A COMPARISON OF THE LATE QUATERNARY SEDIMENTARY SEQUENCE AND PALEOMAGNETIC RECORD OF THE NORTH BAY OUTLET AND A BAFFIN ISLAND FIORD BY ALI RASHID TABREZ SUBMITTED IN PARTIAL FULFILLMENT OF THE REQUIRETVIENTS FOR THE DEGREE OF MASTER OF SCIENCE FACULTY OF SCIENCE LAKEHEAD UNIVERSITY THUNDER BAY, ONTARIO CANADA AUGUST, 1983 ProQuest Number: 10611696 All rights reserved INFORMATION TO ALL USERS The quality of this reproduction is dependent upon the quality of the copy submitted. In the unlikely event that the author did not send a complete manuscript and there are missing pages, these will be noted. Also, if material had to be removed, a note will indicate the deletion. Pro ProQuest 10611696 Published by ProQuest LLC (2017). Copyright of the Dissertation is held by the Author. ^ All rights reserved. This work is protected against unauthorized copying under Title 17, United States Code Microform Edition © ProQuest LLC. ProQuest LLC. 789 East Eisenhower Parkway P.Q. Box 1346 Ann Arbor, Ml 48106 - 1346 TABLE OF CONTENTS Page ABSTRACT i ACKNOWLEDGEMENTS iii LIST OF TABLES iv LIST OF FIGURES V LIST OF MAPS vii LIST OF APPENDICES viii INTRODUCTION General 1 Previous Studies 3 Methods of Study 8 RESULTS Lake Nipissing 13 Lake Nosbonsing 19 Lake Talon 21 Kiosk Lake 23 ^ Cedar Lake 2k McBeth Fiord, Baffin Island 26 DISCUSSION OF RESULTS 30 North Bay Areas 33 McBeth Fiord 63 CONCLUSIONS 76 BIBLIOGRAPHY 80 APPENDICES 89 1 ABSTRACT The lithology of the Late Quaternary lacustrine sequences of five lakes in the North Bay area differs from one lake to another.However , chronostratigraphically equivalent sections of cores taken from the same lake do show similarities in mean grain size, sand percentage and organic and carbonate carbons.The lithology of the Late Quaternary fiord sedimentary sequence of McBeth Fiord,Baffin Island exhibits a slightly higher sand content and lower organic carbon content than the North Bay lacustrine sediments. The magnetic mineral grains deposited on the bottom of lakes and fiords tend to align in the direction of the earth's magnetic field at the time of deposition creating a remanent magnetic field in the sediments.The sedimentary sequences of lakes in the North Bay and McBeth Fiord, Baffin Island areas provides a record of the direction and intensity of the earth's magnetic field for these regions during the Late Quaternary-The declination and inclination values of oriented samples taken from soft-sediment cores of the Late Quaternary lacustrine sequences of the North Bay area and the fiord sequences of McBeth Fiord can be compiled 11 into paleodeclination and paleoinclination logs.The oscillations of the relative paleodeclination logs show a similar character for cores taken from the five lakes and the fiord as do the paleoinclination logs.Marker horizons picked on the character of either the paleodeclination or paleoinclination logs provide a method for chronostratigraphic correlation from one core to another within the North Bay area and also for the McBeth Fiord area. Ill ACKNOWLEDGEMENTS I would like to express my sincere gratitude to Dr.John S.Mothersill for supervision, patience, and his never ending enthusiasm towards my work. I would also like to thank to Dr.T.Griffith, R.Chuchman, K.Pringnitz, A.Mackenzie, Eleanor Jensen, R.Bennett, and D.Crothers for their assistance in the laboratory analyses. Financial support for this study was provided by the Natural Science and Engineering Research Council of Canada through the general grant to the President of Lakehead University and operating grant A4243 to Dr.John S.Mothersill. IV LIST OP TABLES r-*' Page Table 1 Lakes St. Croix and Kylen: estimated ages of 32 inclination features (after Creer and Tucholka,1982) Table 2 Rate of sedimentation in the North Bay areas 3^ Table 2b Area of Lakes, surrounding drainage basin and 45 their relief in the study area Table 3 Average grain size and organic carbon percentages 46 of the North Bay areas Table 4 Heavy minerals present in the sand fraction of the 59 North Bay sediments Table 5 Rate of sedimentation in the McBeth Fiord, Baffin ?2 Island Table 6 Heavy minerals present in the sand fraction of the ?4 McBeth Fiord sediments V LIST OF FIGURES Page Figure 1 Mackereth Corer 7 Figure 2 Paleomagnetic record, lithology, texture and Back Pocket carbon percentages for LU-82-1 (Callander Bay) Figure 3 Paleodeclination logs of North Bay area 15 Figure 4 Paleoinclination logs of North Bay area 16 Figure 5 Paleomagnetic record, lithology, texture and carbon percentages for LU-82-8 (Lake Nipissing) Figure 6 Paleomagnetic record, lithology, texture and carbon percentages for LU-82-9 (Lake Nipissing) Figure 7 Paleomagnetic record, lithology texture and carbon percentages for LU-82-3 (Lake Nosbonsing] Figure 8 Paleomagnetic record, lithology texture and carbon percentages for LU-82-7 (Lake Nosbonsing) Figure 9 Paleomagnetic record, lithology, texture and carbon percentages for LU-82-10 (Lake Talon) Back Pocke' Figure 10 Paleomagnetic record, lithology, texture and carbon percentages for LU-82-13 (Lake Talon) Figure 11 Paleomagnetic record, lithology, texture and carbon percentages for LU-82-11 (Kiosk Lake) Figure 12 Paleomagnetic record, lithology, texture and carbon percentages for LU-82-12 (Cedar Lake) Figure 13 Paleomagnetic record, lithology, texture and carbon percentages for McBeth-1 Figure l4 Paleomagnetic record, lithology, texture for KcBeth-2 Figure 15 Paleodeclination and Paleoinclination logs of 28 McBeth Fiord, Baffin Island Figure 16 "Type” paleodeclination and paleoinclination logs 31 fgr Great Lakes (after Greer and Tucholka, 1982) Vi Figure 1? Cumulative-frequency curves of Lake Talon sands ifS Figure 18 Plot of third moment (skevmess) and fourth moment 51 (kurtosis), using phi (0) scale, for beach and river sands, (after Friedman, I96I, fig.3» p.519) Figure 19 Plot of third moment (skewness) and standard 52 deviation, using phi (0) scale, for beach and river sands, (after Friedman, I98I, fig.^, p.520) Figure 20 Plot of simple skewness measure and simple sorting 52 measure, for beach and river sands, (after Friedman, 1979, figA, p.12) Figure 21 Holocene subdivisions proposed after Andrews and 6^ Ives (1978) and Andrews, 1982 for Baffin Island (for McBeth-1) Figure 22 Holocene subdivisions proposed after Andrews and 6sr Ives (1978) and Andrev/s, I982 for Baffin Island (for McBeth-2) Figure 23 Convolute overturn structure from 3.04 to 3.24m 68 above the sand bed at McBeth-2 site Figure 24 Graded sand beds (turbidites) at WIcBeth-l site 70 Vll LIST OF MAPg Page Map 1 Location map of North Bay areas (See Back Pocket) Map 2 Location map of McBeth Fiord, Baffin Island 25 viii LIST OF APPENDipFS Page Appendix A Lithological discriptions of cores 1- North Bay areas 89 2- McBeth Fiord 93 Appendix B Compilation of grain size data 1- North Bay areas 96 2- McBeth Fiord II6 Appendix G Compilation of organic and carbonate carbons percentage 1- North Bay areas 131 2- McBeth Fiord 140 Appendix D Compilation of paleomagnetic records data 1- North Bay areas l42 2- McBeth Fiord I9I Appendix E Compilation of X-Ray diffraction data 1- North Bay areas 202 2- McBeth Fiords 229 1 INTRODUCTION General The objectives of this study were to compile paleomagnetic logs from oriented samples of cores of Late Quaternary sediments taken from lakes along the North Bay and Fossmill outlet routes from the Great Lakes to the Champlain Sea and from McBeth Fiord,Baffin Island ; to utilize the paleomagnetic logs for chronostratigraphic correlation and absolute time dating of the stratigraphic sequence of these two areas; to relate the sedimentary sequences to the the post- glacial lake phases of the Great Lakes for the Nipissing area; to fit the stratigraphic sequence of McBeth Fiord into late Quaternary chronozones suggested by Andrews and Ives(1978) and Andrews(1982);and to compare the sedimentary sequence deposited in lacustrine and fiord enviroments. During the Quaternary Period, the Great Lakes region was subjected to four glaciations which from oldest to youngest have been designated the Nebraskan , Kansan, Illinoian, and Wisconsinan Stages. However, evidence of only the Wisconsinan Stage is found in the North Bay area. This continental glacier retreated from the region 2 surrounding North Bay about 10,500 to 11,200 years BP. (Terasmae,1980 ; Brest, 1970). As the margin of the glacier receded northward from the study area , glacial melt waters were dammed against the wasting ice front (Lumbers,1971). Subsequent uplift drained many of these lakes leaving fewer and smaller lakes in the topographical depressions. Lake Nipissing is the largest remnant lake in the study area a relect of a very substantial glacial margin lake system that has been described in detail by Hough (1958;1963) and Prest(1970). During early post-glacial time the study area was occupied by part of the North Bay outlet route from Lake Algonquin to the Champlain Sea (Map 1). McBeth Fiord,Baffin Island is situated in a region of active climate change.About 300 years BP a large proportion of the north central plateau of Baffin Island was covered by permanent ice and snow, whereas only about 2% is covered at present. Bradley and Miller(1972) noted that climatic shifts in the order of a decade have substantial effects on the amount of permanent ice and snow on Baffin Island. 3 Previous Studies The last time that glacial ice filled the Lake Huron Basin was during the Port Huron glacial advance which occurred about 13,200 years BP. As glacial retreat occurred Lake Warren(210 m average sea level) and Lake Grassmere (195 m average sea level) formed in the southern part of the Lake Huron basin. Then about 12,500 years BP Lake Algonquin{184 m average sea level) came into existence and drained southward possibly first by the Chicago outlet and later by the Port Huron outlet.There was a brief lowering of the lake level to 171m average sea level during the Kirkfield phase which coihmenced about 12,400 years BP when Lake Simcoe became free of ice and Lake Algonquin discharged directly into Lake Iroquois by the Fenelon Falls-Trent River system (Prest 1970).However this outlet was blocked by a readvance of the Simcoe ice lobe (Deane 1950) and discharge by the Port Huron outlet resumed about 12,200 years BP.Retreat of this ice lobe about 12,000 years BP opened the Kirkfield outlet again but isostatic uplift closed the outlet resulted in raising the lake level to 184 m average sea level. Main Lake Algonquin continued until 11,200 years BP (Prest 1970),or between 10,800 and 10,500 years BP (Terasmae 1980),when glacier retreat allowed the opening of an outlet 4 to the northeast of Lake Huron to the Champlain Sea forming the Lake Stanley phase of the Great Lakes.This resulted in a drop of lake level to 137 m average sea level (Fossmill outlet) and then to 50 m average sea level ( North Bay outlet). The discharge of Lake Stanley via the Fossmill and North Bay outlets resulted in the deposition of a large delta in the northern part of the Champlain Sea.The timing of the drainage of Lake Stanley through outlets in the North Bay area to the Champlain Sea is controversial because of the lack of stratigraphic information (Prest,1970; Karrow et al.,1975; and Terasmae,1980). The Lake Stanley phase ended when isostatic uplift raised the northeastern outlets above lake level which resulted in a gradual flooding of the Huron basin until a stable lake level(184m average sea level) was reached when the Port Huron outlet to the south opened again.This uplift caused the formation of a series of lakes in the topographic depressions along the North Bay outlet route .Continued uplift of the area drained many of the lakes leaving fewer and smaller lakes in the depressions. The largest of the string of small is Lake Nipissing. 5 The stable lake level period of the Lake Huron basin is referred to as the Nipissing phase of the Great Lakes and is usually dated from about 6,000 to 4,500 years BP (Prest,1970;and Terasmae 1979). The Nipissing terrace is well displayed a short distance west of North Bay at an elevation of 700 ft. whereas the present lake level of Lake Nipissing is at 648 ft. Radiocarbon dates on basal organic materials from small lakes at the Nipissing level on Manitoulin Island (Lewis,1968) prove that the Nipissing phase was in existence about 5,500 years BP. Similar evidence from North Bay reported by Lewis(1968) indicates that the outlet to the Ottawa River did not function after 5,000 years BP. Mapping of surficial deposits in the North Bay area has been carried out by Sharpe(1979) and Harrison(1972).Reviews on the deglacial chronology of southeastern Ontario have been published by Prest(1970), Terasmae et al.(1972), and Dreimanis(1977 a,b). Investigations of the Wisconsin glacial history of Baffin Island have shown that the maximum Wisconsin ice cover occurred early in the last glacial, and successive advances were less extensive and local in nature (Pheasant and Andrews,1972; England and Andrews,1973).Investigations of the late and post~glacial marine deposits have been 6 carried out for nearly 20 years on Baffin Island by Andrews.Until fairly recently there has been little systematic attention paid to the establishment of Holocene subdivisions (Andrews and Ives,1978) for Arctic Canada despite a number of radiocarbon dates taken on a wide variety of materials (Lowden and Blake,1978; Miller,1979). However,Andrews and Ives(1978), and Andrews(1982)have suggested delimiting the Holocene of Baffin Island into chronozones comparable to those established for the Nordic Countries. In recent years paleomagnetic studies of late Quaternary sediments have been carried out in Lake Erie (Creer et.al. 1976a), in Lake Michigan (Creer et al.1976b), in Lake Superior (Mothersill ,1979), in Lake Huron (Mothersill ,1981;Mothersill and Brown 1982),in Lake Ontario (Mothersill ,1983),and in Lake Kylen and Lake St.Croix (Banerjee et al.l979). The work has been summarized by Mothersill (1983). These studies based on the natural remanent magnetic directions , resulted in the compilation of suggested type paleodeclination and paleoinclination logs for the Great Lakes area(Creer and Tucholka,1982). FIG. 1. MACKERETH CORER - 6 m 8 Metlriods of Study In May,1982 , nine cores were taken from five lakes in the North Bay area using a Mackereth compressed air corer fitted with a 6 meter long (6cm Internal Diameter) plastic liner (Fig.l). An arbitrary reference line was drawn along the length of the liner before the corer was assembled onshore. Once assembled, the corer was towed behind the Department of Geology's sixteen foot motor boat to the core site and then slowly lowered to the bottom by a nylon rope. An aluminium anchor drum was sunk into the bottom sediment by suction to form the base against which the coring operating could be carried out. Then the plastic liner was slowly forced into the soft sediment by compressed air and once the upper end of the liner had passed the by-pass valve the anchor drum filled with air resulting in the coring device being ejected to the surface. The end of the core liner was bunged with a cap to ensure that the core was retained.The coring operation took approximately one hour and the corer was towed back to shore and disassembled. The water above the core was drained off carefully to ensure that the core was not disturbed. The position of the top of the core in the liner was determined and the liner was cut 9 off several cm above the top of the core. The remaining space above the core was filled with paper towelling to ensure that the soft- sediment core could not shift , and then the top end was capped. The liner was cut into three or four sections to facilitate handling.Each section of the liner was clearly marked to indicate the top and bottom of the section and both ends were capped and taped. In September,1982, two cores were taken from marine sediments in McBeth Fiord, Baffin Island area using a Benthos Piston corer from the CSS Hudson of the Atlantic Geoscience Centre, Bedford Institute of Oceanography, Dartmouth, Nova Scotia. In the laboratory, each section was split longitudinally and the lithology and structure of the sedimentary sequence was described in detail.One half of the core was used for paleomagnetic studies and the other half for grain size ,mineralogy ,and carbon , hydrogen , and nitrogen analyses. Samples were taken at 3 cm intervals in cubed shaped(2cm )plastic boxes in a consistent direction relative to the reference line so that all the samples for each core would be oriented in the same direction The open plastic boxes were pressed slowly into the soft sediment until the box was completely filled. The air was able to escape through a small hole that had been drilled in 10 the bottom of the box prior to the sampling.Then the box filled with sample was carefully cut away from the core and capped with the snap-on top.The bottom hole was covered by scotch tape to prevent drying of the sample, and any sediment adhering to the outside of the box washed off.The oriented samples were measured for remanent magnetic direction and magnetic intensity values using a Minispin 2A fluxgate spinner magnetometer in the University Instrument Room,Lakehead University. Samples were taken at 20cm intervals along the length of the core for grain size analysis and sand percentage determinations.The grain size distribution analyses were carried out on a Micromeritics Sedigraph 5000. Each sample was dried and then a 5g cut was added to a beaker containing a 0.05% solution of Calgon(sodium hexametaphosphate) in double-distilled water to prevent flocculation of the grains.Then the beaker was set in a Bransonic 12 ultrasonic cleaner for at least 20 to 30 minutes to ensure complete grain separation. Wet sieving of the sample through a 0.063mra(4 phi) sieve was carried out to remove the sand fraction .The remaining clay and silt fraction was analyzed on the Sedigraph 5000 to determine the grain-size distribution in the 4 to 12 phi range. The dry weight of 11 the sand fraction was determined and the percentage that it represented of the total sample was calculated as the sand percentage. Cores taken from McBeth Fiord, Baffin Island were split and described at Bedford Institute of Oceanography.Samples were taken at every 25 cm for grain size, mineralogy,organic and carbonate carbon studies,and cube shaped (2 cm) samples were taken at 3 cm intervals as described above for paleomagnetic studies. Grain size analysis of sand samples was carried out on 21 samples from three cores(7 samples from core LU-82-13, 12 samples from core McBETH-l,and 2 samples from core McBETH-2).Each sample was weighed and then sieved on an electrical sieve shaker for ten minutes using a set of 8 inch diameter sieves at half phi(0.50 phi) intervals from 0.5 to <4.0 phi. Petrographic microscopic examination of about 60 thin sections from the 11 cores of the North Bay, and McBeth Fiord, Baffin Island area were made to determine the percentages of heavy minerals present.Heavy mineral separation was carried out on the 4.0 phi fractions using tetrabromoethane (specific gravity,2.94), and sample slides were then prepared for mineral identification, by petrographic microscope. 