karst investigation of the duntroon quarry expansion lands€¦ · 4.1 regional karst geomorphology...

Karst Investigation of the Duntroon Quarry Expansion Lands

October 3, 2007

Prepared for:

Jagger Hims Limited

Prepared by:

Marcus J. Buck, Marcus J. Buck Karst Solutions Dr. Stephen R.H. Worthington, Worthington Groundwater

Karst Investigation of the Duntroon Quarry Expansion Lands October 3, 2007

Marcus J. Buck Karst Solutions Page i Worthington Groundwater

Executive Summary

Worthington Groundwater and Marcus J. Buck Karst Solutions carried out a detailed field investigation and assessment of karst development at the Duntroon Quarry expansion lands and in the vicinity. The work builds on the hydrogeological work already completed by Jagger Hims Limited and is intended to supplement their report.

As a result of a regional survey, a variety of karst features were identified in an area that extends approximately 2 km to the north and 2 km to south of the expansion property. Between these limits and within 700 to 1400 m of the Niagara Escarpment there is either an absence of surface streams or the surface streams sink. To the west of this area there are surface streams that flow to the west, though there are some sinking streams as well. In the area studied, 74 springs were found that discharge from the Amabel aquifer. The majority of these discharge along the Niagara Escarpment where they are found at the head of streams that descend the Niagara Escarpment slope. These streams often sink on reaching an erosional bench on top of the Manitoulin Formation, and 57 springs were found discharging from the Manitoulin Formation at a subsidiary escarpment bordering the Manitoulin bench. The Amabel and Manitoulin springs are typical of springs elsewhere along the Niagara Escarpment, with the larger springs having mean flows of several litres per second.

Four tracer tests were carried out from sinking streams, two of which were on the Amabel plateau and two on the Manitoulin bench. The results were generally similar, with the fastest groundwater pathways to springs having velocities ranging from 500 to 3500 m/day, which is typical of velocities between sinking streams and springs in karst aquifers.

Local-scale investigations were carried out on the expansion lands. This work included continuous water level monitoring at three wells, electrical conductivity and temperature profiling at four wells, tracer testing from four wells to a nearby spring, and continuous monitoring of stage and electrical conductivity at that spring. The tracer testing from the wells gave velocities that ranged from 4 m/day to 1500 m/day, which is typical for tracer tests in karst aquifers when the tracer injections are into boreholes. Calculations show that this corresponds to fracture apertures that ranged from <0.05 mm to 3.7 mm along the traced pathways from the boreholes to the spring. Electrical conductivity and temperature profiling showed abrupt changes at specific horizons in the boreholes, suggesting preferential flow along a limited number of horizons in each well.


Marcus J. Buck Karst Solutions Page ii Worthington Groundwater

A conceptual model of the aquifer was attained from the above measurements, together with observations in Duntroon Quarry and borehole measurements reported by Jagger Hims Limited (2005, 2007b). The uppermost few metres of bedrock are highly weathered. Below this, the weathering is focussed on a limited number of fractures, typically producing enlargements up to several millimetres in size. Openings may be substantially larger along the flow paths between sinking streams and springs, as well as in the vicinity of the larger springs.

Jagger Hims Limited (2005, 2007a) has anticipated that recharge (injection) wells close to the quarry may be necessary to mitigate the lower groundwater levels predicted in the surrounding areas as a result of quarrying. With the distributed percolation recharge to the aquifer in the expansion lands, it is concluded that many small channels and only a much smaller number of conduits (i.e., with a diameter > 1cm) will be encountered during quarrying, and that the modelling by Jagger Hims Limited provides a good representation of the likely discharges. Conduits are most likely to be encountered in the area closest to the largest springs (SW2A and SW2B) where localized grouting might be required if inflows to the quarry become problematic.

The proposed quarries on either side of Grey County Road 31 (i.e., Highland Quarry and Duntroon Quarry expansion) have the potential to impact the SW2 springs located at the southwest corner of the Duntroon expansion lands. These springs derive their groundwater recharge from a catchment area that may extend across portions of each of the proposed quarries. Conversely, impacts on springs along the Niagara Escarpment are likely to be minor. Some of the excess water from dewatering of the quarry will be discharged to the SW9 watercourse. This is a sinking stream located on the Amabel plateau on land owned by Walker Aggregates Inc. to the east of the proposed extraction area. Groundwater tracing indicates that this stream flows rapidly in the subsurface and resurges at 19 springs located along the Niagara Escarpment. The quarry discharge water would represent only a small fraction of the existing maximum flows in the creek and would help sustain flow in the creek and at the springs. The net mean discharge at the springs would be little changed during the period that the quarry is dewatered.

Acknowledgements

We would like to thank the private property owners that kindly permitted us to conduct fieldwork on their lands. We are especially grateful to Bill Franks and his family and to Victor and Emily Smidor for their hospitality while conducting the fieldwork.


Marcus J. Buck Karst Solutions Page iii Worthington Groundwater

Table of Contents Executive Summary ....................................................................................................... i

Acknowledgements....................................................................................................... ii

Table of Contents......................................................................................................... iii

List of Tables ................................................................................................................. v

List of Figures .............................................................................................................. vi

1.0 Introduction........................................................................................................... 1 1.1 Objectives and Scope ................................................................................................ 1 1.2 Report Structure......................................................................................................... 2

2.0 Synthesis............................................................................................................... 2 2.1 Nature of Karstification in the Duntroon Quarry Area................................................. 2 2.2 Regional Patterns of Aquifer Recharge and Discharge ............................................. 3 2.3 Regional-scale Tracer Testing from Sinking Streams................................................ 5 2.4 Local-scale Investigations .......................................................................................... 6 2.5 Karstification in the Bedrock Aquifer at the Duntroon Quarry Expansion Lands........ 6 2.6 Karst Issues Relevant to Quarrying at the Duntroon Quarry Expansion Lands. ........ 7

2.6.1 Use of Groundwater Recharge Wells............................................................. 7 2.6.2 Influence of Karst Conduits on the Drawdown Zone ...................................... 8 2.6.3 Potential Impacts to the SW2 Springs............................................................ 9 2.6.4 Potential Leakage between the Proposed Quarries....................................... 9 2.6.5 Potential Impacts to Niagara Escarpment Springs......................................... 9 2.6.6 Discharge of Quarry Water to the SW9 Watercourse .................................. 10

3.0 Study Methodology ............................................................................................ 12 3.1 Karst Study Area ...................................................................................................... 12 3.2 Field Mapping and Surface Water Monitoring.......................................................... 12 3.3 Climate Monitoring ................................................................................................... 14 3.4 Borehole Monitoring ................................................................................................. 14 3.5 Groundwater Tracing ............................................................................................... 15

4.0 Regional Investigation of Karst ......................................................................... 16 4.1 Regional Karst Geomorphology and Hydrology....................................................... 16 4.2 Karst Development on the Amabel Plateau ............................................................. 23

4.2.1 Observations at the Camarthen Wetland Tributary and Nearby Springs ..... 28 4.3 Karst Development on the Manitoulin Bench ........................................................... 31 4.4 Measurements of Streamflow around the Study Area Perimeter............................. 34


Marcus J. Buck Karst Solutions Page iv Worthington Groundwater

5.0 Investigation at the Manitoulin Bench .............................................................. 35 5.1 Site Description ........................................................................................................ 35 5.2 Results of the Groundwater Trace from Site 114..................................................... 37

6.0 Investigation of the SW9 Watercourse and its Resurgences ......................... 40 6.1 Site Description ........................................................................................................ 41 6.2 Streamflow Losses along the SW9 Watercourse..................................................... 42 6.3 Results of the Groundwater Trace from the SW9 Watercourse............................... 43 6.4 Results of the Groundwater Trace from SW10 ........................................................ 47

7.0 Investigation of the SW28 Watercourse and its Resurgences ....................... 48 7.1 Site Description ........................................................................................................ 48 7.2 Results of the Groundwater Trace at SW28 ............................................................ 51

8.0 Investigation at the Duntroon Quarry Expansion Lands................................. 56 8.1 Water Level Data from BH02-1, BH02-4 and BH03-9.............................................. 56 8.2 Investigations in the Vicinity of the SW2 Springs ..................................................... 56

8.2.1 Site Description ............................................................................................ 57 8.2.2 Monitoring Data at the SW2A Spring and Nearby Boreholes....................... 59 8.2.3 Recharge for the SW2 Springs..................................................................... 61 8.2.4 Groundwater Tracing to the SW2A Spring ................................................... 63

9.0 Conclusions ........................................................................................................ 65

References Cited......................................................................................................... 70

Figures ........................................................................................................... 72

Appendix A: Glossary of Karst Terms.................................................................. 96

Appendix B: Photographs ..................................................................................... 99

Appendix C: Classification and Description of Features.................................. 106

Appendix D: Surface Water Data......................................................................... 146

Appendix E: Groundwater Tracing Data ............................................................ 163


Marcus J. Buck Karst Solutions Page v Worthington Groundwater

List of Tables Table 1. Classification of features inventoried during the field investigation of karst ...........18

Table 2. Number and size of springs and spring groups that occur in each aquifer ...............21

Table 3. Observed utilizations of springs................................................................................23

Table 4. Karst basins identified on the Amabel plateau .........................................................24

Table 5. Surface water monitoring data for SW26 and the nearby springs on May 15 and November 17, 2005............................................................................................31

Table 6. Total discharge (L/s) measured from selected Amabel and Manitoulin springs during high and low flow conditions ........................................................................33

Table 7. Surface water data measured at the Manitoulin escarpment on April 19, 2005 .......39

Table 8. Surface water sites where the tracer was recovered from the SW9 watercourse tracer test...................................................................................................................44

Table 9. Approximate residence times calculated for the ephemeral pond at Site 7 during the groundwater trace ....................................................................................52

Table 10. Surface water data measured at selected sites on May 10, 2005 ..............................53

Table 11. Variations in the relative contribution of sinking stream recharge to total discharge at the SW27 spring group .........................................................................55

Table 12. Groundwater monitor details for monitoring wells located near the SW2A spring.........................................................................................................................59

Table 13. The calculated surface area of the springshed for the SW2 springs .........................62

Table 14. Details of the tracer tests at the SW2A spring on May 12, 2005..............................64


Marcus J. Buck Karst Solutions Page vi Worthington Groundwater

List of Figures Figure 1. Regional map of karst features and surface water monitoring sites .....................72 (fold-out map in back pocket)

Figure 2. Discharge by magnitude of 46 gauged springs in the Amabel Formation and 42 gauged springs in the Manitoulin Formation. ...................................................72

Figure 3. Map of Niagara Escarpment springs located north of County Road 91 ................73

Figure 4. Uranine dye concentrations at springs located below the Manitoulin Formation following the injection at Site 114 on April 19, 2005............................................74

Figure 5. Map illustrating tracing results at springs located below the Manitoulin Formation following the injection at Site 114 on April 19, 2005..........................75

Figure 6. Map illustrating tracing results at various Niagara Escarpment springs following the injection in the SW9 watercourse on April 23, 2005 ......................76

Figure 7. Stream flow measured along the SW9 watercourse downstream from SW9 on April 25, 2005 ........................................................................................................77

Figure 8. Map illustrating tracing results at Niagara Escarpment springs located north of County Road 91 following the injection in the SW9 watercourse on April 23, 2005........................................................................................................................78

Figure 9. Uranine dye concentrations in the two creeks that flow into Franks Pond following the tracer injection in the SW9 watercourse on April 23, 2005 ............79

Figure 10. Uranine dye concentrations at two Amabel springs at Sites 114 and 116 following the tracer injection in the SW9 watercourse on April 23, 2005 ............80

Figure 11. Phloxine dye concentrations in the two watercourses that flow into Franks Pond following the tracer injection at SW10 on April 23, 2005 ...........................81

Figure 12. Map illustrating tracing results at various Niagara Escarpment springs following the injection in the SW28 watercourse on May 10, 2005 .....................82

Figure 13. Map of the SW27 spring group..............................................................................83

Figure 14. Uranine dye concentrations at Site 46/47, located just downstream of the SW27 Spring Group, following the injection in the SW28 watercourse on May 10, 2005 .........................................................................................................83

Figure 15. Water levels in Wells BH02-1, BH02-4 and BH03-9 from May 11 to October 28, 2005....................................................................................................84


Marcus J. Buck Karst Solutions Page vii Worthington Groundwater

Figure 16. Correlation between daily precipitation at the Duntroon Expansion property with water levels in the BH03-9 Well from May 11 to October 28, 2005 ............85

Figure 17. Map of the SW2 springs and nearby monitoring wells..........................................86

Figure 18. Spring discharge at the SW2A spring from April 14 to October 28, 2005............87

Figure 19. Electrical conductivity and temperature at the SW2A spring from April to October, 2005.........................................................................................................88

Figure 20. Water levels at the SW2A spring and adjacent wells from April to October, 2005........................................................................................................................89

Figure 21. Electrical conductivity and temperature profiles at the TW04-1 Well on May 12 and May 26, 2005 .....................................................................................90



Figure 24. Electrical conductivity and temperature profiles at the BH03-9 Well on May 12 and May 26, 2005 .....................................................................................93

Figure 25. Electrical conductivity and temperature profiles at Wells BH03-9, TW04-1, TW04-2, and TW04-3 on May 12 and May 26, 2005 ...........................................94

Figure 26. Tracer concentrations at the SW2A spring following dye injections at Wells BH03-9, TW04-3, TW04-1 and TW04-2 on May 12, 2005..................................95


Marcus J. Buck Karst Solutions Page 1 Worthington Groundwater

1.0 Introduction In September 2005, Jagger Hims Limited completed a geological report and Level 2

hydrogeological assessment as technical support for the application to license the Duntroon

Quarry expansion lands under the Aggregate Resources Act for extraction as a Category 2

quarry. The expansion lands are on the north side of Simcoe Road 91, or adjacent to the existing

quarry but on the opposite side of the road. The report provides an assessment of the geology,

groundwater and surface water resources in the vicinity of the existing quarry and the expansion

lands. During their field investigations, karst features were identified that are described in

Section 4.3.2 of their report. This raised questions regarding the influence of karst in the area

and the implications this may have on the proposed quarry with regards to potential impacts to

local groundwater and surface water resources.

Worthington Groundwater and Marcus J. Buck Karst Solutions have undertaken a field

investigation and assessment of karst development that began in the fall of 2004 and continued

through 2005; this report is the result of that investigation. The karst study builds on the

hydrogeological work already completed by Jagger Hims Limited and is intended to supplement

their report. As such, their results are not reiterated here except where relevant to the discussion

of karst.

1.1 Objectives and Scope

The principal objectives of the karst study are to:

1. Characterize the karst in the vicinity of the proposed quarry expansion.

2. Define the role that the karst plays in the regional hydrogeology.

3. Evaluate the potential for adverse impacts from the proposed quarry expansion to

groundwater and surface water resources and their current uses, and to recommend

measures to minimize and mitigate such potential impacts.

The following tasks were included in the scope of work:

1. Field mapping of key karst features in the study area, including dolines, sinking streams

and springs.

2. Measurements of flow at sinking streams and discharge from springs during high flow in

spring and low flow in summer or fall.



3. Groundwater tracer studies from four sinking streams as well as under natural flow

conditions from four boreholes.

4. Borehole testing at six boreholes, including continuous monitoring of water level, and

electrical conductivity (i.e., specific conductance) profiling. Concurrent with the

borehole testing, a nearby spring was monitored continuously for water level, electrical

conductivity and temperature.

1.2 Report Structure

Following the introduction, a synthesis of the results of the karst investigation is presented. The

study methods are summarized in Section 3. Section 4 presents the results of a regional study of

karst that are based primarily on field mapping and surface water monitoring at the sinking

streams and springs. This provides the framework for understanding the development of karst

regionally. Sections 5 to 8 present the results of more detailed work carried out at specific sites:

a groundwater trace at the Manitoulin bench (Section 5), a groundwater trace at the SW9

watercourse (Section 6), a groundwater trace at the SW28 watercourse (Section 7) and

groundwater tracing and borehole testing on the Duntroon expansion property (Section 8). These

detailed studies test the interpretations of karst development identified during the regional study.

Section 9 is the conclusions. All figures are presented at the end of the report, before the

Appendices. A glossary of karst terms used in the text is provided in Appendix A. All

photographs referenced in the text are presented in Appendix B. The data prepared from the

inventory of karst features, surface water monitoring and groundwater tracing are provided in

Appendix C, D and E, respectively.

2.0 Synthesis

2.1 Nature of Karstification in the Duntroon Quarry Area

It has been known for a long time that some limestone and dolostone aquifers become karstified,

a process by which interconnected solutionally-enlarged fractures develop within them. This

results in increased secondary permeability and more rapid groundwater flow. However, it is

only in recent years that tools have become available that allow karstification to be modelled and

its extent predicted. The first breakthrough was the discovery of non-linear kinetics; that

dissolution rates slow remarkably as the calcium and magnesium carbonate concentrations



approach equilibrium with calcite and dolomite. These results allowed the evolution of karst to

be modelled, and the models showed that karstification occurs in all unconfined carbonate

aquifers (Dreybrodt, 1996).

In recent years, sophisticated numerical modelling with large grids has shown that sparsely

fractured rock, low hydraulic gradients, low CaCO3 concentrations in water recharging the

aquifer, and the occurrence of sinking streams all promote the development of focussed flow

within a smaller number of larger conduits. Conversely, highly fractured rock, high hydraulic

gradients, high CaCO3 concentrations in water recharging the aquifer, and the occurrence of

percolation recharge with no sinking streams all promote the development of a distributed

pattern with a larger number of channels and smaller conduit sizes in the bedrock (Romanov et

al., 2003, 2004; Dreybrodt et al., 2005). Of these factors the type of recharge (percolation or

sinking stream) is probably the most important. The numerical modelling to date has assumed

limestone rather than dolostone bedrock; the slower dissolution of dolomite as compared to

calcite suggests that the tendency towards distributed channel patterns with many channels and

smaller conduit sizes will be accentuated in a dolostone aquifer.

The implications for the Duntroon Quarry area are that there should generally be a distributed

pattern of many small conduits because most aquifer recharge is from percolation rather than

concentrated sinking stream recharge. The solution channels should form an integrated network

and this imparts a relatively high hydraulic conductivity to the aquifer. The channel network

discharges to the surface at numerous small springs. In the locations where there is sinking

stream recharge, there should be the tendency for fewer but larger conduits and larger springs or

spring groups.

2.2 Regional Patterns of Aquifer Recharge and Discharge

A regional study of karst features and spring flow was made in order to understand the patterns

of recharge to and discharge from the Amabel aquifer (see Section 4 for full details). The

southern limit of the field investigation was at 21/22 Sideroad, although a few observations were

also made at the Mad River valley at Devil’s Glen, some 4 km to the south of the site. The

northern limit was the edge of the Pretty River valley, some 2 km north of the site. Between

these limits and within 700 to 1400 m of the Niagara Escarpment there is either an absence of



surface streams or the surface streams sink. Thus, this is typical for karst terrain along the

Niagara Escarpment. There are six enclosed drainage basins in this area, with the largest having

an area of 119 hectares. To the west of this area there are surface streams with flow to the west,

though there are some sinking streams as well (Section 4.2).

In the local setting, there are two erosional escarpments located within the geographical extent of

the Niagara Escarpment. The Amabel and Manitoulin Formation dolostones act as the erosion-

resistant cap rocks that mark their crests. Thus, the escarpments are referred to here as the

Amabel and Manitoulin escarpments. Furthermore, the distinct erosional bench that often occurs

on top of the Manitoulin Formation is referred to as the Manitoulin bench, and this forms a

distinct landform that separates the overlying Amabel escarpment from the Manitoulin

escarpment. As referenced in the text or illustrated in figures, the crest of each escarpment is

defined by the sharp break in slope that often occurs above the steepest part of each escarpment

slope. The two escarpments acts as important landmarks for understanding regional groundwater

flow patterns.

In the area studied, 74 springs were found that discharge from the Amabel aquifer, with the

largest having mean discharges of several litres per second (Section 4.1). Many of the streams

descending the Amabel escarpment slope are fed primarily by discharge from the Amabel

aquifer. These spring-fed streams often sink on reaching the Manitoulin bench. A total of 27

sinking streams were recorded on the Manitoulin bench and 57 springs located along the

Manitoulin escarpment slope drained the Manitoulin Formation with the largest having mean

discharges of several litres per second (Section 4.1). Roughly half of the Amabel and Manitoulin

springs have mean discharges ranging from 0.3 to 3 L/s. The remainder are larger or smaller,

with the largest having mean discharges up to about 10 L/s. The size distribution of the springs

is typical of the Niagara Escarpment, although a few larger springs are known elsewhere on the

Niagara Escarpment.

The enclosed drainage basins and sinking streams provide evidence that karst has developed in

the underlying bedrock of the Amabel Formation. In the case of the Manitoulin Formation, the

observations of karst development along the Manitoulin bench suggests that the formation



becomes karstified where the formation outcrops at the surface or where the overburden is

sufficiently thin to permit groundwater infiltration.

