or silt. This property was described previously by Hewitt and Cowan (1969b). At the time of the visit two pits were being utilized, one for coarse aggregate and one for fine aggregate. Up to 8 m (25 feet) of material was exposed though the gravels are reported to be 21 m (65 feet) thick. In general a coarse upper unit of weakly stratified, poorly sorted, rounded gravel containing 60 to 70 percent
'Number refers to location on Map 2384 (back pocket). 35 Palmerston Area stone overlies a crossbedded medium to coarse sand unit containing as much as 15 percent gravel. The coarse unit was observed to range from 2 to 6 m (7 to 18 feet) in thickness; whether it thickens elsewhere is unknown. These gravels may contain up to 10 percent fines and many of the pebbles and cobbles had a silt film on their surface. Up to 60 percent of the gravel exceeds 2.5 cm (l inch) in di ameter and up to 15 percent may exceed 10 cm (4 inches); the largest boulder ob served was 0.5 m (1.5 feet) in diameter. The pit operation consists of excavating, crushing, and screening with porta ble equipment. These products are then trucked to a permanent washing plant on the property or stockpiled. A full range of washed and crushed products is produced though the bulk of the material goes to a pre-mix concrete plant lo cated on the property and operated by H and M Redi-Mix Limited. Additional data for this property are given in Appendix C and two sieve analyses of sand are given in Appendix D (samples 113A,B). Further outwash deposits occur along major meltwater channels. These are usually 2 to 5 m (5 to 15 feet) thick and consist of medium to very coarse pebble gravel containing 15 to 60 percent stone.
ICE-CONTACT DEPOSITS
Ice-contact deposits provide important local sources of aggregate, especially since they have a greater distribution throughout the map-area than the out wash deposits. The Saugeen Kames contain bodies, which may be quite large, of good ag gregate. Variability of size grading and the presence of silt or till in these depos its may cause extraction costs to increase. Petrographically these materials are similar to the associated outwash (Table 6) and locally this material may be un suitable for high specification products. Observed thicknesses seldom exceed 8 m (25 feet) however thicknesses considerably greater than this have been reported by well drillers (Map 2384, back pocket). Eskers within the map-area may be noded or discontinuous. Consequently thicknesses of contained gravels vary from 2 to 12 m (5 to 40 feet). Materials vary from cobble gravel to fine sand and silt necessitating selective extraction in many pits. Those pits located in the Riverbank, Riverstown, or Mount View Eskers contain only minor amounts of deleterious material such as chert (Table 6) However south and west of Teviotdale chert is deleterious, restricting the use of these gravels.
Clay
The production of brick or tile from glacial clays is known to have taken place at Drew, Drayton, and Fultons Mills (Fultons) in the past and possibly at other locations. At Drayton a clay pit is reported to have existed in the west wall of the Conestogo Valley for the production of drainage tile. Production was pre sumably from glaciolacustrine silt and clay which underlies Tavistock Till in this 36 vicinity though the till itself may have been used as well. At Drew (2.5 km (IVz miles) east of Drew Station) three brick plants situated side by side reportedly produced up to one and one half million bricks each per year (Baker 1906); these were exported from the map-area. Clay extraction was from shallow lacustrine silty sands containing clay bands. White brick was the principal product though the uppermost leached material (red-top clay) was used to make tile. Montgomery (1930, p. 157) described a tile manufacturing plant at Fultons Mills (Fultons). The deposit was described as l m (3 feet) of red burning clay overlying sandy clay. These are believed to be the lacustrine sediments mapped near Fultons during the present survey. No clay deposits were observed during the present survey which would be considered good prospects for future development. Potential sources are surficial lacustrine sediments, buried lacustrine clays located along the Conestogo River, and fine grained tills. All of these have usage restrictions due to their high carbo nate content and the use of fine grained tills would require removal of pebbles.
Engineering Geology
Though no engineering tests were carried out within the course of this sur vey the following comments on the engineering properties of surficial materials may be made. Catfish Creek Till is extremely compact; excavation in this material may re quire ripping or blasting and for some purposes this till may be considered to be rock. Tavistock and Mornington Tills are fine grained and are low to moderately plastic. Both are susceptible to ground ice segregation and subsequent frost heave; low cost roads using these materials for a subgrade may prove impassable in spring. Elma Till has low plasticity and is generally a good foundation material. Frost heaving may occur within this till, particularly in those areas where the till is less sandy. This till may prove to be very compact at depth. Numerous slope failures along the Conestogo River are related to undercut ting by the river itself and to the presence of lacustrine sediments underlying Tavistock Till in the valley walls. Groundwater seepage from lacustrine sedi ments may cause undercutting and failure of the overlying till (Photo 2). The la custrine sediments are also less resistant to fluvial erosion and undercutting would be more rapid where they occur at water level. Areas of fine sand within the ice-contact deposits may provide compaction problems where new roads are being built through them. Boulders may be en countered during excavation throughout the areas underlain by till or ice-con tact stratified drift.
37 Palmerston Area
Agricultural Soils
Weathering of surficial sediments and the formation of soil profiles is esti mated to have begun 13,500 to 14,000 years ago, though in a geological sense, these profiles are not strongly developed. The Grey-Brown Podzolic is the pre- dominent Great Group and the Dark Grey Gleysolic and Organic Great Groups occur in areas which are not well drained (Hoffman et al. 1964). Table 7 relates the present geological mapping to the principal soil catenas used by the Ontario Soil Survey in this area (Hoffman et al. 1952; Hoffman and Richards 1952; Gil lespie and Richards 1954; and Hoffman etal. 1963).
TABLE 7 SOILS MOST COMMONLY DEVELOPED ON QUATERNARY SEDI MENTS WITHIN THE PALMERSTON MAP-AREA.
GEOLOGICAL UNIT CATENA SERIES MEMBERS DRAINAGE Good Imperfect Poor
Alluvial sand, silt, gravel Bottom land - variable drainage
Organic sediments Muck, peat
Lacustrine silt and clay Brantford Brantford Beverly Toledo
Lacustrine fine sands Brant Brant Tuscola Colwood
Outwash sands Fox Fox Brad y Granby
Outwash gravels Burford Burford Brisbane Gilford
Outwash gravels Teeswater Teeswater - -
Ice-contact sands Hillsburgh Hillsburgh - -
Ice-contact gravels Donnybrook Donnybrook - -
Elma Till Harriston Harriston Listowel Parkhill
Mornington Till Huron Huron Perth Brookston
Tavistock Till (clayey silt) Huron Huron Perth Brookston
Tavistock Till (silt till) Harriston Harriston Listowel Parkhill
38 APPENDIX A
MEASURED PLEISTOCENE SECTIONS
1. Footage is given from surface down and is approximate due to variations in unit thicknesses, (l foot = 0.305 m). 2. Elevations given for section tops are approximate. 3. Sections are located on Figure 9 and the N.T.S. grid references refer to the Palmer ston 40 P/15 map sheet.