12 Samples taken at 50cm intervals for X-ray diffractoinetry analysis were dried at room temperature and then finely ground by mortar and pestle .The X-ray diffractometry analysis of the sample was carried out using a Cu-anode with Ni-filter, and scanning rate l/min.{l degree per minute), and a PW 4251 counter with a PW 1366 amplifier. The minerals present were identified based on tables from Smith(1967) , Grim(1968) and Berry(1972). Samples were taken at 0,5,10,50 cm,and then at 50 cm intervals for carbon analysis utilizing a Perkin Elmer Model 240 Elemental Analyzer. Analysis for the total carbon percentage,was carried out on a Ig cut of powdered sample and repeated on a second cut of the sample that had been treated with sulphurous acid.The carbonate carbon percentage was calculated by subtracting the organic carbon percentage from the total carbon percentage. The paleoinclination oscillation peaks of the curves for the Lake Nipissing area were correlated with the oscillation peaks of the type section for the Great Lakes area (Greer and Tucholka,1982). Based on the absolute age suggested for the oscillation peaks of the Great Lakes area absolute ages were assigned to the Lake Nipissing area cores. Dried 2 cm samples were utilized to calculate the fate of sedimentation in im\/yr, and in mg/cpyyr. 13 RESULTS Coring sites LU-82-1 (Callander Bay) ,LU-81-3,and LU-82-7 (Lake Nosbonsing) ,LU-82-8 and LU-82-9 (Lake Nipissing) , LU-82-10, and LU-82-13 (Lake Talon), LU-82-11 (Kiosk Lake) , and Lu-82-12 (Cedar Lake) are shown on Map 1. Lake Nipissing A description of the lithology of core LU-82-1 (Callander Bay) is shown in detail in Appendix A.The core consists predominantly of homogeneous, olive gray,non-calcareous,silty clay. Core LU—82-8(Lake Nipissing) consists of greenish gray to light brown- gray homogeneous, non-calcareous silty clay with a two cm.thick white band occuring at 3.91m and as well as thin white bands from 4.14-4.17m.Core LU-82-9 consists of dark green- gray homogeneous, non-calcareous silty clay. The mean grain size of the silty clay samples analysed from core LU-82-1 (Callander Bay) ranges from 0.0055mm (7.5 0) to 0.0010mm (10.0 0), and the sand percentage of the silt to clay sediments range from 0.5 to 19.0% (Fig.2). The upper 1 m of the core contains a higher percentage of sand and has a larger mean grain size than the lower portion of the core. The sand percentage and grain size generally show 14 an irregular distribution with depth below Im. (Fig.5 and 6). For cores LU-82-8, and LU-82-9 from Lake Nipissing proper the mean grain size ranges from 0.0028mm (8.50) to 0.0010mm (10.0 0), and 0.0019mm (9.00 0) to about 0.0014mm (9.45 0) respectively. The sand percentage for samples from core LU-82-8 ranges from 0.01 to 7.60% and for core LU-82-9 from 0.02 to 0.13%.The higher upper limit of sand percentage in core LU-82-8 is based on one sample taken at 3.91 m depth. Generally ,both cores taken from Lake Nipissing show an irregular distribution of sand percentage with depth. The sediments of Lake Nipissing are composed of major amounts of quartz and K-feldspar,subordinate amounts of plagioclase, and minor amounts of chlorite, kaoline ,illite, vermiculite, dolomite,and calcite (Appendix E).The percentage by weight of the heavy minerals present in the sand fraction ranges from 1.0 to 31.1%, and consists of hornblende(30-40%),epidote(10-15%),garnet both rose and a coloress variety(5-10%), pyroxene(1-5%), tourmaline(1-2%), zircon(1-2%), apatite(1-5%), magnetite (1-2%) and hematite (1-3%).The organic carbon percentage ranges from 1.4 to 4.2 for samples from core Lu-82-1(Callander Bay), and the carbonate carbon percentage ranges from zero to 0.1%. The organic carbon percentage ranges from 0.2 to 2.5% and the LU-82-1 LU-82-3 LU-82-7 LU-82-8 LU-82-9 LU-82-10 DEPTH CALLANDER LAKE LAKE LU-82-II LU-82-12 LU-82-13 LAKE LAKE LAKE (METRES) BAY NOSBONSING NOSBONSING KIOSK CEDAR LAKE NIPISSING NiPiSStNG TALON LAKE LAKE TALON 9 0 9 *90 -9 0 0^ *90 -90__2__^0 -9|0 0 *ao -9L0 Q -SO -9iO Q ^ *9|0-^ Q *90 0i W- 20 .»• {* 30 50^ 80- FIGURE 3. Paleodeclination logs of North Bay area LU-82-1 LU-82-3 LU-82-7 LU-82-8 LU-82-9 LU-82-10 DEPTH CALLANDER LAKE LAKE LU-a2-|| LAKE LU-82-12 LAKE LU-82-13 LAKE (METRES) BAY NOSBONSING NOSBONSiNG KIOSK CEDAR NIPISSING LAKE NIPISSING TALON LAKE LAKE TALON 0 30 60 90 0 30 60 90 0 30 60 90 0 30 60 9,0 10 20- H 30- o\ 40- 50- 60 FIGURE ^ Paleoinclination logs of North Bay area 17 carbonate carbon ranges from zero to 1.1% for core LU-82-8, and the organic carbon percentage rages from 0.9 to 1.7% and the carbonate carbon percentage ranges from 0.0 to 1.6 for core LU-82-9 (Appendix C). The relative declination and inclination of cores LU-82-1 ,LU-82-8, and LU-82-9, are shown in Figures 3 and 4. The declination values for each core were first determined relative to the arbitrary reference line.Then the mean declination was calculated and assigned a zero value,with each declination value determined relative to the mean value.The plots of the relative declination values for each core of the lacustrine sediments form a continuous curve,which swings through a number of oscillations with maximum and minimum amplitudes. The inclination values were plotted directly from the values determined by the Minispin 2A spinner magnetometer (Fig. 4), and also show a continuous oscillating curve for each of the cores. It was not possible to determine whether the cores were taken vertically during the coring operation. However even if some of the cores were not taken vertically it would only result in a decrease in magnitude of the inclination values and the oscillations of the paleoinclination log.The magnetic intensity values for the samples analyzed range 18 from 3.38 to 37.96 uG(0.34-3.79 mT) for core LU-82-1 (Callander Bay),from 13.99 to 335.04 uG(1.39-33.5 mT) for core LU-82-8 , and 14.28 to 63.93 uG(1.45-6.52 mT) for core LU-82-9. 19 Lake Nosbonsing Cores LU”'82~3 and LU-82->7 from Lake Nosbonsing consist of olive black and gray to greenish gray, homogeneous, non-calcareous silty clay(Fig. 7).The mean grain size of samples from core LU-82'-3 range from 0.0025mm (8.67 0)to 0.0013mm (9.67 0)and for LU-82~7 from 0.0019mm (9.00 0) to about 0.0011mm (9.93 0) Fig. 8.The sand percentages of these cores range from 0.9 to 14.0 % and 0.3 to 15.15% respectively.Both cores taken from Lake Nosbonsing show a decrease in grain size and sand percentage with depth. The mineralogy of the sedimentary sequence for Lake Nosbonsing is similar to that of Lake Nipissing.But the percentage of heavy minerals of the sand fraction is less than for Lake Nipissing and ranges from 0.08 to 6.66%. The organic carbon content ranges from 2.62 to 11.16% and the carbonate carbon ranges from zero to 1.2% for core LU-82-3.The organic carbon ranges from 2.7 to 8.7% and the carbonate carbon from zero to 1.1% for core LU-82-7. The plot of the relative paleodeclination values of Lake Nosbonsing cores LU-82-3,and LU-82-7 show a continuous oscillatihg curve for each core although the plots are much more scattered than for the Lake Nipissing cores.The 20 relative declination plots for core LU-82-3 exibits somewhat less scattering than for ^-82-7 (Fig. 7 and 8).Similarly the paleoinclination value plots which show considerable scattering show a general trend of oscillating curves for each core. The magnetic intensity values of both cores range from 1.75 to 6.48 uG (0.18-0.65 mT), and 1.54 to 7.97 uG (0.16-0.79 rtiT) for cores LU-82-3 and LU-82-7 respectively. 21 Lake Talon Core LU-'82-10 consists of olive gray to greenish gray, homogeneous, non~calcareous silty clay with dark bands that occur at 2 to 3 cm intervals throughout the core.Core LU~82~13 consists of olive gray to dark greenish gray, homogeneous, non-calcaleous silty clay with dark bands occuring at 2 to 3 cm intervals to a depth of 1.23m.Sand forms in the lower part of the core from 2.63~2.90 m.The mean grain size of samples of silty clay from these cores ranges from 0.0019mm (9.00 0)to 0.0016mm (9.33 0) for core LU-82-10 (Fig. 9), and from 0.0032 to 0.0011mm (8.33 to 9.92 0) for core LU“82-'13. The sand percentages range from zero to 2.6% and 0.1% to 17.1% for cores LU-82-10 and LU~82~13 respectively for the silty clay.The sand percentage of the lower sandy portion of core LU-82-13 ranges from 84.4 to 96.7% (Fig. 10). The mineralogy of the sedimentary sequence for Lake Talon is similar to that of Lake Nipissing and Lake Nosbonsing,and the heavy mineral percentage of the sand fraction ranges from 0.4 to 5.0%.The organic carbon percentage of core LU-82'"10 ranges from 3.5 to 7.1% and the carbonate carbon ranges from zero to 1.4%.For core LU-82-13 the organic carbon ranges from 1.1 to 5.9% and the carbonate 22 carbon ranges from 0.0 to 1.8%. The relative paleodeclination values of these two cores show continuous oscillating curves with the log for LU-82-10 being the better defined of the two.The paleoinclination plots also form continuous oscillating curves with the curve for LU~82-10 being better defined (Fig. 9 and 10). The magnetic intensity values ranged from 5.89 to 66.40 uG (0.58-6.64 mT) for core LU-'82-10, and 3.17 to 45.91 uG (0.32-4.59 mT) for core LU-82-13. 23 Kiosk Lake Core LU-82-11(Kiosk Lake) consists of olive black, homogeneous,non-calcareous silty clay.The mean grain size ranges from 0.0032mm (8.33 0) to 0.0016mm (9.33 0),with sand percentage varying from 0.1 to 1.5%.The grain size and the sand percentage show an irregular distribution with depth. The mineralogy of the sedimentary sequence is similar to that of Lake Nipissing, Lake Nosbonsing, and Lake Talon.However the percentage of heavy minerals forming the sand fraction is lower and ranges from 0.8 to 2.2% The organic carbon percentage ranges from 6.8 to 9.2% and the carbonate carbon ranges from 0.7 to 2.9%. A pattern of oscillation can be discerned for the paleodeclination and paleoinclination curves despite the scattering of the plots (Fig. 11). The magnetic intensity values of the Kiosk Lake core range from 0.66 to 22.12 uG (0.66-2.21 mT). 24 Cedar Lake Gore LU''82~12 from Cedar Lake consists of brownish black homogeneous,and non-calcareous silty clay (Fig. 12). The mean grain size of samples taken from the core ranges from 0.0026 to 0.0018mm (8.58 to 9.08 0), and the sand percentage from 0.4 to 7.8%. The mineralogy of the sedimentary sequence is similar to the rest of the lakes of the study area, and the percentage of heavy minerals forming the sand fraction ranges from 1.0 to 5.0%. The organic carbon percentage ranges from 9.68 to 12.33% and the carbonate carbon from 0.7 to 2.9%. The paleodeclination and paleoinclination plots show a cosiderable scattering of data for the upper part of the core although for the lower part the log is less scattered and continuous curves can be discerned(Fig. 12). The magnetic intensity values varies from 2.67 to 18.97 uG (0.27-1.93 mT). The detailed lithology, mean grain size, sand percentage, organic and carbonate carbon percentage,relative paleodeclination, paleoinclination and magnetic intensity values for each core have been compiled in Appendices A,B,C and D, 25 Map 2. Location map of McBeth Fiord, Baffin Island. 26 McBeth Fiord The location sites for cores McBeth-1 and McBeth-2 from McBeth Fiord, Baffin Island are shown in Map 2. McBeth-1 core is located at the head of McBeth Fiord,and McBeth-2 core is located on the northeastern distributary of the fiord. The lithology of the sediments of McBeth-1 core was examined on a fresh core surface after the segments had been split longitudinally along the length of the core and is portrayed in Figure 13.It consists of olive gray, homogeneous and non-calcareous silty clay.Sand layers, approximately 2 cm thick, occur at 0.013, 0.026, 0.031, 0.050, 0.075, 0.38, 0.89, 2.01, 2.22, 3.30, 5.05,7.51, and 9.31 meters(Appendix B).The mean grain size of the silty clay sequence,which was determined using the Sedigraph 5000 and wet sieving methods for samples at 0.25m intervals along the length of the core ranges from 0.0055 to 0.00125mm (7.50 to 9.83 0).The sand percentage of the silt and silty clay sequence ranges from zero to 8.5%. McBeth Fiord sediments are composed of major amounts of quartz and K-feldspar, subordinate amounts of plagioclase, and minor amount of chlorite, illite, phlogopite. and 2? vermiculite. The percentage of heavy minerals comprising the sand fraction of the silty clay varies from 2.1 to 5.0%, and consists of major amounts of phlogopite (20-30%), hornblende (10-20%),epidote (5-10%),garnet (1-5%),and minor amount of pyroxene(1-5%), tourmaline(1-2%), apatite(1-2%), magnetite(1-2%) and hematite(1-3%).The organic carbon ranges from 0.31 to 0.78% and the carbonate carbon from zero to 0.3%. The lithology of core McBeth-2 is shown in detail in (Fig. 14).It consists of olive gray, homogeneous and non-calcareous silty clay.Shell fragments occur at 0.52-0.53m. Thinly—laminated silt occurs at 2.93-3.01m, and interbedded silt and clay at 3.01-3.06m. Silty sand forms the succession at 3.06-3.25m.A pebble of granite was found at 3.25m. Only one thin bed of sand (324.5 to 330.5 cm) was noted in this core. The mean grain size of the silty clay and silt sequence of the McBeth-2 core ranges from 0.0019 to 0.0012mm (9.00-9.75 0), and the sand percentage ranges from 1.1 to 4.7%. The mineralogy of the sedimentary sequence is similar to that of core McBeth-1, but the percentage of heavy minerals is greater ranging from 0.5-8.5%.The organic carbon ranges from 0.5 to 1.4% and the carbonate carbon from zero 28 McBeth-1 McBeth-2 DECLINATION INCLINATION DECLINATION INCLINATION FIGURE 15. Paleodeclination and Paleoincllnatton logs of McBeth fiord. 29 to 0.3%. TTie relative declination and inclination values of samples taken from cores McBeth-1 and McBeth-2 are shown in Figure. 15. Unfortunately an arbitrary line had not been drawn along the length of the liner before the corer was assembled for taking the Baffin Island cores.Therefore the declination values of each core segment had to be rotated relative to each other to obtain the best fit. Then the average declination value was determined and the relative declination calculated.The lack of a reference line did not affect the magnitude of the inclination values.The paleodeclination and paleoinclination values of these two cores show continuous oscillating curves. The magnetic intensity values for core McBeth-1 range from 12.60 to 232 uG (1.26-23.20 mT) and for core McBeth-2 from 13.64 to 303 uG (1.36-30.30 mT). 30 DISCUSSION OF RESULTS One of the major problems encountered in studies of the late Quaternary stratigraphic sequence of the Great Lakes basin is that^C has not proved to be a reliable method for dating postglacial lacustrine or outwash deposits because of the " old carbon " contained in the sediments (Mothersill,1982;1983), and (Creer,1982).For example, Creer et al.(1976) suggested an error of 2,000 years for the post-glacial sediments of Lake Michigan; Mothersill(1979) suggested an error of at least 1,700 years for the post-glacial stratigraphic sequence of Thunder Bay, Lake Superior; and Graham and Rae(1980) suggested surface corrections of 1,250 to 1,600 years in the Alpena and Manitoulin Basins, Lake Huron .These errors cannot be applied as a consistent correction throughout the sedimentary sequence. The oscillations of the paleodeclination and paleoinclination curves result from the secular variations of the earth's magnetic field with time. Therefore marker horizons picked on the character of either of these curves could be used for time-parallel correlation from one core to another within the North Bay area. The paleomagnetic method 31 Fio.i6 . 'Type' oalcodec Iination and pa 1eoinclination lops Cor Great Lakes (after Greer and ITicholka, 1982). age [mill enia] 32 Feature Age label (radiocaitx}n years BP) ■y 200 5 1 300 a 2 100 { 2 600 3 500 6 4 050 t 4 750 K 6000 X 6 750 p 8 200 V 9 500 4 10 500 tr 12 100 P 12 800 a 14 300 T 16 500 TABLE 1. Lakes St. Croix and Kylen: estimated ages of inclination features (after Creer and Tuj^olka,1982). 