2.3 Regional-scale Tracer Testing from Sinking Streams

Four tracer tests were carried out from sinking streams, two of which were on the Amabel

plateau and two were on the Manitoulin bench (Table E-1). Full details are given later in this

report in Sections 5, 6, and 7. The results were generally similar, with the fastest groundwater

pathways to springs having velocities ranging from 500 to 3500 m/day. These velocities are

typical of tracer test velocities in karst, as a compilation of 2877 tracer tests in karst in 31

countries gave a median velocity of 1900 m/day (Worthington et al., 2000).

The tracer was detected at multiple springs in each of the four tracer tests. The tracer test from

the SW9 watercourse, which is at the east end of the expansion property, was the longest trace

with flow paths through the Amabel Formation ranging from 400 m to 700 m. The trace also

had the largest number of positive detections at springs (19 sites). Most of the tracer was

recovered at the SW11 springs. At the time of the tracer test, the SW9 watercourse accounted

for 43% of the flow resurging at the SW11 springs, with the remainder being derived from

percolation recharge. During summer, the SW9 watercourse dries up and all of the discharge

from the SW11 springs is from percolation recharge.

The tracer test from the SW28 watercourse, a smaller sinking stream, showed a flow path

through the Amabel Formation extending 300 m to four individual springs within a spring group

at Site SW27, located at the Niagara Escarpment to the east. A series of measurements under a

variety of flow conditions indicated that the SW28 watercourse accounted for 0% to 50% of the

flow resurging at the SW27 spring group, with the remainder being derived from percolation

recharge. As the flow in the SW28 watercourse increased, its relative contribution to the

discharge at the SW27 spring group also increased.

Although flow from sinking streams accounted for a significant proportion of the flow to a

number of springs, at least during springtime, most recharge to the majority of Amabel springs

was from percolation recharge. Flow measurement data for the Manitoulin bench suggest that

percolation recharge is also important to many of the Manitoulin springs, although groundwater



tracing was not conducted to verify this. In the case of the tracer test from Site 114, the sinking

streams roughly accounted for all of the discharge from the closest springs at the Manitoulin

escarpment.

2.4 Local-scale Investigations

Local-scale investigations were carried out at several locations on the Duntroon Quarry

expansion property. Full details are given later in this report in Section 8. Several investigations

were carried out in the southwest corner of the expansion property where there are four

boreholes within 40 m of the SW2A spring. In addition, continuous water level measurements

were made in three boreholes and at the SW2A spring to determine the magnitude and lag of

short-term variations in water levels. Water level variations of up to a few centimetres were

recorded, with lag of a few hours after rain events, showing that there is rapid percolation

recharge to the aquifer. Variations in electrical conductivity at the SW2A spring reflected the

rapid recharge as well as the flushing out of long residence time matrix water. Vertical profiles

at the four boreholes showed abrupt changes in electrical conductivity and temperature at

specific depths in all four boreholes, reflecting flow into or out of the boreholes at specific

horizons. These presumably reflect flow along solutionally-enlarged bedding planes (Figures

21-25).

Natural gradient tracer testing from the four boreholes to the nearby spring revealed groundwater

velocities that ranged from less than 4 m/day to 1500 m/day. Calculations show that this

corresponds to fracture apertures from less than 0.05 mm to about 4 mm along the traced

pathways from the boreholes to the spring.

2.5 Karstification in the Bedrock Aquifer at the Duntroon Quarry Expansion Lands

The upper few metres of the bedrock at the existing quarry and in wells at the expansion property

is fractured and subsequently weathered by dissolution to give a weathered zone. At the existing

quarry it is shown by a high frequency of horizontal and vertical fractures in the top 1 to 3 m or

more, with the fractures often showing solutional enlargement and evidence of weathering,

including oxidation of iron minerals (Photo 21). In boreholes it is shown by low core recovery

and low rock quality designation (RQD) in the top several metres of bedrock.



Below the top few metres the karstification is less apparent. In some boreholes there are low

core recoveries and low RQD at various depths throughout the Amabel, though these are an

indication of fracturing and not necessarily karstification. Lost circulation is a better sign of

karstification and this was noted in five boreholes on the expansion property, where it occurred

at depths of 0.2 to 9.7 m below the top of the bedrock (Jagger Hims Limited, 2005). Abrupt

changes in temperature or electrical conductivity, as measured on profiles in the boreholes, occur

at a number of horizons throughout the Amabel, and are also an indicator of preferential flow

(Section 8.2.2).

The tracer testing from the four boreholes to the SW2A spring indicates fracture apertures up to

about 4 mm. These small apertures are typical of karst aquifers, where most boreholes intercept

open, solutionally-enlarged fractures with apertures of 0.1 - 10 mm, and where few boreholes

intercept fractures that are larger, or where all the apertures are smaller. Since the recharge in

the expansion property is predominantly by widespread percolation, a distributed pattern of

many small channels and conduits is predicted, and the studies carried out support this model.

The implications are that predictions of flow in the aquifer, such as the modelling by Jagger

Hims Limited (2005, 2007a), are likely to be accurate at a large scale, such as for predicting

overall flow to the quarry or to the escarpment. However, model predictions for transport are

unreliable in karst (Scanlon et al., 2003), so the model should not be relied on for estimates of

travel times.

2.6 Karst Issues Relevant to Quarrying at the Duntroon Quarry Expansion Lands.

2.6.1 Use of Groundwater Recharge Wells

Jagger Hims Limited (2005, 2007a) has anticipated that recharge (injection) wells close to the

quarry may be necessary to mitigate the lower groundwater levels predicted in the surrounding

areas as a result of quarrying. The performance of such wells in a karstic aquifer is a function of

the nature of karstification. With the distributed percolation recharge to the aquifer in the

expansion lands, it is anticipated that many small channels and only a much smaller number of

conduits (i.e., with a diameter > 1cm) will be encountered.



The diameter of conduits is expected to increase in a downgradient direction as groundwater

flow converges towards a spring. Thus, the largest apertures are expected near springs. The

expansion lands span a natural groundwater divide between flow eastward to springs along the

Niagara Escarpment and flow westward to the Beaver River. The western half of the expansion

lands also span a local groundwater divide between flow to the northwest and to the southwest to

wetlands and creeks that join the Beaver River. Consequently, conduit apertures throughout

much of the expansion lands are likely to be small. The largest conduits are likely to be found

immediately upgradient from the largest spring, SW2A. Consequently, this area has the largest

probability of substantial return flow to the quarry from recharge wells. However, if the return

flow were excessive then this could be reduced by localised grouting.

2.6.2 Influence of Karst Conduits on the Drawdown Zone

The presence of conduits converging towards the SW2 springs may have the effect of extending

the influence of the drawdown zone around either of the proposed quarries (i.e., Highland Quarry

or the Duntroon Quarry expansion). The conduit networks surrounding each spring strongly

influence the groundwater elevations within their springsheds. However, this effect should be

largely limited to the extent of the springshed for each of the two springs. The springshed for the

SW2B spring is entirely contained within the expansion property. Therefore, drawdown effects

should not be exacerbated outside of the proposed quarry as a result of conduits there. On the

other hand, the SW2A springshed extends to either side of Grey County Road 31. Within its

springshed, the SW2A spring clearly acts as the local base level as indicated by the water

elevations observed in the nearby boreholes. As groundwater flow diminishes during the dry

season, the groundwater elevations converge towards the elevation of the spring. If only one of

the proposed quarries proceeds, then the drawdown effects will likely be propagated along

conduits across Grey County Road 31. In this case, injection wells may not be effective at

maintaining water levels and localized grouting may be required. However, if both quarries

proceed, then the conduits should not exacerbate drawdown effects because the influence of the

conduits leading to the SW2A spring should not extend outside of the SW2A springshed, and the

springshed is entirely contained within the two proposed quarry properties.



2.6.3 Potential Impacts to the SW2 Springs

The SW2B spring and its springshed are entirely contained within the proposed Duntroon Quarry

expansion. Therefore, this spring will be completed removed as a result of quarrying and will no

longer contribute flow to the surface watercourse at SW2.

The proposed quarries on either side of Grey County Road 31 (i.e., Highland Quarry and

Duntroon Quarry expansion) also have the potential to impact the SW2A spring. This spring

derives its groundwater recharge from a catchment area that extends across portions of each of

the proposed quarries. Therefore, quarrying on either side of Grey County Road 31 at either of

the proposed quarries will lead to loss of recharge for the SW2A spring. Furthermore, quarrying

at either of the proposed quarries may lead to complete loss of discharge from the SW2A spring

as a result of the diversion of groundwater flow along conduits intersected by quarrying. In the

case of the Duntroon Quarry expansion, the loss of spring discharge could be mitigated by

discharging excess quarry water into Wetland Unit 6 of the Rob Roy PSW complex during

dewatering, as proposed by Jagger Hims Limited (2005). Once the Duntroon Quarry expansion

is complete and the quarry fills with water, the lake level will not be sufficiently high to permit

seasonal flow into the SW2 watercourse. However, the final lake in the existing quarry will

outflow seasonally into Wetland Unit 6 and any impacts to groundwater beneath the wetland will

be buffered by the final lake in the existing quarry (Jagger Hims Limited, 2007a).

2.6.4 Potential Leakage between the Proposed Quarries

The conduits that currently convey groundwater to the SW2A spring may later create permeable

pathways between the two proposed quarries (Highland Quarry and Duntroon Quarry

expansion), if both quarries proceed. This could cause the final lake levels to equalize in

elevation if there is excessive leakage. On the other hand, if the conduits are generally shallow

(above 512 m a.s.l.), then there may be little leakage along the conduits between the final lakes.

Localized grouting of the intervening bedrock or other mitigation measures might be required if

excessive leakage between the quarries becomes problematic.

2.6.5 Potential Impacts to Niagara Escarpment Springs

Impacts to the majority of springs along the Niagara Escarpment are likely to be negligible.

With the exception of the SW27 and SW11 springs, the Amabel springs located near the



expansion property derive most of their recharge from widespread infiltration across a broad

band of land adjacent to the top of the Niagara Escarpment. It is concluded that these springs

will not exhibit any significant loss of discharge as a result of the proposed quarrying at the

expansion lands. Only those springs located closest to the quarry will exhibit any reduction in

discharge, and even these will still be maintained by percolation recharge. Furthermore, their

recharge should be fully restored once lakes are established in the quarries.

The SW27 and SW11 springs receive part of their recharge from sinking streams. As indicated

by the groundwater tracing, the SW27 springs are the resurgences for the sinking stream at

SW28, and during peak flows in the spring they receive much of their recharge from the sinking

stream. However, the surface catchment for the SW28 watercourse is outside the expansion

lands and will not be affected by the proposed quarry there. Therefore, there will not be any loss

of sinking stream recharge at these springs. Furthermore, these springs will continue to be

maintained by widespread percolation recharge.

The springs most likely to be impacted by the proposed quarry expansion are the SW11 springs.

These are the principal resurgences for the sinking stream located at the east end of the

expansion property, the SW9 watercourse. Groundwater tracing indicates that after sinking, this

stream flows rapidly in the subsurface and resurges at 19 springs located along the Niagara

Escarpment, with roughly 90% of the flow resurging at the SW11 springs. Despite the

significant component of recharge from the sinking stream, the SW11 springs receive an even

greater contribution from widespread percolation recharge on the Amabel plateau, and it is this

percolation recharge that maintains these springs throughout the dry season. Therefore, with

respect to the proposed quarry at the expansion property, it can be concluded that even with a

significant loss of flow in the SW9 watercourse as a result of quarrying, the SW11 springs will

still be maintained by the percolation recharge.

2.6.6 Discharge of Quarry Water to the SW9 Watercourse

Dewatering of the proposed expansion quarry will occur during extraction phases 1, 2, and 3.

Jagger Hims Limited (2007a, Table 4-42) uses computer modelling to determine that the

dewatering will reach an estimated maximum of 19.8 L/s during Phase 3, and that the maximum

dewatering rate will be less than this with concurrent dewatering of the proposed Highland



Quarry. The quarry water will be used for operational needs and the excess will be discharged

into tributaries of the west-flowing Beaver River as well as to the eastward-flowing SW9

watercourse, which provides flow to Batteaux Creek to the east.

From monthly measurements at station SW9 between May 2003 and August 2007, the flow

ranged from zero in the summer months to a maximum of 42 L/s on April 11, 2005 (Jagger Hims

Limited, 2007b). On April 25, 2005, the flow was 39 L/s, and this water sank into the ground

over a distance of 220 m. However, the watercourse extends for at least 250 m farther and it is

clear that very occasionally there must be flows that are substantially more than 39 L/s.

However, the monthly data show that flow is 7 L/s or less for more than 95% of the time. The

water that sinks along the SW9 watercourse was traced to 19 sites with roughly 90% flowing to

the SW11 springs, where at the time of the tracing it accounted for only 43% of the total

discharge. The remaining discharge is from percolation recharge to the aquifer. The flow

resulting from the sinking stream recharge would be reduced during the period that the quarry is

actively dewatering. Thus, the addition of the order of 10 L/s to the creek from dewatering

would help sustain flow in the creek as well as at the SW11 springs. This amount of water

would represent only a small fraction of the existing maximum flows currently observed in the

SW9 watercourse. The excess quarry water could also be used to maintain water levels in two

unevaluated wetlands located along the watercourse, ANSI A and ANSI B, as may be required

seasonally. Any loss in surface flow in the SW9 watercourse could be roughly balanced by the

pumping of excess water from the dewatering operations into the SW9 watercourse. Thus the

net mean discharge from the SW11 springs would be little changed during the period that the

quarry is dewatered. Once the quarry is complete and fills with water, some of the excess water

from the quarry will flow seasonally into the SW9 watercourse (Jagger Hims Limited, 2007a).

Any minor thermal effects at the Amabel aquifer springs as a result of discharging excess quarry

water into the SW9 watercourse would not affect downstream fisheries because after discharging

from the springs the water temperature rapidly approaches surface temperature while flowing

down the talus slope, and because the in-line pond on W. Franks property has a pronounced

thermal impact that overwhelms any temperature effects farther upstream (Jagger Hims Ltd.,

2007a, b).



3.0 Study Methodology Initial site visits were conducted by M. Buck and S. Worthington in 2004. A detailed field

investigation was planned based on the initial observations and conducted from August 2004 to

November 2005.

Some of the field mapping, surface water monitoring and groundwater tracing was conducted in

Nottawasaga Lookout Provincial Park. This work was conducted under a research permit issued

by Ontario Parks (Central Zone).

3.1 Karst Study Area

The detailed study area was defined based on the initial observations. This area encompasses the

Niagara Escarpment extending northward from the 21/22 Sideroad to the Grey-Simcoe County

line, including the adjacent lands above the Escarpment on the east side of the County line.

Thus, the Niagara Escarpment was examined in detail between 2 km north and 2 km south of the

expansion lands.

3.2 Field Mapping and Surface Water Monitoring

Within the study area, field mapping was focused on areas where karst features are most likely to

occur. The principal features mapped are dolines, sinking and losing streams, and springs.

Small-scale features such as karren were not recorded. A group of dolines were observed close

to the prominent cliff along the Niagara Escarpment north of Simcoe Road 91; however, a

detailed inventory was not conducted here because these dolines are located beyond the

influence of the proposed quarrying. All other key karst features were documented and these are

classified and described in Appendix C. Generally, most features were located on a map using a

handheld GPS receiver. The accuracy indicated by the unit was typically ± 5 to 12 m, and a few

repeat measurements on different occasions were consistent with this reported accuracy. In

forested areas, most measurements were taken during spring prior to the emergence of the forest

canopy. This minimized interference and improved signal reception. More detailed ground

surveys were conducted at a few locations where higher resolution mapping was required,

specifically where groundwater tracing was conducted. The ground surveys were conducted

with a Suunto compass and inclinometer and a fibreglass tape, and the surveys were



georeferenced with GPS measurements. The catchment divides for any surface drainage basins

described in the text were defined by the surface topography as indicated by contours on

1:10,000-scale Ontario Base Maps. Two of the Jagger Hims Limited surface water monitoring

sites, SW9 and SW28, are located along watercourses that are referred to repeatedly in the text.

These small watercourses do not have names and are referred to as the SW9 and SW28

watercourses.

Surface water measurements were made at watercourses and springs throughout the study area,

and included measurements of flow, temperature and electrical conductivity. The specific

methods and estimated accuracy for flow measurements are indicated in Appendix D.

Temperature and electrical conductivity were measured using a WTB portable conductivity

meter (Model 340i). The accuracy reported by the manufacturer is ± 0.1°C for temperature and

± 0.5% of the measured value for electrical conductivity. The conductivity was corrected to a

reference temperature of 25°C. The measurements were conducted in April or May when flows

were high, and were repeated during summer or fall when flows were at a minimum. Many of

the springs are located at the head of the many small watercourses located along the Niagara

Escarpment slope, and groundwater discharge was often observed over a distance of several

metres to tens of metres. At many of these sites, temperature and conductivity were measured as

close as possible to where the groundwater first emerges, but discharge was measured farther

downstream to better determine the total discharge. In addition to measurements within the

detailed study area, streamflow measurements were also conducted along the roads that

encompass the perimeter of the study area, first on October 26, 2004, then again on May 16-17,

2005. These measurements were designed to identify any large springs outside of the detailed

study area that might be relevant to the hydrogeology of the study area. All of the surface water

monitoring locations are described in Appendix C and the measurement data are listed in

Appendix D.

Figure 1 (back pocket) is a regional map indicating the location of karst features and surface

water monitoring points. However, due to scale effects, some of the features and monitoring

points could only be illustrated on more detailed maps (Figure 3, 13 and 17). Each feature and

surface water monitoring site was identified using a unique number between 1 and 226 (for

example: “Site 43”). In cases where several interrelated features were located in close proximity,



a number was used to identify the group and lowercase alphabetic suffixes were used to

distinguish the individual features. Similarly, the location of surface water monitoring sites

located at the junction of two or more tributaries was identified with the same number but the

measurements for each tributary were distinguished using alphabetic suffixes, such as “e” for

east tributary. In a few cases where additional features were added, uppercase alphabetic

suffixes were added to distinguish these additional locations.

3.3 Climate Monitoring

Climate data were collected every two minutes from May 9 to November 18, 2005 using a Hobo

Micro Station data logger. The weather station was mounted on a two-metre tripod and was

located in a sizeable field near the east end of the expansion lands (UTM location, NAD27:

560390 m E., 4915174 m N; Photo 20). The attached sensors recorded rainfall, solar radiation,

temperature and relative humidity. The data were post-processed to calculate hourly means and

total precipitation for one hour intervals and then again to calculate daily data.

On October 2, the equipment was checked in the field and a bird nest (American robin) was

discovered inside the top of the rain gauge. This was likely constructed shortly after the weather

station was installed in May. As a result, the timing of precipitation events prior to October 2

should be accurate but the amount of rainfall recorded may be significantly reduced, and small

precipitation events may not have been detected at all. Nevertheless, the timing of the larger

rainfall events proved useful for comparison with groundwater discharge data at springs and

water elevation records for boreholes.

3.4 Borehole Monitoring

Water level measurements with a 15-minute frequency were made at BH02-1, BH03-9 and at the

SW2A spring with Solinst Leveloggers, and at BH02-4 with a Heron Instruments Dipper-log. In

addition, a Solinst Barologger was used for correcting for changes in atmospheric pressure.

Campbell Scientific electrical conductivity/temperature probes and data loggers were used for

borehole profiling and for monitoring the spring at SW2A.



3.5 Groundwater Tracing

Groundwater tracing was conducted at four wells and at four sinking streams. For each

injection at the wells, the dye (previously diluted into four litres of water) was injected by

siphoning it down tubing to below the water table. A further 10 litres of groundwater from the

nearby spring (SW2A) was flushed down the tubing to ensure that all the dye was flushed from

the container and tubing, and a further 70 litres of water was added to each well to ensure that the

dye was flushed into the bedrock. The amount of dye injected was pre-determined from two

equations which give good predictions of tracer concentrations at springs (Worthington and

Smart, 2003). At the sinking streams, all of the flow was observed sinking either at a doline or

gradually into the channel beds.

The tracers used were the fluorescent dyes uranine (also known as sodium fluorescein; Colour

Index 45350) and phloxine B, Colour Index 45410). Both dyes have very low toxicity and are

approved for use in drugs in Canada (Food and Drugs Act, Section C.01.040.2). Water samples

were collected at springs where the dye might flow to. Collection of water samples was either by

hand or using an ISCO Model 3700C 24-bottle automatic water sampler. Samples were

analyzed with a Turner Designs Picofluor filter fluorometer, which has two channels and can

measure concentrations of two different dyes injected at the same time. The detection limit was

found to be about 0.2 parts per billion for uranine and 0.8 parts per billion for phloxine B and

was due to background concentrations of natural organic acids from decayed vegetation.

Samples were analyzed on-site in near real time on a Turner Designs Picofluor filter fluorometer.

The analysis on-site gave approximate results that were ideal for planning sample collection and

subsequent tracer injections. After the completion of the tracer testing all samples were stored at

4°C and later re-analyzed on the filter fluorometer after equilibrating to room temperature for 24

hours. All groundwater tracing data are listed in Appendix E.