SECTION 9 GR 319532 Elevation 1415 0-2 Weathered pebbly to cobbly sand. 2-6 Tavistock Till: slightly pebbly brown clayey silt till (Sample 9). 6-16 Catfish Creek Till: yellowish-greyish brown, stony sandy silt till (Sample 9A).
SECTION 19 GR 218689 Elevation 1375 0-2 Elma Till: light yellowish brown sandy till (Sample 19A). 2-S+ Tavistock Till: greyish brown clayey silt till (Sample 19B). This till is underlain by sand on the west side of the bridge.
SECTION 22 GR383527 Elevation 1485 0-2 Cobble gravel, weathered. 2-10 Tavistock Till: brown silt till; lens of lacustrine silt and clay near base. 10-11 Coarse sand and gravel; variable thickness. 11-17 Stirton Till: grey, gritty, silt till (Samples 22 and 412) - underlain by Catfish Creek Till 100 feet to west.
SECTION 101 GR 383529 Elevation 1525 0-3 Fine sand, yellowish brown to brownish yellow. 3-4 Pale brown silt. 4-10 Tavistock Till: compact yellowish brown, gritty, clayey silt till; blocky structure (Sample 1). 10-10.5 Discontinuous layer of silt and fine sand; contorted. 10.5-16 Stirton Till: dark brown, silty clay till; sparse pebbles (Sample l A). 16-25 Catfish Creek Till: Very hard, stony, yellowish brown sandy silt till (Sample 1C).
SECTION 318 GR 093610 Elevation 1270 0-4 Lacustrine fine sand. 4-8 Elma Till: yellowish brown sandy silt till (Sample 318). 8-9.5 Catfish Creek Till?: very stiff, sandy silt till (Sample 318A).
SECTION 321 GR 043707 Elevation 1165 Section no longer available 0-3 Gritty yellowish brown silt till; few pebbles; (Sample 321). 3-3.5 Discontinuous bed of medium sand. 3.5-5 Elma Till: very stony, yellowish brown, sandy silt till (Sample 321A).
SECTION 327 GR 307524 Elevation 1400 0-12 Tavistock Till: brown, gritty, clayey silt till (Sample 327). 12-20 Stratified silt and clay: contorted in upper 3 feet; more clayey with depth (Sample 327A). 20-23 Stirton Till: grey to dark greyish brown, silty clay till (Sample 327B). 23-26 Covered interval to flood plain; flood plain is underlain by Catfish Creek Till at river.
SECTION 330 GR 353490 Elevation 1475 0-4 Tavistock Till: brown silt till, red shale chips (Sample 330). 4-5.5 Varved yellow silt and greyish brown clay; silt predominates 3:1. 5.5-15 Catfish Creek Till: very gritty, stony, yellowish brown sandy silt till (Sample 330A). 39 Palmerston Area
•o c 0) o. Q. < d) 0) CO
(D Q.
40 SECTION 350 GR 162688 Elevation 1270 0-8 Stratified pebbly fine sand with interbeds of brown silt till, some yellowish brown sandy silt till near base; ice-contact. 8-10 Dark grey to olive grey, lacustrine clayey silt and very fine sand. 10-15 Tavistock Till: dark greyish brown, pebbly, silty clay till (Sample 350); possibly waterlaid in part. 15-23 Catfish Creek Till: light yellowish brown, very compact, sandy silt till (Sample 350A).
SECTION 354 GR 238460 Elevation 1380 0-1 Pebbly sand loam, topsoil. 1-3 Elma Till: yellowish brown, very stony, sandy silt till (Sample 354). 3-3.7 Yellow silt and fine sand (auger). 3.7-S+ Tavistock Till: gritty brown clayey silt till (Sample 354A - auger sample).
SECTION 362 GR 177541 Elevation 1350 0-1 Fine sand, weathered. 1-4 Elma Till: yellowish brown pebbly sandy silt till (Sample 362). 4-6 Tavistock Till: brown silt till, sparse pebbles (Sample 362A).
SECTION 366 GR 291492 Elevation 1380 0-4 Tavistock Till: brown clayey silt till, sparse pebbles (till Sample 366). 4-6.5 Discontinuous varved yellow fine sand and clayey silt. 6.5-17 Tavistock Till: yellowish brown clayey silt till; sparse pebbles (Sample 366A). 17-21 Lacustrine varved clay and silt, and stratified sand. 21-26 Covered interval to stream; 150 feet to west, 4 feet of Stirton Till (dark greyish brown, nearly stone free, silty clay till) occurs beneath the above lacustrine sediments (Sample 364).
SECTION 375 GR 053442 Elevation 1275 0-3 Elma Till: yellowish brown, pebbly, sandy silt till (Sample 375). 3-5 Tavistock Till: brown clayey silt till; sparse pebbles (Sample 375A).
SECTION 379 GR 283716 Elevation 1450 0-15 Elma Till: light yellowish brown, stony sandy silt till; more compact and greyish brown near base (Sample 379). 15-15V2 Pebbly, yellow, fine sand. 15V2-19 Tavistock Till: grey to dark greyish brown, gritty, clayey silt till; sparse pebbles; red shale chips; inclusion of yellowish brown sandy silt till (Cat fish Creek Till); (Sample 379A). 19-25 Covered interval to river with few exposures of Tavistock Till.
SECTION 383 GR 239707 Elevation 1400 0-1 Sand, gravel, washed till. 1-12 Tavistock Till: grey to dark grey, clayey silt till (Sample 383); yellowish brown in upper four feet; some columnar jointing. 12-13 Interbedded fine sand (lower), brown clay with silt laminae and pebbly medium sand (upper). 13-16 Pebbly yellow sand (one foot) overlain by three feet of cobble gravel. 16-28 Tavistock Till?: brown to dark greyish brown clayey silt till (Sample 383A); sparse pebbles, red shale chips; sheared in silt; substratified near base in places; yellowish brown and coarser in upper four feet; may be in sharp contact with Catfish Creek Till. 28-29.5 Laminated yellow silt; discontinuous. 29.5-31.5 Catfish Creek Till: compact, yellowish brown, stony, sandy silt till (Sam ple 383B); silt inclusions, sand lenses. 31.5-45 Weakly laminated, yellow, fine to medium sand and silt. 45-60 Laminated and varved silt and clay.
41 Palmerston Area
SECTION 415 GR 239541 Elevation 1400 0-3.5 Greyish brown, pebbly, sandy silt diamicton; believed to be colluvium consisting of reworked Elma Till. 3.5-4 Yellow silt. 4-5 Tavistock Till: discontinuous brown clayey silt till; weathered; inter calated with lower part of overlying silt. 5-6.5 Catfish Creek Till: yellowish brown, compact, stony sandy silt till (Sample 415).
SECTION 1183 GR 368527 Elevation 1485 0-3 Laminated silt, pale brown; varies to 8 feet of compact yellowish brown silt and fine sand. 3-27 Tavistock Till: brown (10YR4/3), compact gritty clayey silt to silt till; dark greyish brown below 15'; waterlaid at base. 27-35 Compact, stratified, grey, very fine silty sand; slightly contorted; lenses of fine to medium sand.