33 has been used as a secondary method for absolute time dating, of the late Quaternary stratigraphic sequence in the Great Lakes region ( Mothersill,1981; 1982; and 1983, Greer et al. 1976; Greer and Tucholka,1982).Greer and Tucholka (1982) have suggested "type" paleodeclination and paleoinclination logs for the late Quaternary of the Great Lakes area and have designated symbols for the major oscillation swings (Fig. 16).The absolute dates assigned to identifiable features of these paleoinclination oscillation swings are noted in Table 1 . Mothersill(1982) noted that for the Holocene stratigraphic sequence of the Great Lakes area the average period of the oscillations of the paleodeclination and paleoinclination logs were 2600 years based on using the date of 9,000 years BP proposed by Saarnisto (1975) for the cessation of glacial varve deposition in Lake Superior. North Bay area The character of the paleodeclination,as well as for the paleoinclination logs for cores LU-82-1, LU-82-3, LU-82-7, LU-82-8, LU-82-9, LU-82-10, LU-82-11, LU-82-12, and LU-82-13 show similar oscillation trends(Fig. 3 and 4).The Lake Nosbonsing, Kiosk and Gedar logs show a much greater scattering of the paleodeclination and paleoinclination Table 2 RATE OF SEDIMENTATION IN THE NORTH BAY AREA LAKE NIPISSING LAKE NOSBONSING LAKE TALON KIOSK LAKE CEDAR LAKE AGE LU-82-1 LU-82-8 LU-82-9 LU-82-3 LU-82-7 LU-82-10 LU-82-13 LU-82-11 LU-32-12 YEARS BP sa inm/yr ng/cin /yr mm/yr m^/cm /yr tim/yr mg/ca^/yr ow/yr ™j/cro‘/yr mm/yr mg/cm^/yr mm/yr mg/cm 2 /yr wn/yr mg/cm 2 /yr mm/yr mg/cm‘/yr mm/yr mg/cm^/yr r 0- 200 1.00 60.55 0.90 91.91 1.00 63.05 3.25 89.63 1.75 41.96 1.00 24.27 1.00 23.42 1.00 15.12 r-c 200-1300 0.90 66.24 0.54 52.59 0.73 54.40 0.95 22.35 0.36 7.80 0.73 20.33 0.73 21.58 0.73 14.30 0.90 09.40 U) -P:- S-t 1300-2100 1.75 119.73 0.87 62.98 0.62 52.73 0.69 17.94 1.75 43.80 0.37 10.51 0.75 28.79 0.75 13.47 1.30 19.60 t-i- 2100-2600 1.80 160.40 0.80 78.52 0.50 39.39 1.40 34.04 1.20 76.73 0.30 29.07 1.80 132.14 0.80 16.59 2600-3500 1.00 102.19 0.66 51.99 0.89 40.94 0.67 62.71 0.3 33.00 3500-4C50 0.36 34.47 0.66 51.99 0.5 46.5 S. — 4, 4050-4750 0.57 49.40 E--K 4760-6000 0.80 74.87 35 plots resulting from the relatively low magnetic intensity values compared to the other cores, because of the high organic content as well as the high quartz sand content in the case of the Nosbonsing cores .The paleomagnetic logs of the cores from Lake Nipissing and Talon show a fairly well defined trend of oscillations.However,the paleoinclination log of core LU-82-9 from Lake Nipissing shows a much more subdued oscillation pattern. The inclination values for this core are lower than for the other paleoinclination logs compiled for Lake Nipissing which would indicate that this core was not taken vertically. Non-vertical coring would tend to decrease the absolute as well as the relative paleoinclination values and therefore the amplitude of the oscillations. Based on the age of the oscillation peaks assigned by Creer and Tucholka (1982) the rate of sedimentation for the time intervals bracketed by these oscillation peaks can be calculated in mm/yr and in mg/cmVyr (Table 2).It should be pointed out that although the age of these features could be modified as more accurate data becomes available these assigned dates provide the most viable method of dating the sedimentary sequence and calculating the rates of sedimentation available at the present time.The paleoinclination logs usually have been found to be more reliable than the paleodeclination logs 36 (Motlhersill, 1982) and therefore are utilized for dating the cores and determining the rates of deposition with time.The paleodeclination and paleoinclination logs have been replotted at the same scale as the “type" logs for the Great Lakes area for correlation purposes. Five marker horizons have been picked on the paleodeclination log and another four marker horizons have been picked on the paleoinclination log for the core taken from Callander Bay (LU-82-1) for time~parallel correlation purposes.lt cart be noted that there is a strong correlation with the "type" paleomagnetic logs established for the Great Lakes (Creer and Tucholka,1982).Based on the paleomagnetic time scale the core bottomed at 2800 years BP. Seven marker horizons have been picked on the paleodeclination log and another eight marker horizons have been picked on the paleoinclination log for core LU-82-8 and six marker horizons have been picked on the paleodeclination and paleoinclination logs for core LU-82~9. These logs also can be correlated with the "type" section logs. Based on the paleomagnetic time sOale cores LU-82-8 and LU-82-9 would appear to have bottomed in sediments dated at about 6000 and 4500 years BP respectively. 37 The paleomagnetic logs for core LU*'82»3 and especially core LU-82'-7 taken, from Lake Nosbonsing show a much greater scattering of the paleodeclination and paleoihclination plots than did the paleomagnetic logs for the Callander Bay and Lake Nipissing cores.This phenomenon has been noted for paleomagnetic curves from sedimentary sequences with a high organic and quartz sand content resulting in relatively low magnetic intensity values (Mothersill, 1983). The magnetic intensity values for Lake Nosbonsing cores LU~82-'3 and LU~82-'7 range from 1.75 to 6.48 uG (0.18~0.65 raT) and 1.54 to 7.97 uG (0.16-0.80 mT) whereas the magnetic intensity values for LU*^82-8 from Lake Nipissing which has very well defined paleodeclinatiOn and paleoinclination logs range from 13.99 to 335.04 uG {1.40-33.50 mT).However the trend of the oscillating curves can be discerned.lt exibits a similar pattern to the "type" paleodeclination and paleoinclinations logs proposed by Creer and Tucholka (1982). Seven marker horizons have been picked on the paleodeclination and another seven marker horizons have been picked on the paleoinclination curve from both these cores.Based on the paleomagnetic time scale cores LU-82-3 and LU-82-7 would appear to have bottomed in sediments dated at about 4000 years BP. The paleomaghetic logs for cores LU-82-10, and LU-82-13 taken from Lake Talon are well defined and can be correlated to the "type" paleomagnetic logs and also to the other paleomagnetic logs of the cores of North Bay area.Four paleodeclination and paleoinclination marker horizons have been picked from core LU-82-10, and four paleodeclination and four paleoinclination marker horizons have been picked for core LU~82-13. Based on the paleomagnetic time scale cores LU'-82~10 and LU-'82-'13 would appear to have bottomed in sediments dated at about 2750 and 3400 years BP respectively. Three paleodeclination marker horizons and four paleoinclination marker horizons for core LU-'82''ll from Kiosk Lake have been correlated to the paleomagnetic "type" logs.Based on the paleomagnetic time scale this core bottomed in sediments dated at 2600 years BP. Four paleodeclination and three paleoinclination marker horizons have been correlated for the paleomagnetic logs of core LU-82-12 from Cedar Lake with the "type" paleomagnetic logs.Based on these correlations the core bottomed in sediments deposited 2300 years BP.The paleomagnetic logs of the cores from Kiosk and Cedar Lakes show a scattering of the plots and therefore not as well defined logs as for 39 either the Nipissing or Talon cores because the relatively high organic content (organic carbon>10%) has diluted the ferrimagnetic mineral content of the sediments resulting in magnetic intensity values of 0.66 to 22.12 uG (0.07-2.21 mT) and 2.67 to 18.97 uG (0.27-1.90 mT).However the plots of the paleomagnetic logs of these cores show less of a scattering than for the Lake Nosbonsing cores where magnetic intensities are lower because of dilution of the ferromagnetic minerals both by organic matter and the higher quartz sand content. It can be noted that for the cores taken of the North Bay and Fossmill outlets the sand percentage,mean grain size, and organic and carbonate carbon logs compiled in Figures 2, and 5 to 12 cannot be correlated from one lake to another. However these parameters do show a similarity for cores taken from the same lake.Core LU-82-1 (Callander Bay) would appear to have bottomed in sediments dated at about 2800 years BP based on the paleomagnetic time scale.This date can be used to calculate that the average rate of sedimentation from the present to 2800 years BP for the Callander Bay site was 1.1 mm/yr which fluctuated from 0.9 to 1.8 mm/yr (60.55 to 160.40 mg/cni/yr, see Table 2).The sand percentage of this core ranges from 0.5 to 19%, and the 40 mean grain size ranges from 0.0010 to 0.0039mm (10.0 to 8.0 0),£or tlie Tiomogeneous, olive green, silty clay of the sequence. It was not possible to calculate the grain size parameters of these silty clays either by the method of moments (Friedman,1961) or by the graphic method (Folk and Ward,1957) for the entire grain size distribution of the silty clays because the Sedigraph 5000 can only determine grain sizes from 0.063mm (4 0) to 12 0. Cores LU-82-8 and LU-82-9 would appear to have bottomed in sediments dated at about 6000 and 4500 years BP respectively, based on the paleomagnetic time scale.Both cores LU-82-8 and LU-82-9 were taken from sites in the-open and central part of Lake Nipissing.The calculated average rate of sedimentation from the present to 2600 years BP was considerably lower at 0.77 mm/yr (71.5 mg/cm/yr) for site LU-82-8 and 0.71 mm/yr (52.39 mg/cm/yr) for site LU-82-9 than for the Callander Bay site for the comparable time period.The oscillation peaks of the paleoinclination log for core LU-82-8 are well defined and should be accurately dated based on the "type" paleomagnetic log.The average rates of sedimentation for the period between oscillation peaks for this core are compiled in Table 2 for time intervals from the present to 6000 years BP.The rates fluctuated from 0.36 mm/yr ( 34.47mg/cit?/yr) to 1.00 mm/yr (102.19mg/cm7yr) . It should be noted that the relative rates of sedimentation for core sites LU-82-1 from Callander Bay and LU-82-8 from Lake Nipissing show the same trends with the lowest rates of sedimentation occuring between 200 and 1300 years BP followed by an increase from 200 years BP to the present. The rates of sedimentation for core LU-82-9 do not show the same trends as the other two cores although a substantial increase is noted for the past 200 years BP.As pointed out earlier the overall rates of sedimentation of the two cores from Lake Nipissing are comparable and the determinations for the shorter time periods could be inaccurate as a result of the more poorly defined oscillation peaks for the log of core LU-82-9. Cores LU-82-8, and LU-82-9 from Lake Nipissing proper show generally very low sand percentages, of less than 1% and mean grain sizes which range from 0.0010 to 0.0028mm (10.0 to 8.50 0).However, at a depth of 3.85m (about 5200 years BP) in core LU-82-8, the sand percentage does increase to 7% (Fig. 5). The grain size of the sediments forming cores LU-82-8 and LU-82-9 located in the open and central part of Lake Nipissing is substantially finer than for the Callander Bay core for the same time period,and shows the normal 42 decrease in grain size lakeward and further from the sediment source.There is a substantial increase in mean grain size and sand percentage at the top of the sedimentary sequence for the Callander Bay core, which could reflect an increased rate of erosion resulting from the de-forestation of the shore region of the bay area that took place during the last century. There is also a slight increase in mean grain size at the top of core LU-82-8, though not for core LU-82-9 in the central part of Lake Nipissing. Lithologically these two cores from Lake Nipissing proper do show a similarity in grain size for the time period of overlap to 4500 years BP. The organic carbon content for surface interface sediments for core LU-82-1 from Callander Bay is 4.2% and decreases to slightly less than 2.0% below 2.0m whereas the organic carbon content for core sites LU-82-8 and LU-82-9 are about half these amounts for the surface sediments and at depth along the core (Fig. 5 and 6).This would suggest that the relative amount of organic material being deposited on the lake-bottom for Lake Nipissing proper is less than for Callander Bay.Unfortunately there is very little information available on organic matter in the basinal clays of lakes (Friedman,1978).Streams and rivers contain both dissolved 43 and particulate organic matter.The organic content of streams and rivers ranges from 10 to 30 ppm (Clark,1924) and for the temperate areas the organic content of rivers tends to be lower and consists of particulate matter because decomposition is retarded in a cold climate.The organic content deposited in the basinal areas of lakes cannot be matched with a probable source (Friedman,1978).However the two main sources would be terrestrial organic matter from the surrounding watershed and phytoplankton from within the lake.Much of the organic matter tends to be oxidized to form carbon dioxide and water.The silled situation of Callander Bay would result in lower energy conditions than Lake Nipissing proper would tend to allow the deposition of relatively more particulate organic matter. The oxidized and reduced units of the sequence comprise the syndiagenetic phase with the oxidized unit corresponding to the "initial stage" and the reduced unit corresponding to the "early burial stage" of Dapples (1962). Twenhofel (1942) pointed out that the "initial stage" may extend from a few millimeters to as much as 50cm below the sediment interface, depending on such factors as water-depth, rate of sedimentation and amount of organic matter.The lower rates of sedimentation in the open and central part of Lake Nipissing areas, where the lake-bottom sediments contain 44 lower amounts of organic carbon, would allow time for the aerobic bacteria to consume a greater percentage of the entrapped organic matter, resulting in a substantial decrease in the organic carbon.However, at the Callander Bay site where the rate of sedimentation was more rapid there would be less time for aerobic bacteria to consume the organic matter and therefore there would be a greater chance for preservation of more of the organic matter in the early burial stage of the syndiagenetic sequence. The highest values of organic carbon occur just below the water-sediment interface as is generally the case for most lakes in the Great Lakes area (Mothersill,1971) and elsewhere where oxidizing conditions occur at the lake-bottom. Generally the carbonate carbon content of the sediments is low in the Lake Nipissing region, except for a slight increase at the top of core LU-82-9.The source of the carbonate carbon for the North Bay area lakes probably was detrital limestone and dolomite derived from carbonate debris from the paleozoic carbonate strata of the Moose River Basin to the north and brought into the area by glacial action. The greenish color may be due in part to the content of the green phyllosilicates such as illite and chlorite,(Blatt,et al.,1972) and in part to the state of oxidation of iron in the sediments (probably mostly the Fe). 45 AREA OF LAKES, SURROUNDING DRAINAGE BASIN AND THEIR RELIEF IN THE STUDY AREA. Area Elevation Relief Callander Bay: 11 KM’^ 196m Surrounding Drainage Basin: 50 KM 288m 92m Lake Nipissing; 821.5 KM*^ 196m Surrounding Drainage Basin:9500 KM 288m 92m Lake Nosbonsing: 15 KM 235m Surrounding Drainage Basin: 92 KM’^ 364m 129m Lake Talon: 11 KM' 193m Surrounding Drainage Basin: 56 KM’’ 3 79m 186m Kiosk Lake: 11 KM’’ 303m Surrounding Drainage Basin: 54 KM’’ 424m 121m Cedar Lake: 16 KM* 303m % Surrounding Drainage Basin: 35 KM 409m 106m TABLE 2b. ^6 LAKES RANGES OF GRAIN SIZE (0) RANGES OF ORGANIC CARBON Callander Bay 7.5 to 10.0 1.4 to 4.2 (LU-82-1) Lake Nlplssing 8.5 to 10.0 0v9 to 2.5 (LU-82-8) Lake Nlplssing 9.0 0.9 tto 1.7 o 9.4 (LU-82-9) Lake Nosbonslng 8.7 to 9.7 2.6 to 11.2 (LU-82-3) Lake Nosbonslng 9.0 2.7 to 8.7 o 9.9 (LU-82-7) Lake Talon 9.0 3.5 to 7.1 o 9.3 (LU-82-10) Lake Talon 8.3 1,1 o 9.9 to 5.9 (LU-82-13) Kiosk Lake 8.3 6.8 to 9.2 o 9.3 (LU-82-11) Cedar Lake 8.6 to 9.1 9.7 to 12.3 (LU-82-12) TABLE 3 Average gra.ln size and organic carbon percentages of the North Bay areas. 4? Lake Nosbonsing cores LU-82-3, and LU-82-7 show similar sand percentages ranging from 0.30 to 15.15%, and mean grain sizes ranging from 0.0010 0.0025mm (10.0 to 8.63 0).The organic carbon percentage is relatively higher than for the cores of Callander Bay and Lake Nipissing (Table 3 )• The bay in which the two cores were taken is silled by a small island at it's mouth which would result in low energy conditions for the bay allowing the deposition of particulate organic matter in its central portion.The shorter transport distances and lower energy conditions for the smaller lakes of the study area would tend to be more favourable for the deposition of particulate organic matter relative to Lake Nipissing. Also it should be noted that generally for the study area that those lakes having the higher organic carbon content are those that have the coarser mean grain size of the silt-clay fraction (Table 3 ). There is a decrease in organic carbon content for the uppermost part of both cores from Lake Nosbonsing which could be a reflection of increased erosion and detrital deposition over the past 200 years.This distribution of organic matter is certainly not representative of lakes in the Great Lakes area or the other lakes studied in the North I Bay area. Although the relief is greater than for Lake Nipissing much of the clastic sediments may be derived from 48 the island and surrounding shoreline of the bay. It has been pointed out that the paleomagnetic logs for the cores from Lake Nosbonsing,and especially for LU-82-7, show a scattering of the plots and therefore provide less reliable control than for the cores from Callander Bay and Lake Nipissing.However based on utilizing the age of the oscillation peaks of cores LU-82-3 and LU-82-7 Nosbonsing sites show fairly similar rates of sedimentation of 1.07 and 0.98 mm/yr repectively.These would be sedimentation rates similar to that for the Callander Bay site and considerably greater than the two Lake Nipissing proper sites. However,if the rate of sedimentation is calculated in mg/cm/yr then the rates of sedimentation for the Lake Nosbonsing sites is considerable lower than for Callander Bay and the Lake Nipissing proper sites because of the relatively higher organic content for the Nosbonsing sites. The sedimentary sequence for the Lake Talon cores consists of homogeneous, olive gray to greenish gray,silty clay with dark colored bands.These bands are probably concentrations of black unstable iron sulphide mineral hydrothoilite.The silty clay sediments of core LU-82-10 from Lake Talon exhibits sand percentages and mean grain sizes ranging from zero to 2.6% and from 0.0016 to 0.0019mm (9.33 49 to 9.00 0) respectively. Core LU—82-13 has a sand percentage which ranges from 0.1 to 17.1% and mean grain size which ranges from 0.0011 to 0.0032mm (9.92 to 8.33 0). In core LU-82-13 there is a substantial increase in the sand content in the sequence from a depth of 2.25m, to 3.65m, which would have been deposited during the period from 2750 to 3400 years BP. The sand percentage of this sandy portion of the core ranges from 84.4 to 96.7%.The uppermost part of this time interval may have been encountered of the base of core LU-82-10 which bottomed at about 2750 years BP.Although a minor increase in sand percentage occurred in Lake Nipissing at the core LU-82-8 site at a depth 3.85m ( 5200 years BP) no increase was noted in the interval 2750 to 3400 years BP which would indicate that this period of sand deposition in Lake Talon was a local event.All of the samples analysed