The MOE was informed of the groundwater tracing program in advance. One trace was

conducted within Nottawasaga Lookout Provincial Park and a permit was obtained from the

Ministry of Natural Resources in advance to carry out this work. In addition, in areas where the

tracing was conducted near residential properties, a letter was sent to the residents informing

them of the planned groundwater tracing.



4.0 Regional Investigation of Karst The landscape within the study area is dominated by the Niagara Escarpment, an erosional

escarpment that marks the east edge of a regional cuesta. The dolostone of the Amabel

Formation forms the erosion-resistant cap rock of the cuesta and this dolostone often outcrops in

cliffs at or near the brow of the escarpment. To the west, the cuesta surface slopes very gently to

the southwest. For simplicity, the tablelands lying west of the Niagara Escarpment are referred

to as the Amabel plateau. A prominent erosional bench has formed partway down the Niagara

Escarpment slope on top of the dolostone of the Manitoulin Formation. It formed as a result of

preferential erosion of the overlying shale of the Cabot Head Formation. The Manitoulin

dolostone also forms an erosion-resistant cap rock that marks the crest of a smaller escarpment.

Thus, the Niagara Escarpment is marked by two distinct erosional escarpments, the Amabel and

Manitoulin, separated by the Manitoulin bench.

The Amabel plateau and the Manitoulin bench are the focus of the karst study since these are the

areas underlain by soluble carbonate bedrock. The Cabot Head Formation occurs between the

Amabel and Manitoulin Formations. It is predominantly shale and is expected to act as an

aquitard that isolates the two dolostone aquifers. The Manitoulin Formation is underlain by the

Whirlpool Formation, a quartz sandstone that is about 2 m thick. The Whirlpool, in turn, is

underlain by the Queenston and Georgian Bay Formations that consist largely of shales with

interbeds of siltstone and carbonate. Any downward movement of groundwater will be

negligible as a result of these thick sequences of shale with low permeability.

Section 4.1 provides a general introduction to the types of karst features present in the study area.

Sections 4.2 and 4.3 summarize the regional observations of karst development on the Amabel

plateau and Manitoulin bench, respectively. Finally, Section 4.4 summarizes the results of flow

measurements conducted around the perimeter of the study area. The remainder of the report

focuses on specific areas where more detailed work was conducted.

4.1 Regional Karst Geomorphology and Hydrology

Karst terrain is a landscape with distinctive hydrology and landforms arising from a combination

of high rock solubility and well developed secondary permeability. Karst is most common in

limestone, dolostone and gypsum, but can develop in any soluble rock. Solution of bedrock



creates a unique sculpturing of exposed bedrock surfaces with a variety of diverse forms, known

collectively as karren. More importantly, solutional enhancement of fractures and bedding

planes in the bedrock forms interconnected channels, conduits and caves that increase secondary

permeability. These self-organizing channel networks form continuous paths to springs that

potentially permit high flow velocities similar to those of surface streams. These subsurface

channels have the capacity to transport sediment introduced with infiltrating water. Once

channel networks are established, many of the typical features of karst can begin to form, such as

dolines, sinking streams, dry valleys, closed depressions, caves and springs. It is the

establishment of these interconnected channel networks that creates a karst aquifer. A karst

aquifer is defined here is an aquifer with solutionally enhanced secondary permeability, chiefly

characterized by rapid groundwater flow velocities and the occurrence of continuous flow paths

along channels that direct groundwater flow from recharge areas to springs.

Figure 1 (back pocket) is a regional map illustrating the distribution of karst features mapped in

the area. As is common at many areas along the Niagara Escarpment, the prevalence of karst

features is often greatest adjacent to the Escarpment brow where overburden is often thin and

hydraulic gradients are steep. The entire plateau here is underlain by dolostone of the Amabel

Formation, which is known to be highly susceptible to karstification (e.g., Cowell, 1978). There

are few observations of karst development in the Fossil Hill Formation, the dolostone that

directly underlies the Amabel. However, karst is developed in the lateral equivalent of the Fossil

Hill at Waterdown, Ontario. There, the argillaceous dolostone of the Reynales Formation

underlies the Amabel Formation and a karstic aquifer is well developed in both units (Ecoplans

Limited, 2005). In the Duntroon area, the Fossil Hill Formation is not exposed at the surface and

no direct observations were made. For simplicity, the aquifer within the Amabel and Fossil Hill

Formation dolostones will be referred to collectively as the Amabel aquifer.

The most prevalent karst features mapped in the study area are dolines, sinking streams and

springs. Table 1 presents a classification of the karst features and lists their numbers. A more

detailed classification is presented in Table C-1 in Appendix C. A general introduction to the

karst features found locally follows:



Table 1. Classification of features inventoried during the field investigation of karst.

N is the number of features associated with either the Amabel or the Manitoulin Formations.

Feature NAmabel NManit. Explanation

Spring 74 57 Relict, intermittent and perennial springs.

Sinkpoint 7 0 Discrete point at which streamflow is lost at a doline, or at a discrete point along a watercourse.

Sinking stream with discrete sinkpoint(s)

3 3 A watercourse that loses flow to the subsurface at a discrete sinkpoint, often at a doline.

Sinking stream that loses flow gradually along a losing reach

3 24 A watercourse that loses flow to the subsurface by gradual infiltration along a “losing reach”. The infiltration likely occurs where the soil mantle is thin permitting recharge to the underlying karst aquifer.

Dry valley 3 0 A relict fluvial valley that no longer has any surface flow, typically marked by dolines along its length.

Suffosion doline 19 8 Doline formed in the soil mantle.

Monitoring point (surface water)

51 62 Location at a pond or along a surface watercourse where discharge, temperature, electrical conductivity or fluorescence were measured.

Springs utilized for water supply (dug well, cistern)

7 4 A dug well utilizing well tiles or a cistern designed to collect spring water for use as a drinking water supply or for livestock.

Other uses of springs (ponds, pipes)

6 0 Either an artificial pond constructed at a spring, or the presence of a plastic or steel pipe at a spring suggesting former use as a water supply. The intended use is generally unknown.

Karren are the small-scale dissolutional features such as pits, runnels and solution grooves found

on the dolostone surfaces. The observed karren show little relief, generally extending a few

millimetres to a few tens of centimetres into the bedrock as is typical for the Amabel dolostone

elsewhere in Ontario. These small-scale features were not mapped. Karren are present wherever

dolostone is exposed, except in quarries and on some cliff faces where the dolostone has only

recently been exposed. Observations suggest that there are relatively few exposures of dolostone

in the area and most of these are the cliffs located near the crest of the Amabel and Manitoulin

escarpments. A few other small outcrops exist on steep hill slopes where erosion has stripped

the soil exposing the underlying bedrock. Solutionally sculptured boulders of dolostone can

sometimes be found on hilltops where the soil mantle may be thin. Excavations at the Duntroon



quarry demonstrate that the glacial deposits are often quite thin at these locations. Pluhar and

Ford (1970) described typical karren found elsewhere on the Niagara Escarpment.

Dolines are closed karst depressions that are a diagnostic landform of karst. They are more often

called sinkholes in North American literature. All of the dolines in the area would be classified

as suffosion dolines, as described by Ford and Williams (1989, p. 412). Suffosion dolines are the

depressions formed in the unconsolidated glacial sediment that occurs overlies the dolostone

bedrock in the region. They do not require the development of depressions in the underlying

bedrock. However, infiltrating water must be directed to solution channels within the bedrock

that act as drains. Infiltrating water washes soil into the drains. Thus, the drains must be

interconnected to highly efficient pathways for sediment transport that ultimately transport the

sediment to springs. The surface depressions can form either by gradual subsidence of the soil

cover (Photos 1 and 2), or by sudden collapse after soil piping creates a cavity in the soil above

the bedrock drain (Photo 3). White (1988, p. 27) described such dolines as cover subsidence or

cover collapse sinkholes, depending on the mechanism of formation and there are examples of

both in the area. The distinction made between small and large dolines in this study is arbitrary.

Since most of the dolines are small, this distinction serves to highlight the location of larger

dolines on the maps, a few of which are substantial in size.

Although suffosion dolines are common in the area, there are also larger closed depressions

found on the thick glacial deposits that occur in the area as broad, hummocky hills and ridges.

These depressions are as much as 6 m deep and may be over 30 m across, and one example

contained a seasonal pond. These are glacial kettles and good examples can be found towards

the west end of 26/27 Sideroad and to the south of Singhampton Cave. In contrast, the suffosion

dolines are smaller and tend to be located along the base of valleys or where the overburden is

thin.

There are a number of sinking streams in the area. In some examples, the surface watercourses

terminate abruptly at dolines where all of the surface flow is captured into the underlying karst

aquifer (e.g., Camarthen Wetland Tributary sinks at SW26). These provide a clear indication of

karst development. However, the majority of the sinking streams do not sink at dolines but lose

flow by infiltration through the glacial sediment (Photos 4 to 6). There are examples where all of



the infiltration occurs at discrete locations. However, flow is more often lost gradually along a

“losing reach” that may extend for tens to hundreds of metres. For these streams, the

relationship to karst is subtle and cannot be demonstrated unequivocally without groundwater

tracing.

Springs are quite numerous along the Amabel and Manitoulin escarpments but can also be found

on the Amabel plateau. There are also artificial examples within the existing quarry (Photos 22,

23, 24). The majority of the springs occur as discrete concentrations of groundwater discharging

from the Amabel and Manitoulin aquifers. Although very few were observed issuing directly

from bedrock, those that do clearly emerge from solutionally widened conduits (Photos 11 and

13). Most of the springs issue from the base of talus slopes or from thin overburden overlying

the bedrock (Photos 10, 12, 14, 17). In the latter case, the springs occasionally issue from soil

pipes (Photo 9). However, the local geology dictates that most of these likely originate as

springs issuing from the dolostone aquifers. The localized concentrations of flow suggest that

the springs are discharging from karst conduits, to which groundwater flow is focussed from

small to mid-sized springsheds. The springs are not evenly distributed, and in many cases they

are clustered together in close proximity. This is common in karst. Groundwater flow may be

focused toward embayments along the Niagara Escarpment because of steeper hydraulic

gradients towards these areas. However, in many cases the clustering of springs signifies the

tendency for divergent flow to distributary springs. Some of the closely spaced springs that

appear to be interrelated are referred to here as “spring groups”. Within the spring groups,

individual springs may act as underflow or overflow springs, depending on their elevations and

the geometry of the conduit networks that feed them.

Only three of the springs inventoried are unlikely to be associated with the Amabel or

Manitoulin aquifers. One of these at Site 11 likely discharges from the glacial sediment since it

occurs at the edge of a prominent ridge with kettles. The other two springs are located at Sites

204 and 205 and these occur well below the elevation of the Manitoulin Formation. These are

both small springs and their origin is unknown, although they may be discharging from an

overburden aquifer.



Discharge measurements were conducted at most springs during high flow in spring and low

flow in summer or fall such that the typical range of discharge at each spring is known. Table 2

lists the number of springs identified for each aquifer for which there are sufficient data for their

size classification using the scheme of Meinzer (1923, p. 53). Using his metric classification,

springs are classified according to their median discharge into one of eight magnitudes, with

“magnitude 1” being the largest (median discharge greater than 10 m3/s), and “magnitude 8”

being the smallest (median discharge less than 10 cm3/s).

Table 2. Number and size of springs and spring groups that occur in each aquifer.

Aquifer Spring Magnitude *

Mean Discharge (L/s)

Frequency (by range)

Frequency (by magnitude)

31.6 - 100 0 4

10 - 31.6 1

1

3.16 - 10 8 5

1 - 3.16 11

19

0.316 - 1 17 6

0.1 - 0.316 6

23

0.0316 - 0.1 2

Amabel

7

0.01 - 0.0316 2

4

3.16 - 10 7 5

1 - 3.16 10

17

0.316 - 1 11 6

0.1 - 0.316 7

18

0.0316 - 0.1 7

Manitoulin

7

0.01 - 0.0316 0

7

0.316 - 1 0 Overburden 6

0.1 - 0.316 1

1

3.16 - 10 0 5

1 - 3.16 1

1

0.316 - 1 1

Unknown

6

0.1 - 0.316 0

1

* Spring magnitude based on the metric system classification of Meinzer (1923, p. 53) using mean discharge.



None of the springs in the study area is larger than magnitude 4. However, there are a number of

mid-sized springs with peak discharges ranging up to about 60 L/s. The size distribution of

Amabel and Manitoulin springs is illustrated in Figure 2 in half-magnitude intervals. A few of

the springs were grouped, in part because of better availability of data for these spring groups,

but also because those springs are interrelated. The Amabel and Manitoulin aquifers have 19 and

17 springs of magnitude 5, respectively. The spring group at Site 161 is classified as magnitude

4 but this may be overestimated because it is based on the average of only two measurements,

during the spring and fall. Similarly, the majority of other springs are classified using an average

of only two measurements during high and low flow conditions. As such, the magnitude of some

of the springs is overestimated. Nevertheless, good data are available for most of the key springs

and the overall classification is representative.

The discharge measurements made during high and low flow conditions also give an indication

of the variability of discharge at the springs, and the nature of groundwater recharge for the

springs. Those with highly variable discharge, especially those that dry up during summer, are

more likely fed by sinking stream recharge (i.e., concentrated recharge from sinking streams),

whereas those with less variable discharge that continue flowing throughout the summer have a

greater component of percolation recharge (i.e., widespread, diffuse recharge infiltrating either

directly into bedrock or through the soil where the karst is mantled).

Although the majority of springs are interpreted to be karstic, there are four possible exceptions.

Three of these are at Sites 11, 204 and 205, all of which may be discharging from overburden

aquifers. There is also an area about 20 m wide that extends about 200 m along the base of the

Manitoulin escarpment at Site 75 where the ground is saturated much of the year. This appears

to be fed by widespread seepage from the Manitoulin escarpment. This is uncharacteristic, since

at most sites the discharge is focused at discrete springs.

In addition to karst features, a few incidental observations were made of dug wells, cisterns,

artificial ponds and abandoned pipes all located at springs that indicate current and former

utilization of springs (Photos 10, 18, 19). Table 3 lists the number of springs observed where

there is some evidence for use. The majority are dug wells and cisterns. Seven of these are

located along the Amabel escarpment and the remaining four along the Manitoulin escarpment.



These were not investigated to determine whether or not they are still utilized, although most

appeared to be functional. In addition, three sites were identified at or just downstream from

springs where depressions were dug, and earth dams constructed from the excavated soil, to

retain water in a pond. None of these are still utilized and their intended uses are unknown.

Finally, steel or plastic pipes were observed at or downstream from three springs suggesting

some attempt to utilize them as water supplies. However, these are no longer in use and their

former uses are unknown.

Table 3. Observed utilizations of springs.

Aquifer Evidence for use Number

Dug well or cistern 7

Artificial pond with an earth dam constructed from excavated soil

2

Amabel, Fossil Hill (dolostone)

Steel or plastic pipe found near spring 3

Manitoulin (dolostone) Dug well or cistern 4

Overburden (glacial sediment) Artificial pond with an earth dam constructed from excavated soil

1

At least four of the springs are currently utilized as water supplies for residents or for agriculture.

These all occur where potable groundwater may be difficult to obtain otherwise. Although

springs are not widely used today in the vicinity, they probably played a more significant role in

the past when these areas were more extensively farmed. The opportunistic use of perennial

springs would have provided a low cost source of potable water.

4.2 Karst Development on the Amabel Plateau

The Amabel plateau is principally a glaciated landscape where karst landforms are neither

abundant nor obvious. The plateau is mantled with a blanket of glacial sediment. Data suggest

that this sediment varies from less than a metre up to nearly 10 metres in thickness. The paucity

of obvious karst landforms can be attributed to the glacial sediment mantle. Karren are limited

to the few areas where bedrock is exposed. Other karst landforms most likely occur where the

soil mantle is thin, probably less than two or three metres thick. Suffosion dolines are common



within 50 m of the prominent cliff located to the north of County Road 91 along the Niagara

Escarpment. There, the overburden is thin and stress-release has opened up fractures to permit

rapid development of karst. However, only 19 dolines were identified elsewhere on the Amabel

plateau. Additional evidence for karst development comes from the area’s hydrology. A total of

73 springs emerge from either the Amabel or Fossil Hill Formations along the Amabel

escarpment. Their presence indicates that a karst aquifer is developed. The groundwater for

these springs is recharged from the adjacent Amabel plateau. Within a 700 to 1400 metre-wide

band on the plateau adjacent to the escarpment, there is either an absence of surface streams or

the surface streams sink. A series of drainage basins with internal drainage are delineated within

this band, as illustrated in Figure 1. Their characteristics and surface area are summarized in

Table 4. When interpreted together with the spring data, they are indicative of an underlying

karst aquifer.

Table 4. Karst basins identified on the Amabel plateau.

Type Karst Basin

Surface Area (ha) Holokarst Fluvokarst

Key Features

A 66 ●

●

North end: a dry valley with dolines; a relict fluvial gully descending the Amabel escarpment is the former surface drainage outlet. South end: a pond located at the center has no surface outlet.

B 55 ● SW28 watercourse sinks at an ephemeral pond at Site 7.

C 68 ● SW9 watercourse gradually sinks downstream from Site 13B.

D 23 ● No surface watercourses or karst features.

E 25 ● An ephemeral stream originating from the overflow spring at SW2B sinks at large dolines. The discharge from this basin occurs at two large springs, SW2B and SW2A.

F 119 ● The Camarthen Wetland is drained by an intermittent watercourse that sinks at the SW26 doline.

The six karst basins were defined based on surface topography. Although any watercourses

within the basins were investigated in the field, the perimeters were delineated from topographic



contours on 1:10,000-scale Ontario Base Maps. As is typical of karst, the springsheds or

subsurface catchments for the numerous Amabel springs may not always correspond to the

surface catchments defined by topography. The springsheds can only be determined accurately

through subsurface or tracing data. A description of each karst basin follows.

Basin A is 66 ha in area and occupies a large portion of the tablelands within Nottawasaga

Lookout Provincial Park. A broad, shallow valley extends across this drainage basin along the

northeast edge. This valley continues into Basin B, although the two basins are separated by a

slight rise along the valley. There are no active watercourses in Basin A, although there is a

shallow pond within the valley that is probably seasonal. A ditch has been excavated that

extends from this pond to about 100 m to the south where it ends (Photo 15). The ditch may

have been excavated to drain the pond. There is no other surface outlet for this pond. Farther

northwest, there is a series of small to large suffosion dolines that occur along the base of the

valley. Their presence and the lack of any surface channels indicate that this is a karst dry

valley. A relict fluvial gully extends from just west of the doline at Site 1 to the Niagara

Escarpment slope. It is initially quite shallow but increasingly becomes incised as it approaches

the Amabel escarpment where it is 35 m wide and 4.5 m deep (Photo 16). It continues down the

escarpment slope to an elevation of about 460 m a.s.l. where it ends rather abruptly. This

suggests that the stream that once eroded this gully may have entered a proglacial lake at that

elevation. If so, then the development of subsurface drainage must have occurred quite early

while this lake was still present. Analysis of discharge from springs along the Niagara

Escarpment suggests that groundwater flow in this basin is likely towards the northwest to a

series of springs at Sites 25, 26, 27, 29, 30 and 31. Although there are numerous springs located

farther to the east, their combined discharge is insufficient to account for all of the groundwater

recharge from this basin.

Basin B is 55 ha in area. Surface runoff collects in the centre of the basin during spring runoff to

form an area with a mosaic of numerous shallow pools, and flow is from pool to pool without

any defined channel. This seasonally flooded area has a surface area of about 2 ha and is drained

by the SW28 watercourse, a stream that normally sinks into the overburden beneath an

ephemeral pond at Site 7. Groundwater tracing indicates that the sinking stream resurges at a

series of springs at SW27, located 300 m to the east. During high flow, the stream overflows the



pond and continues flowing on the surface towards the Amabel escarpment to the east.

Groundwater tracing was conducted there and the results are reported in Section 7.

Basin C is 68 ha in area. A series of shallow ponds and unevaluated wetlands (Stantec

Consulting, 2005) occupy the base of a broad, shallow valley extending across the catchment.

These are drained by the SW9 watercourse, an intermittent stream that gradually sinks into the

overburden downstream from Site 13B. During high flow, the watercourse extends at least 250

m beyond Site 14D. It was not observed flowing any farther than this during this study.

Groundwater tracing indicates that the stream resurges primarily at the SW11 spring group. A

detailed investigation was conducted and the results are reported in Section 6.

Basin D is a closed depression with a surface area of 23 ha that is located almost entirely within

the expansion lands. There are no surface watercourses, although shallow pools form at the

lowest points during spring thaw. The base of the depression is entirely mantled in glacial

deposits and no dolines were found. Since this area is cultivated, it is possible that any suffosion

dolines may have been deliberately filled, and small dolines may have been eradicated by tilling.

Observations elsewhere in Ontario indicate that refuse and fieldstones are commonly dumped

into suffosion dolines on agricultural lands, and small dolines are often buried as a result of

tilling. Any surface runoff must infiltrate into the overburden. The direction of groundwater

flow from this basin is not known. However, it likely contributes some groundwater to each of

the surrounding catchments.