SECTION 1234 GR 292456 Elevation 1370 0-4 Tavistock Till: brown silt till. 4-6+ Catfish Creek Till: yellowish brown, stoney, sandy silt till.
SECTION 1264 GR 278470 Elevation 1300 0-4 Tavistock Till: brown clayey silt till. 4-20 Stratified sand and silt. 20+ Stirton Till: dark grey, pebbly, clayey silt till.
SECTION 1280 GR 291535 Elevation 1425 0-3 Elma Till: yellowish brown sandy silt till (overlies sand at one point). 5-4+ Tavistock Till: gritty brown clayey silt till.
SECTION 1308 GR 280468 Elevation 1300 0-5 Brownish yellow medium sand; gravelly coarse sand at base. 5-11 Varved clay, silt and sand; lower part more distal varves than upper part; minor faulting and slumping. 11-13 Dark greyish brown massive clayey silt with pebbles, cobbles and incor porated clay and silt; possibly till or waterlaid till. 13-16 Yellowish grey weakly laminated silt, few pebbles and cobbles and bands (4-6 inches) of greyish brown silty clay till. 16-19 Stirton Till?: grey clayey silt till (Sample 2).
SECTION 1405 GR 222483 Elevation 1355 0-2 Elma Till: weathered, pebbly sandy silt till. 2-5 Yellow silt and very fine sand. 5-6 Tavistock Till: brown clayey silt till.
SECTION 1517 GR 307530 Elevation 1400 0-1 Weathered medium gravel. 1-13 Tavistock Till: gritty clayey silt till; oxidized yellowish brown in upper 10 feet, dark greyish brown at base. 13-19 Covered interval. 19-24 Varved grey to yellow silt and grey clay; silt bands 4-6 inches; clay bands 0.5-1.5 inches. 24-27 Dark grey silty clay.
SECTION 1521 GR 312509 Elevation 1400 0-1 Silt. 1-24 Tavistock Till: brown silt till; appears to fine downwards. 24-28 Stratified grey to pale brown silt; contorted in upper part. 28-30 Catfish Creek Till: grey to olive grey, compact, stony sandy silt till.
42 SECTION 1538 GR 237472 Elevation 1390 0-2 Brownish yellow sand. 2-4 Elma Till: mottled, compact, pebbly sandy silt till (Sample 6); this till predominates to west. 4-5 Tavistock Till: yellowish brown, slightly pebbly, clayey silt till (Sample 6A); this till predominates to east. SECTION 1542 GR 301498 Elevation 1360 0-6 Yellow fine sand and silt; few clay bands. 6-7V2 Interbedded fine sand and pebbly clay; includes 2 inch band of diamicton. 7V2-11 1/^ Interbedded sand and gravel; cross laminated sands indicate southerly flow. HVfe-12 Compact, massive, yellow silt; may be contorted and up to 1.5 feet thick. 12-16 Tavistock Till: brown clayey silt till; to south till is overlain by 3 feet of gravel only. 16-19 Covered interval. SECTION 1543 GR 298487 Elevation 1375 0-2 Stratified gravel, sand, and clay; weathered. 2-16 Tavistock Till: brown to dark greyish brown, gritty silt clay till; very stiff; inclusions of contorted yellow silt; (Sample 7). 16-26 Catfish Creek Till: hard stony, yellowish brown silt till; unoxidized lower part is olive grey in colour. 26-36 Covered interval; with outcrops of Catfish Creek Till. SECTION 1604 GR 197497 Elevation 1360 0-3 Tavistock Till: brown, gritty silt till. 3-3.5 Coarse pebble gravel, discontinuous. 3.5-5 Catfish Creek Till: yellowish brown, stony, sandy silt till. SECTION 1616 GR 268528 Elevation 1430 (Probe sample) 0-1 Fine sand, weathered. 1-4 Elma Till: yellowish brown, gritty sandy silt till. 4-4V4 Tavistock Till: brown gritty, silt till. SECTION 2254 GR 148713 Elevation 1250 0-1 Dark brown weathered sand and gravel. 1-10 Horizontally stratified, uniform coarse pebble and cobble gravel; cobble- boulder lag at base; pebble content — 809o dolostone, 99o limestone, 119k Precambrian. 10-13 Stratified yellowish brown fine to very fine sand and light grey medium sand. 13-17 Catfish Creek Till?: yellowish brown, stony, compact, sandy silt till; soft in upper part (Sample 302). 17-18.5 Brown (10YR5/3) to dark greyish brown clayey silt with few grits and pebbles; compact and till like; silt laminae and stringers of sandy silt till. 18.5-26-*- Catfish Creek Till: yellowish brown to grey compact, stony sandy silt till; sand lenses; (Sample 302A). 26-45 Covered interval to river. SECTION 2256 GR 144714 Elevation 1250 0-1 Soil horizon developed in sand: dark brown A horizon and BIR horizon. 1-4 Till: yellowish brown sandy silt till with lenses on interbeds of yellow, fine sand. 4-10 Silty fine sand: pale yellow to light yellowish brown; slightly pebbly; no apparent stratification; till-like but soft; upper 12 inches is more stony with lenses or beds of sandy silt till and reddish brown gritty silt till.
43 Palmerston Area
10-11 Till: yellowish brown (10YR5/4), compact gritty silt to sandy silt till, similar to 15-19 foot interval. 11-14 Interbedded yellow fine sand and yellowish brown gritty silt till; beds 0.5-1.5 inches thick. 14-15 Pale brown fine sand. 15-19 Catfish Creek Till?: compact yellowish brown (10Y 5/4) sandy silt till; flaky fracture; springs at upper contact. 19-23 Interbedded pebbly sand and yellowish brown till-like sandy diamiction.
SECTION 2259 GR 137713 Elevation 1250 0-15 Pebble and cobble gravel: horizontally stratified; uniform; rounded. 15-21 Till: light yellowish brown (10YR6/4) silt to sandy silt till; inclusions of reddish brown (2.5YR4.5/4) gritty silt till near upper contact. 21-22 Yellow silt and brown clayey silt; contorted; compact; few grits and pebbles; lenses of sandy silt till; thicker elsewhere in exposure and in places is replaced by sand. 22-30 Till: light brownish grey to yellowish brown gritty sandy silt till. 30-40 Laminated to cross laminated, grey to yellow, fine sand; sparse pebbles; outcrops below water level.
SECTION 2524 GR 084665 Elevation 1250 0-2 Brown silt till. 2-4 Elma Till: yellowish brown sandy silt till.
SECTION 2606 GR 128715 Elevation 1200 0-2 Sand, few pebbles. 2-7 Medium to coarse stratified gravel; base of units contain thin beds of till- like gritty clayey — possibly waterlaid Tavistock Till. 7-10 Catfish Creek Till: yellowish brown, compact, sandy silt till.