are well to moderately sorted, negative to positively skewed, and mesokurtic to leptokurtic based on determination of the grain size parameters using moment measures after Friedman (1961).Based on the shape of the cumulative curves of the grain size distribution of each sample based on the work of Visher, 1969, beach rather than river deposition would be indicated (Fig. 17). In addition the samples were analyzed by compiling graphs of different combinations of grain size parameters. These graphs were; IGURE ^7. Cumulative-frequency curves of Lake Talon sands. CUMULATIVE PERCENT PROBABILITY SCALE 51 kurtosis versus skewness (Fig. 18), skewness versus standard deviation (Fig. 19), arid simple skewness measure versus simple sorting measure (Fig. 20). For the skewness versus standard deviation the Lake Talon sands plot in the beach environmental field and in the skewness versus kurtosis and skewness versus simple sorting measure most of the Lake Talon sand samples plot in the beach environment field.This provides substantial evidence that the sands deposited at the LU-82-13 site were beach sands. Therefore it v/ould appear that beach sands were deposited at site LU-82-13 from 2750 to 3400 years BP and were onlapped by lacustrine silty clay basinal sediments deposited from 2750 years BP to the present.This would indicate a transgressive sequence and that Lake Talon increased in size after 2750 years BP. The organic carbon percentage is highest at the sediment-water interface and generally decreases with depth,for the two cores from Lake Talon which is the normal organic distribution for lakes which have oxidizing conditions at the lake-bottom. The sediments of both cores contain less than 2% carbonate carbon,that is probably detrital carbonate as previously noted.The relief of the surrounding catchment basin for Lake Talon is greater than 52 KURTOSIS FIGURE 18 . Plot of third moment (skewness) and fourth moment (kurtosls), using phi (0) scale, for beach and river sands, (after Friedman 9 1961 fig.3, p.519). SKEWNESS 53 STANDARD DEVIATION IGURE i§. Plot’of third moment (skewness) and standard deviation, using phi 03) scale, for beach and river sands^ (after Friedman,1961, fig.4, P.52Q). SKEWNESS 54 SIMPLE SORTING MEASURE (SO^) FIGURE 20.Plot of Simple Skewness Measure and Simple Sorting Measure for beach and river sands,(after Friedman,1979, fig.4, p.l2) SIMPLE SKEWNESS MEASURE 55 for the other small lakes (Nosbonsing, Kiosk and Cedar) which could account for the relatively lower organic content of LU-82-10 (3.47-7.14%) and uppermost part of LU-82-13 (3.80-5.19%) because of increased clastic input.The decrease in the organic carbon content below 3.0m in LU-82-13 is a result of the dilution of the organic material by the substantial increase in coarse clastic material.This increase in the sand content below 2.5m in core LU-82-13 is reflected in a decrease in magnetic intensity for that part of the section and a scattering of the paleodeclination and paleoinclination plots. The well defined paleomagnetic curves for the basinal lacustrine sequence for Lake Talon reflects higher magnetic intensity values resulting from a higher ferrimagnetic mineral content. The calculated average rate of sedimentation from the present to 2600 years BP is lower for core LU-82-10 relative to LU-82-13 both in inm/yj^ (0.65 versus 0.96) and in mg/cra/yr (37.6 versus 57.1). These rates of deposion range between the rates for the core site at Callander Bay and the core sites of Lake Nipissing proper (Table 2). The sedimentary sequence for the Kiosk Lake core consists of homogeneous, olive black, very fine grained silt to coarse grained clay. The grain size analyses of samples 56 from core LU-82-11 from Kiosk Lake gave sand percentage ranging from 0.1 to 1.5%, and the mean grain size ranges from 0.0016 to 0.00125mm (9.33 to 8.83 0), both of which exhibit an irregular distribution with depth. The organic carbon percentages are highest at the top of the core just below the water-sediment interface (9.2%) and show • a progressive decrease with depth which has already been pointed out is the usual situation for well-aerated lakes. The carbonate carbon percentage is somewhat higher for the upper part of the core. The dark color of the sediments probably results for the most part from both the high organic content and to a lesser extent and the reduced state of the iron content in the sediments. The area of the surrounding drainage basin of Kiosk Lake is about five times that of the lake area which is comparable to the ratio for Lake Talon. However the organic carbon content of the sediments is considerably greater than for the stratigraphic sequence of Lake Talon. The average rate of sedimentation from 2500 years to the present is about 0.8 mm/yr and ranges from a low of 0.5 mm/yr (8.4 mg/cm/yr) from 1300 tp 2100 years BP to a maximum of 1.5 mm/yr (22.7 mg/cm/yr) from the present to 200 years BP.These rates of sedimentation are similar to that of core site LU-82-13 for Lake Talon in mm/yr, however the rate in mg/cm/yr is considerably 57 less.Therefore the higher organic content of the sediments of Kiosh Lake appear to reflect a greater input of organic material and a lower amount of detrital material.The lower amount of detrital material could be a reflection of the lower relief of the surrounding watershed of Kiosk Lake relative to Lake Talon (Table 2b). The increased rate of deposition in the immediate past probably reflects the logging operations carried out for slightly more than 100 years. The sedimentary sequence at Cedar Lake consists of homogeneous, brownish black, fine grained silt.The grain size analyses of samples from Cedar Lake core LU-82-12 gave sand percentages ranging from 0.0 to 4.1%, with the mean grain size ranging from 0.0018 to 0.0026mm (9.08 to 8.58 0). The sand percentage and mean grain size increase very slightly with depth. There is a slight increase in the sand content (+5%) for the interval from 1.0 to 2.0m (1200 to 2000 years BP based on the paleomagnetic chronology).Once again this appears to be a local increase in sand content that is not reflected in the record of the other lakes of the study area.The organic carbon content of this core is higher than for any of the other lake-cores from the North Bay area. There is a relatively higher organic carbon 58 percentage, at the top of the core (13%) versus an average of about 10 percent for the rest of core which is the normal distribution of organic carbon in a stratigraphic sequence of an aerated lake. The consistent brownish black (5YR2/1) of the sediments probably results from the high organic content of the sediments.The scattering of the paleodeclination and paleoinclination plots (Fig. 12) is a result of the relatevely low magnetic intensity values ranging from 2.67 to 18.97uG (0.27 to 1.93 mT) resulting from the dilution of detrital ferromagnetic minerals by the high organic content of the sediments. The surrounding drainage basin for Cedar Lake is 2.2 times the lake area (Table 2b), and the maximum relief is lower (106m)than for the other three small lakes in the study area.The relative lower relief of the Cedar Lake drainage basin could account for the high organic content of the sedimentary sequence.Although the average rate of sedimentation of 1.1 mm/yr from the present to 2100 years BP was comparable with the Other lakes of the area it is quite low (14.5 mg/crn/yr) if expressed in weight/area/year. The mineralogy of the sedimentary sequences of the lakes studied in the North Bay area consists of major amounts of quartz,subordinate plagioclase and orthoclase Table 4• THE HEAVY MINERALS PRESENT IN THE SAND FRACTION OF THE SILTY CLAY IN THE NORTH BAY AREAS CORE SITES HORNBLENDE EPIDOTE GARNET PYROXENE TOURMALINE ZIRCON APATITE HEMATITE MAGNETITE LU-82-1 (Callander Bay) 20 - 30% 5-10% 1-5% 1-5% 0 - 1% 0-1% 1-3% 1-2% 0 - 1% LU-82-8 (Lake Nipissing) 30 - 40% 10 - 15% 5 - 10% 1 - 5% 1 - 2% 1-2% 1-5% 1 - 3% 1 - LU-82-9 (Lake Nipissing) 25 - 40% 10 - 15% 5 - 10% 1-5% 0 - 1% 0-1% 1-5% 1 - 2% 0 - 1% LU-82-3 (Lake Nosbonsing) 10 - 20% 5 - 10% 1-5% 1-3% 1 - 2% 0-1% 1-3% 1 - 2% 0 - 1% \o LU-82-7 (Lake Nosbonsing) 10 - 20% 5-10% 1-5% 1-3% 1 - 2% 0-1% 1-3% 1 - 2% 0 - 1% LU-82-10 (Lake Talon) 10 - 15% 5 - 15% 1-5% 1 - 5% 1 - 2% 0-1% 1 - 2% 1 - 3% 0 - 2% LU-82-13 (Lake Talon) 10 - 15% 5-10% 1-5% 1 - 5% 1 - 2% 0-1% 1-2% 1 - 3% 0 - 2% LU-82-11 (Kiosk Lake) 5 - 10% 2-5% 1-5% 1-5% 0 - 1% 0-1% 1-2% 1 - 2% 0 - 1% LU-82-12 (Cedar Lake) 5 - 10% 1 - 5% 2 - 3% 1-3% 0 - 1% 0 - 1% 1-2% 0-2% 0 - 1% 60 feldspar, and minor amounts of chlorite, kaolin, illite, vermiculite, dolomite, and calcite.The percentage of heavy minerals of the sand fraction ranges from 1 to 31% in the lakes of the study area.The sediments of the Lake Nipissing cores show the maximum percentage(1 to 31%) of heavy minerals contained in the sand fraction of the sediments rather than in the silt fraction. Lake Nosbonsing cores contained 1 to 7%, heavy minerals in the sand fraction. Lake Talon from 0.4 to 4.0%, Kiosk Lake 0.8 to 2.0% and Cedar Lake from 0 to 1%. The heavy sand grains consist of a wide variety of minerals with major amounts of hornblend(30-40%), epidote(10-20%), garnet(both rose and colorless variety) 5-10%,and minor pyroxene (5-10%), tourmaline(1-2%), rutile (1-2%), zircon(1-2%), apatite(1-5%), magnetite(1-2%) and hematite (1-3%) as shown in Table There is little change in the heavy minerals present from lake to lake in the North Bay area.The heavy minerals are those which would be expected to be derived from the Pre-Cambrian biotite and hornblende rich gneissic rocks, and the granitic and monzonitic rocks that comprise the Precambrian outcropings in the study area. The etched surface of the mineral grains of the sand fraction of the sediments suggest that the grains underwent chemical as well as physical weathering.Etched grains constitute good evidence of 61 solution.However it is not always clear that etching was achieved after, rather than before deposition (PettiJohn,1975). Hydration and hydrolysis of minerals is the first step in the chemical alteration of parent minerals such as the feldspars to clay minerals (Degens,1965).The main clay minerals of the sediments from the lakes of the study area are kaolinite. illite, vermiculite, and chlorite. Hydrogen ions combine with the aluminum silicate radical of the orthoclase to form the new clay minerals under conditions of intense weathering and decomposion. Muscovite and K-feldspar as well as plagioclase, may provide the alumina and silica necessary for forming kaolinite which is the most common weathering product of feldspar (Brownlow,1979).Vermiculite forms primarily from the partial weathering of muscovite and biotite (Jackson,1964;Brownlow,1979).Illite found in soils is probably to a great extent simply inherited from pre-existing sedimentary illite of diagenetic origin, or from the partial weathering of igneous and metamorphic muscovite (Berner,1971).Most sedimentary chlorite is probably derived from pre-existing chlorite, although limited amounts form from later layer-type silicates during weathering (Jackson,1964;Brownlow,1979). Most chlorites have a low ion-exchange capacity and are nonswelling 62 (Brownlow,1979). Therefore the kaolinite, and vermiculite would appear to be, at least in part, products of the post-glacial weathering cycle of the Precarabrian bedrock of the North Bay area.The chlorite, illite and part of the kaolinite and vermiculite would appear to be products of the glacial deposits and pre-existing sediments that underwent at least second-cycle weathering and erosion.Only a fraction of the feldspar underwent complete alteration to clay minerals as orthoclase and plagioclase are two of the most abundant minerals of the sediments of the lakes of the North Bay area. 63 McBeth Fiord There is a good correlation of the paleodeclination as well as the paleoinclination logs for cores McBeth-l and McBeth-2 from McBeth Fiord, Baffin Island (Fig. 13 and 14). There are nine well defined declination and inclination oscillations for the McBeth-l core and eight declination and inclination oscillations for McBeth>-2 .These well defined paleodeclination and’ paleoinclination oscillations should provide a method of time-parallel or chronostratigraphic correlation from one core to the other. The paleodeclination and paleoinclination logs from both the cores from McBeth Fiord show a strong similarity to the "type" paleomagnetic logs established for the Great Lakes (Greer and Tucholka,1982), and also to the logs compiled for the Lake Nipissing area.The "type" paleodeclination and paleoinclination logs for the Great Lakes also appears to correlate with paleomagnetic logs for the Lake District of England(Creer,1976b). Therefore it would appear to be reasonable to assume that the McBeth paleomagnetic logs can be correlated with the "type" paleomagnetic logs for the Great Lakes area and that the suggested geomagnetic time scale be tentatively applied to the McBeth paleomagnetic logs.But due to the westward drift (secular change) of the 64 earth's magnetic field with time the ages assigned to the paleomagnetic features probably would be about 200 years older than for the ages assigned to these paleomagnetic features for the Great Lakes area. As this region is nearer to the magnetic north pole the paleoinclination values should be greater than for the Great Lakes area and it can be noted that in the McBeth Fiord area the paleoinclination values range from 60 to 90 versus 20 to 70 for the Great Lakes area. The cores would appear to have bottomed in sediments dated at about 9500 and 4750 years BP for cores McBeth-1 and McBeth-2 respectively. Both core taken from McBeth Fiord,Baffin Island are correlated to subdivisions of the Holocene proposed by Andrews and Ives (1978) and Andrews,1982 based on the selection of isochronous boundaries at 10,000, 9.000, 8,000, 5,000, and 2.500 years BP (Fig. 21 and 22). The lithology of the sedimentary sequences cored at the two sites in McBeth Fiord consists predominantly of sandy, coarse grained clay to very fine grained silt with subordinate thin beds of sand.For core McBeth-1, taken from the head of the McBeth Fiord the sand percentage of the coarse grained clay to very fine grained silt ranges from 0.22 to 8.48%, and the mean grain size ranges from 0.00125 65 (a) 1 Subatlantic 2 3 4 Subboreal Atlantic 8 Boreal 0 Pre-Boreal 10 FIGURE 21. Holocene subdivisions proposed after Andrews and Ives (1978) and Andrews (1982), for Baffin Island. . .. i ^Q-7/^ a) Chronostratigraphlc subdivision of Norden Region (Mangerud et al.,1974). b) Chronostratigraphic/geochronological subdivision for the Canadian Arctic (Andrews and Ives,1978:Andrews,1982). c) Paleodeclination and Paleoincllnatlon logs of McBeth-1. HOLOCENE SERIES 66 McBETH-2 Cc) I’A 1.1:1'INCLI- NATION DECLINATION INCLINATION ^ ClIlU'NOi.OCY (a) (b) -90 0 "98 45* 90* YF.Ai:S lil’. 1 Subatlantic Windy L 2500 Subboreal Iglutallk to w M PwS 5000 ? CO w ?; u o Atlantic Kangllo o.J o 3: Boreal Cockburn Pre-Boreal Remote L 10 ■' ;URE 22. Holocene subdivisions proposed after Andrews and Ives (1978) and Andrews (1982), for Baffin Island. , 1 a) Chronostratigraphlc subdivision of Norden Region (Mangerud et al.,1974). b) Chronostratigraphlc/geochronological subdivision for the Canadian Arctic (Andrews and Ives,1978:Andrews,1982). c) Paleodecllnatlon and Paleolnclination logs of McBeth-2. 67 to 0.0017mm (9.83 to 9.17 0). Thin sand beds which are 2 to 3 cm thick, occur at 0, 0.013, 0.027, 0.031, 0.075, 0.38, 0.89, 2.01, 2.22, 3.30, 5.05, 7.51, and 9.31 meters and consist of 74.0 to 94.4% of sand sized particles.All of the samples analysed were plotted using different combinations of grain size parameters. For skewness versus standard deviation, skewness versus kurtosis and simple skewness versus simple sorting measure the McBeth Fiords sands plot in the river environment field (Figures 18 to 20). The sediments contain less than 1% organic and carbonate carbons in core McBeth-1, and there is a decrease in organic carbon percentage with depth. The small amount of organic carbon in the fiord sediments would result from the low amounts of terrestrial organic matter. Carbonate carbon is probably detrital and derived from the adjacent rocks. The second core, McBeth-2,located on the northeastern distributary of McBeth Fiord,consists predominantly of coarse clay with a mean grain size ranging from 0.0014 to 0.0019mm (9.58 to 9.00 0).The sand percentage of this lithology which ranges from 0.55 to 4.66% is somewhat lower than for the coarse clay at McBeth-1.Only one thin bed of sand from 3.24 to 3.30 depth was noted in this core.There is a convolute overturn structure from 3.04 to 3.24m above the 68 1 - (/) LiJ CC h- 2 - UJ z 3 - X I- 4 - QL LU Q 5- FIGURE 23 . Convolute overturn structure from 3.04 to 3.24m above the sand bed at McBeth-2 site. sand bed.It would appear that the sand acted as a sole on which slumping of a thin segment of the overlying coarse clay unit took place probably shortly after deposition as the clay strata above 3.0m does not show any structural distortion (Fig. 23).This is substantiated by the paleodeclination and paleoinclination plots which show a scattered distribution for the thin slump interval but form a continuous and well defined log for the sandy clay sequence above 3.0m depth.These points would indicate that the slumping took place shortly after deposition of the thin distorted section from 3.04 to 3.24m depth and would have occurred about 2600 years BP based on the paleomagnetic time scale.A pebble of granite breccia was found at a depth of 3.25m in the McBeth-2 core below the slump structure.lt may have been deposited by ice rafting. In core McBeth-1 site fourteen sand beds occur with eleven of these beds occuring from the top of the core to 3.30m depth. However at the site of the core McBeth-2 site only one sand bed was found at 3.31m depth. As the river at the head of the fiord provides the main source of clastic sediment input to the fiord it would be likely that the sediments comprising the normal deposition of sandy, coarse grained clay would show a decrease in grain size away from 70 0 SAND SILTY CLAY 1 - SAND SILTY CLAY 2 - SAND SILTY CLAY 3 - SAND SAJID 4 - SILTY CLAY 5 - SAND 6- SILTY CLAY 7- SAND 8- SILTY CLAY 9- SAND SILTY CLAY 10- FIGURE 24. Graded sand beds (turbidltes) at McBeth-1 site DEPTH IN METRES 71 site McBeth-l at the head of the fiord to McBeth-2 on the northeastern distributry of the fiord. I In core McBeth~l,the normal deposits consisting predominantly of sandy clay are interbedded with the thin beds of graded sand, which would appear to result from turbidite deposition.These sand beds are moderately sorted,negative to strongly positively skewed and platykurtic to leptokurtic, fine to very fine grained sand, (based on the graphic paramaters of Folk and Ward,1957 and the moment measures of Friedman,1961).A graded sand sample was taken from the McBeth-1 core site at about 3.48ra along the length of the core for thin section study.lt was clearly noted by microscope studies that the fine grained sand units are graded, fining upward. The interbedding of the normal deposition of coarse grained clay with graded sands commonly occurs in turbidite successions and if these graded sand beds are turbidites it should be possible to correlate, sand beds from McBeth~l (Fig. 24) to the sand single sand bed encountered in McBeth-2 at 3.31m. Based on the paleomagnetic time scale the sand bed in McBeth-l would be dated about 4000 yeats BP and would correlate with a series of sand beds in McBeth-l at about 2.30m depth. 