Basin E is 25 ha in area. It is located at the southwest corner of the expansion lands but also

extends across Grey County Road 31 onto the Highland Quarry property. An ephemeral

watercourse extends from the overflow spring at SW2B to the perennial spring at SW2A. The

watercourse continues from there southward to the swamp on the south side of Simcoe Road 91.

This swamp is Unit 6 of the Rob Roy Swamp PSW (Stantec Consulting, 2005). Some of the

flow in the watercourse sinks at two large dolines located just downstream from the SW2B

spring. Water infiltrating within Karst Basin E is interpreted to discharge from the SW2B and

SW2A springs. Their combined discharges are measured weekly at SW2 by Jagger Hims

Limited. A detailed investigation was carried out and the results are reported in Section 8.



Basin F is 119 ha in area. An unevaluated wetland, the Camarthen Wetland (Stantec Consulting,

2005) occupies the centre of this basin. It has a surface area of about 30 ha and is drained by the

Camarthen Wetland Tributary at its south end. This intermittent watercourse flows about 200 m

to the southeast where it sinks into the large doline at SW26. This doline has not been observed

overflowing. The sinking stream and its subsurface continuation are considered further in

Section 4.2.1.

The six drainage basins can be categorized as either holokarst or fluviokarst, depending on the

presence or absence of any surface streams. Cowell and Ford (1983) used this classification for

the Bruce Peninsula, Ontario, to characterize karst development there. The northern portion of

Basin A and all of Basin D are holokarstic and do not contain any active surface watercourses.

The surface runoff infiltrates into the overburden or into the dolines where it recharges the

underlying Amabel aquifer. The southern portion of Basin A and Basins B, C, E and F contain

ponds, wetlands or surface watercourses that either sink abruptly at a doline (Basin F) or

infiltrate through the overburden to recharge the Amabel aquifer. Detailed investigations

conducted at several of these sites confirm rapid flow velocities to springs that are diagnostic of

karst aquifers. The karst basins closest to the Amabel escarpment likely contribute recharge that

is directed to the escarpment springs. The intervening area lying between these basins and the

Amabel escarpment is holokarstic. Within this area, surface watercourses are absent, as are

springs discharging from the mantle of glacial sediment overlying the Amabel. The western

portion of Basin D and all of Basin E likely provide recharge for the two springs at SW2B and

SW2A. These form the headwater of a watercourse that flows westward towards the Beaver

River.

To the west of the six karst basins, there are frequent ponds, wetlands and surface watercourses

that occupy the low-lying areas. These flow westward towards the Beaver River or southward

towards the Mad River. Although this area was not widely investigated, investigations at two

sites indicate that karst has developed within this area as well. Groundwater tracing and other

observations near the SW2A and SW2B springs demonstrate that a karst aquifer is well

developed in Basin E, which is within the Beaver River subcatchment. Edward Lake is drained

by a watercourse flowing southward and is within the Mad River Subcatchment. A few

observations along this watercourse indicate that it is discontinuous. About 54 L/s were



observed sinking into the overburden at Site 173 on April 14, 2005 (Photo 4). The stream likely

resurges farther downstream at the spring at Site 174, about 150 m farther south. A month later,

the flow was about 32 L/s farther upstream at SW25 but the watercourse was dry farther

downstream at Site 172. At that time, the spring at Site 174 was discharging about 14 L/s, and

beyond this the stream gradually sank into the overburden and the watercourse was dry beyond

Site 175. The subsurface flow from this watercourse may flow towards the Mad River gorge or

it may simply resurge farther downstream along the same watercourse. These two sites are good

examples of sinking stream development that can be expected throughout the area where the

overburden is sufficiently thin and permeable.

4.2.1 Observations at the Camarthen Wetland Tributary and Nearby Springs

The largest sinking stream on the Amabel plateau within the study area sinks at the large doline

at SW26. This doline is located 1.35 km south of the existing quarry (Figure 1). Stantec

Consulting (2005) referred to this watercourse as the Camarthen Wetland Tributary. Jagger

Hims Limited has conducted monthly flow measurements in the watercourse since November

2003 at two sites: 1) just upstream from the doline, and about 40 m farther upstream at SW26A.

SW26A is located a short distance downstream from where the stream crosses beneath a trail

through twin steel culverts and is a better site for measuring flow more accurately. For the past

three years, peak spring flows at SW26A have ranged from about 60 to 100 L/s (Jagger Hims

Limited, 2007b). From the doline, the watercourse can be followed upstream for 200 m into the

south end of a swamp. At that point, the watercourse is fed by overland flow from numerous

small, shallow pools in an area forested by mixed coniferous and deciduous trees. This swamp

was identified by Stantec Consulting (2005) as an unevaluated wetland, the Camarthen Wetland.

It extends 1.1 km to the north to within 150 m of the existing quarry. The surface catchment for

the wetland and the watercourse is 119 ha (Karst Basin F), based on topography.

There is no indication that there is any significant loss of flow along the Camarthen Wetland

Tributary until it reaches the SW26 doline where all the flow is lost. The stream enters the

doline and sinks through clastic fill and leaf litter at the base. The doline is roughly 22 m in

diameter and 4.0 m deep. Bedrock is not exposed and the doline is formed within the mantle of

glacial deposits. The watercourse just upstream from the doline has incised into the glacial



deposits to a depth of about 2.2 m and the channel bed is coarse gravel and cobbles with no fines,

thus indicating rapid velocities during peak flow. The coarse material in the channel is likely

residual from erosion of the glacial sediment and is probably not transported from farther

upstream. There is no indication of any surface overflow channel extending beyond the doline

and Jagger Hims Limited has not observed the doline flooding at any point since monitoring

began in 2003. The doline appears to be located within a broad, shallow depression. Prior to the

development of this sinkpoint, there may have been a large pond within this depression.

About 100 m to the southeast of the SW26 doline, there are several small suffosion dolines in a

small woodlot (Sites 167, 168 and 169). These are located more or less along the base of a broad

shallow valley. The largest of the dolines is 10 m long, 5 m wide and 1.4 m deep. Their origin is

unclear, but they may be relict sinkpoints for a large pond that may have existed prior to the

formation of the SW26 doline.

There are three other closed depressions located to the north of the SW26 doline that are

interpreted to be suffosion dolines. The first is located 150 m north of the SW26 doline at Site

164. It is located close to the head of a shallow fluvial gully incised into the glacial deposits.

This gully can be traced using contours on the Ontario Base Map all the way to the Amabel

escarpment. However, only the first and last 100 m of its path can be readily discerned in the

field where steeper slopes have led to more pronounced stream incision. The two other

depressions are located 70 m farther down this gully at Sites 165 and 166. The largest is 7 m

long, 6 m wide and 1.0 m deep. None of the three depressions appear to be active and there is no

channel along the base of the gully to indicate recent flows. The depressions may have been

sinkpoints for the Camarthen Wetland Tributary prior to the formation of the SW26 doline.

Alternatively, they may be relict springs, but this seems less likely. No other karst features were

found in the immediate vicinity of the SW26 doline.

There are numerous springs located along the Amabel escarpment to the east of SW26. The

closest is a group of springs located between Sites 152 and 159. The streams discharging from

these springs converge into a single watercourse at Site 161, so these springs are referred to as

the 161 spring group. The escarpment was not investigated on the south side of 21/22 Sideroad.

However, flow was measured crossing the road from the south at Sites 162 and 163. The first is



a small watercourse at the base of the escarpment slope and the second drains a wetland feature

located next to 21/21 Sideroad, and both may be spring-fed. Farther to the north, there are

springs at Sites 149, 147, 146 and at SW22. There is minimal discharge from the intermittent

spring at Site 146 so this water may be derived from the adjacent escarpment slope. However,

all of the other springs discharging from the escarpment slope are likely discharging from the

Amabel aquifer. Most of them are at the elevation of the Amabel or Fossil Hill Formations and

the spring at Site 159 issues from talus only a few metres below an outcrop of Amabel dolostone.

Table 5 lists the measurements of discharge, electrical conductivity and temperature in the

Camarthen Wetland Tributary and at the various springs during moderately high and low flow

conditions in 2005. The Camarthen Wetland Tributary provides an obvious source of sinking

stream recharge to the Amabel aquifer. The electrical conductivities measured there were

significantly lower than at any other site in the study area. It had values of 195 µS/cm in May

and 270 µS/cm in November. There was a wide variation in the electrical conductivities

measured at the springs, especially in May. However, only the central springs within the 161

spring group had low values suggesting recharge from the Camarthen Wetland Tributary. The

values measured at Sites 152s, 153, 154, 156 and 157 ranged from 266 to 274 µS/cm on May 15.

These values were lower than at any other springs within the study area. The adjacent springs at

Sites 159 and 152n had somewhat higher values but not as high as the other sites located farther

to the north and south. The anomalous values of electrical conductivity at the 161 spring group

are an indication that these springs may be the resurgences for the Camarthen Wetland Tributary.

Assuming this to be correct, the contribution of sinking stream recharge to the 161 spring group

can be calculated from the discharge measurements. During May, sinking stream recharge

would have contributed roughly 53% of the total recharge. The remaining recharge would have

had an electrical conductivity of about 381µS/cm, much closer to the values observed at most of

the other springs. During November, sinking stream recharge would have contributed roughly

16% of the total recharge. The remaining recharge would have had an electrical conductivity of

about 511 µS/cm, a value more typical of the majority of springs. Presumably, the remaining

recharge is derived from percolation recharge, or widespread infiltration of precipitation through

the glacial deposits that overlie the Amabel aquifer. During peak flow, the relative contribution

of sinking stream recharge to the 161 spring group should be at its highest and its relative

contribution should diminish as flows in the sinking stream decrease.



Table 5. Surface water monitoring data for SW26 and the nearby springs on May 15 and

November 17, 2005.

May 15, 2005 November 17, 2005

Site Q (L/s)

EC (µS/cm)

Temp (°C)

Q (L/s)

EC (µS/cm)

Temp (°C)

SW26 25 195 7.3 0.35 270 1.0

SW22 8 524 6.6 0.37 543 7.6

146 0.3 487 7.3 0 — —

147, 148 1 4 464 7.9 0.6 516 8.3

149, 150 1 0.5 443 7.2 0.25 513 6.5

152n 0.2 384 6.5 0.11 488 3.8

152s 4 271 6.4 0.44 443 6.6

153 10 266 5.7 0.5 445 7.1

154 1 266 5.9 0.7 446 6.5

156 7 269 5.7 0 — —

157 5 274 5.6 0 — —

159, 160 1 6 369 6.5 0.5 514 3.7

161 2 47 282 — 2.2 473 —

162 3 478 7.3 0.1 480 2.8

163 12 411 10.8 4 445 4.3

1 Measurements were made immediately downstream from the springs on May 15, but were better measured farther downstream at alternate sites on November 17.

2 Data for Site 161 are calculated from measurements at Sites 152, 155, 158 and 160. The data for Site 161 represent the combined discharge from the spring group.

4.3 Karst Development on the Manitoulin Bench

The Manitoulin bench is nearly continuous along the Niagara Escarpment within the study area.

The distribution of karst features along the Manitoulin bench and the adjacent escarpment

indicates that karst is developed where the mantle of glacial sediment is thin and sufficiently

permeable. A total of eight suffosion dolines, 27 sinking streams and 59 springs were observed.

Of these, the vast majority occur where the Manitoulin bench is planar and has a gentle slope,



regardless of the width of the bench. These are the areas where overburden is probably two or

three metres thick at most and any surface runoff is able to infiltrate through the soil mantle.

Of the 6.6 km investigated along the Niagara Escarpment between the Grey-Simcoe County line

and 21/22 Sideroad, there are only two short intervals where the Manitoulin bench appears to be

absent. The first is north of County Road 91 where there is a large cliff formed in the Amabel

dolostone. The prominent talus slope beneath this cliff is continuous without any break at the

elevation of the Manitoulin. However, there may be a narrow erosional bench buried beneath the

talus. The second location is on the north side of 26/27 Sideroad where there is a prominent

embayment in the Niagara Escarpment and where the glacial deposits may be thicker.

Elsewhere, the nature of the bench varies considerably. It ranges from about 10 to 500 m in

width. In places it forms a planar surface with a very gentle slope where the mantle of glacial

sediment is thin, but elsewhere the surface is marked by more rolling topography and deeply

incised gullies indicative of thicker glacial deposits. Two moraines lie on the bench, both

characterized by gentle rounded crests at an elevation of about 455 to 460 m a.s.l. The first

extends from County Road 91 almost to 26/27 Sideroad. The second extends from 0.5 to 1.1 km

north of 26/27 Sideroad. Their subtle expression and gentle contours may reflect lacustrine

reworking. Clearly, there is considerable variation in the form and thickness of glacial sediments

that overly the Manitoulin bench.

Two areas were observed along the Manitoulin bench where the overburden is thin and surface

water is able to infiltrate into the Manitoulin aquifer. The first stretches from Site 113 in the

north to Site 112 in the south (Figure 1). Water discharging from the Amabel aquifer issues from

a series of 14 small springs located along the base of the talus slope at the west edge of the

bench. Each spring is at the head of a small watercourse. Some of these watercourses sink

almost immediately upon reaching the Manitoulin bench, either at suffosion dolines or by

infiltration into the overburden. The larger watercourses extend farther out across the bench but

these, too, gradually infiltrate and none of the streams were observed extending completely

across the bench. These sinking streams are expected to resurge at the numerous springs located

along the Manitoulin escarpment. Two groundwater traces were conducted here and these

confirm that the sinking streams resurge at springs located along the Manitoulin escarpment.

The results of the groundwater traces are reported in Sections 5.0 and 6.4.



The second area is much larger and is located north of 26/27 Sideroad. It extends from west of

Site 49 in the north to Site 74 in the south (Figure 1), a distance of nearly two kilometres. Here,

the Manitoulin bench ranges from 200 to 500 m in width, has a slope of less than 5 m per 100 m,

and forms a distinct planar surface. Once again, water discharging from the Amabel aquifer

issues from a series of 11 small springs located along the base of the talus slope at the southwest

edge of the bench. Each spring is at the head of a small watercourse that descends to the

elevation of the bench then gradually infiltrates into the overburden. Most of the streams sink

completely within 50 m, although a few extend somewhat farther. No suffosion dolines were

observed. Along the Manitoulin escarpment, there are a total of 22 small springs. Most of these

emerge just below the crest of the escarpment. Dolostone often outcrops at the crest and the

springs are typically located within a few metres down the slope. A few of the springs issue

from overburden farther down the escarpment slope but these, too, likely discharge from the

Manitoulin aquifer. The lack of suffosion dolines may reflect the properties of the soil or the

immaturity of the karst.

The measured discharges from the springs support the interpretation that the Manitoulin springs

are fed in part by the sinking streams on this segment of the Manitoulin bench. Table 6 indicates

the total discharge from both the Amabel and Manitoulin springs during high flow in spring and

low flow in fall. The widely distributed but small springs issuing from the Amabel here suggest

that each spring has a small catchment fed by the adjacent holokarst on the Amabel plateau. The

total discharge from the Manitoulin springs is approximately double that of the Amabel springs,

regardless of season. This is consistent with the Manitoulin springs having twice the effective

catchment area as a result of capturing the flow from the Amabel springs. No groundwater

tracing was conducted in this area.

Table 6. Total discharge (L/s) measured from selected Amabel and Manitoulin springs during high and low flow conditions.

Aquifer Selected Springs May 9-13, 2005

Nov. 18-19, 2005

Amabel (34, 35, 36, 37, 38, 39, 40, 41, 42, 43, 44) 10 0.9

Manitoulin (49, 50, 51, 52, 54, 55, 56, 57, 58, 59, 60, 61, 62, 64, 65, 67, 68, 70, 71, 72, 73, 74)

20 1.6



In contrast to the previous two areas, the southern segment of the Manitoulin bench extending

from County Road 91 to 21/22 Sideroad has little evidence of karst development. One small

suffosion doline was noted at Site 134 in 2005, although later that year it was filled in when the

fields were tilled. There are also two small watercourses that gradually sink into the overburden

that are fed by springs at Sites 133 and 136. However, no springs were detected anywhere along

the Manitoulin escarpment. The glacial deposits in this area appear to be thicker and the two

largest watercourses crossing the bench have incised deeply into the overburden without

intersecting bedrock. This indicates that the thicker mantle of glacial deposits has limited

infiltration and inhibited karst development.

The one remaining segment of the Manitoulin bench extends for 700 m south of 26/27 Sideroad.

The bench here is quite narrow and has a greater slope than elsewhere. Although the Manitoulin

dolostone often outcrops along the crest of the Manitoulin escarpment here, it appears that the

mantle of glacial sediment on the bench is thicker. Despite this, there are two streams that

gradually infiltrate into the overburden. The first originates at a small perennial spring issuing

from the Amabel aquifer at Site 77. The stream sinks eventually after flowing as much as 200 m,

despite peak flows of less than 2 L/s. A second stream originates at a large perennial spring

issuing from the Amabel aquifer at Site 86. This stream does not sink until it approaches within

20 m of the Manitoulin escarpment where the overburden is thin, just downstream from SW21C.

The series of springs at Sites 84 and 85 are the likely resurgences. Although the glacial sediment

cover on the Manitoulin bench is thicker at this segment, the presence of several springs at the

elevation of the Manitoulin escarpment indicates that surface water is able to infiltrate into the

Manitoulin aquifer, at least close to the escarpment, and that karst has likely developed here.

4.4 Measurements of Streamflow around the Study Area Perimeter

Streamflow was measured at all watercourses that potentially originate in or adjacent to the

detailed study area. These measurements were made along public roads and were taken during

low flow conditions on October 26, 2004 and again during moderate flow conditions on May 16

to 17, 2005. The data are listed in Table D-1 in Appendix D. Figure 1 illustrates the monitoring

locations as well as the recorded flows.



The data are consistent with the discharges measured farther upstream at the numerous springs

that occur at the head of these creeks. A number of the streams located along 31/32 Sideroad

and Pretty River Road likely originate at a series of karst springs located along the Manitoulin

and Amabel escarpments within Grey County and represent discharge from the Amabel and

Manitoulin aquifers. The watercourses located farther south along Pretty River Road as well as

along Grey Sideroad 30 may be fed in part by discharge from the Amabel aquifer. Alternatively,

there could be significant discharge from glacial deposits. Regardless, there is no indication that

there may be any karst springs there that are significantly larger than those observed within the

detailed study area.

5.0 Investigation at the Manitoulin Bench An investigation was conducted at the Manitoulin bench to characterize the karst, to compare

aquifer recharge and discharge, and to determine groundwater flow velocities in the Manitoulin

aquifer. In addition to field mapping and measurements of spring discharge, a preliminary

groundwater trace was conducted here in anticipation of more complex tracing from the SW9

watercourse.

5.1 Site Description

Field mapping of karst features and springs was conducted at the Manitoulin escarpment to the

north of Simcoe County Road 91. The results are illustrated in Figure 3. At this site, there is a

prominent erosional bench formed on top of the Manitoulin Formation that clearly separates the

Amabel and Manitoulin escarpments. Bedrock is often exposed near the crest of the Amabel

escarpment and there is some talus intermixed with glacial deposits extending to the base of the

slope. The Manitoulin bench slopes gently to the northeast and is covered with a continuous

blanket of glacial deposits. Most of the bench is currently tilled where it is sufficiently wide.

The transition from the Manitoulin bench to the Manitoulin escarpment is abrupt and the

escarpment has a relatively steep slope. The thin-bedded dolostone that often outcrops near its

crest is the resistant cap rock that must underlie the distinct erosional bench. The Manitoulin

bench narrows to the north and eventually disappears. At this point, the crest of the Amabel

escarpment is marked by prominent cliffs ranging from 10 to 20 m in height. The extensive talus



apron beneath this extends to well below the Manitoulin Formation and the erosional bench is

absent or buried beneath Amabel talus.

One other prominent landform occurs at the site, a ridge of glacial sediment situated 50 m

northeast of and parallel to the Manitoulin escarpment. This low, gentle ridge is tentatively

interpreted to be a moraine. Its gentle contours suggest lacustrine reworking from a proglacial

lake.

A number of small springs were located at the base of the Amabel escarpment along the edge of

the Manitoulin bench. There are also a few suffosion dolines located close to the springs, and

some of the flow from the springs is obviously captured at these features. When flows are

sufficiently high, the discharge from the larger springs flows out across the bench for some

distance before gradually sinking into the soil. Although two of these streams extended to within

a few metres of the Manitoulin escarpment during peak spring runoff, they were never observed

flowing over the escarpment. The quantity of water discharging from the springs indicates that

most of the water must be discharging from the Amabel aquifer farther up the slope.

Similarly, there is a series of small springs located all along the base of the talus slope beneath

the Manitoulin escarpment. At Sites 101 and 102, there are poorly defined channels extending

up the talus slope to discrete springs near the crest, located just below outcrops of dolostone.