SECTION 2691 GR 244710 Elevation 1400 0-1 Pebbly sand, weathered. 1-5 Tavistock Till: yellowish brown gritty silt to clayey silt till; sand laminae and lenses; at one point is 8 feet thick with no sand included. 5-10 Laminated to varved silt and clay. 10-11 Cobbly medium to fine sand; cemented. 11-21 Laminated pale yellow to yellowish brown medium to fine sand.
SECTION 2700 GR 173685 Elevation 1260 0-2 Pebbly sand; discontinuous. 2-9 Tavistock Till: brown clayey silt till. 9-14 Stratified silt and fine sand; few grits. 14-15 Catfish Creek Till: stony, yellowish brown sandy silt till.
SECTION 3320 GR 287614 Elevation 1460 0-2 Elma Till: yellowish brown sandy silt till; discontinuous and replaced by stratified drift from place to place. 2-9 Tavistock Till: brown clayey silt till (Sample 313).
SECTION 7599 GR 306522 Elevation 1410 0-3 Elma Till: yellowish brown sandy silt till (Sample 599). 3-4 Sand. 4+ Tavistock Till: brown clayey silt till.
44 APPENDIX B
Till analyses (sample locations are plotted on Map 2383 , back pocket). NOTES 1) Except for pebble lithologies all laboratory analyses were carried out by the Mineral Research Branch, Ontario Division of Mines. 2) Sand-silt boundary, 0.62 mm; silt-clay boundary 0.002 mm; Md is median diameter in mm. 3) Pebble counts on 8-32 mm fraction. 4) Carbonate analyses on minus 200 mesh fraction using Chittick Apparatus. 5) Heavy mineral sparations on -60 to +120 mesh fraction using tetrabromoethane (S.G. 2.96). 6) Till identification: CC-Catfish Creek Till; S-Stirton Till; T-Tavistock Till; E-Elma Till; El-silt till occurring in Saugeen Kames but related to Elma ice; L-lacustrine sediments. 7) Till samples accompanied by question marks (?) or asterisks (*) were not used to compute group means. 8) Fabric orientations are computed vector means.
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APPENDIX C Pits are located by property number on Map 2384, back pocket
Descriptive data for gravel or sand pits visited during the field survey. Notes: 1) Estimated or inferred resources include the area immediately surrounding a pit. Resources are indicated as follows: Small (S) - less than 1.5 million tons; Medium (M) - 1.5 to 5.0 million tons; Large (L) more than 5.0 million tons. 2) Asterisks within pebble lithology data indicate presence at pit but not recorded in sample. 3) Pits are numbered on an alphanumeric system by County, Township, concession, and lot. Locations not surveyed.
4) Pebble lithologies are for 10-40 mm sized pebbles. 5) Sieve analyses for sand samples are given in Appendix D.
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SIEVE ANALYSIS MESH -10 -14 -18 -25 -35 -45 -60 -80 -120 -170 -230 Sample +14 +18 +2S +4S +60 +80 +120 +170 +230 H-Dust No. loss 25 2.4 5.6 13.1 33.8 26.8 10.0 4.6 2.1 0.6 0.3 0.7 27 6.2 6.0 6.6 9.8 8.0 7.6 7.8 9.2 6.5 6.1 26.2 73A 0.1 0.2 2.4 15.6 38.3 29.4 10.8 1.9 0.5 0.8 73B 0.1 0.1 0.9 7.3 23.0 29.2 19.1 7.1 4.9 8.3 80 9.7 13.7 16.3 28.3 18.7 7.0 1.9 0.8 0.4 0.3 2.9 87 4.1 3.8 5.2 12.6 21.0 19.9 13.5 7.4 3.3 2.4 6.8 96A 1.2 1.3 2.6 8.2 14.8 14.4 11.4 8.0 4.3 3.4 30.4 96B 12.9 8.3 7.0 8.5 6.4 3.8 2.2 1.7 1.0 0.8 47.4 100 3.2 4.3 6.2 10.5 10.9 10.0 9.9 12.4 8.2 6.9 17.5 103 1.7 1.3 1.7 3.7 4.7 5.1 10.0 14.4 9.3 9.5 38.6 113A 0.2 0.8 5.2 15.8 24.2 24.7 15.2 5.7 4.2 4.0 113B 2.4 5.4 12.7 31.8 24.7 12.8 5.7 2.7 0.6 0.2 1.0 119 0.6 1.4 3.6 18.1 36.0 22.3 11.1 4.7 1.2 0.4 0.6
Sieve analyses of sand samples from gravel or sand pits. Sample numbers as for pit numbers on Map 2384 (back pocket). Analyses on minus 10 mesh fraction. Sample Number Field Description
25 Coarse sand in east dipping foresets 27 Gravel from esker 73A Laminated, well sorted medium sand unit 73B Fine sand bed two feet thick 80 Matrix of outwash gravel 87 Sand from interbedded sand and gravel in esker 96A Gravel unit, esker 96B Gravel unit, esker 100 Sand from interbedded sand and gravel in esker 103 Laminated sand with gravel interbeds, esker 113A Crosslaminated uniform sands, outwash 113B Pebbly sand, outwash 119 From six inch sand bed five feet below surface in sequence of inter bedded sand and gravel, outwash
57
SELECTED REFERENCES
Baker, M.B. 1906: Clay and clay industries of Ontario; Report of the Ontario Bureau of Mines, vol.15, Part II, 127p.
Beards, R.J. 1967: Guide to the subsurface Palaeozoic Stratigraphy of Southern Ontario; Ontario Dept. of Energy and Resources Management, Paper 67-2, 19 p.
Beards, R.J., Mcbean, D.D., and Sanford, B.V. 1969: Gas and oil fields, pipelines, compressor stations and refineries; Toronto-Windsor area, Ontario; Ontario Dept. of Energy and Resources Management, Petroleum Re sources Section, Map 69-1.
Caley, J.F. 1941: Palaeozoic geology of the Brantford Area, Ontario; Geol. Surv. Canada, Mem. 226, 176p.
Chapman L.J. and Putnam, D.F. 1943a: The moraines of southern Ontario; Trans. Roy. Soc. of Canada, vol. 37, Section IV, p.33-41. 1943b: The physiography of southwestern Ontario; Scientific Agriculture, vol. 24, No. 3, p.101- 125. 1949: The recession of the Wisconsin glacier in southern Ontario; Trans. Roy. Soc. Canada, vol. 43, Ser. 3, p.23-52. 1951: The physiography of southern Ontario; University of Toronto Press, 284p. 1966: The physiography of southern Ontario; University of Toronto Press, 2nd ed. 386p. 1972: Physiography of the southcentral portion of southern Ontario; Ontario Dept. Mines and Northern Affairs and Ontario Research Foundation, Map 2226, scale one inch to four miles.