72 7 Table 5- RATE OF SEDIMENTATION IN McBETH FIORD, BAFFIN ISLAND McBeth - 2 FEATURE AGE YEARS BP McBeth - 1 Label mm/yr mg/cm /yr mm/yr mg/ctn'^/yr r 0 200 1.00 74.70 1.5 92.74 r- S 200 1300 0.54 47.10 0.73 50.58 s-e 1300 2100 0.37 31.35 0.62 49.89 2100 2600 1.20 120.85 1.80 141.47 t-3- 5-‘K_ 2600 3500 0.61 61.43 1.67 152.91 3500 4050 1.09 87.88 4050 4750 1.00 80.63 4750 6000 0.76 64.71 K-?. 6000 6750 0.93 78.84 6750 8200 0.69 66.23 A-V 8200 9500 0.61 67.62 73 Generally the high sand content results from the sand particles being carried in a flow of fresh water over the more dense marine waters of the fiord before an inter-mixing of the fresh water and marine water occurs.Studies of Tingin and Itirbilung fiords, Baffin Island that are currently being carried out at Lakehead University on these fiords show a sand content in excess of 10%. However, this type of fiord deposit was not found at the two sites in McBeth Fiord.Generally a basinward thickening of the sedimentary sequence may be noted from McBeth-1 to McBeth-2,especially from the present to 2500 years BP (Fig. 21 and 22).The rate of sedimentation at the head of the fiord (McBeth-1) was relatively lower both in mm/yr and in mg/cnf/yr from the present to 4750 years BP than for the northeastern distributary (McBeth-2) Table 5 . The sedimentary sequence of McBeth Fiord,Baffin Island is composed of major amounts of quartz, K-feldspar, subordinate amounts of plagioclase, and minor amounts of chlorite, phlogopite, illite, and vermiculite.The percentage of heavy minerals ranges from 2 to 4.54% in core McBeth-1 ,and from 0.51 to 8.52% in core McBeth-2.Both cores show a decrease in the percentage of heavy minerals with depth. Heavy minerals consists of ma jor amounts of Table 6. THE HEAVY MINERALS IN THE SAND FRACTION OF THE SILTY CLAY .IN THE McBETH FIORD, BAFFIN ISLAND CORE SITES PHLOGOPITE HORNB LENDE EPIDOTE GARNET PYROXENE TOURMALINE APATITE HEMATITE MAGNETIT McBETH - 1 20 - 30% 10 - 20% 5-10% 1-5% 1-5% 1-2% 1-2% 1-3% 1 - 2% McBETH - 2 20 - 30% 10 - 15% 5 - 10% 1-5% 1-3% 0-1% 0-1% 1 - 2% 1 - 2% 75 phlbgopite(20-30%),hornblend(10-15%), epidote(5-10%), and garnet both rose and colorless variety(1-5%), and minor amounts of pyroxene(1-5%), tourmaline(1-2%), magnetite(1-2%),and hematite(1-3%) as shown in Table 6.The surface texture of phologopite and other minerals grains are quite fresh in appearance.The type and appearance of the mineral grains of the sand fraction suggests that the sediments were derived from Precambrian granitic gneiss and migmatite, undifferentiated plutonic, sedimentary and volcanic rocks of the adjacent area that had been subjected principally to physical weathering.The absence of kaolinite and presence of the mica mineral phlogopite in the McBeth Fiord sediments indicate that these sediments were not subjected to extensive chemical weathering.The illite found is probably, to a great extent, simply inherited from pre-existing sedimentary illite of diagenetic origin or from the partial weathering of igneous and metamorphic muscovite (Berner,1971). Most sedimentary chlorite is probably derived from pre-existing chlorite, although limited amounts form from later layer-type silicates during weathering (Jackson,1964;Brownlow,1979). Vermiculite forms primarily from the partial weathering of muscovite and biotite (Jackson,1964;Brownlow,1979). 76 CONCLUSIONS It was hoped that cores taken in the North Bay area would have penetrated to the glacial deposits in order to ascertain the timing of the North Bay (through Lake Nipissing, Trout Lake and Talon Lake) and the Fossmill (through Lakes Nipissing,Nosbonsing,Kiosk and Cedar) outlets draining water to the Champlain Sea.Unfortunately the post-glacial sedimentary sequence was thicker than expected and it was not possible to obtain cores to the glacial deposits with the coring device available. The Nipissing transgression is dated at 5,750+ years BP (Sly and Lewis, 1972).The oldest sediments cored in the study were dated at 6000 years BP (core LU-82-8 from Lake Nipissing proper).This indicates that the basal sediment in the core could represent the beginning of the Nipissing phase of the Great Lakes. At that time isostatic uplift of the North Bay area had occurred and separate lakes formed along the North Bay and Fossmill outlet routes. This would account for the different lithologies from lake to lake. Chronostratigraphic correlation of the lacustrine stratigraphic sequences utilizing paleomagnetic logs would appear to be the most viable of correlation tools available 77/ at this time•Scattering problems develop in the plots of the paleodeclination and paleoinclination values when the magnetic intensities of the stratigraphic sequence are low. Usually this is caused by a decrease in the ferromagnetic mineral content due to high quartz sand and/or a high organic content.However, the repeatable oscillation pattern of the "type" paleodeclination and paleoinclination logs can still be ascertained. This study clearly indicates that paleodeclination and paleoinclination logs can be utilized for chronostratigraphic correlation from one core to another within the North Bay area as well as for McBeth Fiord,Baffin Island. The paleomagnetic logs of McBeth Fiord can be correlated with the "type" paleomagnetic logs established for the Great Lakes area by Greer and Tucholka(1982). Utilizing the geomagnetic time scale of the "type" logs for assigning absolute dates to the cores of McBeth Fiord would appear to be valid. However the absolute dates of the paleomagnetic markers would probably be 200 years older for the McBeth area than for the Great Lakes area. Dating the age of the cores provides sufficient information to calculate the rate of sedimentation for intervals in mm/yr as well as in mg/cm/yr with time. 78 The chronostratigraphic subdivisions of the Holocene of Baffin Island proposed by Andrews and Ives (1978),and Andrews (1982) based on the selection of isochronous boundaries at 10,000, 9,000, 8,000, 5,000, and 2,500 years BP, can be applied to the two cores of McBeth Fiord based on the paleomagnetic time scale. The predominant lithology of the North Bay lakes and McBeth Fiord is silty clay, but the sand fraction percentages of the silty clay of the lacustrine sedimentary sequence (North Bay outlet) except for Callander Bay and Lake Nosbonsing show lower sand percentages than for the fiord sequence. Generally the organic carbon percentage of the lacustrine sequence is higher than for the fiord sequence and is undoubtedly due to the greater availability of terrestrial organic matter in the North Bay area.Carbonate carbon percentage of both areas range in between 1 to 2%, denoting that both areas probably contain detrital carbonate derived from the adjacent source areas. The mineralogy and grain surfaces of the sedimentary sequence in the North Bay lakes sampled show that both physical and chemical weathering were ^active.For example the 79 etching and fracture, surfaces of the grains strongly indicates chemical weathering, either prior to erosion or during the transportation of the sediments.Whereas in the McBeth Fiord area the appearance of the mineral grains and presence of phlogopite would indicate that the sediments are basically a product of physical weathering. 80 BIBLIOGRAPHY Andrews,J.T.,1982.Chronostratigraphic division of the Holocene Arctic Canada.In Chronostratigraphic subdivision of the Holocene (Mangerud,J.,Birks,H.J.B., and Jager,K.D.,Editors)^Striae, 16, pp.56-64.Uppsala• Andrews,J.T. and Ives,J.D1978. "Cockburn" nomenclature and the Late Quaternary history of the Eastern Canadian Arctic.Arctic and Alpine Res., 10,pp.617-633. Andrews,J.T.,Hears,G.H.,Miller, and Pheasant,D.R.,1972. 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Quaternary geology of Canada.In Geology and economic minerals of Canada. Edited by R.J.W.Douglas. Geological Survey of Canada,Economic Geology Report 1,pp.675-764. Saarnisto,M,1975.Stratigraphic studies of the shoreline displacement of Lake Superior.Canadian Journal of Earth Sciences, 12, pp.300-319. Sharpe,D.R. 1979. Quaternary geology of the Merrickville area. Southern Ontario. Ontario Geological Survey Report 180.54p. Sly,P.G., and Lewis,C.F.M.1972. The Great Lakes of Canada. 24th International Geological Congress Excursion, 88 Quaternary Geology and Limnology, A43, pp.1-92. Smith,J.V.1967. X-ray powder data file 1-5. American Society for Testing and Materials, Philadelphia, 685p. Terasmae,J.1980. Some problems of Late Wisconsin history and geochronology in southeastern Ontario. Canadian Journal of Earth Sciences,17,pp.361-381. Terasmae,J., Karrow,P.F., and Dreimanis,A.1972. Quaternary stratigraphy and geomorphology of the eastern Great Lakes region of southern Ontario.24th.International Geological Congress, Montreal,P.Q.,Field Excursion A42.75p. Terasmae,J., and Hughes,O.L.1960. Glacial retreat in the North Bay area, Ontario. Science,131,pp.1444-1446. Visher,G.S.,1969, Grain-size distributions and depositional processes.Jour. Sed. Petrol., 39, pp.1074-1106. APPENDIX A Lithological discriptions of cores 1- North Bay areas LU-82-1 (Callander Bay) LU-82-8 (Lake Nipissing) LU-82-9 (Lake Nipissing) LU-'82-3 (Lake Nosbonslng) LU-82-7 (Lake Nosbonsing) LU-82-10 (Lake Talon) LU-82-13 (Lake Talon) LU-82-11 (Kiosk Lake) LU-82-12 (Cedar Lake) 2- McBeth Fiord McBeth-1 Me Beth-2 LITHOLOGICAL DISCRIPTIONS OF CORES LU~82’“1(CALLANDER BAY): 0-2.36 meters silty clay, olive gray(5Y4/l), homogeneous,non-calcareous.2.36-3.79 meters silty clay, olive green(5Y4/1), homogeneous,and non-calcareous. LU-82-3(LAKE NOSBONSlNG): 0-1.10 meters silty clay olive blackish gray(5Y3/l), homogeneous, non-calcareous,and not very compact, color gradually darkens to olive black{5Y2/1).1.10-2.86 meters silty clay olive black (5Y2/1),homogeneous,non-calcareous,and more compact. 2.86-3.43 meters silty clay color change to dark greenish gray(5GY4/1), homogeneous,non-calcareous,and compact.3.43-4.33 meters silty clay greenish gray(5GY5/1),homogeneous, non-calcareous,and compact. LU-82-7(LAKE NOSBONSlNG):0-0.53 meter silty clay olive gray(5Y4/l), homogeneous, non-calcareous,and loose compact.0.53-2.58 meters silty clay olive blackish gray(5Y3/l),homogeneous,non-calcareous, and slightly more compact.2.58-2.63.,2.63-2.98 meters silty clay olive gray(5Y4/1),homogeneous, non-calcareous, and more compact.2.98-3.66 meters silty clay greenish gray(5GY6/1), homogeneous, non-calcareous, and compact. LU-82-8(LAKE NIPISSING):0-3.13 meters silty clay greenish gray(5GY6/1), homogeneous,non-calcareous,and firm compact. 3.13-3.63 meters same color but non-homogeneous in nature. From 3.63 meters color change upto 3.73 meters silty clay dark greenish gray(5GY4/1),homogeneous,non-calcareous, and firm compact. But from 3.73 meters color gradually changes 90 into olive gray(5Y4/l) upto 3.91 meters.From 3.91 meters abrupt color change upto 3.96 meters separated by 2cm white-gray band to dark greenish gray(5GY4/1). But from 4.03-4.14 meters silty clay complete color change to light brownish (5YR6/1) , homogeneous, and calcareous.4.14-4.17 meters small white band again separates, a color change black to a much brownish gray (5YR6/l).At 4.19 meters small white band 1-2 cm and at 4.22 meters color again change to greenish gray(5GY4/l) upto 4.30 meters silty homogeneous, and calcareous,followed by light brownish gray(5YR6/1). 4.30-4.66 meters pattern continues once more until the end of the core. LU-82-9(LAKE NIPISSING):0-.20 meter silty clay, dark greenish gray(5GY4/1), homogeneous,non-calcareous, and fairly loose compact. 0.20-3.25 meters silty clay greenish gray(5GY6/1), homogeneous, non-calcareous and more compact. LU-82-10(TALON LAKE):0-1.00 meter silty clay olive gray(5Y4/l), homogeneous,non-calcareous, loose compact,and dark band at 2-3 cm intervals found throughout section(core),but from 1.00-1.90 meters it becomes more compact.l.90-2.11 meters silty clay , homogeneous,non-calcareous,and color changes to greenish gray(5GY6/1), and even more compact. 91 LU-82~11(KIOSK LAKE):0-1.00 meter silty clay olive black(5Y2/1), homogeneous,non»calcareous,and a brownish gray(5YR4/1),band running the whole lenth of section(core) on the outer edges(5 mm width) loose compact.1.00-1.05meters gap.1.05-1.80 meters olive black(5Y2/1), and again band running down the core section for about 40 cm. But at about 1.80 meters color becomes slightly darker near the bottom of the core section (i.e.,at about 2.19 meters). LU-82-12(CEDAR LAKE):0-0.85 meter silty clay, brownish black(5YR2/1), homogeneous, non-calcareous, and very loose compact. 0.85-0.88 meter gap in core section.0.88-1.88 meters silty clay, brownish black(5YR2/1), homogeneous, non-calcareous,loose compact, and darker diagonal bands are found throughout the core section. Again from 1.88-2.06 meters gap in core section.2.06-2.75 meters silty clay, brownish black(5YR2/1),homogeneous,non-calcareous, and quite loose compact. LU-82-13(TALON LAKE);0-1.23 meters silty clay, olive gray(5Y4/l), homogeneous,non-calcareous,loose compact,darker bands are found at 2-3 cm intervals throughout the core section(l cm width). At 1.23 meters no more bands, but it becomes more compact. 1.70-2.63 meters silty clay, dark greenish gray(5GY5/1), homogeneous, non-calcareous,and more 92 compact.2•63-2.90 meters sandy portion(i.e., about 25 cm ) same color ,firm compact till 3.61 meters. 93 Lithological Discriptions of McBeth-1 site. 0 - 0.13 meter silty clay, surface oxidized to moderately dark yellowish brown (10 YR 3/3) with sand bed 1-2 cm thick, olive gray (5Y 3/2). 0.13 - 0.25 meter silty clay , li^t olive gray' (5Y 4-5/2) with darker mottlings. 0.25 - 0.265 meter sand, olive gray (5Y 3/2) and (5Y 2.5/2). 0.265 - 0.80 meter silty clay, moderate olive brown (5Y 4/2) Interbedded sand and clay, olive gray (5Y 3/2) and olive brown (5Y 4/2). 0.80 - 1.55 meters silty clay, olive brown (5Y 4/2) with dark yellowish brown (7.5^ 2/0) mott lings, fine sand layer occurs at 1.30 meters. 1.55 - 1.64 meters silty clay, olive brown (5Y 4/2) decreased mottllngs. 1.64 - 1.82 meters silty 1clay, olive gray (5Y 3/2) grading to fine sand. 1.82 - 1.84 meters interbedded clay and sand, dark olive brown (5Y 4/1) and olive gray (5Y 3/2). 1.82 - 1.995 meters once again Interbedded clay and sand, dark olive brown (5Y 4/1) and dark olive gray )5Y 3/1), clay shows mottllngs of dark yell- owish brown (7.5YR 2/0). 1.995 - 2.19 meters silty clay, dark olive gray to brown (5Y 3-4/1), with bloturbations of dark yellowish brown (7.5YR 2/0).2.19 - 2.21 meters sand bed, dark olive gray (5Y 3/2). 2.21 - 2.25 meters silty clay, dark olive brown (5Y 4/1), with dark yell with brown (7.5"® 2/0) mottllngs. 2.25 - 4.94 meters silty clay, dark olive brown (5Y 4/1) with dark yellowish brown (7.5YR 2/0) mottllngs and some olive gray (5Y 3/2) mottllngs occurs at 4.34 - 4.35 and 4.70 - 4.73 meters. 4.945 - 4.96 meters sand bed, very dark olive gray (5Y 2.5/1). 4.96 - 6.13 meters silty clay, dark olive brown (5Y 4/1) with distinct mottllngs of dark yellowish brown (7.5 YR 2/0) and some olive gray (5Y 3/2), sand bed occur at 6.12 - 6.13 meters, olive gray (5Y 3/2). 6.13 - 6.295 meters Interbedded clay and sand, dark olive brown (5Y 4/1) and olive gray (5Y 3/2). 94 6.295 - 6.79 meters silty clay, dark olive brown (5Y Vl) with sand layers. 6.79 - 6.895 meters clay, dark olive brown (5Y 4/1) interbedded mottled clay and clay with fine sands (6.895 - 7.00 meters). 7.00 - 7.99 meters silty clay , dark olive brown (5Y 4/1) with sandy silt, dark yellowish brown C7.5YR 2/0). 7.99 - 9.12 meters silty clay, dark olive brown (5Y 4/1) with some fine sand. 9.12 - 9.13 meters silty sand, dark olive brownish gray (5Y 3.5/1). 9.13 - 9.85 meters silty clay, dark olive brown (5Y 4/1) with distinct mottlings of dark yellowish brown (7.5 YR 2/0), fine sand bed occurs at 9.25 meters. 95 Lithological Discription Of McBeth-2 site. 0 - .32 meter silty clay, dark olive gray (5Y 4/1) with horozontal mottlings of darker olive gray (5Y YR 2.5/1) and dark yellowish brown (7.5 YR 2.0) irregular less coinnran mottlings. 0.32 -0.63 meter mottlings, shell fragments found at 0.52- 0.53 meter. O.63 - 0.95 meter once again horizontal mottlings. 0.95 - 2.35 meters silty clay ^dark olive brown (5Y 4/1) with bioturbation dark yellowish brown (7.5 YR 2/0) and dark olive gray (5Y 3//) mottlings.2.45 - 2.85 meters silty clay, dark olive brown (5Y 4/1) with dark yellowish brown (7.5 YR 2/0) sll^tly horizontal mottlings. 2.88 - 2.91 meters silt, dark olive brown (5 YR 4/1) and dark olive olive brownish gray (5Y 3.5/1). 2.91 - 3.06 meters sllty&clay, interbedded (5Y 3.5/1) and (5Y 4/1). 3.06 - 3.245 meters silt, dark olive gray (5Y 4/1) with dark olive brown clasts. 3.245 - 3.305 meters sand, dark olive gray (5Y 3/1) fine to coarse at bottom clayey sily, dark olive brown, with (7*5 YR 2.0) interbedded silty clay. 3.305 - 3.42 meters silty clay , very dark olive (2.5Y 2.5/0). 3-42 - 3-95 meters silt, dark brown mixed with darker mottlings. 3.95 - 4.97 meters silty clay, dark olive brown (5Y 4/1) with some faintly horizontal bioturbation, dark yellowish brown (7.5 YR 2/0) and very dark olive gray (2.5 Y 2.5/0) mottling. 