However, similar channels were not observed at the majority of the springs, and the streams

generally flow beneath the talus to emerge at the base of the talus slope. Like the Amabel

springs above, the quantity of water discharging from these springs indicates that most of the

water must be discharging from the Manitoulin aquifer farther up the slope, with the exception of

the few springs located to the northwest where the Manitoulin bench is absent or buried. These

closely spaced springs, referred to as the SW11 spring group, have a combined discharge that

ranges up to 70 L/s at peak flow. Most of their discharge may issue directly from the Amabel

aquifer 80 m farther up the slope.

The discharge from the Manitoulin springs collects in the two watercourses that feed into an

artificial pond, referred to here as “Franks Pond”. The two watercourses, one flowing from the

northwest (SW11 watercourse) and the other from the southeast (SW12 watercourse), occupy the

base of the valley that lies between the escarpment and the adjacent moraine. The SW11



watercourse is fed by groundwater discharge from the Manitoulin and Amabel aquifers. The

SW12 watercourse extends for 450 m to just north of Simcoe Road 91. Like the other

watercourse, there are springs located along much of its length, although these are more widely

dispersed. Much of its flow is from groundwater discharging from the Manitoulin aquifer.

Franks Pond occupies a notch cut into the moraine from the combined flow of these two

tributaries. Between the tributaries, there are a few additional springs located at the base of the

talus slope at Sites 93, 94, 95, 96, 97, 98 and 101 that provide some flow directly into the pond.

5.2 Results of the Groundwater Trace from Site 114

A groundwater trace was conducted on April 19, 2005. A small amount of uranine (3.25 g) was

injected into a small sinking stream perched on the Manitoulin bench. The dye was injected into

the stream just downstream from the Amabel spring at Site 114 (Figure 3). At the time, the

stream was observed gradually sinking into the overburden over a distance of about 22 m. Water

samples were collected periodically at the nearby springs below the escarpment until measured

fluorescence approached background values at key monitoring sites. A total of 19 sites were

monitored extending from the SW12 watercourse at Site 105 in the east to springs at Site 227 in

the north. The three springs located near the top of the escarpment slope at Site 99, 100 and

100A were only sampled once.

Sufficient samples were taken at most locations to adequately define breakthrough curves for the

trace. The measured background fluorescence ranged from 0.2 to 0.6, expressed as µg/L of

uranine, which is equivalent to parts per billion (ppb). The tracer was detected at eight sites and

the peak concentrations of the tracer after subtracting background fluorescence are indicated in

Table 7. The tracer concentrations at Sites 96, 97, 98, 101 and 102 are shown in Figure 4.

Tracer arrival first occurred at Site 102, a convenient monitoring point at the base of the

escarpment slope along a watercourse extending down from the springs at Sites 99 and 100. The

peak tracer concentration measured at Site 102 was 5.9 µg/L, and this occurred 47 minutes after

injection. Two springs located just to the north of Site 102 had similar breakthrough curves.

Spring 98 had the highest peak concentration (12.4 µg/L), but the peak did not occur until about

2 hours after injection. The discharge from spring 98 sinks into the overburden about 15 to 20 m

to the north. Spring 97 had a peak concentration of 6.5 µg/L, and this occurred about 1.6 hours

after injection. This spring is probably located downstream from the spring at 98, which would



explain the similar shape of the breakthrough curves and the more subdued response at Site 97.

Positive traces were also observed at Sites 101 and 96. These are very small springs emerging

from overburden with relatively little flow. At Site 101, the peak tracer concentration was

1.0 µg/L and this occurred about 4 hours after injection. At Site 96, there was insufficient data to

identify the peak. This spring may also be downstream from the spring at Site 98. About 5

hours after injection, the tracer concentrations at Sites 99, 100 and 100A were 0.8, 1.0 and 1.0

µg/L above typical background fluorescence values measured at the other sites suggesting

positive traces to these springs. The relatively low values reflect the sampling time, long after

the peak would have passed. At about the same time, the measured fluorescence in the stream

just downstream from the injection site had returned to near background levels (0.8 µg/L).

The groundwater trace established flow direction and velocities from the sinking stream at Site

114 to a series of closely spaced springs located nearby on the escarpment slope. The

groundwater velocities are consistent with rapid flow along solutionally enlarged conduits. This

interpretation is supported by the presence of the suffosion dolines along the western edge of the

Manitoulin bench. The loss of overburden at these dolines can only be attributed to subsurface

transport of sediment along enlarged fractures or conduits with sufficient velocities to transport

clay, silt and sand. Flow from the other sinking streams located nearby is expected to behave in

a similar fashion, flowing rapidly along channels and conduits to join the major flow paths to the

springs. Figure 5 illustrates the spatial relationships between the injection site and the springs

where the dye was recovered. Once through the overburden, enlarged fractures and bedding

planes in the bedrock would have directed the flow to springs near the crest of the Manitoulin

escarpment (e.g., the spring at Site 99). From there, some of the flow clearly followed surface

channels down the talus slope. However, some flowed through the talus and overburden to the

series of springs at the base of the slope at Sites 96, 97, 98 and 101.

Discharge, electrical conductivity and temperature were also monitored during the trace and the

results for relevant sites are also presented in Table 7. It is apparent that the total recharge to the

Manitoulin aquifer from the five sinking streams is similar to the discharge measured near the

crest of the escarpment at Sites 100A, 99 and 100. Similarly, the calculated electrical

conductivities and temperatures of their combined flows are also quite similar. It is not

surprising that the temperatures varied slightly between the recharge and discharge since this



would have been influenced by air temperature. However, the measured recharge and discharge,

as well as the electrical conductivities are very similar (i.e., within measurement error).

Table 7. Surface water data measured at the Manitoulin escarpment on April 19, 2005.

Feature Type is indicated by the following codes: GI1, small intermittent spring; GP1, small perennial spring; M, monitoring point along a surface watercourse. Peak [UR] is the peak concentration of the tracer uranine after subtracting the measured background fluorescence. Measurements of flow Q are approximate, generally ± 30%. EC and Temp are the specific conductivity and temperature of the water.

Site No. Type (code)

Peak [UR] (µg/L)

Qrecharge

(L/s) Qdischarge

(L/s) EC

(µS/cm) Temp (°C)

114 GI1 6 305 5.5

115 GI1 0.2 310 5.9

116 GP1 5 313 6.0

117 GI1 0.5 310 6.3

118 GP1 1 305 5.1

100A GI1 1.0 3.8 306 6.6

99 GI1 0.8 2 305 5.5

100 GI1 1.0 9 306 5.7

102 M 5.9 5.5 307 7.2

101 * GI1 1.0 2 *

98 GI1 12.4 2 305 5.7

97 GP1 6.5 1.5 311 4.8

96 * GI1 0.2 1 *

Total recharge on Manitoulin bench (Sites 114, 115, 116, 117, 118)

12.7 308 5.7

Total discharge near top of talus slope (Sites 100A, 99 and 100)

14.8 306 5.9

* Flows at Sites 101 and 96 were not measured on April 19, 2005. However, measurements were made at these sites during similar flow conditions on April 18, 2005.

The tracing results at Sites 102 and 98 suggest mixing of groundwater, either within the bedrock

aquifer or perhaps in the talus. Although the most rapid flow was to Site 102, the peak

concentration of uranine at Site 98 was twice that for Site 102. This supports the interpretation



that groundwater from the other sinking streams located nearby to the south was mixing with the

groundwater from the sinking stream at Site 114. While much of the combined discharge flowed

rapidly down the surface channel to Site 102, some water flowed down through the talus to the

small spring at Site 98, and this water must have had less mixing with water from the other

sinking streams. Unfortunately, it cannot be determined if the mixing took place within the

bedrock aquifer or in the talus, so little can be determined about the configuration of conduits

within the Manitoulin aquifer.

The measured tracer velocities from the groundwater trace are within the expected range for

karst. Calculations based on a model of diffuse flow through the soil mantle, conduit flow in the

Manitoulin aquifer, and the measured tracer velocity to Site 102 indicate that 1) the majority of

the residence time for the trace was likely in the soil mantle, and 2) the flow through the

overburden was likely dispersed over a relatively large area (throughout the entire area of

saturated soil surrounding the stream) and not focused at just a few discrete points along the

sinking stream.

The groundwater tracing conducted at the Manitoulin bench indicates that karst has developed in

the Manitoulin Formation where the soil mantle is thin, supporting the interpretation of karst

features mapped at this site.

6.0 Investigation of the SW9 Watercourse and its Resurgences

The SW9 watercourse is one of the few surface streams located on the Amabel plateau close to

the Niagara Escarpment and, like most of the other watercourses, it sinks before reaching the

Escarpment. It is possible that dewatering of the proposed expansion quarry could affect this

watercourse, so a detailed study was conducted to: 1) determine the nature of streamflow losses

along the SW9 watercourse, 2) determine where the sinking stream resurges, 3) determine travel

times to the resurgences, and 4) better define the relationship between groundwater flow in and

between the Amabel and Manitoulin aquifers. In addition to a groundwater trace conducted at

the SW9 watercourse, a trace was conducted simultaneously from a small sinking stream perched

on the Manitoulin bench at Site SW10.




Figure 6 illustrates the location of the SW9 watercourse relative to key springs located along the

Niagara Escarpment. Jagger Hims Limited (2007b) have monitored surface flows monthly along

the creek at SW9 since May 2003. The stream generally dries up for several months of the year

during summer and fall but flows reach about 40 L/s during peak spring runoff. The lower reach

of the SW9 watercourse was mapped during the spring of 2005. From SW9, a small, defined

channel extends 100 m upstream to where it drains an area forested in cedars that floods each

spring to a depth of a few tens of centimetres.

Downstream from SW9, the watercourse was traced for nearly 500 m. Along this reach, a

defined channel is usually absent, and most of the watercourse can only be mapped by following

the stream during peak flows. Although there are a few shallow depressions along this reach,

there is no clear indication that dolines have formed. However, there are outcrops of dolostone

on either side of the watercourse starting at Site 13A and extending for about 200 m downstream.

These indicate that the overburden is often thin beneath the watercourse, and probably less than

one or two metres thick. The slightly hummocky nature of the ground surface in this wooded

area suggests that karst processes may be active along this reach. About 20 m downstream from

this reach, the watercourse continues as an obvious ditch that extends for 100 m through a

forested area to the edge of a grassy meadow. From here, the path of the stream was traced for

an additional 150 m across the meadow by following the obvious path where the stream had

melted the snow a few days prior to mapping. Bedrock does not outcrop along the final 270 m of

the watercourse where the overburden may be thicker.

Farther to the east, numerous suffosion dolines were observed on the Amabel plateau. Most are

quite close to the Niagara Escarpment, but a few are as much as 100 m from its crest. Many of

these dolines are distinctly elongated indicating the strong influence of underlying fractures in

the Amabel dolostone. Although these features were not mapped, there appears to be a greater

concentration of dolines where the Amabel dolostone forms a prominent cliff at the crest of the

escarpment. These observations suggest that stress release from unloading along the Niagara

Escarpment has opened up many of the fractures in the dolostone close to the Escarpment, and

this has encouraged the rapid development of integrated channel networks leading to the

formation of the suffosion dolines. Although karst processes were not likely responsible for



initial enlargement of the fractures, the structural unloading has permitted the rapid development

of karst. Observations elsewhere indicate that suffosion dolines are uncommon farther from the

escarpment.

It was anticipated that the SW9 watercourse should resurge at some of the springs located along

the Niagara Escarpment to the east, since the hydraulic gradients should be steepest in this

direction. The stream sinks near the centre of a sizeable promontory so subsurface flow could

potentially resurge anywhere around the perimeter. Although there are large springs located at

the north and south of the promontory, the sinking stream was expected to resurge at the

concentration of springs located almost due east at the SW11 spring group. The substantial

flows observed here indicate a large catchment close by, and the sinking stream recharge from

the SW9 watercourse seemed to be the likely source.

6.2 Streamflow Losses along the SW9 Watercourse

The preliminary observations of the SW9 watercourse suggested that it gradually loses flow

starting at Site 13A where dolostone first outcrops close to the watercourse. On April 23, 2004,

the flow measured at SW9 was 6 L/s and all of this sank gradually into overburden about 40 m

farther downstream in the vicinity of Site 13A. To better understand the nature of flow losses, a

series of flow measurements were made along the watercourse the next year on April 25 during

high flow. The results are illustrated in Figure 7. Discrete losses of flow were only observed at

Sites 14C and 14D. At the first site, 6 L/s was observed diverging from the main stream and

sinking into overburden within a shallow depression. Similarly, 2 L/s was observed sinking into

the overburden at a shallow pool at the terminus of the stream at Site 14D. There may have been

similar discrete losses of flow farther upstream, but these could not be detected because the

overall streamflow was greater and small decreases in flow could not be detected. Nevertheless,

it is concluded that the 39 L/s observed flowing at SW9 was gradually lost to infiltration over a

distance of 220 m. The streamflow losses appear to have been dispersed over the entire distance

of this reach as indicated by the overall slope of the streamflow-distance curve. However, it is

more likely that there was a series of small discrete losses where the overburden cover was thin

and underlain by solutionally enlarged fractures in the Amabel dolostone.



At the regional scale, the loss of flow along the lower reach of the SW9 watercourse represents a

significant concentration of sinking stream recharge from a surface catchment area of about 68

ha. Although this sinking stream recharge may enter a conduit network draining to only a few

closely spaced springs, the loss of flow over a distance of 220 m during high flow conditions

increases the probability of the groundwater flowing through a larger network to more widely

dispersed springs.

6.3 Results of the Groundwater Trace from the SW9 Watercourse

A groundwater trace was conducted from the SW9 watercourse on April 23, 2005. A small

amount of uranine (99.3 g) was injected into the stream about 23 m upstream from SW9 at Site

12. This location is about 60 m upstream from the beginning of the losing reach. The dye

solution was rapidly mixed in the stream by turbulent flow in a narrow channel (Photo 7). Water

samples were collected periodically at a total of 55 sites located along the Niagara Escarpment

from Site 76 in the north to Site SW22 in the south (Figure 6). These sampling sites encompass

all of the springs issuing from the Amabel and Manitoulin aquifers around the perimeter of the

promontory where the SW9 watercourse sinks. Water samples were collected manually at most

sites to provide for greater spatial resolution. An ISCO autosampler was used to collect samples

more frequently at SW11E located at the downstream end of the SW11 watercourse, the largest

watercourse entering Franks Pond. This stream is fed by the SW11 spring group. Sampling

continued at key sites until the measured fluorescence approached background values.

Sufficient samples were taken at many of the locations to adequately define breakthrough curves

for the trace. The tracer was clearly detected at a total of 19 sites. In addition, above-

background fluorescence concentrations were measured at an additional four sites but low

concentrations and sampling frequency make interpretation inconclusive. The results are

summarized in Table 8. Figure 6 illustrates the spatial relationships between the sinking stream

and all of the springs sampled during the groundwater trace and Figure 8 shows details where the

majority of the dye was recovered. Tracer concentrations at Sites SW11E and 105 are illustrated

in Figure 9.



Table 8. Surface water sites where the tracer was recovered from the SW9 watercourse tracer test. Feature Type is indicated by the following codes: GI1, small intermittent spring; GP1, small perennial spring; GP2, large perennial spring; M, monitoring point along a surface watercourse. Peak [UR] is the peak concentration of the tracer uranine after subtracting the measured background fluorescence. Measurements of flow Q are approximate, generally ± 30%. EC is the specific conductivity and Temp is the water temperature.

Site Type (code)

Peak [UR] (µg/L)

Qrecharge

(L/s) Qdischarge

(L/s) EC

(µS/cm) Temp (°C)

SW9 M 30 361 4.7 SW21C M 0.2 9 378 4.9 88 (89) GI1 0.8 4 341 3.3

90 GI1 0.6 2.5 SW21D M 0.4 2 248 3.9 227w GI1 4.5 1 340 2.3

SW11D GP1 13.0 4 346 4.1 227e GI1 10.9 2 345 4.2

SW11B GP2 11.9 6 342 4.0 228 GP1 13.4 0.6 346 4.3

SW11A GP2 15.6 4 348 4.4 91 GI1 16.3 2 348 4.4 92 GP1 7.7 3 336 3.9 93 GI1 2.7 2 *

SW11E M 11.4 70 94 GI1 1.7 2 * 95 GI1 2.4 4.5 * 96 GI1 0.3 1 * 97 GP1 0.7 2 328 4.8 98 GI1 0.4 2 *

101 GI1 0.3 2 * 102 M 1.0 4 328 4.8 105 M 0.3 20 513 3.1 114 GI1 4.1 6 * 116 GI1 5.9 5 *

SW12A M 0.2 133 (134) M 0.2 5 * 643 4.4

136 GP1 0.4 3 * Allogenic recharge on Amabel plateau

(The SW9 watercourse, at SW9) 30 361 4.7

Discharge at the Niagara Escarpment (Sites SW11E, 94, 95, 96, 97, 101, 102)

88 — —

* Measurements of flow, electrical conductivity and temperature were made under similar flow conditions between April 18 and 23.



At Site SW11E, the first arrival of the tracer occurred 3.6 hours after injection and the tracer

peaked at a concentration of 12.1 µg/L 8.0 hours after injection. The majority of the dye cloud

passed within the first 24 hours and the measured fluorescence returned to background levels

within six days. The stream at this site is fed by spring discharge from Sites 227, SW11D,

SW11C, SW11B, 228, SW11A, 91 and 92, or the SW11 spring group. The measured

fluorescence at the individual springs 12 hours after injection ranged from 5 to 17 µg/L. Since

these sites are upstream from SW11E, the peak would have passed about four hours earlier so

these values are well below the peak tracer concentrations. Nevertheless, the dye cloud clearly

passed all of these springs and at relatively high concentrations. It is concluded that the SW11

spring group is the primary resurgence for the SW9 watercourse.

Dye was also recovered at several other springs. The peak tracer concentrations at Sites 114 and

116 were at least 4.6 and 6.3 µg/L, respectively (Figure 10). Clearly, some of the flow from the

SW9 watercourse resurged at these Amabel springs. As discussed in Section 5, the discharge

from these springs sinks on the Manitoulin bench and resurges at several nearby springs located

along the Manitoulin escarpment at Sites 96, 97, 98, 99, 100, 100A, 101 and 102. Therefore, it is

not surprising that the dye was also recovered at these springs, where the peak tracer

concentrations ranged from 0.3 to 1.0 µg/L. Their peak concentrations were lower because the

springs are located farther downstream and because of high dispersion in the intervening talus.

Dye was also recovered at three other Manitoulin springs located just to the northwest at Sites

93, 94 and 95. Once again, their peak tracer concentrations were relatively low, ranging from

1.7 to 2.7 µg/L.

In addition, low concentrations of the tracer also appeared to be detected at seven other sites

(105, SW12A, 133, 136, 89, 90, and SW21D). However, there were too few samples and the

dye concentrations were too low at all of these sites to assess dye recovery with confidence.

By combining the tracing data with measurements of discharge, the mass of dye recovered at the

various springs can be calculated from integration of the breakthrough curves. Since the

discharge measurements are accurate to ± 30%, the calculated recoveries can be used to

approximate the distribution of flow to the various springs where the tracer was recovered. Of

the 99.3 g of uranine that was injected into the SW9 watercourse, about 64 g of the dye was



recovered at the various springs. The remaining dye would have been lost due to photodecay,

microbially mediated decomposition, and to adsorption onto organic matter and sediment. The

recovery of about 64% is typical of groundwater traces in karst, especially considering that the

stream sinks through overburden before entering the Amabel aquifer. About 58 g of the dye

were recovered at the SW11 springs, as measured at SW11E. In contrast, about 5 g of dye was

recovered from all of the other springs combined. Therefore, about 90% of the flow lost along

the lower reach of the SW9 watercourse resurges at the SW11 spring group. The remainder is

distributed amongst the various other springs to the north (SW21C, SW21D, 90, 88) and south

(Sites 133, 136, 114 and 116, and from Site 93 to Site 105).

During the groundwater trace, the electrical conductivities measured at all of the individual

SW11 springs were nearly identical, ranging from 340 to 348 µS/cm. These values are very

similar to the electrical conductivity measured at the SW9 watercourse a few hours earlier in the

day, which had a value of 361 µS/cm. The consistent values for the conductivities indicate that

the groundwater was well mixed prior to issuing from the Amabel aquifer. The minor variations

likely reflect the introduction of minor infiltration recharge from the talus slope. The wide

distribution of the springs at the base of the talus slope may be partly due to a pattern of

divergent flow through the talus as the various streams descended the escarpment slope.

However, the distribution of the SW11 springs over a width of 120 m cannot be fully explained

by this mechanism, indicating that there must be a pattern of distributary flow in the Amabel to

several Amabel springs hidden beneath the talus near the crest of the escarpment. Furthermore,

the position of the springs at Sites 91 and 92 suggests that some of the discharge from the

Amabel aquifer sinks into the Manitoulin aquifer immediately upon reaching the elevation of the

Manitoulin bench. This water must then flow through the Manitoulin aquifer to springs hidden

beneath the talus on the Manitoulin escarpment above Sites 91 and 92. This all points to a

pattern of distributary flow in the Amabel aquifer to a series of Amabel springs spaced over a

distance of about 100 m.