Cooper, A.J. 1975a: Pre-Catfish Creek tills in the Waterloo area; unpublished M.Sc. thesis, University of Waterloo, Ontario, 178p. 1975b: Quaternary geology of the Goderich (40P/12) and Seaforth areas, Huron and Perth Counties; p.l 19-120 in Summary of Field Work, 1975, by the Geological Branch, Ontario Div. Mines, MP 63, 158p.
Cowan, W.R. 1972: Pleistocene geology of the Brantford Area, Southern Ontario; Ontario Dept. Mines and Northern Affairs, IMR 37, 66p. 1974: Quaternary geology, Wingham (40P/14) and Lucknow (40P/13) areas, southern Ontar io; p.189-191 in Summary of Field Work, 1974, by the Geological Branch, Ontario Div. Mines, MP59, 206p. 1975a: Quaternary geology of the Woodstock area, southern Ontario; Ontario Div. Mines, GR 119, 91p. 1975b: Quaternary geology of the Walkerton area (41A/3) Bruce and Grey Counties; p.l 11-112 in Summay of Field Work, 1975, by the Geological Branch, Ontario Div. Mines, MP63,158p. 1976a: Quaternary geology of the Orangeville area, southern Ontario; Ontario Div. Mines, GRl41,98p. 1976b: Quaternary geology of the Palmerston area, southern Ontario; Ontario Div. Mines, Map P. 1185, scale 1:50,000.
Cowan, W.R., Karrow, P.F., Cooper, A.J. and Morgan, A.V. 1975: Late Quaternary stratigraphy of the Waterloo-Lake Huron area, Southwestern Ontario; p.180-222 in Geol. Assoc. Canada, Mineralogical Assoc. Canada, Geol. Soc. America (N.C.S.) Field Trips Guidebook Part B, 330p.
59 Palmerston Area
Davies, L.L. and Mcclymont, W.R. 1962: Palmerston Sheet, Bedrock Topography Series; Ontario Dept. Mines, Prelim. Map P. 166, scale l inch to 3 miles.
de Vries, H. and Dreimanis, A. 1960: Finite radiocarbon dates of the Port Talbot Interstadial deposits in Southern Ontario; Science, June 10, vol. 131, No. 3415, p.1738-1739.
Dreimanis, A. 1961: Tills of southern Ontario; p.80-96 in "Soils in Canada", R.F. Legget (ed), Royal Soc. Canada, Spec. Publ. No. 3, 229p. 1962: Quantitative Gasometric Determination of Calcite and Dolomite by Using Chittick Ap paratus; Jour. Sed. Pet., Vol.32, No.3, p.520-529. 1964: Pleistocene geology of the St. Thomas area (West Half), southern Ontario; Ontario Dept. Mines, Prelim. Map, P. 238, scale 1: 50,000.
Dreimanis, A., and Karrow, P.F. 1972: Glacial history of the Great Lakes - St. Lawrence region, the classification of the Wiscon- sin(an) Stage, and its correlatives; p.5-15 in Section 12 (Quaternary Geology), 24th session International Geological Congress, 226p.
Elson, J.A. 1961: The Geology of Tills; p.5-17 in Proceedings of the Fourteenth Canadian Soil Mechanics Conference, 13 and 14 October 1960, NRC Associate Committee on Snow and Ice Mechanics, Technical Memorandum No. 69, 290p.
Feenstra, B.H. 1975a: Late Wisconsin stratigraphy in the northern part of the Stratford-Conestogo area, southern Ontario; Unpublished M.Sc. Thesis, University of Western Ontario, Lon don, 232p. 1975b: Quaternary geology of the Markdale area (41A/7), Grey County; p.l 16-118 in Sum mary of Field Work, 1975, by the Geological Branch, Ontario Div. Mines, MP 63, 158p.
Gillespie, J.E., and Richards, N.R. 1954: Soil Survey of Grey County; Ontario Soil Survey, Report No. 17, Guelph, 79p.
Guillet, G.R. 1964: Gypsum in Ontario; Ontario Dept. Mines, IMR18, 126 p. 1967: The clay products industry of Ontario; Ontario Dept. Mines, IMR22, 206p.
Gwyn, Q.H.J. 1971: Heavy mineral assemblages in tills and their use in distinguishing glacial lobes in the Great Lakes area; Unpublished Ph.D. Thesis, University of Western Ontario, 192p.
Hewitt, .D.F and Cowan, W.R. 1969a: Sand and gravel in southern Ontario, 1967-1968; Ontario Dept. Mines, IMR29, 105p.
Hewitt, D.F. and Cowan, W.R. 1969b: Sand and gravel in southern Ontario; Ontario Dept. Mines, OFR5029, supplement to IMR29, 149p.
Hoffman, D.W., Richards, N.R., and Morwick, F.F. 1952: Soil survey of Huron County; Ontario Soil Survey, Report No. 13, lOlp.
Hoffman, D.W., and Richards, N.R. 1952: Soil survey of Perth County; Ontario Soil Survey, Report No. 15, 68p.
60 Hoffman, D.W., Matthews, B.C. and Wicklund, R.E. 1963: Soil survey of Wellington County, Ontario; Ontario Soil Survey, Report No. 35, 69p.
Hoffman, D.W., Matthews.B.C., and Wicklund, R.E. 1964: Soil associations of southern Ontario; Ontario Soil Survey Report No.30, 21 p.
Karrow, P.F. 1963: Pleistocene geology of the Hamilton-Gait area; Ontario Dept. Mines, GR16, 68p. 1968: Pleistocene geology of the Guelph area; Ontario Dept. Mines, GR61, 38p. 1971: Quaternary geology of the Stratford-Conestogo area; Geol. Surv. Canada, Paper 70-34, lip. 1973: Bedrock topography in southern Ontario: a progress report; Geol. Assoc. Canada, Proc., vol.25, p.67-77. 1974: Till stratigraphy in parts of southwestern Ontario; Geol. Soc. America Bull., vol.85, p.761-768. 1977: Quaternary geology of the St. Marys area, southern Ontario; Ontario Div. Mines, GR148, 56p.
Keele, J. 1924: Preliminary report on the clay and shale deposits of Ontario; Geol. Surv. Canada, Mem. 142,176p.
Leverett, F. and Taylor, F.B. 1915: The Pleistocene of Indiana and Michigan and the history of the Great Lakes; United States Geol. Surv., Monograph 53,529 p.
Liberty, B.A. and Caley, J.F. 1969: Geology, Bruce Peninsula area, Ontario; Geol. Surv. Canada, Map 1194A, Scale 1:253,- 440 (Geology 1940-1958).
Liberty, B.A. and Bolton, T.E. 1971: Paleozoic geology of the Bruce Peninsula area, Ontario; Geol. Surv. Canada, Mem. 360, 163p.
Logan, W.E. 1863: Superficial geology; p.886-930 in Geology of Canada; Geol. Surv. Canada, 983p. Superfi cial geology p.886-930. Accompanying Atlas published 1865, 42p.