4.97 - 5.11 meters silty clay, dark olive gray (5Y 3/1). APPENDIX B Compilation of grain size data 1- North Bay areas LU-82-1 (Callander Bay) LU-82-8 (Lake Niplssing) LU-82-9 (Lake Niplssing) LU’'82-3 (Lake Nosbonsing) LU-82-*7 CLake Nosbonsing) LU-82-10 (Lake Talon) LU-82-13 (Lake Talon) LU-82-I1 (Kiosk Lake) LU-82-12 (Cedcir Lake) 2- McBeth Fiord McBeth-1 McBeth-2 96 Mean grain size and sand percentages of cores. LU-'82'-l(CALLANDER BAY) DEPTH MEAN GRAIN SIZE SAND % (cm) (Phi) 5 7.66 16.80 25 7.53 19.00 45 8.87 13.80 65 9.80 4.33 85 9.00 8.03 105 10.00 0.60 125 9.17 0.80 145 9.50 1.20 165 9.50 1.40 185 9.63 2.00 205 8.90 4.00 225 9.23 2.60 245 8.30 3.32 265 9.30 0.60 285 9.40 0.80 305 8.27 2.90 325 9.00 2.00 9? 345 9.07 2.20 365 9.50 0.52 98 LU-82-3(LAKE NOSBONSING) DEPTH MEAN GRAIN SIZE SAND % (cm) (Phi) 5 8.70 2.16 25 9.17 13.49 45 9.23 12.67 65 8.67 11.26 85 9.07 12.52 105 9.03 5.76 125 9.50 6.29 145 8.97 14.00 165 9.13 12.74 185 9.30 6.11 205 9.13 11.88 225 9.23 6.56 245 8.87 11.40 265 9.00 10.00 285 8.97 6.60 305 9.13 1.20 325 8.97 13.20 345 8.63 1.40 99 365 9.37 1.20 385 9.67 0.90 405 9.30 1.25 100 LU'’82-7(LAKE NOSBONSING) MEAN GRAIN SIZE SAND % cm) (Phi) 5 9.10 0.90 25 9.33 8.65 45 9.30 1.20 65 9.20 11.60 85 9.13 10.44 105 8.97 8.75 125 9.07 15.15 145 9.13 8.10 165 9.33 2.20 185 9.23 7.66 205 9.30 1.29 225 9.43 5.91 245 9.57 0.30 265 9.67 1 .43 285 9.23 1.69 305 9.93 0.60 325 9.73 1.00 345 9.33 1.68 865 9.73 0.30 101 LU-82-8(LAKE NIPISSING) DEPTH MEAN GRAIN SIZE SAND % (cm) (Phi) 5 8.66 0.30 25 8.50 0.20 45 8.83 0.12 65 9.33 0.10 85 9.16 0.08 105 9.10 0.04 125 9.16 0.03 145 9.33 0.12 165 9.23 0.22 185 9.27 0.20 205 9.27 0.08 225 9.63 0.02 245 9.36 0.10 265 8.66 0.16 285 9.40 0.08 305 8.66 0.01 325 9.73 0.01 345 9.57 0.12 102 365 9.27 0.66 385 9.30 7.60 405 9.53 0.06 425 10.00 0.06 445 8.93 0.02 103 LU-82-9(LAKE NIPISSING) MEAN GRAIN SIZE SAND % cm) (Phi) 5 9.25 0.06 25 9.33 0.06 45 9.33 0.02 65 9.25 0.05 85 9.33 0.04 105 9.25 0.06 125 9.43 0.02 145 9.33 0.01 165 9.17 0.02 185 9.25 0.03 205 9.08 0.08 225 9.25 0.00 245 9.33 0.13 265 9.16 0.05 285 9.25 0.02 305 9.25 0.00 325 9.33 0.00 104 LU-82-10(TALON LAKE) DEPTH MEAN GRAIN SIZE SAND % (cm) (Phi) 5 9.00 0.79 25 9.16 0.51 45 9.33 1.14 65 9.00 2.39 85 9.00 2.63 105 9.16 1.54 125 9.33 0.00 145 9.33 0.61 165 9.16 0.49 185 9.16 0.56 205 9.08 0.59 105 LU-82-11(KIOSK LAKE) DEPTH MEAN GRAIN SIZE SAND % (cm) (Phi) 5 8.95 1.14 25 9.08 1.33 45 9.00 0.99 65 9.00 0.85 85 9.16 0.01 105 9.33 0.75 125 9.16 0.73 145 9.16 1.53 165 9.00 1.16 185 8.83 0.85 205 8.83 1.53 106 LU-82-12(CEDAR LAKE) DEPTH MEAN GRAIN SIZE SAND% (cm) (Phi) 5 9.08 1.80 25 8.67 1.51 45 8.67 2.56 65 8.67 1.83 85 8.67 0.42 105 8.92 7.83 125 8.58 3.55 145 8.58 2.75 165 8.67 2.93 185 8.58 4.15 107 LU-82-13(TALON LAKE) DEPTH MEAN GRAIN SIZE SAND% (cm) (Phi) 5 9.00 0.66 25 9.33 0.65 45 9.67 0.57 65 9.33 0.34 85 9.67 1.44 105 9.92 0.28 125 9.50 0.13 145 9.50 0.36 165 9.83 0.29 185 8.92 0.55 205 8.67 1.35 225 8.67 5.03 245 8.33 17.15 265 8.42 74.35 285 9.17 49.56 305 8.83 32.14 325 9.08 26.60 345 9.17 56.41 3365 9.J7 38.8] GRAIN-SIZE ANALYSIS OF LAKE TALON*(NORTH BAY) AREA, (GRAPHIC METHOD, AFTER FOLK & WARD,1957) DEPTH MEAN INCLUSIVE GRAPHIC STANDARD INCLUSIVE GRAPHIC SKEWNESS KURTOSIS (K g) (cm) (Mz) DF7IATION («I ) (SK j) 265 3.32 0.A4 Well Sorted -0.16 Coarse skewed 1.06 Mesokurtlc 275 3.26 0.52 Moderately Sorted +0.07 Near Symmetrical 0.94 285 3.36 0.60 -0.26 Coarse skewed 1.09 305 3.53 0.50 Well Sorted -0.38 Strongly coarse 1.09 Skewed 325 3.57 0.48 -0.37 1.54 Leptokurtic 345 3.49 0.40 -0.24 Coarse skewed 1.23 365 3.38 0.52 Moderately Sorted -0.34 Strongly coarse 0.93 Mesokurtlc Skewed * LU-82-13(LAKE TALON) 108 109 99-99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2-1 0:5 0.2 0.1 0.05 0.01 0.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60- 70 80 90 95 98 99 99.8 99.9 99.99 110 99-99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0 1 0.05 .111 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0 5.0 Phi Scale 99.99 99^9 99,8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0,5 0.2 0.1 0.05 0.01 0.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 112 Phi Scale 99,99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 0.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 113 Phi Scal< 99,99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 CS.OI 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 114 ^9-99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 115 LU-82-13 (Lake Talon Depth: 365 ctr 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 OO.Ol 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 116 McB-1(McBETH,FIORD) DEPTH MEAN GRAIN SIZE SANDf (cm) (Phi) 0 25 9-00 16.06 50 9.00 2.20 75 9.33 2.59 100 9.33 3.40 125 9.33 1.36 150 9.33 2.35 175 9.50 0.57 200 9.33 4.42 225 9.58 2.68 250 9.58 8.48 275 9.58 1.78 300 9.58 1.96 325 9.50 2.91 350 9.67 3.07 375 9.67 0.81 400 8.92 1.06 425 9.67 0.38 11? o 450 9.83 1.66 475 9.67 0.62 500 9.50 5.26 525 9.83 0.34 550 9.83 1.32 575 9.33 0.51 600 9.33 1.75 625 9.25 0.81 650 9.08 0.80 675 9.00 0.51 700 9.50 0.18 725 9.33 0.00 750 9.42 1.64 775 9.58 0.32 800 9.58 1.37 825 9.42 0.16 850 9.50 0.97 875 9.42 0.83 900 9.67 0.22 925 7.50 3.79 950 9.17 2.06 975 9.17 0.28 GRAIN-SIZE ANALYSES OF McBETH-1 FIORD, BAFFIN ISLAND (GRAPHIC METHOD, AFTER FOLK-.& WARD,l93J) DEPTH MEAN INCLUSIVE GRAPHIC STANDARD INCLUSIVE GRAPHIC SKEWNESS KURTOSIS ( K g) (cm) ( Mz ) DEVIATION (fl ) (SKj. ) 0 3.37 0.78 Moderately Sorted -0.34 Strongly coarse skewed 1.62 Leptokurtic 26 3.10 0.80 -0.15 Coarse skewed 0.81 Platykurtic 38 2.72 0.89 -0.24 0.79 89 3.29 0.61 +0.07 Near-Symmetrical 1.06 Mesokurtic 201 3.00 0.53 -0.39 Strongly coarse skewed 0.87 Platykurtic 222 3.19 0.60 +0.17 Coarse skewed 0.93 Mesokurtic 330 2.63 0.57 +0.16 1.87 Leptokurtic 505 3.11 0.61 +0.26 1.03 Mesokurtic 751 2.95 0.68 +0.27 0.83 Platykurtic 931 3.22 0,71 +0.03 Near-Symmetrical 0.98 Mesokurtic 118 119 0.5 1.0 1.5 2.0 2.5 3.0 3v5 4.0 5.0 Phi Scale 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 0.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 120 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0 5.0 Phi Scale 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 0.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 121 MCBETa-1 DEPTH:38 cm 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 I 0.5 0.2 0.1 0.05 0.01 00.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99,99 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 122 Phi Scale 123 0.1 1.0 1.5 2.0 2.5 3.0 3.5 4.© 5.0 Phi Scale 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 124 Phi Seal. 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 . 2 1 0.5 0.2 0.1 0.05 0.01 ^.01 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 99,99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 o Phi Seal 126 Phi Seal 99.99 99.9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 12? 99.99 99,9 99.8 99 98 95 90 80 70 60 50 40 30 20 10 5 2 1 0.5 0.2 0.1 0.05 0.01 UO.Ol 0.05 0.1 0.2 0.5 1 2 5 10 20 30 40 50 60 70 80 90 95 98 99 99.8 99.9 99.99 McBETH-1 PEP Phi Scale 129 McB-2(McBETH,FIORD) DEPTH MEAN GRAIN SIZE SAND% (cm) (Phi) 0 9.08 6.10 25 9.00 3.57 50 9.08 5.93 75 9.67 6.10 100 9.50 0.89 125 9.50 2.99 150 9.50 8.52 175 9.58 1.37 200 9.33 2.91 225 9.58 4.10 250 9.42 0.81 275 9.50 1.01 300 9.58 0.51 325 9.58 3.44 350 9.58 2.57 375 9.75 2.38 400 9.50 1.13 425 9.50 2.27 130 450 9.58 1.82 475 9.67 4.12 500 9.50 3.64 APPENDIX C Compilation of organic and carbonate carbons percentages 1- North Bay areas LU-82-1 (Callander Bay) LU-82-8 (Lake Niplssing) LU—82-9 (I,ake Niplssing) LU’-'82~3 (Lake Nosbonslng) LU-82-7 (Lake. Nosbonslng) LU-82-10 (Lake Talon) LU-82-13 (Lake Talon) LU-82-11 (Kiosk Lake) LU-82-12 (Cedar Lake) 2- McBeth .Fiord McBeth-1 McBetli-2 131 LU-82-1 (CALLANDER BAY) EPTH TOTAL ORG. GARB. (cm) C.% C.% C.% 0 4.11 4.21 0.0 5 3.45 3.45 0.0 10 3.19 3.09 0.1 50 2.23 2.24 0.0 100 2.02 1.96 0.06 150 1.89 1.88 0.01 200 1.84 1.99 0.0 250 1.52 1.49 0.03 305 1.51 1.36 0.15 132 LU-82-3 (LAKE NOSBONSING) DEPTH TOTAL ORG. CARB. (cm) C.% C.% C.% 0 6.51 5.84 0.67 5 6.04 5.50 0.54 10 6.35 5.79 0.56 50 8.29 8.06 0.23 100 8.82 8.48 0.34 150 8.64 8.21 0.43 200 10.69 9.47 1.22 250 10.91 11.16 0.00 305 5.05 4.85 0.20 405 3.02 2.62 0.40 133 LU~82-'7 (LAKE NOSBONSING) DEPTH TOTAL ORG . GARB. (cm) C.% C.% C.% 0 5.93 5.46 0.47 5 8.29 8.03 0.26 10 8.40 7.48 0.92 50 8.76 8.02 0.74 100 9.45 8.71 0.74 150 7.79 6.72 1.07 200 8.49 7.45 1.04 250 8.65 7.69 0.96 305 3.13 2.72 0.41 365 2.79 3.00 0.00 13-4- LU-82-8 (LAKE NIPISSING) DEPTH TOTAL ORG . GARB. (cm) C.% C. % C.% 0 2.77 2.46 0.31 5 1.71 1.44 0.27 10 1.00 0.94 0.06 50 1.00 1.02 0.00 100 0.93 0.83 0.10 200 0.81 0.75 0.06 250 0.75 0.77 0.00 300 0.64 0.73 0.00 350 0.71 0.70 0.01 410 0.72 0.67 0.05 450 1.23 0.18 1.08 135 LU-82-9(LAKE NIPISSING) DEPTH TOTAL ORG. GARB. (cm) C.% C.% C.% 0 2.11 1.74 0.37 5 1.90 1.59 0.49 10 2.85 1.24 1.61 50 1.24 1.18 0.06 100 1.22 1.17 0.05 200 1.13 1.14 0.00 250 1.00 1.08 0.00 300 0.87 0.87 0.00 136 LU-82"10(TALON LAKE) DEPTH TOTAL ORG. GARB. (cm) C.% C.% C.% 0 7.27 7.14 0.13 5 6.56 5.26 1.30 10 7.58 6.35 1.23 50 5.91 4.47 1.44 100 4.88 4.16 0.72 150 6.16 6.30 -0.14 205 2.51 3.47 -0.96 137 LU-82-13(TALON LAKE) TOTAL ORG. GARB. (cm) C. % C.% C. % 0 5.46 4.54 0.92 5 6.62 4.98 1.64 10 7.68 5.91 1.77 50 7.22 4.44 1.78 100 4.92 3.80 1.12 200 4.01 3.50 0.51 300 1.38 1.50 0.00 350 1.37 1.06 0.31 138 LU-82~11(KIOSK LAKE) DEPTH TOTAL ORG, GARB, (cm) C. % C. % C. % 0 10.51 9.25 1.26 5 10.34 8.29 2.05 10 10.66 8.79 1.87 50 11.60 8.63 2.97 100 8.99 7.93 1.06 150 8.34 7.64 0.70 200 8.31 6.82 1.49 139 LU-82-12(CEDAR LAKE) TOTAL ORG. CARD. (cm) C.% C.% C.% 0 15.19 12.33 2 .86 5 14.69 13.22 1.47 10 12.33 11.61 0.72 50 12.29 10.50 1.79 100 12.37 10.51 1.86 150 11.57 9.68 1.89 200 11.64 10.16 1.48 250 12.50 10.05 2.45 14 0 McB-1{McBETH,FIORD) DEPTH TOTAL ORG. CARS. (cm) C.% C.% C.% 50 0.63 0.62 0.02 100 0.87 0.78 0.09 150 0.92 0.64 0.28 200 0.90 0.72 0.18 250 0.81 0.49 0.32 300 0.39 0.18 0,19 350 0.66 0.62 0.04 400 0.69 0.49 0.20 450 0.72 0.55 0.17 500 0.49 0.45 0.04 550 0.51 0.57 0.00 600 0.23 0.51 0.00 650 0.34 0.30 0.04 700 0.40 0.38 0.02 750 0.39 0.37 0.02 800 0.39 0.36 0.03 850 0.48 0.41 0.07 900 0.40 0.35 0.05 950 0.32 0.3] 0.01 1^1 McB~2(McBETH,FIORD) DEPTH TOTAL ORG . CARB. (cm) C.% C.% C.% 0 1.50 1.36 0.14 50 1.37 1.19 0.18 100 1.18 1.05 0.13 150 0.91 0.73 0.18 200 0.85 0.62 0.20 250 0.90 0.61 0.29 300 0.80 0.60 0.20 350 0.69 0.51 0.18 400 0.63 0.55 0.08 450 0.81 0.68 0.13 500 0.63 0.66 0.00 APPENDIX D Compilation of paleomagnetic records data 1- North Bay areas LU-82-1 (Callander Bay) j LU-82-8 (Lake Nipisaing) LU-82-9 (Lake Nlpissslng) LU-82-3 (Lake Hosbonslng) LU-82-7 (Lake Nosbonsing) LU-32-10 (Lake Talon) LU-82-13 (Lake Talon) LU-82-11 (Kiosk Lake) LU-82-12 (Cedar Lake) 2- McBeth Fiord McBeth-1 MeBeth-2 142 LU~82-1(CALLANDER BAY) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (cm) (relative) (uG) 1 299.8 53.2 4.08 4 329.4 50.8 3.38 7 306.7 49.3 3.79 10 278.5 51.8 7.83 13 290.3 54.0 11.49 16 292.8 52.7 9.42 19 282.0 50.8 10.80 22 281.9 45.7 14.21 25 279.2 48.0 13.56 28 275.6 49.1 14.88 31 281.7 48.6 17.46 34 275.1 46.9 12.75 37 277.0 46.4 12.79 40 273.4 48.6 17.28 43 272.9 47.6 14.74 46 270.3 51.6 25.72 49 264.6 49.1 22.19 52 260.9 44.0 21.57 143 55 262.2 49.3 23.66 58 262.3 48.6 26.20 61 252.7 50.2 25.66 64 263.9 52.0 20.48 67 249.5 47.3 28.74 70 253.3 45.9 29.59 73 250.6 47.8 33.64 76 250.7 44.4 28.34 79 252.6 43.3 27.65 82 262.2 42.1 19.10 85 262.3 39.0 26.94 88 267.3 41.2 20.87 91 265.0 36.5 26.29 94 263.9 36.4 21.46 97 266.4 34.8 23.21 100 272.6 37.4 20.48 103 265.9 29.4 22.57 106 274.9 33.4 16.66 109 279.1 32.5 16.64 112 277.6 33.8 22.16 115 273.7 30.1 18.89 118 273.9 23.9 20.42 121 275.5 22.5 18.07 124 271.4 29.0 22.12 12 7 280.0 33.0 13.88 130 281.2 32.4 21.57 133 282.2 30.1 20.65 136 276.8 32.5 20.93 139 280.0 34.4 17.56 142 279.0 36.3 21.02 145 278.7 31.1 19.79 148 274.8 35.1 18.89 151 277.7 41.5 20.33 154 272.0 40.5 22.21 157 273.8 38.0 17.30 160 276.9 32.2 18.45 163 276.4 39.1 17.59 166 274.2 39.7 22.26 169 278.0 37.5 18.63 172 272.6 37.2 19.52 175 275.2 36.9 15.51 178 273.8 38.7 19.62 181 271-7 36.2 19.82 184 274.1 39.2 18.98 187 271.9 40.0 20.21 190 272.3 37.6 15.13 193 269.4 41.5 18.26 196 281.7 45.5 16.53 145 199 266.6 36.6 14.54 202 274.1 32.3 19.04 205 271.2 36.4 11.21 208 269.6 35.6 14.01 211 269.0 38.2 13.81 214 269.5 35.8 15.07 217 265.1 38.9 17.61 220 267.9 33.7 13.13 223 266.7 44.0 22.84 226 269.9 44.0 24.46 229 268.8 42.5 20.33 232 254.0 35.3 20.57 235 262.7 42.0 35.82 238 260.4 47.6 28.36 241 261.0 44.7 25.21 244 261.0 40.3 23.68 247 270.5 41.8 16.60 250 261.5 33.3 23.45 253 261 .4 35.8 20.93 256 268.0 35.6 31.66 259 271.0 39.3 36.36 262 268.0 40.1 32.60 265 268.6 44.8 31.12 268 271.1 43.3 37.96 1^6 271 267.0 34.6 29.87 274 271.6 29.8 36.99 277 270.1 30.1 26.42 280 265.9 32.2 26.94 283 276.4 27.5 28.36 286 279.3 23.9 32.96 289 274.7 28.6 28.77 292 278.1 27.4 29.08 295 276.6 26.3 28.84 298 279.8 20.3 23.76 301 280.8 24.6 27.09 304 283.8 26.5 27.95 307 284.6 21.8 27.19 310 284.2 19.3 20.72 313 284.0 14.3 22.23 316 283.2 17.5 20.62 319 283.6 15.0 24.15 322 284.3 14.6 25.02 325 278.9 14.7 20.43 328 285.3 22.4 19.10 331 279.5 10.4 19.21 334 274.8 19.3 13.81 337 282.2 18.3 16.90 340 283.3 14.2 16.61 147 343 282.9 18.6 21.09 346 280.5 20.7 18.57 349 126.2 18.1 20.43 352 114.4 13.3 20.45 355 120.2 17.5 18.68 358 107.9 12.4 25.39 361 110.9 10.1 16.22 364 109.6 9.0 15.42 367 115.4 6.6 21.64 370 115.7 10.5 21.66 148 LU-82-3(LAKE NOSBONSING) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (CM) (RELATIVE) (uG) 1 344.2 0.2 1.75 4 345.4 32.5 4.00 7 349.5 24.0 3.43 10 345.5 17.1 1.26 13 351.7 21.2 2 .46 16 343.4 10.8 1.13 19 350.6 9.9 1.92 22 349.1 6.5 1.31 25 352.8 2,4 1.53 28 347.5 17.3 0.93 31 353.4 8.6 0.60 34 354.2 -7.5 1.01 37 337.3 11.5 1.01 40 346.1 6.8 0.53 43 0.3 19.9 1.12 46 351.0 31.9 1.41 49 348.8 25.3 0.84 52 351.0 23.4 0.67 1^9 55 340.6 23.2 0.66 58 334.2 15.5 0.73 61 339.0 34.8 0.54 64 351.4 18.2 0.56 67 350.0 17.7 0.65 70 341.2 29.2 0.75 73 321.1 34.1 0.51 76 339.6 32.4 0.39 79 334.4 34.7 0.52 82 346.0 28.1 0.25 85 336.2 39.3 0.58 88 350.0 16.0 0.54 91 332.0 33.3 0.70 94 345.3 23.2 0.36 97 332.1 14.6 0.3 2 100 331.0 11.5 0.35 103^ 337.7 20.8 0.34 106 331.4 34.2 0.32 109 329.9 20.6 0.41 112 355.0 22.7 0.40 115 355.2 -2.9 0.32 118 341.3 22.0 0.41 121 306.3 12.5 0.59 124 338.7 45.5 0.44 15 Ov 127 355.8 32.8 0.43 130 340.6 16.5 0.30 133 347.8 17.6 0.21 136 356.8 12.5 0.29 139 349.2 37.0 0.32 142 331.8 39.2 0.32 145 2.3 24.7 0.29 148 348.4 26.1 0.26 151 350.1 34.6 0.26;: 154 1.8 19.0 0.52 157 349.9 53.2 0.25 160 358.9 35.6 0.37 163 326.3 57.5 0.21 166 12.3 12.3 0.16 169 352.1 33.0 0.18 172 329.4 40.1 0.35 175 357.6 10.2 0.39 178 359.2 31.1 0.42 181 346.0 15.8 0.41 184 357.7 29.7 0.30 187 345.2 47.2 0.27 190 351.8 31.7 0.43 193 7.9 41.2 0.31 196 357.3 64.5 0.30 151 ms9 2smi.2^. 3 61.3,1 01.29.' W^J7 ze..ai 0)..33® 6).£R 3.T.XL ®..2& 3J®^.33 116.32 01.62? 25U11. T.2>. 301.4. 0'.4,4 2;iAi 3S6 .A- 37.2' 01.64. 2?n7/ 8.x 8. .11 0.49' 220J 115.1. 33.4. 0).4il 2233 44,. 6. 44.6. 0.-5 5 226.. 1’.3. 33.2 0.301 22a> 353)..T 44U.0) 0 .2 7 Z322 7/.21 35..9> 0.42? 23;5^ 112. J7 3:6 ..9t 0.22? 2HS3 3E46.22 40 .'.2; 01.431 23im IIT/.X 40'.6 &..22> 2#m 3B3.J7 42.x 0?i.3jli 2»F7 35m3) 18.41 01.3X 250J 20J.6.. 46.01 01.3395 253^ 233. ,2i 3 3,.3. 0?..34i 2SE& T.m 2 7.31 02.. 315 2293 lS4i.55 25.11 01.331 2622 3S2.,H 29.2’ 01.. 4] 26ffi 2i.m 14i.0) 01.463 260} a43:,..9.' 56.2' 0j..3®} 152 271 5.1 8.1 0.60 274 351.0 38.6 0.43 277 342.4 33.7 0.40 280 34.8 36.2 0.37 283 354.8 32.4 0.35 286 353.4 33.0 0.16 289 7.8 24.2 0.39 292 350.2 38.0 0.20 295 15.5 36.8 0.25 298 352.3 31.9 0.37 301 21.4 29.5 0.33 304 12.8 25.0 0.72 307 14.5 39.5 0.57 310 27.0 52.4 0.56 313 5.2 35.5 0.57 316 14.7 40.9 0.55 319 3.9 37.1 0.50 322 9.8 46.2 0.94 325 1.3 36.8 0.60 328 6.2 36.7 0.42 331 10.0 49.5 0.80 334 347.7 42.8 0.99 337 9.5 54.5 0.99 340 5.0 43.6 0.50 153 343 5.5 35.2 0.87 346 14.2 14.2 0.62 349 349.2 39.0 1.42 352 356.2 45.8 1.50 355 9.1 40.4 1.23 358 13.4 41.5 1.38 361 14.6 53.7 1.53 364 25.2 55.2 2.45 367 20.3 52.3 4.08 370 12.9 57.7 4.51 373 11.5 63.3 4.42 376 14.9 59.0 3.34 379 4.9 54.9 1.83 382 16.5 58.0 1.50 385 13.5 55.2 2.28 388 18.1 54.7 2.33 391 7.6 56 3 2.52 394 23.1 53.7 2.15 397 19.3 52.2 2.61 400 12.5 53.1 4.04 403 27.9 59.3 3.77 406 14.7 58.5 4.13 409 29.8 59.0 4.60 412 27.2 58.4 5.29 15^ 415 23.0 58.5 5.98 418 20.6' 57.5 6.48 421 36.6 61.8 4.50 424 21.6 54.0 4.91 427 30.1 54.5 4.32 430 27.2 50.1 4.45 433 33.8 40.7 4.54 436 29.1 62.1 2.25 155 LU-82'-7(LAKE NOSBONSING) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (cm) (relative) (uG) 1 48.2 27.2 3.30 4 13.5 22.0 1.55 7 52.2 24.2 1.32 10 60.9 44.1 1 .47 13 59.3 70.0 0.67 16 35.9 40.8 0.94 19 55.1 46.5 1.55 22 42.2 39.1 1.61 25 52.5 40.8 1.51 28 53.3 32.4 0.86 31 50.0 24.5 0.72 34 66.0 36.1 0.71 37 66.6 33.5 0.72 40 60.0 49.5 0.67 43 59.5 51.8 0.78 46 69.0 52.5 0.85 49 57.0 47.7 0.75 52 49.1 42.0 0.70 156 55 53 .4 36.6 0.54 58 51.0 40.7 0.71 61 67.9 55.5 0.37 64 78.7 58.4 0.57 67 90.0 54.8 0.84 70 62.2 60.7 0.70 73 48.7 44.0 0.73 76 52.8 40.2 1.16 79 59.5 49.1 0.64 82 74.7 52.3 0.39 85 76.4 45.0 0.25 88 114.2 63.5 0.26 91 39.8 57.3 0.46 94 90.0 56.3 0.19 97 100.3 57.2 0.33 100 82.2 53.0 0.39 103 70.8 55.6 0.46 106 91.5 59.6 0.39 109 79.0 58.8 0.43 112 109.4 43.3 0.29 115 56.3 53.9 0.29 118 79.0 60.6 0.45 121 60.6 44.5 0.33 124 82.2 47.4 0.40 157 127 67.9 48.5 0.28 130 81.4 47.9 0.26 133 333.4 85.0 0.25 136 72.9 59.7 0.57 139 81.7 36.6 0.32 142 50.0 70.1 0.51 145 53.1 56.0 0.25 148 66.0 59.2 0.20 151 315.0 76.4 0.22 154 57.1 68.3 0.29 157 108.4 58.1 0.38 160 50.8 56.5 0.47 163 95.3 47.4 0.34 166 66.3 11.4 0.29 169 87.3 31.1 0.27 172 96.5 35.9 0.29 175 117.6 52.2 0.43 178 71.9 45.2 0.41 181 45.9 53.0 0.40 184 52.0 49.2 0.33 187 43.5 45.7 0.41 190 54.5 55.1 0.24 193 39.8 56.9 0.15 196 72.9 42.6 0.19 158 199 36.9 63.4 0.30 202 32.6 59.3 0.31 205 107.9 47.1 0.25 208 133.3 37.5 0.49 211 62.5 52.3 0.47 214 71.9 42 .4 0.37 217 57.4 59.7 0.45 220 84.5 62.2 0.35 223 105.1 64.7 0.33 226 92.5 63.9 0.28 229 105.4 68.1 0.43 232 130.6 59.3 0.38 235 70.0 62.7 0.40 238 17.8 38.3 0.38 241 353.3 56.6 0.49 244 24.9 42.9 0.33 247 30.3 29.9 0.25 250 62.6 23-2 0.36 253 74.9 63.1 0.32 256 25.6 56-6 0.27 259 50.4 40.0 0.41 262 55.8 38.4 0.21 265 15.7 62.2 0.38 268 50.6 32.4 0.32 159 271 348.7 80.2 0.32 274 187.1 75.4 0.17 277 31.2 40.5 0.27 280 90.0 24.4 0.32 283 148.0 66.8 0.13 286 68.2 42.9 0.47 289 64.9 57.7 0.52 292 101.2 44.2 0.76 295 93.2 45.5 0.82 298 84.4 53.6 0.65 301 94.3 57.1 1.05 304 100.4 54.8 1.12 307 133.5 51.6 1.34 310 152.3 60.8 1.89 313 120.4 45.9 2.91 316 135.0 67.0 2.96 319 113 .0 59.3 3.63 322 105.9 72.4 3.02 325 120.0 69.1 3.78 328 124.1 66.5 5.09 331 124.6 64.3 4.76 334 130.7 58.5 2.37 337 117.5 51.3 2.76 340 97.5 49.4 1.07 160 343 98.5 63.3 346 80.7 55.4 1.86 349 88.6 64.8 2.60 352 97.1 71.7 3.57 355 110.9 72.4 3.26 358 116.8 69.9 7.94 361 109.5 66.2 7.97 364 117.2 65.6 7.50 367 108.8 64.1 7.25 370 128.8 64.6 6.47 I6l LU-82'-8(LAKE NIPISSING) DECLINATION INCLINATION MAGNETIC INTENSITY CM) (relative) (uG) 1 276.6 51.3 13.99 4 282.9 55.4 24.32 7 287.1 55.0 42.75 10 301.3 74.8 52.32 13 299.7 68.3 52.27 16 284.4 77.5 44.64 19 293.1 71.3 53.65 22 303.1 67.7 40.81 25 265.2 63.9 40.17 28 267.6 66.9 65.51 31 268.5 71.5 55.52 34 270.0 66.7 43.47 37 260.1 68.5 52.37 40 259.1 64.6 55.24 43 269.3 66.4 59.42 46 260.6 62.3 51.51 49 248.5 66.7 67 .03 52 234.6 72.5 53.86 162 55 235.1 60.4 43.86 58 241.3 64.3 53.76 61 238.1 59.8 50.47 64 233.9 61.4 55.79 67 253.5 59.8 63.42 70 257.9 58.4 54.30 73 249.3 60.0 52.64 76 256.6 55.2 55.06 79 258.9 54.2 51.61 82 268.6 52.5 53.94 85 273.3 56.7 51.95 88 275.5 59.8 52.11 91 268.2 62.0 38.27 94 269.0 57.8 49.62 97 264.0 57.5 55.09 100 254.4 58.4 52.07 103 248.8 49.7 39.18 106 249.6 62.6 50.45 109 247.1 62.9 49.53 112 250.1 63.3 51.10 115 250.6 64.6 55.37 118 242.5 59.0 38.24 121 240.7 64.3 44.78 124 242.3 58.5 51.13 163 127 238.4 68.7 51.95 130 254.4 69.3 64.89 133 241.4 68.0 55.87 136 255.3 67.6 69.73 139 247.7 65.1 44.22 142 249.2 68.6 50.22 145 261.4 73.9 70.92 148 249.2 72 .8 72.08 151 2 74.6 69.0 31.96 154 256.7 72.1 60.19. 