Table 8 includes a comparison of the sinking stream recharge to the Amabel aquifer at the SW9

watercourse with the discharge from the principal resurgences along the Niagara Escarpment.

The springs at Sites 114 and 116 are not included in the sum of the discharge since they are

upstream from some of the resurgences at the base of the Manitoulin escarpment. Roughly 34%



of the combined flow from the resurgences was derived from the SW9 watercourse. Similarly,

only about 43% of the recharge for the SW11 spring group was from the SW9 watercourse.

While there may be some streamflow losses farther up the SW9 watercourse that contribute

sinking stream recharge to the Amabel aquifer, the presence of various wetlands there suggest

that any additional sinking stream recharge from there is minimal. Therefore, it is concluded that

although these springs obtain a significant component of sinking stream recharge (i.e., from the

SW9 watercourse) they receive an even greater component from widespread percolation

recharge on the Amabel plateau. This indicates that there must be significant infiltration through

the soil mantle overlying the Amabel aquifer and from a large area. With respect to the proposed

quarry at the expansion property, it can be concluded that even a significant loss of flow in the

SW9 watercourse as a result of quarrying would not cause the SW11 springs to dry up. The

paucity of surface streams elsewhere on the Amabel plateau near the escarpment implies that

many of the other escarpment springs are fed primarily by percolation recharge as well and these,

too, are not likely to be significantly impacted by the proposed quarrying.

6.4 Results of the Groundwater Trace from SW10

A groundwater trace was conducted from Site SW10 on the Manitoulin bench (Figure 3). A

small amount of phloxine B (8.7 g) was injected into the sinking stream just downstream from

the water supply system (Photo 8). At the time, the SW10 stream sank into the overburden just

upstream from the doline at Site 124, within 20 m of the base of the Amabel escarpment. The

nearest point along the crest of the Manitoulin escarpment is 150 m to the northeast. This trace

was conducted simultaneously with the SW9 watercourse trace so the same water samples

collected for that trace were also analyzed for phloxine B.

The tracer concentrations measured at Sites SW11E and 105 are illustrated in Figure 11. A good

breakthrough curve was obtained for SW11E. The first arrival of the tracer was 6 hours after

injection and the measured fluorescence returned to background levels 34 hours later. The

concentration of phloxine B reached a peak of 1.9 µg/L above background fluorescence 14 hours

after injection. The characteristic shape of the breakthrough curve provides evidence that flow

from the sinking stream at SW10 resurged at the SW11 springs, although the peak concentration

was low. During the trace, the flow measured at SW10 was only 0.2 L/s whereas the combined

discharge from the SW11 springs was 70 L/s. Therefore, the observed low peak in tracer



concentration at the SW11 springs was a result of substantial dilution. The few measurements at

the individual SW11 springs indicate that the tracer was recovered at all of these and at similar

concentrations as those measured at SW11E. However, there were too few samples to

adequately define breakthrough curves for the individual springs. Nevertheless, the results of the

trace established a subsurface connection to the conduit(s) feeding the SW11 springs and the

observed tracer velocity is typical for flow through solutionally enlarged conduits in karst.

At Site 105, background fluorescence was more variable than at SW11E (Figure 11). Two

individual measurements were well above background fluorescence and suggest that the tracer

was also recovered at this site. However, this interpretation is not conclusive.

The peak concentrations were too low to determine if subsurface flow connections exist to any

other springs.

7.0 Investigation of the SW28 Watercourse and its Resurgences The SW28 watercourse is one of the few surface streams located on the Amabel plateau close to

the Niagara Escarpment and, like the SW9 watercourse, it sinks before reaching the Escarpment

(Figure 1). A groundwater trace was conducted from this site to: 1) characterize the nature of

groundwater recharge from the stream, 2) determine where the sinking stream resurges, 3)

measure groundwater flow velocities, and 4) determine the relative importance of sinking stream

and percolation recharge to regional springs.


Figure 12 illustrates the location of SW28 along a small watercourse, the surface catchment for

the watercourse, and the various springs located nearby along the Niagara Escarpment. The

surface catchment for the SW28 watercourse is about 55 ha, or slightly smaller than that for the

SW9 watercourse. Observations were made during moderately high flow conditions and, from

these, it is estimated that peak flows during spring runoff each year are likely in excess of 20 L/s.

There are virtually no defined stream channels throughout the catchment. During peak runoff

each spring, an area of shallow, interconnected pools forms in the center of the catchment along

the base of the broad shallow valley. Part of the seasonally flooded area extends southward



through a reforested area towards 26/27 Sideroad. The seasonally flooded area also extends

northward across open forest and meadows. Although no longer farmed, this valley was once

tilled and surface channels may have been eradicated. Surface runoff collects in this low area

then winds its way through the interconnected pools to a poorly defined channel that drains to the

east. Runoff follows this grassy channel only a short distance before entering a shallow,

ephemeral pond occupying a shallow basin at Site 7. Here, the water infiltrates into the

overburden beneath the pond. The size of the pond varies as a function of the flow entering from

the watercourse. Flows were occasionally measured just upstream from the pond at SW28. It is

only during brief periods of peak runoff that the capacity of the sinkpoint is exceeded and the

pond overflows the basin. The excess water exits the basin at the east end and continues on the

surface towards the Amabel escarpment. Although the flood waters initially follow a fairly

defined path, any stream channel that may have existed there once has since been eradicated by

tilling. However, a distinct fluvial gully has formed where the watercourse approaches the

Amabel escarpment. This is incised into the glacial deposits that overlie the Amabel dolostone.

The gully gradually deepens as it approaches the escarpment and at the brow it has cut down to

expose the Amabel dolostone.

The SW28 watercourse and the seasonally flooded area that forms its headwaters dry up during

the summer. On April 22, 2005 the stream was in flood and the flow measured just downstream

from the pond was about 10 L/s at Site SW28A. At that time, the stream continued on the

surface to the beginning of the gully, or about 100 m upstream from the Amabel escarpment. No

discrete sinkpoints were observed and the water appeared to be gradually infiltrating into the

overburden along this reach, much like the SW9 watercourse along its lower reach.

Furthermore, there was no indication that the stream had extended any farther at any time that

spring. Nevertheless, it is likely that the SW28 watercourse does occasionally flow over the

Amabel escarpment from time to time.

There are a number of springs located along the Amabel escarpment to the east of the sinking

stream at SW28. The largest is a group of springs at SW27, at the head of a perennial

watercourse that descends the escarpment slope. These springs are located at the south edge of

the SW28 flood channel where it first descends the escarpment. Figure 13 is a map illustrating

the location of the individual springs within the SW27 spring group. The adjacent Amabel



plateau slopes very gently towards the escarpment here and the brow of the escarpment is

marked by a sharp break in slope. Bedrock crops out where the SW28 watercourse has cut

through the overburden at the crest of the escarpment. A total of 10 individual springs were

documented there. Of these, six are perennial, four are intermittent and one is relict. All of the

discharge from the springs converges into a single channel a short distance downstream and this

flows continuously down the Niagara Escarpment. The combined flow from the springs was

measured occasionally at Sites 46 and 47. Jagger Hims Limited measures the flow every month

farther downstream at Site SW27. Their measurements indicate that the flow ranges up to 40 L/s

and that the stream only stops flowing when it occasionally freezes during winter (Jagger Hims

Limited, 2007b).

The next largest spring is located 150 m to the south at Site 48. It is at the head of a watercourse

that is also continuous down the Niagara Escarpment. Water discharges from overburden at the

head of an obvious fluvial gully where the landowner has installed a dug well to make use of the

spring as a water supply. Jagger Hims Limited measures the spring discharge monthly a short

distance downstream at SW20. There, the flow has ranged up to 19 L/s during spring runoff and

the stream was only observed drying up during very dry weather (Jagger Hims Limited, 2007b).

There are six additional springs located along the Amabel escarpment within 800 m of SW28

(Sites 41, 42, 43, 44, 45 and 77). One is located 170 m south of the SW20 spring at Site 77.

This small perennial spring appears to emerge from a bedrock conduit. Discharge there ranges

up to 1.5 L/s. The remaining five Amabel springs are distributed along the Amabel escarpment

to the north of the SW27 springs. These are all small with flows ranging up to 2 L/s. The spring

at Site 44 issues from talus a few metres below a bedrock scarp, located near the top of the

escarpment. It dries up during the summer. The other springs are perennial and they all issue

from talus at the base of the Amabel escarpment. All five springs form the headwaters for

discontinuous watercourses that gradually lose their flow to infiltration into the overburden. The

streams at Sites 45 and 77 flow the farthest where the Manitoulin bench is less distinct. The

remaining four streams infiltrate within a few tens of metres where the Manitoulin bench is quite

distinct. Presumably, these streams provide recharge to the underlying Manitoulin aquifer.



There are also a number of small springs distributed along the Manitoulin escarpment farther to

the east. These springs were not investigated in any detail, but are likely fed by a combination of

percolation recharge on the Manitoulin bench and sinking stream recharge from the various

small sinking streams that issue from the Amabel escarpment.

7.2 Results of the Groundwater Trace at SW28

A groundwater trace was conducted from the SW28 watercourse on May 10, 2005 when all of

the flow from the watercourse was sinking at the ephemeral pond. A small amount of uranine

(24.75 g) was injected into the stream at Site SW28, about 10 m upstream from the pond. Water

samples were collected periodically at all six of the nearby springs located below the Amabel

escarpment until measured fluorescence approached background levels where the dye was

detected. The springs were sampled for seven days with sufficient frequency such that any dye

should have been detected if conduit connections exist. An ISCO autosampler was used to

collect water samples in the SW27 watercourse at Sites 46 and 47, a short distance downstream

from the spring group. In addition, most of the individual springs in the SW27 spring group

were also sampled, but less frequently. Finally, two samples were collected from the ephemeral

pond 50 and 85 hours after injection to measure the residual concentration of the dye.

After the injection into the creek, the dye was rapidly washed into the pond. For the next few

hours, the dye cloud was clearly visible as a crescent-shaped band that gradually moved across

the pond as clear water from the SW28 watercourse gradually displaced it (Photo 6). About 3

hours after the injection, the band had moved roughly halfway across the pond. There was no

indication from the movement of the dye cloud that there was any focused infiltration of the

water through the overburden. At 11 hours after the injection, the dye was barely visible in the

pond and 27 hours after injection the dye was no longer visible. The two measurements of

fluorescence in the pond at 50 and 85 hours after injection indicate that there was very little

residual dye left in the pond. These observations are consistent with the residence times

calculated for water entering the pond based on a few measurements made over the course of

four days, as shown in Table 9. During this period, the pond was observed gradually decreasing

in area and volume as the flow entering the pond from the SW28 watercourse diminished.

Although the measurements are approximate, they clearly indicate that the residence time on

May 10 would have been about five hours.



Table 9. Approximate residence times calculated for the ephemeral pond at Site 7 during the groundwater trace.

Date (mm/dd/yyyy)

Time (hr:min)

Surface Area (m2)

Volume (m3)

Discharge (L/s)

Residence Time (hr)

05/09/2005 13:30 636 130 7.5 4.8

05/10/2005 6:00 6

05/11/2005 9:00 5.4

05/12/2005 7:50 288 40 3 3.7

05/13/2005 18:45 80 10 3 0.9

The tracer was clearly detected at the SW27 springs and the measured fluorescence just

downstream from these springs is shown in Figure 14. The first arrival of the dye was 10 hours

after injection. The dye reached the peak concentration of 0.33 µg/L above the background

fluorescence at 22.7 hours after injection. Sampling was discontinued 7 days after injection at

which point the dye concentration was 0.07 µg/L above background. Although the peak

fluorescence was only double that of the background, the measurement noise was low so the data

clearly show a well defined breakthrough curve as the dye cloud passed the sampling site.

Table 10 presents the surface water data measured at the SW28 watercourse and the various

springs located nearby on May 10 during the trace. First, it should be noted that the sum of the

discharges from each of the individual SW27 springs was 9.5 L/s less than the flow measured

just downstream at Site 46. Only the largest springs were measured as it was impractical to

measure every little spring, and some of the discharge was emerging all along the various

channels. During the groundwater trace, the individual SW27 springs showed a wide variation in

response to the passing dye cloud. The four springs (Figure 13) located to the northwest

(SW27B, C, D and A) all showed a positive response with peak values ranging from roughly 0.5

to 0.2 µg/L above background fluorescence. Within this group of four springs, there appeared to

be a gradual decrease in peak tracer concentration from spring SW27B located at the northwest

to spring SW27A located to the southeast. Furthermore, a positive response was not detected at

springs E, F and G and the background fluorescence at these springs was significantly lower than

that measured at Sites 46 and 47 along the SW27 watercourse. These observations suggest that



there are two sets of springs at this site, each fed by groundwater from a different source but with

some degree of mixing occurring between them. The conductivity data support this

interpretation as well. There is a consistent increase in electrical conductivity from a value of

375 µS/cm at the northwest spring (SW27B) to 416 µS/cm at the southwest spring (SW27G).

This gradual rise is consistent with mixing between groundwaters of different composition.

Table 10. Surface water data measured at selected sites on May 10, 2005. Feature Type is indicated by the following codes: GI1, small intermittent spring; GP1, small perennial spring; GP2, large perennial spring; M, monitoring point along a surface watercourse. Peak [UR] is the peak concentration of the tracer uranine after subtracting the measured background fluorescence. Measurements of flow Q are approximate, generally ± 30%. EC is the specific conductivity. Temp is the water temperature.

Site No. Type (code)

Peak [UR] (µg/L)

Qrecharge

(L/s) Qdischarge

(L/s) EC

(µS/cm) Temp (°C)

SW28 M N/A 6.0 381 9.3

43 GP1 not detected 0.8 399 6.7

44 GI1 not detected 2.0 413 6.9

45 * GP1 not detected 1.0 430 5.9

SW27B GP1 0.5 3.0 375 6.0

SW27C GI1 0.4 1.5 377 6.2

SW27D GP1 0.4 1.5 379 6.2

SW27A GI1 0.2 3.0 387 6.3

SW27E GP1 0 1.0 409 6.5

SW27F GP1 0 1.5 411 6.3

SW27G GI1 0 2.0 416 6.3

46 M 0.327 23 386 6.5

48 (at SW20) GI2 not detected 12 452 6.4

77 GP1 not detected 1.0 412 5.2

Allogenic recharge on Amabel plateau (SW28)

6.0 381 9.3

Discharge at resurgences (SW27B, C, D, A)

9.0 380 6.2

Total discharge at SW27 spring group (Site 46)

23 386 6.5

* Measurements were made on May 9 at Site 45 under similar flow conditions.



The electrical conductivities at the first four springs, SW27B, C, D and A, were within 6 µS/cm

of that of the sinking stream at SW28. However, the electrical conductivities at the first three

springs (SW27B, C and D) were below that of the sinking stream recharge at SW28 on May 10.

This is probably a result of temporal variations in water composition. The electrical conductivity

measured at SW28 during the previous afternoon was 372 µS/cm, indicating that the electrical

conductivity of the recharge was rising. Thus, the water composition at the springs was showing

a delayed response to variations at the sinking stream. The mean travel time of the dye

calculated from the tracing data for Site 46 was approximately 71 hours. Since the residence

time in the ephemeral pond was about 5 hours, the residence time of the dye in the overburden

and bedrock aquifers should have been about 66 hours. This residence time is consistent with

the observed values for electrical conductivity at these springs and at SW28.

The electrical conductivities measured at the remaining springs at SW27E, F and G were all

somewhat higher. These springs are probably fed by percolation recharge so the higher electrical

conductivities reflect the longer residence time of the groundwater within the overburden and

bedrock aquifers.

The low tracer concentrations measured at the SW27 springs were due to three factors: 1) the

substantial dilution that took place when the tracer entered the pond, 2) the very high dispersion

that resulted from infiltration through the overburden beneath the pond, and 3) the loss of dye

resulting from decomposition and adsorption. Roughly 10% of the tracer was recovered at the

SW27 watercourse at Site 47. This low recovery is expected because: 1) uranine is sensitive to

daylight so some photo-decay would have occurred during the time that it resided in the pond, 2)

the water in the pond had to infiltrate through a significant volume of glacial sediment before

entering the Amabel aquifer so much of the dye would have been lost due to adsorption onto the

fine-grained sediment, and 3) much of the dye may have been lost through microbially mediated

decomposition, especially while infiltrating through the soil.

At the remaining five springs located at Sites 43, 44, 45, 48 and 77, the measured fluorescence

remained at background levels and no dye was detected (Figure 12). Therefore, it is concluded

that the SW27 spring group is the principal resurgence for the sinking stream at SW28, and

within the SW27 spring group, most of the groundwater flow from the SW28 watercourse



probably resurges at the four closest individual springs (SW27A, B, C and D). Once again, a

distributary pattern of flow is exhibited, but the subsurface flow from SW28 is directed to four

springs all within 20 m of each other.

Several measurements of discharge, electrical conductivity and temperature were made at SW28

and at the SW27 watercourse at Site 46, and these are listed in Table 11. The relative

contribution of sinking stream recharge to the SW27 spring group is estimated from this data by

comparing the flows at SW28 with the discharge from the SW27 spring group (measured at Site

46). These estimates are only approximate because the actual contribution of sinking stream

recharge is controlled by the rate of infiltration through the overburden beneath the ephemeral

pond and this is likely to vary somewhat from the flow at SW28. Nevertheless, the relative

contribution of sinking stream recharge clearly decreases as the flow in the SW28 watercourse

decreases. The relative contribution varied from a maximum of about 50% on May 10 after

heavy rainfall to 0% during the summer and fall when the SW28 watercourse is dry. Had

measurements been made earlier in the spring when runoff is higher, the discharge at the SW27

spring group would have been dominated by sinking stream recharge.

Table 11. Variations in the relative contribution of sinking stream recharge to total discharge at the SW27 spring group.

SW28 (sinking stream recharge) SW27 spring group (Site 46)

Date (mm/dd/yyyy)

Q (L/s)

EC (µS/cm)

T (°C)

Q (L/s)

EC (µS/cm)

T (°C)

Percent Allogenic Recharge

05/14/2005 11 373 11.4 22 401 8.0 50

05/09/2005 7.5 373 15.9 25 379 8.7 30

05/10/2005 6 381 9.3 23 386 6.5 26

07/28/2004 0 — — 3 481 9.0 0

11/19/2005 0 — — 1.1 492 4.8 0

Even though the SW27 spring group receives a relatively large contribution of sinking stream

recharge from the SW28 watercourse during wet weather, it still receives much of its recharge

from widespread percolation through the soil mantle. In other areas where sinking streams are



absent, springs must be recharged entirely by percolation recharge. It is concluded that the

Niagara Escarpment springs, such as those located at SW27, will not exhibit losses of discharge

as a result of the proposed quarrying at the expansion lands. Only those springs located closest

to the quarry will exhibit any reduction in discharge, and even these will still be maintained by

percolation recharge.

8.0 Investigation at the Duntroon Quarry Expansion Lands

Two studies were undertaken at the Duntroon Quarry expansion lands: 1) continuous monitoring

of water levels in three boreholes from across the site, and 2) more detailed studies of the SW2A

spring and the four boreholes located next to it.

8.1 Water Level Data from BH02-1, BH02-4 and BH03-9

Continuous water level measurements were made in three monitoring wells in 2005 to determine

if there are short-term variations in water level, as sometimes occurs in karst aquifers. The three

wells were chosen to reflect the range in onsite conditions. Earlier monthly water level

measurements by Jagger Hims Limited showed that BH02-4 had the greatest and BH03-9 had

the least variation in water level of all the wells on the expansion property. These two wells

were monitored as well as BH02-1, where the range in water level was intermediate.

Results are shown in Figure 15. The period monitored from early May to late October coincided

with the recession from high water levels in the spring to low water levels in the early fall, with

an overall fall in water levels of about 5.4 m at BH02-4, 3.5 m at BH02-1, and 0.2 m at BH03-9.

Precipitation data for the same period are shown in Figure 16. Major precipitation events usually

coincide with rises in the water table of 1-2 cm. These changes occur within hours of the

precipitation event, and are most easily visible in the expanded plot of BH03-9 (Figure 16).

8.2 Investigations in the Vicinity of the SW2 Springs

There are four monitoring wells located near a pair of karst springs at the southwest corner of the

Duntroon Quarry expansion property. These are located well away from the influence of the

Niagara Escarpment and these springs are at the head of a watercourse that flows to the Beaver

River to the west. As such, they provide an excellent opportunity to investigate the subsurface

characteristics of karst development as well as the hydraulic properties of the dolostone aquifer



away from the Escarpment. Investigations conducted at this site include: 1) continuous

monitoring of discharge, electrical conductivity and temperature at the SW2A spring, 2)

conductivity and temperature profiling of the four wells, and 3) groundwater traces conducted

from each of the four monitoring wells to the SW2A spring under natural flow conditions.

8.2.1 Site Description

Figure 17 is a map illustrating the key features of the SW2 watercourse located at the southwest

corner of the Duntroon Quarry expansion lands. The watercourse drains via a culvert beneath

Simcoe Road 91 to the wetland located directly to the west of the existing quarry. Jagger Hims

Limited monitors the streamflow weekly where it crosses the road at SW2. The watercourse is

fed primarily by discharge from two springs. SW2A is a perennial spring located 110 m

upstream from the road, and SW2B is an ephemeral spring located 370 m farther upstream. The

SW2B spring issues from a small, discrete depression in the overburden in a small valley. This

spring only flows for a few days during peak runoff and its discharge may reach 20 L/s or more.