Montgomery, R.J. 1930: The ceramic industry of Ontario; Ontario Dept. of Mines, vol.39, part IV, 196p.
Parks, W.A. 1903: Fossiliferous rocks of southwest Ontario; Ontario Bureau of Mines, vol.12, p.141-156.
Prest, V.K. 1970: Quaternary geology of Canada; p. 676-764 in Geology and Economic Minerals of Cana da, R.J.W. Douglas, ed., 838p.
Putnam, D.F. and Chapman, L.J. 1943: The drumlins of southern Ontario; Trans. Royal Soc. Canada, Section IV, p.75-90.
Sanford, B.V. 1961: Subsurface stratigraphy of Ordovician rocks in southwestern Ontario; Geol. Surv. Cana da, Paper 60-26, 54p. 1969: Geology Toronto-Windsor Area, Ontario; Geol. Surv. Canada, Map 1263A, scale 1:250,000.
Sanford, B.V. and Quilliam, R.G. 1959: Subsurface stratigraphy of Upper Cambrian rocks in southwestern Ontario; Geol. Surv. Canada, Paper 58-12, 33p. 61 Palmerston Area
Sharpe, D. R. 1975: Quaternary geology of the Durham area (41 A/2), Grey County; p.113-115 in Summary of Field Work, 1975, by the Geological Branch, Ontario Div. Mines, MP63, 158p.
Taylor, F.B. 1909: Field work on the Pleistocene deposits of southwestern Ontario; Geol. Surv. Canada, Summary Rept. 1908, p.103-111. 1910: Field studies of the Pleistocene deposits of southwestern Ontario; Geol. Surv. Canada, Summary Rept. 1909, p. 164-167. 1912: Pleistocene deposits of southwestern Ontario; Geol. Surv. Canada, Summary Rept. 1911, p.262-268. 1913: The moraine systems of southwestern Ontario; Royal Canadian Inst. Trans., vol 10, p.l- 23. 1939: Correlatives of the Port Huron morainic system of Michigan in Ontario and western New York; America Jour. Sci., vol. 237, No. 6, p.375-388.
Terasmae, J., Karrow, P.F., and Dreimanis A. 1972: Quaternary stratigraphy and geomorphology of the eastern Great Lakes region of south ern Ontario; Guidebook, Excursion A42, 24th International Geological Congress, 75p.
Warren, Harry V., and Delavault, Robert E. 1961: The lead, copper, zinc, and molybdenum content of some limestones and related rocks in southern Ontario; Econ. Geol. vol. 56, No. 7, p.1265-1272.
Williams M.Y. 1919: The Silurian geology and faunas of Ontario Peninsula, and Manitoulin and adjacent is lands; Geol. Surv. Canada, Mem. Ill, 195p.
Wright, H.E. Jr. 1971: Retreat of the Laurentide ice sheet from 14,000 to 9,000 years ago; Quaternary Re search, vol. l,p.316-330. 1973: Tunnel valleys glacial surges, and subglacial hydrology of the Superior lobe, Minnesota; Geol. Soc. America, Mem. 136, p.251-276.
62 INDEX
PAGE PAGE Aggregate...... 29,35,36 Garnet ratios, table ...... 12 See also: Gravel; Sand. Gibralter Moraine ...... 22 Agricultural soils ...... 38 Glacial history (of Georgian Bay Alluvium ...... 30 Lobe)...... 31 Analyses: Glacial meltwaters ...... 23 Chemical: Gravel: Salina Formation...... 5 Outwash ...... 24,35 Trace element: Resources ...... 34 Salina Formation...... 6 Ground ice segregation ...... 37 Ground moraine ...... 22 Bass Islands dolostone ...... 6 Drumlinized ...... 18 Bedrock surface ...... 7 Ground water seepage ...... 37 Blasting...... 37 Guelph Formation...... 3 Bois Blanc Formation...... 6 Brick...... 36 Heavy minerals ...... 9,13 Plants ...... 37 James Murray Constr. Ltd...... 35 Catfish Creek Till ...... 8-9,31,37 Jasper conglomerate...... 19 Channel: Fills ...... 24 Kames...... 21 Meltwater ...... 23-24,30 See also: Saugeen. Systems...... 24 Kettle holes ...... 30 Chert ...... 29,35 Content in Elma Till ...... 18,19 Late Wisconsinan...... 31 Clasts, flaggy ...... 18 Clay ...... 36 Maple Lane Moraine...... 16 Red-top...... 37 Marl ...... 30 Varved ...... 29 Maryhill Till...... 12 Collapse features in stratified drift . . . . 25 Meltwater channels ...... 23-24,30 Conglomerate, Jasper...... 19 Mitchell Moraine ...... 19 Molluscs ...... 30 Deposits: Moraine, end ...... 21 Alluvial ...... 30 Moraine, recessional...... 26 Ice-contact...... 36 Moraines: Terrace ...... 24 Gibralter ...... 22 Drift, ice-contact stratified ...... 25 Maple Lane ...... 16 Drift border, attenuated ...... 18 Mitchell...... 19 Drumlins ...... 22,23 Orangeville...... 21,33 See also: Tees water. Seaforth ...... 22 Dundalk till plain ...... 3,22 Singhampton ...... 22 Dundas Valley, Buried ...... 7 Walkerton ...... 21 Wawanosh ...... 19 Economic geology ...... 34 Morainic features...... 25 Egerton Esker...... 28 Mornington Till...... 16,17-18,23,33,37 Elma Till ...... 13,18-21,22,23,29,33,37 Mount View Esker...... 16,28,33 End moraine...... 21 Muck ...... 30 Engineering geology...... 37 Erie Interstadial ...... 29,31 Natural gas...... 6 Eskers...... 21,23,28,29,36 Nissouri Stadial...... 9,31 Egerton ...... 28 Mount View...... 16,28,33 Ontario Soil Survey ...... 38 Riverbank ...... 29 Orangeville Interlobate Moraine ...... 33 Riverstown...... 28,33 Outwash: Subglacial origin ...... 29 Braided ...... 24 Gravel ...... 24,35 Faulting...... 26 Flutings...... 16,17,22,23,30 Peat ...... 30 Frost heave ...... 37 Pleistocene Sections, Measured, appendix ...... 39
63 PAGE PAGE Port Bruce Stadial ...... 12,18,21,31 Port Huron...... 21 Port Huron Stadial...... 21 Stirton Till...... 9-12,16,33 Port Stanley Till ...... 16,33 Stratford till plain ...... 3,22 Proglacial lakes ...... 29 Striations...... 12
Riverbank, locality ...... 28 Tavistock Till ...... 12-17,23,28,33,37 Riverbank Esker ...... 29 Teeswater drumlin field ...... 3,18,33 Riverstown...... 28 "Teeswater till" ...... 18 Riverstown Esker ...... 28,33 Tile...... 36 Till: Salina Formation...... 3 Catfish Creek ...... 8-9,31,37 Sand: Elma...... 13,18-21,22,23,29,33,37 Buried glaciofluvial ...... 25 Maryhill...... 12 Resources ...... 34 Mornington ...... 16,17-18,23,33,37 Sheet ...... 24 Port Stanley ...... 16,33 Varved ...... 29 Stirton ...... 9-12,16,33 Saugeen kame-moraines ...... 3,22 Tavistock...... 12-17,23,28,33,37 Saugeen Kames . . . . 21,24,26,30,33,35,36 "Teeswater"...... 18 Till ...... 21 Till, hummocky ...... 21 Seaforth Moraine...... 22 Till fabric...... 9,12 Sediments: Till plains: Lacustrine ...... 29 Dundalk ...... 3,22 Organic ...... 30 Stratford ...... 3,22 Postglacial ...... 30 Tills, Pre-Catfish Creek ...... 7 Silt, varved...... 29 Silurian ...... 3-6 Varved clay, sand, silt...... 29 Singhampton Moraine ...... 22 Slope failures ...... 37 Walkerton Moraine ...... 21 Soil profiles ...... 38 Walkerton Valley...... 7 Stadials: Wawanosh Moraine ...... 19 Nissouri...... 38 Wingham area ...... 23 Port Bruce ...... 12,18,21,31
64 D
'J-
Ministry of Hon. Frank S. Miller Minister Natural Dr. J.K.Reynolds Resources Deputy Minister Ontario
Ontario Geological Survey Map 2383 PALMERSTON Southern Ontario Quaternary Geology
NTS40P/15 Scale: 1:50000
82000' fs^- i U"30'
)j f X: ^^•^s^'V-''' JF*\ Map 2383
MAP COVERAGE: INDUSTRIAL MINERALS, QUATERNARY OR PLEISTOCENE GEOLOGY SERIES (EXCLUDING PRELIMINARY MAPS)