157 253.5 65.5 71.95 160 258.2 67.8 68.08 163 270.1 70.2 64.93 166 254.8 64.9 71.15 169 256.9 60.9 71.58 172 275.4 55.3 70.68 175 275.8 51.2 70.62 178 273.9 52.0 80.73 181 277.4 47.7 55.11 184 268.8 53.4 66.75 187 263.1 47.6 56.97 190 259.3 44.8 59.95 193 268.6 57.5 56.02 196 271.2 55.9 54.69 164 199 263.7 52.7 48.07 202 262.4 62.2 58.01 205 263.0 66.1 62.43 208 259.7 58.4 52.91 211 279.2 57.3 58.77 214 265.3 74.3 57.05 217 253.4 61.6 60.14 220 264.1 56.8 54.04 223 264.0 55.8 66 - 94 226 262.1 55.7 82.88 229 260.1 58.0 69.14 232 264.6 60.0 73.98 235 265.2 61.9 76.60 238 266.7 55.0 76.53 241 259.7 56.4 74.70 244 260.5 65.8 88.85 247 258.9 62.4 85.12 250 259.4 64.8 105.48 253 258.6 63.9 95.95 256 255.6 62.4 79.18 259 231.8 56.5 56.14 262 250.0 62.8 88.26 265 246.2 62.8 98.49 268 243.4 65.1 82.68 « 165 271 231.5 63.8 93.08 274 249.4 68.8 103.83 277 256.1 67.9 121.62 280 251.6 66.2 115.55 283 229.7 76.6 94.38 286 259.9 64.3 91.77 289 257.5 72 .4 92.67 292 247.3 67.8 102.67 295 263.1 65.7 114.03 298 258.1 64.2 112.82 301 273.9 64.3 112.53 304 257.8 64.6 108.57 307 255.7 68.8 103.35 310 261.6 68.2 111.16 313 243.6 72.6 115.71 316 248.4 70.1 112.79 319 242.4 60.0 106.94 322 236.6 55.7 103.33 325 264.2 71.5 100.16 328 247.5 64.4 93.75 331 243.0 68.1 134.42 334 254.6 67.9 125.11 337 246.9 76.5 114.46 340 252.5 67.2 112.89 166 343 250.5 65.7 114.54 346 253.6 59.6 147-20 349 249.2 54.6 93.57 352 241.5 70.7 109.60 355 241.3 64.9 95.01 358 257.5 63.4 101.98 361 262.2 63.8 107.85 364 263.2 61.2 106.67 367 253.0 67.3 93.52 370 254.6 73.1 81.02 373 228.0 63.7 62.02 376 266.2 65.1 26.74 379 287.0 63.6 24.96 382 285.4 67.3 34.42 385 271.4 64.9 14.29 388 285.2 64.1 12.64 391 267.6 68.1 28.30 394 270.7 65.2 41.96 397 276.0 56.6 23.13 400 264.6 55.8 36.02 403 277.7 40.6 201.07 406 271.7 39.6 94.18 409 267.1 20.5 100.51 412 264.6 31.4 78.04 16? 415 280.3 39.3 149.01 418 274.2 25.0 172.47 421 262.7 26.2 169.18 424 262.9 18.8 89.34 427 270.8 31.7 124.60 430 277.7 49.4 230.14 433 271.7 27.9 121.13 436 268.2 31.1 127.82 439 260.4 20.5 96.25 442 269.7 31.3 178.50 445 276.7 43.8 333.06 448 266.2 38.6 335.04 451 264.0 26.9 131.19 454 270.4 36.4 190.51 ' l- 457 264.0 29.1 215.11 460 261.7 29.7 218.90 463 256.7 13.1 96.48 466 260.3 23.3 129.23 168 LU-82-9(LAKE NIPISSING) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (cm) (relative) (uG) 1 306.7 43.6 27.76 4 327.3 43.2 20.21 7 315.4 34.6 14.28 10 308.2 44.5 17.76 13 306.2 48.2 23.29 16 315.8 45.5 16.54 19 299.1 55.4 28.30 22 299.5 49.3 34.03 25 305.4 57.6 38.44 28 308.2 57.9 32.53 31 307.0 52.9 30.98 34 303.1 54.5 35.68 37 307.4 51.2 31.88 40 299.2 55.8 26.12 43 309.1 56.6 28.77 46 306.1 58.4 29.35 49 311.5 50.9 22.72 52 293.7 59.1 41.16 55 297.3 52.9 48.44 58 292.7 56.3 39.42 61 299.2 57.0 39.83 64 305.3 60.7 37.79 169 67 305.5 56.8 29.71 70 297.6 56.7 34.40 73 281.6 53.7 29.44 76 296.9 53.2 35.98 79 302.7 61.8 35.16 82 300.7 57.9 41.56 85 288.8 54.3 30.69 88 296.3 57.4 39.40 91 301.5 53.9 24.84 94 300.7 55.7 21.66 97 318.6 58.6 29.18 100 296.8 52.6 35,91 103 312.5 48.9 34.18 106 299.1 50.8 51,48 109 296.2 50.4 48.39 112 292.9 52.5 37.77 115 300.1 52.9 41.47 118 310.3 56.8 33.45 121 293.2 54.0 39.83 124 300.6 49.0 41.28 127 299.2 51.2 33.17 130 297.0 48.7 47,65 133 293.7 51.3 53.19 136 302.7 49.8 49.16 1?0 139 299.3 49.7 54.21 142 298.4 49.8 56.22 145 309.2 51.6 47.22 148 300.9 55.7 62.00 151 296.0 55.4 47.66 154 293.3 54.5 60.93 157 302.2 54.5 47.81 160 296.9 50.7 58.20 163 290.6 49.9 57.47 166 289.5 49.3 66.11 169 282.3 50.2 63.76 172 291.4 48.5 62.50 175 275.0 50.0 54.77 178 288.4 46.5 54.78 181 287.9 49.4 52.94 184 283.3 50.5 54.70 187 288.2 49.8 54.97 190 289.7 47.9 61.77 193 287.0 49.5 54.12 196 287.7 48.7 61.69 199 289.0 50.8 63.93 202 287.7 55.7 56.57 205 294.1 54.1 49.12 208 286.0 49.5 56.57 1?1 211 283.2 50.4 52.25 214 286.3 48.8 57.61 217 269.8 51.3 55.13 220 269.1 46.8 45.96 223 273.5 45.7 47.24 226 275-1 45.5 56.54 229 277.7 48.7 45.67 232 284.0 51.4 40.90 235 284.2 49.1 41.89 238 280.8 44.3 51.73 241 274.5 47.6 47.75 244 275.3 48.0 34.53 247 284.3 41.3 37.13 250 281.0 48.1 36.01 253 291.4 44.0 48.54 256 289.7 41.4 45.87 259 280.6 43.4 42.33 262 282.4 44.0 30.71 265 280.5 44.5 41.91 268 279.5 43.2 53.54 271 283.6 41.5 37.31 274 281.3 41.6 47,85 277 276.4 39.9 43.87 280 277.5 42.3 38.40 172 283 282.0 41.0 43.66 286 267.3 39.7 41.56 289 264.8 38.7 37.19 292 265.0 39.0 37.66 295 282.5 44.5 42.44 298 277.5 42.2 53.15 301 266.6 41.8 43.83 304 265.6 49.5 33.95 307 286.8 35.7 37.52 310 288.8 38.2 33.19 313 292.9 38.2 34.33 316 288.2 22.2 28.61 319 301.3 21.7 35.71 322 289.9 37.0 46.97 325 293.2 45.8 55.25 328 296.4 45.7 48.48 331 300.9 50.4 35.94 1?3 LU-82-10(TAI^ON LAKE) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (cm) (relative) (uG) 1 68.4 42.9 7.61 4 43.3 30.9 5.89 7 43.2 47.6 12.32 10 42.7 49.4 14.70 13 39.6 44.9 16.82 16 48.8 46.9 18.66 19 48.7 47.0 19.89 22 55.5 48.7 25.45 25 42.4 44.4 20.96 28 62.0 47.7 20.09 31 60.2 41.8 24.18 34 70.2 44.8 30.43 37 82-1 44.6 28.36 40 54.9 33.2 20.92 43 52.6 36.1 21.30 46 58.3 40.4 25.59 49 59.9 41.7 24.82 52 64.2 46.1 24.48 1?4 55 67.8 47.0 24.02 58 73.6 52.6 27.15 61 80.8 49.0 24.36 64 67.5 49.5 18.14 67 55.3 47.8 20.99 70 82.3 55.6 29.12 73 72.2 52.3 32.07 76 59.7 49.5 24.12 79 75.9 51.0 25.14 82 69-8 49-7 20.81 85 77.2 47.4 33.63 88 72.9 48.4 16.21 91 75.6 44.1 30.02 94 71.7 47.7 25.26 97 50.8 35.0 17.30 100 67.9 40.6 19.53 103 52.6 38.2 30.21 106 52.2 46.1 43.62 109 56.5 50.2 38.44 112 59.9 54.2 24.52 115 65.7 55.0 41.29 118 66.9 56.4 38.36 121 78.3 56.9 31.32 124 79.3 57.2 31.47 175 127 77.7 59.1 44.5 3 130 72.4 57.9 35.34 133 73.9 57.0 32.10 136 71.6 52.9 28.02 139 77.0 54.8 31.35 142 69.9 54.7 36.40 145 74.5 55.8 34.76 148 69.4 51.8 31.81 151 67.8 53.1 29.25 154 72.7 50.8 36.44 157 72.3 48.3 39.00 160 75.7 49.0 43.91 163 71.1 46.1 42.03 166 67.3 47.3 39.20 169 67.8 46.7 41.41 172 64.1 44.9 32.64 175 66.3 47.5 26.98 178 71.4 46.3 33.64 181 76.3 48.7 35.27 184 73.2 47.4 39.25 187 68.9 46.4 31.74 190 78.4 47.3 50.64 193 70.9 47.4 66.40 196 68.5 45.3 39.47 176 199 69.2 48.2 32.40 202 68.4 48.7 27.34 205 63.8 46.9 19.92 208 65.3 45.2 14.92 211 70.3 46.5 13.80 214 56.7 42.2 9.57 177 LU-82-11(KIOSK LAKE) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (CM) (RELATIVE) (uG) 1 44.3 37.4 2.07 4 18.6 22.9 0.67 7 108.4 89.0 0.95 10 105.5 73.1 3.75 13 139.4 61.8 7.85 16 43.7 63.3 1.47 19 100.6 58.5 5.02 22 338.7 67.8 4.29 25 178.2 57.6 4.64 28 119.5 70.0 5.22 31 344.2 31.2 0.30 34 345.9 15.7 0.74 37 351.4 42.4 4.29 40 1.1 34.3 1.62 43 70.4 64.6 6.01 46 79.5 58.3 3.43 49 73.1 59.8 5.80 52 83.8 61.0 6.44 178 55 74.4 56.7 4.20 58 94.9 57.3 10.17 61 56.4 66.8 2.17 64 96.9 68.7 7.76 67 30.3 68.9 0.70 70 96.8 62.8 5.07 73 78.5 58.0 2.22 76 87.4 48.8 3.18 79 53.7 46.6 2.03 82 73.8 59.1 4.33 85 78.8 55.1 5.15 88 83.4 61.3 4.80 91 100.9 51.6 5.28 94 86.4 52.4 3.37 97 100.2 50.8 6.90 100 130.1 49.2 5.34 103 95.5 45.2 11.10 106 92.8 52.9 8.05 109 79.1 44.1 3.23 112 87.2 49.1 8.03 115 86.1 43.5 3.20 118 90.3 45.2 3.29 121 81.2 46.5 8.57 124 79.4 38.2 3.28 179 127 63.8 38.5 3.23 130 65.0 43.3 5.85 133 68.6 48.3 7.12 136 67.4 49.6 7.50 139 73.0 52.8 6.14 142 85.6 51.5 2.44 145 95.8 54.9 3.13 148 79.8 64.0 2.67 151 92.5 43.1 3.39 154 74.9 56.8 1.38 157 119.2 39.3 14.2 5 160 96.1 58.1 3.39 163 97.0 62.2 3.72 166 95.0 43.3 3.57 169 87.4 60.0 1.66 172 102.2 49-4 4.76 175 84.6 43.0 4.19 178 96.9 42.2 4.50 181 99.4 40.8 7.18 184 105.0 50.4 5.09 187 89.3 37.6 7.89 190 93.9 56.2 2.66 193 89.3 39.5 5.27 196 91.3 34.6 4.12 180 199 115.3 40.0 5.14 202 18.0 30.4 22.12 205 140.3 27.0 18.28 208 76.0 50.1 5.43 211 179.0 16.8 9.75 214 63.2 30.5 7.39 317 102.5 49.6 8.86 220 83.7 39.6 16.39 181 LU-82-12(CEDAR LAKE) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (cm) (relative) (uG) 1 168.5 "30.8 2.67 4 217.2 31.6 8.27 7 270.1 10.1 20.14 10 249.8 9.8 17.10 13 148.1 59.1 19.97 16 128.2 56.0 1.37 19 319.5 28.0 1.55 22 200.9 -48.7 3.68 25 292.4 -12.3 0.70 28 279.9 -23.0 1 .47 31 300.7 -17.7 8.07 34 296.2 -26.2 6.06 37 259.1 17.0 7.96 40 273.4 18.5 7.70 43 277.1 37.9 4.37 46 284.9 19.1 2.19 49 231.7 11.5 2.19 52 199.5 30.5 7.38 182 55 86.4 46.7 1.84 58 217.9 61.1 4.87 61 244.4 32.4 9.48 64 249.4 38.4 7.85 67 239.8 31.4 11.57 70 248.5 20.1 4.64 73 258.2 23.0 4.66 76 245.0 38.0 7.81 79 255.7 24.3 5.68 82 227.7 41.2 13.97 85 242.5 38.9 17.73 88 250.6 29.1 14.93 91 253.4 32.4 18.97 94 254.7 36.7 15.69 97 252.7 34.3 12.75 100 258.2 34.0 13.05 103 267.2 24.8 6.72 106 266.1 31.1 15.51 109 266.2 31.9 14.50 112 271 .4 34.8 13.84 115 267 .0 40.5 12.37 118 258.8 42.9 11.38 121 242.9 32.5 11.25 124 247 .0 33.0 11.92 183 127 245.3 33.7 9.86 130 242.1 30.4 9.86 133 239.5 34.2 13.87 136 243.4 34.8 14.25 139 258.3 33.4 12.24 142 246.1 34.7 11.63 145 274.8 45.5 11.61 148 269.0 46.1 11.38 151 251.3 40.1 14.56 154 259.8 46.4 17.42 157 263.8 37.7 7.19 160 268.4 51.0 8.26 163 237.2 43.2 7.04 166 230.8 44.5 14.14 169 254.8 56.6 7.19 172 251.4 45.9 5.85 175 259.0 48.6 7.02 178 251.2 46.9 7.47 181 255.7 42.8 10.24 184 288.6 46.1 6.27 187 254.8 9.4 13.78 190 264.8 31.5 16.24 193 257.1 23.3 5.60 196 235.8 50.2 17.41 im 199 223.5 45.8 21.47 202 224.8 47.7 21.04 205 219.7 42.5 13.82 208 227.3 50.7 10.14 211 222.6 44.8 15.88 214 250.7 50.2 15..55 217 247.1 52.0 10.78 220 240.4 63.5 10.79 223 216.2 53.1 16.95 226 212.2 47.4 14.68 229 217.9 43.9 8.. 96 232 212.6 53.6 17.89 235 215.4 48.4 14.15 238 218.4 52.6 16.82 241 219.5 51.8 11.53 244 219.5 61.3 12.24 247 229.6 51.1 14.30 250 231.7 51.4 13.37 253 199.8 59.2 7.67 256 178.0 63.1 11.06 185 LU-82'<13( TALON LAKE) DEPTH DECLINATION INCLINATION MAGNETIC INTENSITY (cm) (relative) (uG) 1 288.6 66.9 8.72 4 217.9 56.2 3.17 7 175.5 72.4 14.19 10 205.1 78.1 17.05 13 213.9 79.6 28.67 16 220.2 72.4 19.12 19 204.7 69.0 24.35 22 215.1 70.5 32.55 25 222.2 72.2 30.34 28 220.6 76.5 29.33 31 239.0 74.8 25.70 34 265.2 71.6 29.95 37 252.4 72.0 28.63 40 256.1 75.5 29.45 43 258.6 79.0 25.69 46 245.9 76.8 27.48 49 238.9 81.0 27.08 52 247.3 84.3 26.31 186 55 190.1 88.0 26.61 58 187.7 84.9 23.79 61 182.4 77.1 32.95 64 150.9 84.1 24.00 67 169.4 81.8 22.02 70 192.8 77.6 28.62 73 183.2 82.8 34.73 76 218.0 82.7 19.83 79 202.2 82.8 22.83 82 213.1 81.1 33.93 85 319.4 83.1 22.98 88 212.3 82.4 31.20 91 196.1 80.4 18.24 94 223.2 79.3 16.82 97 207.6 76.4 28.08 100 206.8 77.8 25.26 103 256.0 78.8 29.40 106 204.9 78.0 24.42 109 216.0 79.0 25.64 112 199.1 78.5 45.91 115 159.9 77.9 40.07 118 154.1 80.0 35.13 121 151.7 76.9 31.53 124 148.1 77.8 32.27 187 127 138.9 77.5 36.17 130 129.4 82.7 25.88 133 159.8 80.3 30.62 136 169.5 84.0 17.34 139 143.3 81.2 18.85 142 142.2 84.9 18.32 145 154.2 83.1 15.54 148 200.0 83.4 23.01 151 268.7 86.5 18.95 154 220.4 78.5 28.05 157 220.7 83.8 28.57 160 212.3 85.7 30.09 163 214.2 79.0 29.48 166 215.9 82.0 21.70 169 210.2 85.6 21.80 172 228.0 83.7 24.11 175 217.7 83.2 14.69 178 209.4 79.5 13.82 181 185.3 84.4 11.07 184 198.3 79.8 10.55 187 199.7 86.1 9.38 190 224.1 75.8 8.64 193 224.3 81.9 8.14 196 247.3 79.1 7.94 188 199 297.6 74.7 5.34 202 238.1 80.0 7.51 205 249.9 80.7 6.97 208 256.2 79.3 5.88 211 257.9 79.3 5.04 214 233.1 81.9 6.28 217 266.9 77.9 6.95 220 262.9 79.2 6.65 223 266.2 70.8 5.86 226 246.4 77.1 6.23 229 235.9 73.7 5.81 232 265.7 71.8 5.00 235 202.1 75.5 5.42 238 256.2 71.3 7.15 241 265.1 63.8 7.68 244 246.5 69.6 6.07 247 260.9 74.7 3.95 250 245.4 69.7 6.32 253 234.0 77.5 5.30 256 268.0 74.2 7.30 259 229.9 71.0 3.62 262 264.0 73-8 7.10 265 251.7 65.4 6.88 268 346.7 64.8 6-24 189 271 272.7 67.5 11.22 274 135.6 81.4 7.08 277 290.5 83.1 7.34 280 240.9 71.6 9.23 283 244.9 64.4 8.14 286 349.3 78.7 5.43 289 301.4 77.9 4.29 292 298.7 57.0 2.78 295 73.3 82.4 4.91 298 242.3 72.7 4.12 301 276.6 58.3 4.50 304 238.7 64.5 5.09 307 279.0 73.0 5.71 310 253.3 67.5 5.35 313 281.0 65.4 6.48 316 242.1 71.3 4.61 319 274.7 73.1 5.51 322 281.9 68.5 5.53 325 251.9 75.5 4.39 328 267.9 58.4 7.68 331 221.7 70.6 5.56 334 239.4 66.5 7.38 337 242.1 60.8 9.39 340 266.7 61.6 5.49 190 343 275.2 43.4 4.28 346 307.9 16.6 4.84 349 334.5 42.5 5.21 352 168.9 70.1 7.87 355 247.3 71.7 7.34 358 307.8 81.4 7.02 361 61.6 78.8 5.75 191 McBETH I Location 69°31.9'N 69fM7.5'W Dej^]i Pod ination Inclination Intensity (cm) Reading Rotated 2 153.1 59.9 53.3 5 234.3 81.5 12.6 8 193.0 70.5 26.6 11 218.6 45.5 23.9 14 196.4 64.3 26.3 17 203.5 79.5 28.8 20 156.2 76.6 31.5 23 183.3 75.7 25.2 26 155.2 70.1 31.9 29 168.2 64.4 35.3 32 139.2 66.4 69.7 35 127.7 44.1 81.7 38 142.6 6.5 52.1 41 111.3 68.2 37.4 44 147.6 80.7 25.3 47 62.0 77.8 44.9 50 132.0 75.2 28.2 53 99.9 69.9 30.2 56 151.2 64.3 30.3 59 157.4 71.0 38.4 62 154.4 73.9 42.2 65 171.9 68.4 35.7 68 172.8 71.4 39.9 71 161.1 63.6 37.5 74 167.7 58.0 41.8 77 163.6 19.4 31.4 80 352.2 157 54.5 29.0 83 292.1 124 74.2 39.0 86 269.9 96 79.6 47.7 89 315.2 147 79.0 26.3 92 86.7 278 81.7 34.2 95 36.3 228 79.5 36.8 98 43.3 235 83.3 45.8 101 2.6 194 80.4 39.8 104 19.4 211 86.9 44.8 107 10.6 202 82.9 40.4 no 337.4 169 83.7 37.9 113 346.6 178 80.2 42.1 116 351.9 183 82.2 44.0 119 337.6 189 83.7 42.3 122 326.9 158 86.5 49.2 125 345.1 177 81.6 42.3 128 256.8 88 85.8 37.5 131 335.6 167 77.9 32.7 134 338.9 170 83.1 38.1 137 169.8 1 84.6 28.2 140 322.8 154 84.4 32.1 143 353.2 185 81.3 39.1 192 )ntinued ?cl 1 nation Incl1 nation Intonsity idTng Rotated 17.3 149 84.4 33.7 !8.8 160 87.8 39.8 .0.2 142 83.6 32.9 57.7 119 75.8 69.5 )0.2 122 62.9 67.5 )1.2 133 75.8 79.1 '6.7 108 76.8 66.6 >1.1 93 74.6 57.3 .0.3 142 66.8 48.1 !5.5 57 62.7 55.8 !7.9 59 56.7 77.1 !4.4 56 48.8 75.3 '0.9 102 83.8 56.0 4.5 146 53.6 80.1 1.0 153 77.9 34.9 5.4 157 83.9 40.4 2.8 174 79.3 38.4 5.4 167 81.3 31.8 1.1 223 81.8 22.9 9.3 101 71.3 24.8 6.4 168 79.7 30.7 6.0 118 83.3 32.2 4.3 146 80.0 25.4 0.6 202 85.1 38.9 8.9 40 85.8 28.1 4.1 86 77.6 23.4 9.7 181 88.1 29.3 3.1 196 72.4 31.6 4.9 187 71.4 42.8 9.1 262 73.3 74.6 ?.3 155 81.5 36.3 3.2 216 80.7 21.1 1.3 185 68.1 25.4 3.2 213 73.5 19.4 3.7 208 72.9 25.6 ).8 242 69.6 28.3 1.6 227 67.0 25.8 ).4 233 69.6 22.1 ).2 232 75.6 18.2 1.6 108 71.6 24.1 !.5 221 72.3 86.8 .0 207 74.8 23.6 .7 216 74.8 19.6 .3 186 65.9 24.4 .6 197 64.4 27.5 .7 223 64.4 21.8 .6 213 62.9 16.3 .1 226 70.1 18.7 193 I Continued Pep Peelination Inciination Intensity Reading Rotated 291 214.0 227 63.6 20.6 294 218.4 231 69.2 20.2 297 212.2 225 71.4 21.1 300 194.7 207 70.6 27.9 303 193.3 206 68.6 25.5 306 205.7 218 67.9 25.3 309 217.4 230 69.1 35.9 312 207.7 220 69.1 28.2 315 198.4 211 65.2 29.0 318 213.7 226 68.6 26.8 324 203.6 216 62.3 25.3 327 206.1 219 67.4 28.6 330 189.2 202 64.1 20.2 333 186.5 199 64.5 25.2 336 154.3 167 74.9 54.2 339 153.4 166 49.1 108.2 342 198.1 211 75.0 31.4 345 245.2 258 64.8 17.3 348 5.7 18 79.2 27.7 351 11.9 25 84.8 26.7 354 5.1 18 87.3 36.5 357 346.8 0 69.6 58.7 360 117.9 130 84.2 21.9 366 33.4 46 81.0 23.4 369 64.6 77 84.6 26.4 372 83.6 96 81.6 20.7 378 54.2 67 81.2 21.9 382 150.8 233 76.7 20.4 385 124.8 211 77.3 23.2 388 151.7 238 65.9 17.5 391 6.6 89 74.4 48.7 394 57.9 141 80.8 19.9 397 76.3 159 78.7 20.6 400 111.4 194 81.8 18.7 403 149.6 232 85.8 27.0 406 120.2 203 78.8 16.3 409 96.7 179 86.4 28.1 412 114.4 197 84.4 28.9 415 87.8 170 84.2 25.9 418 150.5 233 81.4 33.8 421 106.4 189 82.3 26.7 424 90.3 173 78.1 27.5 427 34.1 117 66.1 45.2 430 128.9 211 78.7 53.1 433 100.4 183 77.4 31.9 436 94.4 177 77.0 49.9 439 72.5 155 80.6 25.9 442 77.8 160 76.9 31.3 445 79.6 162 79.1 35.3 448 104.3 187 76.4 29.2 19^ ETH I Continued th Dec1ination Inciination Intensity Reading Rotated 99.9 183 84.4 32.2 78.1 161 83.9 30,9 98.9 181 83.8 30.4 83.4 166 81.6 32.2 83.9 166 83.9 28.8 127.8 210 83.2 26.8 102.4 185 80.3 29.3 67.1 150 85.6 33.8 81.8 164 79.6 31.8 71.2 154 81.2 30.6 72.8 155 78.6 34.4 83.6 166 80.4 32.5 63.7 146 79.9 28.1 30.1 113 82.2 32.7 52.7 135 81.0 35.1 38.4 121 82.5 35.6 6.1 89 79.7 62.4 313.8 36 71.5 71.2 20.2 103 83.6 42.8 34.6 117 85.2 26.3 27.4 110 80.8 31.2 26.7 109 79.6 29.9 73.1 156 83.6 20.7 36.8 119 83.3 27.4 26.1 109 82.4 22.4 35.8 118 81.9 26.4 24.8 107 81.2 26.9 42.8 125 78.6 33.2 120.8 27 85.9 25.3 232.6 139 79.2 22.0 215.6 122 79.0 25.8 215.4 122 80.5 29.9 203.9 110 75.4 24.9 205.2 112 75.7 36.6 207.8 114 78.7 42.1 203.1 no 77.5 36.6 196.6 103 78.7 59.5 225.8 132 78.7 33.1 204.1 111 76.3 43.3 208.6 115 79.3 45.1 215.1 122 77.3 36.8 222.4 129 77.7 40.9 222.8 129 77.9 38.8 211.8 118 80.8 37.8 228.4 135 80.3 35.3 230.8 137 82.2 37.7 255.5 162 82.6 41.7 234.6 141 82.8 40.2 232.6 139 82.4 42.8 195 McBETH I Continued Oe])th Declination Incl inatioti Intensity Reading Rotated 598 223.4 130 81.8 33.9 601 222.8 129 82.1 33.4 604 226.8 133 83.0 34.6 607 265.2 172 82.3 29.9 610 251.5 158 82.4 31.5 613 248.1 155 79.9 28.8 616 275.1 182 77.5 31.8 619- 275.2 182 81.0 28.3 622 265.5 172 78.7 64.7 