For the rest of the year, the flows measured at SW2 are a good measure of the discharge from the

SW2A spring since the relative contribution from local surface runoff is negligible. This spring

issues from a bedrock conduit beneath a small spring pool (Photo 13). Here, the discharge can

reach 35 L/s or more but during extended dry weather it drops to as little as 0.1 L/s. Flows

measured at SW2 since 1996 indicate that flows range up to 59 L/s and the lowest base flows

observed during summer or fall each year generally range from 0.5 to 1.0 L/s (Jagger Hims

Limited, 2007b). Observations indicate that the watercourse occasionally freezes up briefly

during winter. These are the only times when the watercourse has not been observed flowing,

although there are no observations at the spring to determine if it continues flowing.

The flow characteristics at the two springs suggest that they may be interrelated and exhibit an

overflow-underflow relationship. The SW2B spring is at a higher elevation, its discharge rises

and falls rapidly and it is dry most of the year, characteristics typical of an overflow spring. In

contrast, the SW2A spring is perennial with less variation in flow, temperature and electrical

conductivity, characteristics typical of an underflow spring. However, a connection between the

two springs has not been verified and the SW2B spring could be underdrained by another spring,

perhaps at the wetland located at the northwest corner of the expansion property, identified as

Unit 2 of the Rob Roy PSW by Stantec Consulting (2005).



There is a defined channel extending downstream from the SW2A spring to the road. However,

a defined channel is generally absent farther upstream. At the SW2B spring, a poorly defined

channel extends downstream for 50 m to the north end of a large, shallow depression at Site 16.

This depression is roughly 40 m long, 15 m wide and 1.6 m deep at its deepest point near the

west end. When the SW2B spring starts to flow, the stream enters this depression and a pond

forms. The presence of dolostone outcrops just outside of the depression on the northwest side

suggests that overburden is thin beneath the depression. Although the depression may be formed

by karst processes, its origin is not entirely clear. Regardless, when the SW2B spring stops

flowing, the depression does drain completely over the course of a few days. When the spring

discharge is sufficiently high, the depression floods completely and a much larger pond forms

that is only a few decimetres deep for much of its extent. A suffosion doline to the south at Site

17 also floods and the excess flow continues on the surface to the west. The stream follows a

shallow drainage swale across the field to enter the perennial watercourse just downstream from

SW2A. Where the ephemeral watercourse crosses the field, any surface channel that may have

existed along the drainage swale would have been eradicated by tilling. There is a second

suffosion doline in the middle of the field at Site 18 that is 12 m long, 9 m wide and 40 cm deep.

Its morphology has probably been impacted by tilling as well. A tiny depression at the north

edge appears to have formed recently and suggests that a little of the streamflow sinks here.

There are four boreholes located close to the SW2A spring. Their locations relative to the spring

are shown in detail within the inset in Figure 17. Table 12 lists the details of the four monitoring

wells. The BH03-9 well was drilled in 2003 and it extends through the entire thickness of the

dolostone in the Amabel and Fossil Hill Formations. This hole was cored and the hole was

terminated in shale 0.6 m into the Cabot Head Formation. The three remaining wells were rotary

drilled without coring in 2004. The driller logs indicate that they terminate in grey/blue “shale-

limestone”. However, the depths at the reported dolostone-shale contacts are up to 4.4 m above

that measured in BH03-9. As such, these holes may not penetrate through the entire thickness of

the Fossil Hill Formation. In addition, the top of each well was grouted and steel casings were

installed to depths up to 7.0 m. Therefore, measurements of hydraulic properties, temperature

and water chemistry in these wells will not reflect the development of karst in the upper few

metres.



Table 12. Groundwater monitor details for monitoring wells located near the SW2A spring.

* Wells logs for the three wells drilled in 2004 are based on drill cuttings and not cores, so the shale-limestone contact reported near the base of the holes may not be at the top of the Cabot Head Formation.

8.2.2 Monitoring Data at the SW2A Spring and Nearby Boreholes

Discharge at the SW2A spring was monitored continuously from April to October 2005.

Discharge ranged from <0.1 L/s to 35 L/s (Figure 18). Following rain events, discharge

generally increased within a period of hours and increases were up to several litres per second.

Electrical conductivity and temperature were also measured continuously at SW2A during this

period (Figure 19). The rapid fluctuations exhibited in the electrical conductivity data for July

are the result of instrumental noise, i.e. some instability in the electronics of the conductivity

meter. However, the instrumental noise is negligible in the remainder of the data. The electrical

conductivity of the spring water is inversely related to spring discharge. This relationship is

normal and reflects the longer residence times of the groundwater in the aquifer during the

summer compared to the spring.

There are several short-term increases in electrical conductivity. The most marked is the

increase from 536 to 579 µS/cm, which coincided with 42 mm of rain between June 13 and June

17, 2005. There are smaller increases following 22 mm of rain on May 13-15, 11 mm of rain on

May 27-28, and 35 mm of rain on September 25-30. All these increases reflect the flushing out

of longer residence time groundwater in the aquifer matrix. In many karst springs an initial

increase in electrical conductivity is followed by a substantial drop; this is absent at the SW2A

spring and reflects the absence of sinking streams rapidly recharging the aquifer via conduits.

Designation Diameter

(mm)

Top of Pipe Elev.

(m)

Ground Elevation

(m)

Depth ofWell (m)

Elevation at Top of Shale

(m)

Depth of Overburden

(m)

Depth of Casing

(m)

BH03-9 102 518.93 518.5 39.5 479.6 1.6 4.0

TW04-1 152 517.53 517.1 34.1 483.2 * 1.5 7.0

TW04-2 152 518.11 517.5 34.1 483.9 * 1.2 3.0

TW04-3 152 518.63 518.0 37.5 481.1 * 1.2 2.7



There was a gradual increase in spring temperature from 5.5°C in late April to 9.6°C in October.

The probe was located in the spring pool next to the conduit orifice to minimize the influence of

surface temperatures. Thus, the temperatures should reflect the fluctuations in aquifer conditions

that result from heat conduction and groundwater movement. Short-term variations following

rain events were minimal indicating that the effects of short-term fluctuations in weather are

significantly dampened within the aquifer. Once again, this indicates an absence of sinking

streams recharging the aquifer. Much of this signal suppression likely occurs within the

overburden mantle above the dolostone aquifer. Furthermore, the peak in spring discharge

temperature did not occur until mid-October, about 2 to 3 months after the peak in surface

temperatures. This suggests that the groundwater discharging from the SW2A spring has a mean

residence time in the order of months during the summer and fall.

Correlation of the continuous record of water level at the SW2A spring with the continuous

record in BH03-9 and manual measurements in TW04-1, TW04-2, and TW04-3 show a

convergence of levels over the summer as spring discharge decreased (Figure 20). BH03-9 and

TW04-3 had similar levels, which were consistently lower than levels in the two remaining

wells. This suggests that BH03-9 and TW04-3 are better connected by high-permeability

pathways to the spring. TW04-1 had the highest water level, indicating the lowest permeability

connection to the spring.

Electrical conductivity and temperature profiles were taken at the four wells located near the

SW2A spring. Initial profiles were taken on May 12, 2005 using a probe with a 24 m cable. A

probe with a 60 m cable was used on May 26, 2005, which enabled the profiling to the bottom of

the boreholes. A blockage at a depth of 15.3 m in TW04-3 prevented profiling of the full depth

of that borehole. Results are shown in Figures 21 – 24 for individual boreholes and the results

are shown together in Figure 25. Only the data below the bottom of the casing in each well are

plotted in the figures.

The temperature profiles in the boreholes show that the lower parts of the boreholes were close

to isothermal, with temperatures of 7.7 – 8°C reflecting deep aquifer temperatures. The upper

parts of the boreholes had lower temperatures that either reflect heat conduction or mixing with

colder water recharging the aquifer from the surface. Electrical conductivity values generally



ranged from 400 – 480 µS/cm on May 12 and 450-550 µS/cm on May 26. The increase

observed after 2 weeks reflects the diminished dilution by lower conductivity recharge water.

Abrupt changes occurred in temperature and/or electrical conductivity in all four boreholes.

These abrupt changes cannot be explained by heat conduction and advection, and must reflect

flow into and/or out of the boreholes at specific horizons, such as at elevations of 490 and 502 m

in TW04-1, 487 m in TW04-2, 513 and 515 m in TW04-3 and 488, 498, 502 and 511 m in

BH03-9. These abrupt changes presumably reflect flow along solutionally-enlarged bedding

planes. The contrasts observed in electrical conductivity and temperature between boreholes

provides additional evidence for localised flow along fractures. The fracture apertures are

calculated from the groundwater tracing data (see Section 8.2.4).

8.2.3 Recharge for the SW2 Springs

Six karst drainage basins were identified on the Amabel plateau, as indicated in Section 4.2. The

SW2A and SW2B springs lie within Basin E and are the likely locations for groundwater

discharge from this basin. The perimeter of the basin is defined by the topographic high points

that encompass the area surrounding the springs. However, the actual springshed for the two

springs may be significantly different from this surface catchment.

Jagger Hims Limited has measured flows weekly at SW2 since June 2000. Therefore, there is a

fairly complete record of flows for six years from September 2000 to September 2006. Within

this period, about 4 measurements per year were missed, typically around Christmas and early

January when the flows are intermediate. Therefore, the calculated mean flow at SW2 should be

adequate to calculate the total annual discharge of groundwater from the two springs. The mean

flow at SW2 for the six year period was 9.0 L/s. In addition, Jagger Hims Limited (2005,

Section 4.2.2) calculated a water budget for the region based on climate data from the Thornbury

Slama Station of Environment Canada, located 25 km northwest of the expansion lands. For the

30 Year Normal (1971-2000) they calculated an annual surplus after evapotranspiration of 395

mm. They also calculated the annual surplus for 2003 and 2004 to be 436 and 505 mm,

respectively. Observations indicate that there is no surface runoff leaving Karst Basins D and E,

except what discharges from springs SW2A and SW2B. Thus, any surface runoff within the

springshed is captured underground thereby contributing recharge to the karst aquifer. Thus, the



total groundwater recharge can be estimated using the value for annual surplus, and the

combined size of the springsheds for the SW2A and SW2B springs can be determined using the

total annual discharge calculated from the mean flow at SW2.

Table 13 indicates the calculated area of the springshed for the likely range of groundwater

recharge that may occur for this area. Basin E as defined by topography has an area of only 25

ha, significantly less than the calculated area of the springshed of about 56 to 72 ha. Clearly, the

groundwater discharging from the SW2 springs comes from a much larger area than Karst

Basin E. The area of the springshed is constrained by the elevation of the land surface. For

groundwater to flow to the SW2 springs, the piezometric surface (and the ground elevation) must

be above 515.7 m a.s.l., or the elevation of the SW2A spring. Thus, the area of the springshed

can be approximated by the surface topography since only a limited contiguous area lies above

that elevation. This indicates that the springshed probably includes a portion of Karst Basin D

and the area encompassing Karst Basin E, possibly extending as far west as the “Central

Wetland” on the Highland Quarry property (Azimuth Environmental Consulting, 2006). This

wetland is identified as Unit 5 of the Rob Roy PSW by Stantec Consulting (2005). Azimuth

Environmental Consulting (2006) conducted continuous water level monitoring with a data

logger in OW4, a groundwater monitoring well located roughly 200 m northwest of the SW2A

spring near the east edge of the Highland Quarry property. Their data show distinct responses to

precipitation events, and during dry weather the water table converged to an elevation of 515.7

m, the same elevation as the SW2A spring. This indicates preferential flow along solutionally

enlarged channels to the SW2A spring and provides additional evidence that the springshed for

the SW2A spring extends west of Grey County Road 31. Therefore, the proposed quarries on

either side of Grey County Road 31 (i.e., Highland Quarry and Duntroon Quarry expansion)

have the potential to impact the SW2A spring.

Table 13. The calculated surface area of the springshed for the SW2 springs.

Climate Data Groundwater Recharge (mm)

Mean Spring Discharge (L/s)

Springshed Area (ha)

30 Year Normals 395 9.0 72

2003 Data 436 9.0 65

2004 Data 505 9.0 56



8.2.4 Groundwater Tracing to the SW2A Spring

Natural gradient tracer testing was carried out from the four boreholes located near the SW2A

spring. The substantial discharge from the spring combined with the lack of other springs nearby

indicated that there was convergent flow from a large area to the spring. Accordingly,

monitoring was only carried out at one location, at the spring orifice. Percolation tests were

carried out in the four wells by injecting 17 litres of spring water into the wells and then

monitoring the recovery to static water levels. Wells BH03-9 and TW04-3 recovered to static

levels in less than one minute, whereas Wells TW04-1 and TW04-2 were much slower. Wells

BH03-9 and TW04-3 also had static water levels closest to the elevation of the spring, suggesting

that these two wells were connected to the spring by the largest-aperture pathways. Accordingly,

the first two tracer tests were carried out at these wells.

The ISCO autosampler was used for sampling at the spring. This was supplemented at times by

manual sampling. Details of the tracer tests are given in Table 14 and Figure 26.

The dyes from the first two injections arrived at the spring in less than one hour and,

subsequently, dye concentrations returned close to background values within 3 hours. Dye

injections were then made into the two remaining wells. There were good breakthrough curves

for three of the four traces. The fourth trace was from Well TW04-1. This well had the highest

hydraulic gradient to the SW2A spring so it was anticipated that it would have the slowest

groundwater velocity to the spring. It is presumed that the main pulse of dye arrived at the

spring after sampling was terminated 112 hours after injection.

The traces from BH03-9 and TW04-3 gave groundwater velocities of 38 m/hour and 62 m/hour,

respectively. These values are typical of flow along open solutionally-enlarged fractures in karst

aquifers. The fracture apertures calculated for these traces are 2.7 mm and 3.7 mm, respectively,

calculated using the cubic law. Alternatively, if the flow were through circular channels, then

the Hagen-Poiseuille equation gives channel diameters of 4.3 mm and 6.1 mm, respectively.

These calculations assume smooth-walled fractures or channels. In reality, the walls are likely to

be rough and the actual apertures would be somewhat larger. The traces from TW04-1 and

TW04-2 gave apertures that are less than 0.5 mm (Table 14). In the case of TW04-1, the

calculated apertures are maximum values and assume that the tracer arrived at the spring soon



after sampling ended. The range in apertures for the four tests is typical of karst aquifers, where

most boreholes intercept solutionally-enlarged fractures with apertures in the range 0.1 mm – 10

mm and where aperture widths vary considerably between wells.

It is concluded from the tracer tests at the four wells that the aquifer is karstic and that aperture

widths in the mm range are common and transmit much of the flow. A few larger apertures

likely exist between sinking streams and their resurgences since the sinking streams provide

concentrations of groundwater recharge. Larger apertures should also occur immediately

upgradient from springs where the groundwater flow becomes focussed, and the largest apertures

should occur upgradient from the largest springs. In other areas, the aperture widths should be

much like those at the four wells where they range up to a few mm in width. The implications of

these conclusions are discussed in the final conclusions (Section 9.0).

Table 14. Details of the tracer tests at the SW2A spring on May 12, 2005.

Parameter BH03-9 TW04-3 TW04-1 TW04-2

Tracer Uranine Phloxine B Phloxine B Uranine

Tracer mass (g) 2.34 12.8 10.8 12.3

Time of injection (hr:min) 14:15 14:50 17:55 18:07

Distance to spring (m) 17 24 18 35

Time elapsed to tracer arrival at spring (hr) 0.28 0.26 >119 2.9

Time elapsed to peak concentration at spring (hr) 0.45 0.39 >119 9.9

Groundwater velocity from time to peak concentration (m/hr) 38 62 <0.15 3.5

Head difference to spring (m) 0.041 0.048 0.427 0.727

Hydraulic gradient 0.0024 0.0020 0.024 0.021

Fracture aperture (mm) 2.7 3.7 <0.05 0.27

Channel diameter (mm) 4.3 6.1 <0.09 0.44

Reynolds number if fracture 21 49 <0.002 0.20

Reynolds number if channel 35 80 <0.003 0.33



9.0 Conclusions Regional and local investigations were carried out in the study area to determine the nature and

extent of karstification. The regional investigation identified the principal karst features in an

area that extends approximately 2 km to the north and south of the expansion property. Here, the

landscape is dominated by glacial deposits so the karst features are focused in those areas where

the overburden is thin, especially along the watercourses or close to the Escarpment brow. The

typical diagnostic features of karst such as dolines are not common and many of the features are

subtle. However, within 700 to 1400 m of the Niagara Escarpment there is either an absence of

surface streams or the surface streams sink. This is typical for karst terrain along the Niagara

Escarpment, and six enclosed drainage basins were delineated in this area. Some of the

groundwater flow from there discharges to west-flowing creeks but the majority flows to a series

of springs discharging from the Amabel aquifer at the Niagara Escarpment. The presence of

numerous small to mid-size springs located all along the Escarpment provides further evidence

that a karst aquifer has developed in the Amabel Formation dolostone.

Four tracer tests were carried out from sinking streams, two on the Amabel plateau and two on

the Manitoulin bench. The results were generally similar, with the fastest groundwater pathways

to springs having flow velocities ranging from 500 to 3500 m/day, which is typical of

groundwater velocities between sinking streams and springs in karst aquifers. The field

observations and tracer tests also confirmed that a karst aquifer has developed in the Manitoulin

Formation wherever the overburden is sufficiently thin to permit infiltration, and part of the

discharge from the Amabel aquifer at the Niagara Escarpment infiltrates into the Manitoulin

aquifer. It is concluded that a significant proportion of the discharge at the Manitoulin springs is

derived from groundwater recharge on the Amabel plateau. This verifies the importance of the

monitoring program established by Jagger Hims Limited (2005, 2007b) at the Manitoulin

springs.

Local-scale investigations were carried out on the expansion lands. This work included

continuous water level monitoring at three wells, electrical conductivity and temperature

profiling at four wells, tracer testing from four wells to a nearby spring, and continuous

monitoring of stage and electrical conductivity at that spring. The tracer testing from the wells

gave velocities that ranged from less than 4 m/day to 1500 m/day, which is typical for tracer tests



in karst aquifers when the tracer injections are into boreholes. Calculations show that this

corresponds to fracture apertures that range from < 0.05 mm to about 4 mm along the traced

pathways between the boreholes and the spring. Electrical conductivity and temperature

profiling showed distinct changes at a few horizons in the boreholes, suggesting preferential flow

along a limited number of horizons in each well. The data from the Amabel Formation are

typical of karst aquifers.

A conceptual model for the aquifer was developed from the regional and local studies, from the

observations in the Duntroon Quarry, and from the borehole measurements reported by Jagger

Hims Limited (2005). The uppermost few metres of the bedrock are highly weathered. Below

this, the weathering is focussed on a limited number of fractures, typically producing

enlargements up to several millimetres in size. Openings may be substantially larger along the

flow paths between sinking streams and springs, as well as in the vicinity of the larger springs

where groundwater flow is more focused. The following are the conclusions with respect to the

proposed quarry expansion:

1) Jagger Hims Limited (2005, 2007a) has anticipated that recharge (injection) wells close to the

quarry may be necessary to mitigate the lower groundwater levels predicted in the surrounding

areas as a result of quarrying. With the recharge to the aquifer in the expansion lands dominated

by distributed percolation, it is anticipated that many small channels and only a much smaller

number of conduits (i.e., with a diameter > 1 cm) will be encountered. Thus, the modelling by

Jagger Hims Limited generally provides a good representation of the likely discharges at the

expansion property. Conduits are most likely to be encountered in the area encompassing the

largest springs, at SW2A and SW2B, and it is possible that localized grouting or other mitigation

measures might be required there if inflows to the quarry become problematic. The lack of

sinking streams or springs elsewhere on the expansion property indicates that there is a much

lower probability of encountering large conduits beneath the remainder of the expansion lands.

2) The presence of conduits converging towards the SW2 springs may have the effect of

extending the influence of the drawdown zone around either of the proposed quarries (i.e.,

Highland Quarry or the Duntroon Quarry expansion). The conduit networks surrounding each

spring strongly influence the groundwater elevations within their springsheds. However, this



effect should be largely limited to the extent of the springshed for each of the two springs. The

springshed for the SW2B spring is entirely contained within the expansion property. Therefore,

drawdown effects should not be exacerbated outside of the proposed quarry as a result of

conduits there. On the other hand, the SW2A springshed extends to either side of Grey County

Road 31. Within its springshed, the SW2A spring clearly acts as the local base level as indicated

by the water elevations observed in the nearby boreholes. As groundwater flow diminishes

during the dry season, the groundwater elevations converge towards the elevation of the spring.