LEGEND
CENOZOIC QUATERNARY RECENT
13 Alluvium: silt, sanrf, gravel,
12 Bog deposits: muck, marl, peat.
PLEISTOCENE LATE WISCONSINAN
11 Lacustrine fine sand; some silt.
10 10 Lacustrine silt and clay.
9 Silt till .occurring locally within Saugeen Kames,
8 Glaciofluvial outwash sand; minor gravel.
7 Glaciofluvial outwash gravel and gravelly sand.
6 Ice-contact stratified drift: sand, gravel, silt; minor fill. 6a Mainly gravel. 6b Mainly sand.
5 ELMA TILL: stony sandy silt to silt till.
4 MORNING TON TILL: silty clay til!.
3 TAVI STOCK TILL: clayey silt to silt till.
2 CATFISH CREEK TILL: stony sandy silt till.
1 SALINA FORMATION: dolostone (tefes JuncfiodY.l and shale. r X.x^:MH
Deposits on this sheet are mapped where they reach one metre or more in thickness. Thinner deposits are not shown.
SYMBOLS
County boundary.
Township boundary.
••--\ - .950' Topographic contours. *
Drumlin or drumlinoid ridge.
X Glacial fluting.
Esker. 9^/Kurtwille Q
©*5X. .SalumJl \ Ice-contact slope; enclosed area indicates kettle hole.
Small meltwater channel; (direction of flow inferred, uncertain).
Hummocky topography.
Terrace escarpment.
^\ u/^x Geological boundary, actual or interpreted. r^Nl\. PS,^fc. x,\ f.7 l' x i.
Geological boundary, gradational.
\'^~ ' ffif^ W'i i \ - M W:--.-T*^~^' X Gravel or sand pit. ^^Ix'/ 6^^fNSl'ia™ .332 Till sample locality.
For other conventional symbols refer to 1:50000 National Topographic System maps.
kS-V ^ SOURCES OF INFORMATION ^Si. :A -•p^rker^C^ss( " " Geology by W, R. Cowan and assistants, 1972, 1973.
Aerial photography: Forest Resources Inventory, Ministry of Natural Resources, Toronto: National Air Photo Library, Department of Energy, Mines and Resources, Ottawa.
Water well records of the Water Quality Management Section, Ministry of the Environment, Toronto.
Preliminary map, (ODM) P, 1185 Quaternary Geology of the Palmerston Area, scale 1:50 000 issued 1976.
Cartography by A. DiMarco , Surveys and Mapping Published W77 Branch, 1976. Scale 1:50000 Topography from Map 40P/15 of the National Topo graphic System,
Metres 1000 234 7 Kilometres Magnetic declination in the area was approximately 7" West in 1972. C Chains so 40 3 Miles i Ministry of Hon. Frank S. Miller Natural Minister Dr. J. K. Reynolds Resources Deputy Minister Ontario
'^AL V \ "**nr X. Ontario Geological Survey -.-sil V^i^Ffc1 Map 2384 PALMERSTON Southern Ontario Granular Resources
i. l K NTS 40P/15 Scale: 1:50000 \ 3 . 'Mortckli. X ' JP^
B2"00' 44^30'
MAP COVERAGE: GRANULAR RESOURCES SERIES (EXCLUDING PRELIMINARY MAPS)
\,( A\^4\ \ ; y SYMBOLS J / ' : ' ' LEGEND ^ y'Cemetery jvHamstbn- Gravel and gravelly sand having x V /"'"'' cartsiOerebt? lateral and vertical CENOZOIC uniformity. Probability of local!rig QUATERNARY economic oepcsjjs is moderate (o n ;ah wtiers ares! extent is sufficient. RECENT Area underlsin by stratified drift which zsntains localized masses of useabie !3 Alluvium: silt, .^anrf, grai/nl. granular agiteoates. Exploration ar.a development ccst rr.sy fje fugti. iJL^-^-T Moderate probability ttlocating Oeposifs f? Bog JeycjsFVs.1 "luc*. /j/art, ped!. lor local use; tot Drobebi/ity o! locating lime commercial deposits. PLEISTOCENE a^^ Area containing no granular aggregates ol si'sniiicarit e/tterit. LAIE WISCONSINAN Lacustrine fine sane/; some s/H. 30 Location of property: (see 70 Lacustrine sil! and clay. Sartf or gra^f / ptf, 10 9 Sill till occuniny locally v/itliin O Wafer rve(/ location irdicat/nB thickness *2E vi uvbttfuttJert overlying reported thickness ot granular materials? fs indicates material is sandj, 8 (rlacioH'jvial outwash sand; minor Geological tojno'a/t, acf us,' o' interprefeo. 7 ulaciciluvial outwash gravel and gravity sarvj. -- -- - Geological boundary, gradations! G ice-contact stratified drift: serf, grace', silt; minor till. Ga Mainly gravel. 6ti Mainly sand.
i L.LMA TILL: stony sandy si!t to sil! till.
MORNINGTON TILL: silty clay till.