625 288.3 195 74.5 24.1 628 275.2 182 75.1 24.3 631 232.8 139 77.8 28.3 634 266.4 173 76.5 27.2 637 245.7 150 70.1 35.9 640 253.9 160 75.8 61.1 643 251.1 158 76.5 71.6 646 233.4 140 72.6 38.7 649 244.1 151 73.4 44.5 652 279.7 186 76.8 52.0 655 260.0 167 76.3 83.9 658 283.6 190 68.3 66.0 661 265.2 172 72.5 47.4 664 282.4 189 63.2 123.9 667 235.0 142 66.6 60.1 670 288.6 195 77.9 43.2 673 241.6 148 81.8 70.3 676 259.5 166 72.8 79.0 679 273.8 100 74.2 25.1 682 257.5 164 63.1 92.9 685 275.5 182 68.5 138.9 688 345.5 252 72.9 142.7 691 1.9 269 55.0 71.9 694 106.9 129 74.1 67.3 697 103.9 126 73.6 82.1 700 116.4 139 65.8 130.1 703 128.5 151 74.3 117.67 706 151.7 174 69.7 110.8 709 169.9 192 72.9 38.1 712 251.4 274 82.6 50.0 715 218.7 241 72.3 50.0 718 225.4 248 65.3 74.2 721 233.6 256 79.3 102.9 724 188.3 211 80.9 101.7 727 203.3 226 73.9 118.1 730 175.4 198 63.3 113.2 733 160.1 183 57.8 127.5 736 149.9 173 45.5 232.3 739 280.7 303 76.7 87.1 742 185.1 208 74.4 23.1 745 190.5 213 81.1 49.3 196 McBETH Continued Depth Declination Inc1ination Intensity Reading Rotated 748 194.6 217 76.3 19.3 751 176.3 199 67.4 78.6 754 239.4 262 82.5 21.4 757 195.7 218 73.9 18.1 760 195.2 218 79.1 16.4 763 195.2 218 77.9 33.9 766 169.9 192 74.1 82.6 769 186.5 209 68.6 19.9 772 193.3 216 82.3 21.0 775 184.7 207 76.2 24.9 778 186.4 209 72.9 25.2 781 202.6 225 78.6 50.3 784 194.7 217 75.9 33.7 787 191.9 214 76.4 42.6 790 183.7 206 79.8 29.6 793 180.5 203 70.3 29.2 796 203.3 226 80.4 38.5 799 199.9 223 79.5 25.6 802 189.4 212 76.2 26.5 805 184.3 207 79.7 24.3 808 185.7 208 74.4 35.8 811 197.3 220 75.2 61.7 814 168.5 191 70.3 71.8 817 185.6 208 79.1 29.8 820 185.9 208 75.2 25.4 823 184.3 207 79.2 27.6 826 191.7 214 72.9 27.8 829 186.8 210 74.1 30.9 832 184.8 207 79.4 39.6 835 194.9 217 76.9 25.9 838 191.8 214 73.8 29.9 844 335.9 220 64.6 6.7 847 311.6 196 77.1 10.8 850 294.5 181 66.8 6.6 856 318.9 203 62.6 5.6 859 336.4 221 51.5 20.9 862 341.6 226 65.0 26.9 865 346.9 231 61.3 35.0 868 347.6 232 50.1 46.0 871 348.7 233 69.1 48.9 874 340.2 225 68.8 19.3 877 357.5 242 78.3 17.6 880 5.1 250 67.4 70.9 883 58.4 303 77.1 72.2 886 324.8 209 78.6 86.1 889 274.9 159 56.8 97.1 892 302.3 187 49.1 90.3 895 298.5 183 54.7 86.7 898 287.8 172 53.9 90.3 197 Continued Pop Peel illation Incl ination Intens i ty Reading Rotated 901 252.8 137 63.9 76.1 904 237.1 122 61.9 78.8 907 140.6 25 27.3 90.3 910 159.7 44 55.3 46.4 913 159,3 44 56.7 31.5 916 200.8 85 23.1 78.2 919 189.8 74 40.1 53.1 922 109.8 -6 64.4 113.6 925 292.8 177 44.9 200.3 928 330.8 215 33.3 127.3 931 320.5 205 30.3 44.1 934 8.1 250 45.5 13.5 937 350.1 235 71.7 39.8 940 356.8 241 70.2 42.7 943 359.6 244 65.9 29.5 946 352.2 237 66.2 34., 1 949 352.9 237 72.5 29, .6 952 4.3 249 67.8 28. ,2 955 1.0 246 62.0 27. .5 958 355.0 240 67.9 27.8 961 4.8 249 78.5 28.0 964 0.1 245 77.4 26.7 967 1.3 246 72.1 24.1 198 ■ McBET■ H '2 ! Location ':668)9^°1367 ■ 5G0O' -N Depth ' Peelination Inc1ination Intens1ty ‘■Reaiding -Rotated 2 180.0 -10.8 21.7 5 179.0 36.1 37.3 8 .170.0 57.2 37.2 11 186.1 64.5 44.6 14 223.2 85.2 36.5 17 337.5 89;6 43.8 20 142.1 86.4 38.3 23 76.1 81.6 47.4 26 113.0 85.0 47.0 29 39.9 83.3 48.9 32 102.2 84.9 46.7 35 117.1 78.7 51.2 38 63.2 79.1 49.1 41 91.9 80.1 58.8 44 138.7 79.7 46.9 47 64.1 76.0 55.1 50 110.7 78.5 48.8 53 76.9 78.4 45.6 56 77.4 77.8 39.9 59 46.7 74.7 42.8 62 73.0 74.8 43.6 65 87.6 74.9 40.4 68 59.5 80.6 49.1 71 73.4 83.6 50.2 74 40.6 81.6 46.6 77 40.5 79.9 45.4 80 63.8 85.3 54.1 83 73.2 84.9 54.5 86 54.4 80.6 56.1 89 87.9 83.2 62.5 92 130.3 79.5 64.6 95 170.1 81.5 79.9 98 56.2 76.9 59.7 101 314.9 59 70.7 57.0 104 312.2 57 75.9 52.3 107 306.9 51 74.7 55.1 no 271.1 16 78.7 56.8 113 267.3 12 79.6 65.4 116 281.4 26 80.2 55.9 119 298.8 43 76.3 58.3 122 313.0 58 73.2 77.9 125 289.2 34 31.9 62.3 128 327.2 72 81.1 56.1 131 274.9 19 82.7 51.7 134 346.0 91 81.5 50.5 137 345.1 90 82.7 67.1 140 354.0 99 79.5 46.9 143 359.6 105 74.9 52.5 199 2 Continued Dq^c 1 ination I n_c 1 j na_M or i 11 lUqn '> j t^ Reading Rotated 146 345.9 90 76.6 41.6 149 7.3 112 85.5 56.1 152 20.4 125 77.9 45.2 155 61.1 166 83.8 54.7 158 97.0 202 84.6 75.8 161 69.4 174 87.7 75.1 164 309.5 54 78.4 66.8 167 327.4 72 80.0 81.8 170 305.8 50 85.1 78.2 173 324.3 69 86.4 77.9 176 2.4 107 84.9 71.8 179 38.1 143 85.9 85.2 182 51.1 156 83.9 80.9 135 46.0 155 85.1 93.1 188 73.5 178 87.6 77.1 191 43.3 148 81.6 80.9 194 59.1 164 82.9 80.0 197 120.5 225 81.4 86.1 200 49.7 154 83.9 73.1 203 127.1 132 84.2 78.9 206 87.2 222 84.1 73.1 209 77.6 182 87.8 79.6 212 113.4 218 85.2 89.3 215 78.8 183 84.5 93.9 218 77.5 182 83.2 107.3 221 52.9 157 79.6 114.4 224 51.2 156 82.5 94.7 227 59.8 164 79.1 112.8 230 56.5 161 79.7 102.0 233 24.2 129 84.2 118.1 236 6.7 111 80.6 90.9 239 7.2 112 80.8 103.3 242 13.1 118 80.0 78.5 245 5.1 no 78.2 84.2 248 146.4 106 79.3 74.9 251 115.0 75 84.2 70.3 254 105.7 65 82.3 85.9 257 106.9 66 84.9 78.5 260 151.3 111 83.2 92.9 263 90.6 50 85.4 103.2 266 60.8 20 84.1 101.9 269 102.7 62 85.7 78.6 272 119.5 79 80.9 96.9 275 93.4 53 81.4 100.6 278 133.6 93 79.9 93.4 281 83.8 43 83.1 120.3 284 90.4 50 83.6 108.4 287 112.1 72 76.3 121.4 200 McBeth 2 Continued Depth Uec1inatlon Inclination Intensity Reading Rotated 112.1 72 81.4 217.4 85.0 45 81.5 188.2 264.7 224 27.3 302.5 100.8 60 73.5 116.9 89.6 49 75.5 96.8 68.2 28 75.3 114.5 234.9 194 46.3 86.9 256.7 216 19.7 150.7 168.1 128 64.8 79.3 137.9 97 63.5 41.2 76.7 36 48.7 45.4 56.2 16 62.4 65.0 26.4 -14 77.0 60.1 193.6 153 68.5 64.4 210.9 170 44.4 75.8 153.5 113 77.9 51.7 175.9 135 74.5 100.3 172.4 132 73.6 92.2 179.6 139 70.9 132.9 246.7 206 65.4 100.2 248.9 208 69.2 105.9 283.8 243 84.7 66.6 287.1 247 52.5 53.9 252.4 212 62.2 113.2 102.0 62 87.3 71.2 244.4 204 78.7 90.3 234.2 194 81.2 106.6 269.3 229 70.7 97.7 271.9 231 72.2 88.5 312.8 272 72.3 70.3 324.4 284 73.3 108.8 7.0 327 65.1 86.6 334.2 294 50.4 83.9 321.5 281 30.7 38.1 32.2 352 73.4 67.3 103.9 163 59.7 44.5 155.2 215 64.1 29.9 221.3 281 16.9 13.6 274.1 334 46.8 23.3 272.8 332 83.4 67.8 212.1 252 40.1 97.1 213.8 253 56.5 86.4 196.9 236 56.7 28.9 336.9 36 77.7 73.1 205.6 265 79.2 80.8 258.9 318 76.0 74.8 201.3 261 71.7 127.4 c^o4riojir^o^ij\i>Xi—i-c••»—-b>^>X—iC*oouo)oUou)cDoyCDiUODcJo'^c'o^a^jocr-'iCcroiccroiCcnAcnjoLjcno4Lijio.jcioijuS)iU CO),O ojoru\3)rC\>orOorL—>‘wi—to•(c—ou•(J—U*JoUoo)>ro^rv>Doi>rD\5'r£o5 0'^-p»^-•030^^o<.DC^lCoO''J■Ci*—•oocnrv)UDCTiOJO'vi-c»t—•cotnnoiiscriooO'vii—‘OOuit\3kr)crioJO'^-&t—*u3cr>u)0 201 McBeth 2 Continued Peelination Inclination In tensity Reading Rotated 433 206.3 266 66.0 128.6 436 202.6 262 59.1 85.0 439 183.8 243 71.4 73.2 442 154.9 214 55.5 76.5 445 196.1 256 67.0 89.6 448 179.9 239 68.2 93.4 451 163.3 223 77.2 73.9 454 186.6 246 62.1 70.3 457 154.1 214 66.1 90.4 460 157.1 217 67.8 86.0 463 162.2 222 64.7 82.8 466 165.5 225 65.6 87.4 469 177.6 237 59.1 83.1 472 161.0 221 45.1 76.1 475 177.4 237 80.2 100.1 478 161.4 221 66.9 67.8 481 142.5 202 76.7 67.6 484 209.0 269 77.7 149.8 487 287.4 347 83.6 47.3 490 159.5 219 83.5 89.2 493 69.9 129 87.9 69.7 496 189.7 249 79.5 85.5 499 209.8 269 83.3 83.1 502 180.2 240 73.2 125.8 505 173.9 233 80.5 149.5 APPENDIX E Compllatllation of X-Ray diffraction data 1- North Bay areas LU-82-1 (Callander Bay) LU-82-8 (Lake Nipxssing) LU-82-9 (Lake Nipisslng) LU’-82-3 (Lake Nosbonslng) .■LU-82-7 CLake Nosbonsing) LU-82-10 (Lake Talon) LU-82-13 (Lake Talon) LU-82-11 (Kiosk Lake) LU-82-12 (Cedar Lake) 2- McBeth Fiord McBeth-1 McBeth-2 cn 0J- iS r CO" I— i.n - Gi - 4^ QUARTZ (/-8J./J r_D- iliJ tD- ilD -\]- '•J- iXl m- cn- ■T;ilite(1.99A) CQ OJ- oj- 4i - Calcite/Dolomite CD - tu i[Ci- 03 co- I ij Quartz(2.5A) DJ ■"J- '-3- r' d Lu CH- Quartz(2.5A) CO 1 cn- CO Dolomite(2.5A) hO I' I 'I co I OJ- co- CO -J co - Dolomite(2.9A) ro -1 CD- tX3- ro ^FELDSPAR r\i cn- Kaolinite ^■^^ARTZ cn- ro (3.5A) --] fjj- (3.34A) oj- ro - --] - QUARTZ (4.24A) ijj- ijj- m 00 m- lin- en cu- co- * rn cn -Quartz »X1‘ ijj- cn - - cn LH- -trr l-bl-g&dNHS i.n '3 CO" OJ' m ^ i 5 ■ QUARTZ (1.82A) UD IJD- 03- -ti 03 Illite(1.9A) -x]- 03 cn- m- : I Dolomite(l.9A) fJD OJ" OJ- -fc. 03 ■ 01 03 iLQ- Calcite(2.9A) 03- 0.1 ■■ i3D - .]- Quartz(2.5A) -0- 0.1 133 m- iT!- oo 03 oo* Dolomite(2.64A) OJ- OJ - i33 • ?=“ Calcite(3,03A) ro -J 03- 03- r-j FELDSPAR ■ rvi -3 m- ^ . QUARTZ cn- ro ^g=r-^aollnl te ( 3. A9A> -3 OJ" ^ '*(4.021) OJ- rvi S Z Z-~CTbite QUARTZ -3 ^ (4.24A) m ijj" f 03- m -]- i- -3- s iT.i OH" •v tn- I—h f" ij.1' Chlorite(7.OlA) uJ- iT.i ■ cn i'£|- 03- Quartz m -]- -3- cn- f.n -trr cn - in IJL)—; i- I'.n - no •3 COp'J QUARTZ - (1.82A) roH IJ — UIJ3D - 3 — 33 OJ - Uj_^ ^'pk -fi. - ilQ - i.n—: X Illite(l. 98A) cn—; 33 4^ - OJ - 0.1—; 0J~ IJJ - OiJDJ —'; ro - Calcite(2.28A) 03-; 0.1 ro - -J' -0— ~ quartz(2.43A) r rn - c cn— I 0K0 5 iOjJJ— -; S' rn - I OJ— Cui - V CD - S - ro - '3^oloinite(2.8A) -0 to IJQ— 3^- FELDSPAR fJ3' o ro - -O”; -s] ro - iji— ^^UARTZ cn ro - (3.34A) -0 iOJ~ OJ ro - ^Albite (3.7A) -■■] - v^QUARTZ (4^24A) ro OQ cu CTi ■j— m I m— en- rol - Oj“ OJ ITI jThlorite(7.6A) LD-- cn - Quartz ijj— cn ■ ro - iTt- cn ijj" C3 OJ" H-• m - V- o 133 iXl' '^QUARTZ (1.82A) 133- -fi 03 -^]- -Ci 03 cn- Illite(1.99A) en- i3D 0.1 ■ CO" -fi 03 111 133 ijQ- 133- sr—=-— Calcite(2.9A) <3- 4 f CTi J. tn- cn- CT' OJ*- L 0.1- I—^ iTi - t— cri 1X1— iXr Quart z/Vemiculite cri i -J- cn- l~S^lor1 teClS.yeA) cn ~cnr i.n - 1-0 C3 OJ' cn - Q ■ "D QUARTZ . 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LOCATION MAP OF NORTH BAY OUTLET AREAS FOSSMILL OUTLE T NORTH BAY OUTLET —±> 0 MILES 10 79° 30 79°00 78^30' I _l _l DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARS PALEO- PALEO-- METRES) (Phi units) (°/o) MAGNETIC PALEO- C.% C.°/o DECLINATION INCLINATION INTENSITY INCLINATION 4JG CALENDAR 34 5 6 78 9 10 0 50 100 0 5 1015 0 5 0 100 200300 (YRS.BP) 0 1 0-2.36 meters silty clay, tr—‘ - 200 olive gray (5Y4/1), homo- 1.0 • geneous, non-calcareous. i i 1300 2.36-3.79 meters silty 20 f - clay, olive green (5Y4/1), homogeneous, and non- 2100 3.0 ■ calcareous. A? 26001 4.0. 2800 5.0- FIGURE 2 . LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. LU-82-1 (CALLANDER BAY) DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARS PALEO- PALEO- MAGNETIC PALEO- (METRES) (Phi units) (°/o) C.°/o C.°/o DECLINATION INCLINATION INTENSITY INCLINATION CALENDAR 34 5 6 7 8 9 10 0 50 100 0 5 1015 0 5 -90 0 90 O' 30" 60" 90" 0 100 200300 (VRS. BP) 0 A- - 200 •*' 0- 3. 13 ilUy cl*y * * * . ; Q gretrflHh 'jr*y (SGT6/1), hotno‘jeneou'. . non-C4 I C ^reou i . dnd f1n« 3.13-3.63 r ^ iweteri color but mjn- K 1300 1.0 hCMnogeneOuS lo odlure, From C-- .... • 3,63 meters color change up * « to 3.73 in^ters stlty tley dark greenish gray (SGY4/1) / . V—D hcanogeneous, non-ca I careous, a / .•* ^ and firm compact. Bui from 2100 3.73 nelers color gradually •« • a * changes Into ol Ive gray (SCY4/1 ) up to 3-Vl laeters. 3’-* * :.. ̂ From 3.91 meters abrupt color 20 2600 change up to 3.96 aietors •* >.* • * - Separated by 2 c* white-gray band to dark greenish gray * ^ • (SCY4/1). 6ut from 4.03- 4.14 meters silly clay com- *».• . :*•* plete color change to light brownish gray (5YH6/I ) . , f*. homogeneous, and calcareous. . a • ^ 4.14-4.17 meters small white 3 500 3.0’ band again separates, a col- i: or change black to a much . brownish gray (5YR6/1). At • • . Ivy.— a * 4.19 meters small white band • • • 1- ? cm and at 4,2? meters • a •• 4050 color again change to green- ish gray (6GY4/1) up to 4.30 —F meters silty flcmogeneous. • ♦ *-P and calcareous, lollowed by 40. light brownish gray (5YN6/I). • • 4 750 4.30-4,66 meters pattern con- tinues once more until the end of the core. • • Ve-r G" 6000 50 FIGURE .7 LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. LU-82-8 ( L. NIPlSSiNG ) S/ND PERCENTAGE ORGANIC CARB PALEO- PALEO- MAGNETIC PALEO- DEPTH LITHOLOGY MEAN GRAIN SIZE (Phi units) (%) C.°/o C.°/o DECLINATION INCLINATION INTENSITY INCLINATION METRES) xiG CALENDAR w 0 100 2003QQ (VRS. BP) 34 56 789 10 0 50 100 0 5 1015 0 5 0 30 60* 90 0 t * , ■ i 2 00 0-.20 meter silty clay, dark I 't greenish gray (5GY4/1), V y 1.0 %: ». 1300 homogeneous, non-calcareous, 1: 2100 and fairly loose compact. I 2 600 20 A* 3500 0.20-3.25 meters silty clay ••• greenish gray (5GY6/1), 4050 3.0 homogeneous, non-calcareous 4500 and more compact. 4D\ 5.0 FIGURE . LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. LU-82-9 ( L.NIPISSING) DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARS PALEO- PALEO- MAGNETIC PALEO- (METRES) (Phi units) (%) C.7o C.7o DECLINATIOM INCLINATION INTENSITY INCLINATION MG CALENDAR 3 4 0 5 1015 0 5 - 90‘ 0 .90 0 100 200300 (YRS. BP) 0 ■ * —5^ 6^ 7 8 9 10 0 50 100 ,i...I -1 1 ‘ - > * t *!■ ‘ r 0-1.10 meters silty clay, olive blackish gray (5Y3/1),I homogenous, non-calcareous, 200 1 0 .and not very compact, color . - gradually darkens to olive black (5Y2/1). 1.10-2.86 ft meters silty clay olive 1300 2D- .black (5Y2/1), homogeneous, f 'non-calcareous, and more % 2100 compact. 2,86-3.43 meters silty clay color change to 2 600 3,0- .dark greenish gray (5GY4/1), homogenous, non-calcareous, and compact. 3.43-4.33 meters silty clay greenish 3500 40. .gray (5GY5/1), homogeneous, non-calcareous, and compact. 4000 FIGURE 7 . LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. LU-82-3 (L.NOSBONSING ) DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARB PALEO- PALEO- MAGNETIC PALEO- METRES) (Phi units) i°/o) C.°/c C.7c DECLINATION INCLINATION INTENSITY INCLINATION ;uG CALENDAR 34 5 6 7 8 9 10 0 50 100 0 5 1015 0 5 0 100 2OO3Q0 (YRS. BP) 0 1 0-0.53 meter silty clay olive gray (5Y4/1), homo- 200 geneous, non-calcareous, and loose compact, 0.53- 1300 1.0 • 2.58 meters silty clay 2100 olive blackish gray (5Y3/1), homogeneous, non- 2D- calcareous, and slightly more compact. 2.58-2.63 2.63- 2 600 2.98 meters silty clay ol- 3.0 ive gray (5Y4/1), homogen- eous, non-calcareous, and 3500 more compact. 2.98-3.66 meters silty clay greenish 4000 4.0 J gray (5GY6/1), homogeneous, non-calcareous, and compact 5.0 FIGURE ^ . LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY, TEXTURE AND CARBON PERCENTAGES. LU-82-7 ( L.NOSBONSING ) DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARB PALEO- PALEO- MAGNETIC PALEO- (METRES) (Phi units) (°/o) C.7o C.7o DECLINATION INCLINATION INTENSITY INCLINATION uG CALENDAR 34 56 789 10 0 50 100 0 5 1015 0 5 -90 0 90’ 0 100 200300 (YRS.BP) * 0 -TT '4 ^ 0-1.00 meter silty clay 2 00 olive gray (5Y4/1), homo- geneous, non-calcareous, 1 0 . loose compact, and dark 1300 . - band at 2-3 cm intervals found throughout section 12100 (core), but from 1.00- 20 1.90 meters it becomes |2 600 - more compact. 1.90- 2750 2.11 meters silty clay, homogeneous, non-calcar- 3.0- . eous, and color changes greenish gray (5GY6/1), and even more compact. 40. 5.0 • FIGURE ? . LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. LU-82-10 ( L.TALON ) DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARS PALEO- PALEO- MAGNETIC PALEO- (METRES^ (Phi units) (7o) C.7o C.7o DECLINATION INCLfNATION INTENSITY INCLINATION juG CALENDAR 34 5 6 78 9 10 0 50 100 0 5 1015 0 5 0 100 2003QQ (YRS. BPJ 0 0-1.23 meters silty clay, ~2 OO olive gray (5Y4/1), homo- geneous, non-calcareous, 1.0 loose compact, darker ■ 1300 ■ bands are found at 2-3 cm intervals throughout the core section (1 cm 2100 20 _width). At 1.23 meters - no more bands, but it becomes more compact. 2G00 1.70-2.63 meters silty i « : ao .clay, dark greenish gray / (5GY5/1), homogeneous, non-calcareous, and more 3400 compact. 2,63-2.90 40. .meters sandy portion (i,e., about 25 cm) same color, firm compact till 3.61 meters. 5.0- FIGURE 10 . LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. LU-82'13 ( L.TALON) DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARS PALEO- PALEO- MAGNETIC PALEO- METRES) (Phi units) (°/o) C.'Yo C.°lo DECLINATION INCLINATION INTENSITY INCLINATION 34 56 789 10 0 50 100 0 5 1015 0 0 0-1.00 meter silty clay olive black (5Y2/1), homo- geneous, non-calcareous, 1.0 and a brownish gray (5YR4/1), band running the whole length of section (core) on the outer edges 2J0 (5 mm width) loose compact 1.00-1.05 meters gap. 1.05- 1.80 meters olive black (5Y2/1), and again band 3.0 ^ Jrunning down the core sec^ tion for about 40 cm. But at about 1.80 meters color becomes slightly darker near 40 the bottom of the core sec- tion (i.e., at about 2.19 meters). 50 FIGURE // LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. LU-82-11 (KIOSK L.) DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARS PALEO- PALEO-- MAGNETIC PALEO- (METRES) (Phi units) (%) C.°!o C.°A DECLINATION INCLfNATION INTENSITY INCLINATION JuG CALENDAR 34 56 789 10 0 50 100 0 5 1015 0 5 -90 0 90 0* 30 60' 90 0 100 200300 (YRS. BP) 0 1 • • ' ■ . . t . - 0-0.85 meter silty clay, brownish black (5YR2/1), • • ♦ homogeneous, non-calcar- '• ' .. 1/ 1.0 eous, and very loose com- ./• • t . s' * ■ < pact. 0.85-0.88 meter gap B 1300 in core section. 0.88-1.88 »• • meters silty clay, brownish * • 20 black (5YR2/1), homogeneous, • - non-calcareous, loose com- • > mF • 12100 pact, and darker diagonal • • • • 2300 bands are found throughout 3.0- the core section. Again from 1.88-2.06 meters gap in core section. 2.06-2.75 meters silty clay, brownish 40. black (5YR2/1), homogeneous, non-calcareous, and quite loose compact. 5.0- FIGURE /^. LATE QUATERNARY STRATIGRAPHY SEQUENCE OF NORTH BAY OUTLET AREA : PALEOMAGNETIC RECORD , LITHOLOGY, TEXTURE AND CARBON PERCENTAGES. LU-82-12(CEDAR U DEPTH LITHOLOGY MEAN GRAIN SIZE SAND PERCENTAGE ORGANIC CARS PALEO- PALEO- MAGNETIC PALEO- (METRES) (Phi units) (o/o) c.% c.% DECLINATION INCLINATION INTENSITY INCLINATION juG CALENDAR (YRS. BP) 34 56789 10 0 50 100 0 5 1015 0 5 -90' 0 ^ 90 0 100 200300 01 -f-JT-" * V • • 200 • Vy. 1300 1.0- 2100 2 600 « 20- 3500 4050 3.0- 4750 40. 6000 5.0- • 6750 V ’ •• * , 60- 8200 ZO- « 9500 8.0' 9.0- I I ' 10.0. FIGURE 3 , LATE QUATERNARY STRATIGRAPHY SEQUENCE OF McBETH FIORD, BAFFIN ISLAND PALEOMAGNETIC RECORD , LITHOLOGY , TEXTURE AND CARBON PERCENTAGES. McBETH-1 DEPTH LITHOLOGY MEAN RAIN SIZE SAND PERCENTAGE ORGANIC CARB PALEO* PALEO-* MAGNETIC PALEO- (METRES) (i ’hi units) (^/o) C.°/o c.% DECLINATION INCLINATION INTENSITY INCLINATION CALENDAR 34 56789 10 0 50 100 9 5 10 1.5 0 0 100 2003QO (YRS.BP) -1 « * 0 2 00 ■ 1300 1.0 2100 • V V • 20 2 600 3500 m 30 40 « • • 4050 4 . 4750 50- 60- FIGURE /4 . LATE QUATERNARY STRATIGRAPHY SEQUENCE OF McBETH FIORD, BAFFIN ISLAND : PALEOMAGNETIC RECORD , LITHOLOGY, TEXTURE AND CARBON PERCENTAGES. McBETH - 2