3 TAWSTOCK TILL, dayey Mi! to silt tii!.
t-oi Qfhei convent-ynal symbols refer to 1:50 OOfi Nations! lopCQraohic System maps.
j8#9U^-—rt^ W// \Vj l SALMA FORMAT/CM: t/n/ostoiiti an rf sr.ele i ^ .•^ i Airfi x ,/s; ^-~ Deposits on this sheet nw mapped where Ihtty reocii one mil's or /nore in MiM/iess. Thinner deposits me mt showf.
V. Teviotdrti^"' -.X?^"^ ,i 'l
LIST OF PROPERTIES
CARRICK TOWNSHIP 42. Co-). /^, fat 4, 87, Con. VI, lot el. 43. Cot. rt, to! 7. 96. Can. VI, I'jt 25. 44. Con. rt, lo! 8. SS. Con. VI, lot 25, EGREMONT TOWNSHIP 4b. CM. VI, lot 6. 100. Con. VI, lot 38. 46. Con. 71, lot 29. 101. Con. VI!, lot P? F.G.K 47. Con. rt/, lot l. 1C2. Con, vii. Sot se. 2. Cot., l, lo! 30. 48. Oj'i. rt/, lot Z?. 103. Con. VI', lo! 32. 3. Cor,. IV lot e. 49. Con. '/Ut. lot 13. tC'4. Con. VII, h! 39. 4. Cor.. IV, lot 7. 50. Con. VIII, lot ?5. r05. Can. VIII, lot 6. NORMANBY TOWNSHIP M. Con. IX, lot 5. 106. Con. VI li, lot 34. 52. Con. IX, lot 9. 107. Con. IX, lot S. 5. Cor,. IV. mi ffi. 53. Co:,. IX, lo! 23. IDS. Cor.. IX. lot 34. 54. Can. X. lvl S. X. lo! 35. 'A\ ' Auto Wrecker W.CM. 105. Can, E. Cor.. A, lot 72. 55. Con. X, lot 3. 110. Con. X!, lot 33, A . x^i'Vi'^r? : Brotherston e 7. Con. O, lot 66. 56. Can. X, lot 9. 111. Con. XII, lot II. ^. ,_ 8. Con. fl. lot 72, bf. Con. XI, lot 6. J IS. Can. Jill, lol 14. 58. Con. M. let li. 113. Con. XIII. M 4. HOWICK TOWNSHIP 59. Cun. XI, M 23, 114. Cor,. XIII, lot S. SO. Con. X/, lo! 25. 115. Con. XIII, lot 7. 9. Co/i. li!, lo! 33. 61. Con. XII, lot ?, lie. Can. XIII, lot 15. 10. Cor. IV, Iot3?. 6F. Con. m, lot 5. 117. Con. XIII, M IS. tt. Con. VI fi. M 32. 63. Can. XII. lot 6. 118. Con. XIV, hi S. 13, Ccn. XII. let 30. 64. Can. m, lot 7. 119. Ccr.. XIV, lot 21. 13, Con. XS. lot 31. 65. Curi. XII, lot 10. l M. Con. XV, Sot 15. WALLACE TOWNSHIP 66. Can. XII, lot 53. m. Cun. XV, lot ?3, 67. ECR,lot1?. 11?. Con. Jtif, lot 27. H. Con. Ill, lot ?5. W. WGtl, lot 4. 113. Con. XVI: lot 13. )5. Con. ///, M 40. 69. WGft, lot 13. 124. Con. XVI, lot 16. 7(5. COP. V, lot SC. 70. 'f/QR. M 13. 125. Con. XVI. lot 21. 17, Cor:. VI, lot 29. T.. WGR, lot '3. IPS. Con. XVI: lyt 21. IS. Can, VI, lot 33. 197. Con. XVI, lot 23. 13. Con, VI, lot 35. MARYBOROUGH TOWNSHIP 1?9. Con. XVII, lot St. PO. CD/I. VI, tot 44. 109. Con. XVI!, lot ??. SI, Cor, VII. lot 7. 130. Con. XVII, lot 3?. •22. CM VII, Ini 3.T. 131. Con. XVII. ict 35. 23, Ccf. VII, lot 37. 139. C-j'i. XVII, lot 39, ?4. Ccn. VII. tot 38. 133. Can. XVIII, lor?!. fs. Con, VHl, lot 16. 134. Con. XVIII, lot 33. 26. Con. VIII, lot 22. 135. Con. XVW, lot 33. li. Con. IX, lot 29. 136. Con. A, lot 6. 2S. Can. X, lot 11. f37. Cai,. f, lot 7. 23. Cor,. K!, ict 3, 138. Con. A, lots. '/^ O 139. Con, C. lot 71. ARTHUR TOWNSHIP 140. Con. C, lot 74 30. Con. i, lot rf. 141. Con, C, lot 113. 3). Con. t, lot 11. 142. Con. D, lot 52, 32. Con. I, M 12. MINTO TOWNSHIP 143. Coi.. D, lol 55. 33. Con. II, lain. r 44. Can D, lot 72. 8S. ten. /, tot 27. ^-'"Pifkifei p^x^ 7 34. Con. III, lot S. j.:"', xi( Se. Con. I, lot 41. PEEL TOWNSHIP 35. Con. III, lot 9. SJ, Con, It, lot 31. 36. Con. IV, fat 7. 145. Con, XIII l^t f. S8. Con. //, lot 34. 37. Con. IV, lot 7 89. Con. II, lot 36. 146. Con. XiV.ictf. 38. Con. V, lot 1. 147. Con. XVIII, lot T. M. Con. III, lot li. 39. Con, V, lot i. 91. Co/i. III, lot 3!. 143. Cor,, fi, hi '5. V, lo! B. 40. Con, 9S. Con. IV, iol Si. 41. Can. V, la! 7. WEST LUTHER TOWNSHIP 93. Con. V, lot 5. 94. Con. V, M 22. 149. Con. VII, lots. 55. Con, /, lot 32, 150. Con. VIII. lot 3. 96. Co-). V, lot 35.
SOUKCES OF INFORMATION
Geology by W. R. Cowan and assistants, 187! , 1373. /V// f -' '——* 55W^- wi^-* ^^\ s*,"?/' xioyIfi .' -3^r ^/&S// X ^ - .-r^-'^Jp^^-'- Di-aytoii ^ sx r.-xii J , ,^*^^Xft^ ) ils^S/ /V'. 3 \ i lim^^^:^-^ Water well record'; of rfic Water Quality Mmiauenieiit ^^^fiOft. x^v^. Section, tdinisiry oj the Environment, Toronto. Prslimirtury map, (ODM) P. USS Quaicrnaiy Geology LLINGTON •jf the Pafrnerston Area, sra/e 1:50000 issued 1576. Cartcsraoh'/ Oy A. DiMarco , Surveys ana Mapping Scale 1:50000 Uranf.b. 1976. Topograofi'/ from Mep 40P,15 c' the Nations! Tops- graphic S r stem. Metres innn ci 7 Kilometres Magnetic declination in trie area was approximately |-FT H1 I-T H I^L, 7' West in 19/2.
Chains 80 40 a Miles