If only one of the proposed quarries proceeds, then the drawdown effects will likely be

propagated along conduits across Grey County Road 31. In this case, injection wells may not be

effective at maintaining water levels and localized grouting may be required. However, if both

quarries proceed, then the conduits should not exacerbate drawdown effects because the

influence of the conduits leading to the SW2A spring should not extend outside of the SW2A

springshed, and the springshed is entirely contained within the two proposed quarry properties.

3) The proposed quarries on either side of Grey County Road 31 (i.e., Highland Quarry and

Duntroon Quarry expansion) have the potential to impact the SW2 springs. These springs derive

their groundwater recharge from a catchment area that extends across portions of each of the

proposed quarries. Therefore, quarrying on either side of Grey County Road 31 at either of the

proposed quarries will lead to loss of recharge for the SW2A spring. Furthermore, quarrying at

either of the proposed quarries may lead to complete loss of discharge from the SW2A spring as

a result of the diversion of groundwater flow along conduits intersected by quarrying.

4) The conduits that currently convey groundwater to the SW2A spring may later create

permeable pathways between the two proposed quarries, if both quarries proceed. This could

cause the final lake levels to equalize in elevation if there is excessive leakage. On the other

hand, if the conduits are generally shallow (above 512 m a.s.l.), then there may be little leakage

along the conduits between the final lakes. Localized grouting of the intervening bedrock or

other mitigation measures might be required if excessive leakage between the quarries becomes

problematic.

5) Impacts to the majority of springs along the Niagara Escarpment are likely to be negligible.

With the exception of the SW27 and SW11 springs, the Amabel springs located near the



expansion property derive most of their recharge from widespread infiltration across a broad

band of land adjacent to the top of the Niagara Escarpment. It is concluded that these springs

will not exhibit any significant loss of discharge as a result of the proposed quarrying at the

expansion lands. Only those springs located closest to the quarry will exhibit any reduction in

discharge, and even these will still be maintained by percolation recharge. Furthermore, their

recharge should be fully restored once lakes are established in the quarries.

The SW27 and SW11 springs receive part of their recharge from sinking streams. As indicated

by the groundwater tracing, the SW27 springs are the resurgences for the sinking stream at

SW28, and during peak flows in the spring they receive much of their recharge from the sinking

stream. However, the surface catchment for the SW28 watercourse is outside the expansion

lands and will not be affected by the proposed quarry there. Therefore, there will not be any loss

of sinking stream recharge at these springs. Furthermore, these springs will continue to be

maintained by widespread percolation recharge.

The springs most likely to be impacted by the proposed quarry expansion are the SW11 springs.

These are the principal resurgences for the sinking stream located at the east end of the

expansion property, the SW9 watercourse. Groundwater tracing indicates that after sinking, this

stream flows rapidly in the subsurface and resurges at 19 springs located along the Niagara

Escarpment, with roughly 90% of the flow resurging at the SW11 springs. Despite the

significant component of recharge from the sinking stream, the SW11 springs receive an even

greater contribution from widespread percolation recharge on the Amabel plateau, and it is this

percolation recharge that maintains these springs throughout the dry season. Therefore, with

respect to the proposed quarry at the expansion property, it can be concluded that even with a

significant loss of flow in the SW9 watercourse as a result of quarrying, the SW11 springs will

still be maintained by the percolation recharge.

6) Jagger Hims Limited (2005, 2007a) proposes discharging some of the excess water from

dewatering of the proposed expansion quarry into the SW9 watercourse. This water could be

used to maintain water levels in the two unevaluated wetlands located along the watercourse,

ANSI A and ANSI B, as required seasonally. The quarry discharge could also be used to sustain

flow in the SW9 watercourse to compensate for any loss of surface runoff within its catchment



during wetter periods. Since the SW9 watercourse sinks in its channel and resurges at the SW11

springs and other nearby springs along the Escarpment, the discharge water can also be used to

supplement flows at the Escarpment springs during drier periods. The quarry discharge water

would represent only a small fraction of the existing maximum flows in the SW9 watercourse.

Any minor thermal effects at the Amabel aquifer springs as a result of the quarry discharge

would not affect downstream fisheries because after discharging from the springs, the water

temperature rapidly approaches surface temperatures while flowing down the talus slope and

because the in-line pond on W. Franks property has a pronounced thermal impact that

overwhelms any temperature effects farther upstream (Jagger Hims Ltd., 2007a, b). The quarry

discharge water could be used to maintain the net mean discharge at the springs during the period

that the quarry is dewatered. Once the quarry is complete and fills with water, some of the

excess water from the quarry will flow into the SW9 watercourse seasonally (Jagger Hims

Limited, 2007a).

Report prepared by:

Marcus J. Buck, B.Sc., P.Geo. Stephen R.H. Worthington, Ph.D., P.Geo. Marcus J. Buck Karst Solutions Worthington Groundwater



References Cited Azimuth Environmental Consulting, 2006. Level 2 Hydrogeological Assessment Report

Highland Quarry. Unpublished report prepared for M.A.Q. Aggregates Inc, March 31, 2006,

Cowell, D.W., 1978. Karst Geomorphology of the Bruce Peninsula, Ontario. Unpublished M.Sc. thesis, McMaster University, Hamilton, Ontario, 231 p.

Cowell, D.W. and D.C. Ford, 1983. Karst hydrology of the Bruce Peninsula, Ontario, Canada. Journal of Hydrology, Vol. 61, p. 163-168.

Dreybrodt, W., 1996. Principles of early development of karst conduits under natural and man-made conditions revealed by mathematical analysis of numerical models. Water Resources Research, Vol. 32, p. 2923-2935.

Dreybrodt, W., Gabrovšek, F.,and Romanov, D., 2005. Processes of Speleogenesis: a Modeling Approach. Karst Research Institute at ZRC SAZU, Postojna – Ljubljana, 376 p.

Ecoplans Limited, 2006. South Waterdown Subwatershed Study, Stage 1 Final Report, Vol. I, xlvi + 534p. and Vol. II (10 Appendices).

Field, M.S, 2002. A Lexicon of Cave and Karst Terminology with Special Reference to Environmental Karst Hydrology. National Center for Environmental Assessment, U.S. Environmental Protection Agency, Washington. EPA/600/R-02/003, 214 p. Available online at www.epa.gov/ncea

Ford, D.C. and P.W. Williams, 1989. Karst Geomorphology and Hydrology. Chapman & Hall, New York, 601 p.

Jagger Hims Limited, 2005. Duntroon Quarry Expansion Geological Report and Level 2 Hydrogeological Assessment, Lot 25 and Part Lot 26 Concession 12 and Part Lot 25 Concession 11, Clearview Township, County of Simcoe. Unpublished report prepared for Geogian Aggregates and Construction Inc., Vol. 1, 182 p., Vol. 2 (Figures) and Vol. 3 (Appendices).

Jagger Hims Limited, 2007a. Duntroon Quarry Expansion, Clearview Township, County of Simcoe, Level 2 Hydrogeological Assessment Addendum, Cumulative Impact Assessment Proposed Expansion and Proposed MAQ Highland Quarry, Computer Groundwater Modelling, Response to Agency Comments. Unpublished report prepared for Walker Aggregates Inc.

Jagger Hims Limited, 2007b, Duntroon Quarry Expansion Groundwater and Surface Water Monitoring Program Addendum Lot 25 and Part Lot 26 Concession 12 and Part Lot 25 Concession 11, Clearview Township, County of Simcoe. Unpublished report prepared for Walker Aggregates Inc.



Meinzer, O.E., 1923. Outline of Ground-Water Hydrology. U.S. Geological Survey, Water Supply Paper 494, 71 p.

Pluhar, A. and D.C. Ford, 1970. Dolomite karren of the Niagara Escarpment, Ontario, Canada. Zeitschrift für Geomorphologie, Vol. 14, p. 392-410.

Romanov, D., Gabrovsek, F., and Dreybrodt, W., 2003. The impact of hydrochemical boundary conditions on the evolution of limestone karst aquifers. Journal of Hydrology, Vol. 276, p. 240-253.

Romanov, D., Gabrovsek, F., and Dreybrodt, W., 2004. Modeling the evolution of karst aquifers and speleogenesis. The step from 1-dimensional to 2-dimensional modeling domains. Available online at www.speleogenesis.info.

Scanlon, B.R., Mace, R.E., Barrett, M.E., and Smith, B., 2003. Can we simulate flow in a karst system using equivalent porous media models? Case study, Barton Springs Edwards Aquifer, USA, Journal of Hydrology, Vol. 276, p. 137-158.

Stantec Consulting Ltd., 2005. Duntroon Licence Expansion Level 2 Natural Environment Technical Report. Unpublished report prepared for Georgian Aggregates & Construction Inc., October 7, 2005.

White, W.B., 1988. Geomorphology and Hydrology of Karst Terrains. Oxford University Press, New York, 464 p.

Worthington, S.R.H., Davies, G.J., and Ford, D.C., 2000. Matrix, fracture and channel components of storage and flow in a Paleozoic limestone aquifer, in Wicks, C.M., and Sasowsky, I.D., eds., Groundwater flow and contaminant transport in carbonate aquifers: Rotterdam, Balkema, p. 113-128.

Worthington, S.R.H., and Smart, C.C., 2003. Empirical determination of tracer mass for sink to springs tests in karst. In: Sinkholes and the Engineering and Environmental Impacts of Karst; Proceedings of the ninth multidisciplinary conference, Huntsville, Alabama, Ed. B.F. Beck, American Society of Civil Engineers, Geotechnical Special Publication, No. 122, p. 287-295.


Marcus J. Buck Karst Solutions Figures, Page 72 Worthington Groundwater

Figures

(Located in back pocket) Figure 1. Regional map of karst features and surface water monitoring sites.

Figure 2. Discharge by magnitude of 46 gauged springs in the Amabel Formation and 42

gauged springs in the Manitoulin Formation. The springs have modest discharges, ranging from magnitude 4 (10-100 L/s) to magnitude 7 (0.01-0.1 L/s) using the spring classification of Meinzer (1923).


Marcus J. Buck Karst Solutions Appendix A, Page 96 Worthington Groundwater

Appendix A: Glossary of Karst Terms The following definitions are intended to aid the reader in understanding the terms used in the text, and they are not necessarily universal. In some cases, the use of the terms has been restricted to be relevant or appropriate to the context of this study, or the definitions are those of the authors as they have used them in the text.

The United States Environmental Protection Agency has prepared an extensive lexicon of cave and karst terminology (Field, M., ed., 2002) that can be downloaded free from their website (www.epa.gov/ncea). Some of the definitions used here were derived from those in the EPA document, although they are all modified.

bare karst: A karst where the soil is thin or absent and karst landforms occur on the exposed bedrock.

cave: A natural hole in the ground that is large enough for human entry. In the context of hydrology, a cave is a conduit with dimensions that are large enough for human passage.

channel: (karst channel) Dissolutional voids in the bedrock that form continuous flow paths with a minimum diameter of about 1 mm that is sufficient to permit rapid groundwater flow velocities. Flow is generally laminar in smaller channels with a diameter of less than 10 mm.

conduit: (karst conduit) Relatively large dissolutional voids in the bedrock that form continuous flow paths with a minimum diameter of about 10 millimetres. Although flow may be either turbulent or laminar, flow velocities in karst conduits are relatively rapid. Worthington et al. (2000) used empirical data to show that flow velocities in karst conduits range from about 0.0001 to 1 m/s, with a mean velocity of 0.022 m/s.

conduit flow: Groundwater flow within conduits. Flow may be either turbulent or laminar. See conduit.

doline: A topographically closed depression, commonly circular or oval in plan view. Five genetic types are commonly recognised, though many dolines have more than one mechanism of formation. Collapse dolines are caused by the collapse of bedrock into an underlying void, and often have steep sides. Solution dolines are caused by solution of the bedrock and centripetal flow to a central conduit drain. Suffosion dolines are caused by the subsidence or down-washing of unconsolidated sediments into an underlying conduit drain in bedrock. Subsidence dolines are caused by the subsidence of bedrock above a solution void. Buried dolines are ancient dolines that have been filled in by unconsolidated sediments, such as glacial deposits.

dry valley: A valley that lacks a permanent surface stream. In karst, dry valleys form initially by normal fluvial processes but as karst develops, surface runoff is eventually captured underground, at which point the valley becomes inactive or relict.



epikarst: The upper portion of the bedrock, beneath the soil, that is characterized by extensive fracturing, and enhanced solution and weathering. Significant water storage and transport occur in this zone.

fluviokarst: A landscape with both fluvial and karst landforms. The dominant landforms are valleys cut by surface streams, but the surface streams are captured underground as the karst develops. Fluviokarst commonly forms where karst is mantled by thick, impermeable soil. Surface streams initially perched on the soil are eventually captured underground as they erode through the soil mantle and come into contact with the bedrock.

holokarst: A karst landscape with little or no surface runoff or streams, and often characterized by well developed karst landforms.

karren: Small-scale dissolution features on soluble rocks, such as limestone and dolostone.

karst: A landscape that forms as a result of solutionally enhanced secondary permeability in the bedrock, and characterised by rapid groundwater flow velocities and the occurrence of solution features such as karren, dolines, bedrock channels, caves, sinking streams, and springs.

karst aquifer: An aquifer with solutionally enhanced secondary permeability, chiefly characterized by rapid groundwater flow velocities and the occurrence of continuous flow paths along channels that direct groundwater flow from recharge areas to springs.

mantled karst: A karst where the bedrock is covered by unconsolidated sediment.

recharge: The process of the addition of water to groundwater. Reference is made to two types of recharge in the text. Sinking stream recharge is the concentrated recharge that is derived from surface streams that sink, either at discrete points such as in dolines, or more gradually along a losing reach. In the local setting, the surface streams are perched upon glacial sediment that isolates the stream water from the karst aquifer until the water sinks. Percolation recharge is the widespread and diffuse infiltration of precipitation either directly into the bedrock, or through the glacial sediment where the karst is mantled. Sinking stream recharge exhibits wide variations in rate and chemistry in response to precipitation and it infiltrates rapidly. In contrast, percolation recharge exhibits much less variation in rate and chemistry in response to precipitation and it infiltrates slowly.

resurgence: A spring principally fed by one or more sinking streams. Resurgences are characterised by a wide range in discharge and chemistry, and the water typically becomes turbid after heavy rain.

runnel: A groove on the surface of the bedrock formed by dissolution.

sinkhole: Synonymous with doline (sinkhole is chiefly used in the United States). A cover collapse sinkhole is a suffosion doline that forms by sudden collapse of unconsolidated sediment into an underlying cavity formed by soil piping above a solutionally widened drain in the bedrock. A cover subsidence sinkhole also forms by soil piping and downwashing of sediment into a solutionally widened drain in the bedrock but the overlying sediment gradually subsides.



sinkpoint: A discrete location where a surface stream sinks underground into a conduit.

sinking stream: A surface stream which sinks underground, either at a sinkpoint, or along a losing reach where flow is lost by gradual infiltration into the ground.

soil piping: The transport of material through pipes in unconsolidated sediments. The soil pipes are typically round and a few mm to a few cm in diameter but may be larger. In mantled karst, soil pipes can permit rapid infiltration of surface water into the underlying karst aquifer.

spring: A natural outflow of groundwater to the surface.


Marcus J. Buck Karst Solutions Appendix B, Page 99 Worthington Groundwater

Appendix B: Photographs Contents Page Photos 1 - 6 ............................................................................................................................. 100

Photos 7 - 10 ........................................................................................................................... 101

Photos 11 - 16 ......................................................................................................................... 102

Photos 17 - 20 ......................................................................................................................... 103

Photos 21 - 24 ......................................................................................................................... 104

Photo 25................................................................................................................................... 105



Photo 1. Group of suffosion dolines located to the west of SW28 watercourse at Site 9. The ephemeral pond occasionally floods to the edge of these dolines when runoff is high.

Photo 2. Suffosion doline at Site 8 drained by a large soil pipe at the base. This doline formed by soil subsidence and downwashing of fines into an underlying karstic drain.

Photo 3. A suffosion doline at Site 10 that formed by sudden collapse of the soil into an underlying cavity. The doline is 1.8 m deep with slightly overhanging walls. Such dolines are also called cover collapse sinkholes.

Photo 4. A sinking stream at Site 173 at the west edge of Grey County Road 31 2.4 km south of the Duntroon Quarry. The stream emerges from the culvert in the foreground and sinks as it crosses the field in the background. The stream likely resurges 150 m to the south at a spring at Site 174.

Photo 5. The SW28 watercourse in the foreground flows into the ephemeral pond in the background where it sinks through the overburden. The stream resurges 300 m to the east at the SW27 springs.

Photo 6. Two hours after the uranine injection at SW28, the dye cloud had migrated partway across the pond as it was displaced by new water entering from the watercourse. The estimated residence time in the pond was 5 hours.



Photo 7. The uranine injection into the SW9 watercourse a short distance upstream from SW9. The sinking stream resurges at the SW11 springs and a number of other springs located along the Niagara Escarpment to the east.

Photo 8. The phloxine B injection into a small sinking stream on the Manitoulin bench just downstream from the water supply system at SW10. The stream resurges at the SW11 springs and possibly at other springs along the Manitoulin escarpment.

Photo 9. Small intermittent spring emerging from a soil pipe at Site SW27g. The spring is at the elevation of the Amabel Formation not far below the crest of the Amabel escarpment (visible in the background).

Photo 10. A dug well located at an Amabel spring at Site 147. This small perennial spring issues from overburden at the elevation of the Amabel Formation along the Amabel escarpment slope. Backpack for scale.



Photo 11. Small perennial spring at Site 77 emerging from a bedrock conduit in the Amabel Formation. A pond was once excavated just downstream but the stream has since eroded through the earth dam and the pond is now drained.

Photo 12. Small spring issuing from the base of the talus slope along the Amabel escarpment at Site 39. The stream continues flowing across the Manitoulin bench but gradually infiltrates into the overburden over a distance of over 100 m.

Photo 13. SW2A spring with the outlet channel in the background. The water emerges from a bedrock conduit at the base of the pool to the right of the staff gauge (vertical steel pipe).

Photo 14. View looking upslope towards a small perennial spring at Site 29. The spring seeps from the overburden at the base of the 5-metre high erosional escarpment that has formed near the top of the Manitoulin Formation.

Photo 15. Ditch extending from an intermittent pond in the distant background (not visible) to where it ends abruptly in the foreground at Site 6.

Photo 16. Relict fluvial gully that once drained the Amabel plateau in Nottawasaga Lookout Provincial Park. The view is upstream from the crest of the Amabel escarpment. Any surface runoff now drains into dolines on the plateau.



Photo 17. The SW2B spring emerges from a small depression in the overburden located in this small valley. At the time, about 20 L/s was discharging from the ephemeral spring. In the distant background, the stream enters a large ephemeral pond occupying a relatively large depression.

Photo 18. A derelict concrete cistern constructed at a small perennial spring at Site 159. Spring water still issues from the talus and some of the flow is captured in a bucket and directed into the hose. A small bedrock scarp is just visible at the crest of the Amabel escarpment in the background.

Photo 19. A dug well located at a small spring near the crest of the Manitoulin escarpment at Site 52. The steel cistern collects water, which then feeds the hose visible in the foreground.

Photo 20. The Hobo weather station used to monitor temperature, relative humidity, rainfall and solar radiation during the spring, summer and fall of 2005. It was located at the east end of the expansion property.



Photo 21. The north wall of the Duntroon Quarry. The upper few metres of the dolostone are well fractured and distinctly weathered. Many of the fractures are parallel to bedding and a few extend for more than 100 m. Beneath this, the dolostone is only cut by a few prominent vertical fractures that are often visible from rusty weathering. Otherwise, weathering in the lower dolostone is distinctly less and it retains a blue-gray colour.

Photo 22. The south wall of the Duntroon Quarry at the middle settling pond (Site 21). Here the interreefal dolostone is well fractured parallel to bedding, although fracturing and weathering is most pronounced in the upper few metres. A large spring issues from various points along a prominent fracture just above the pond, with most of the discharge occurring close to the large earth dam at the right. The remaining discharge is over a width of about 10 m toward the left side of the photo.

Photo 23. Small intermittent springs issuing from various fractures in the wall of the Duntroon Quarry at Site 22, located below the asphalt plant. The springs are highly visible because of the dark green algae growing on the moist rock.

Photo 24. Small intermittent spring located at Site 24 below the asphalt plant in the Duntroon Quarry. The spring issues from bedding planes at the base of the upper fractured zone.



Photo 25. View across the centre of Karst Basin D during the spring melt in 2005. This is one of two closed drainage basins at the expansion property. There are no surface outlets for this basin and any surface runoff collects in two shallow pools at the lowest elevation, visible in the centre of the photograph. The water in the pools gradually infiltrates into the overburden. The internal drainage and lack of surface watercourses suggest that surface water infiltrates readily into the underlying karst aquifer.


Marcus J. Buck Karst Solutions Appendix C, Page 106 Worthington Groundwater

Appendix C: Classification and Description of Features Contents Page Table C-1: Classification of features inventoried during the field investigation......................107

Table C-2: Location and description of features inventoried during the field investigation ....108

Table C-3: Incidental observations of groundwater use at springs........................................144



Table C-1: Classification of features inventoried during the field investigation

Code is an identifier for classifying and plotting features. N is the number of features associated with either the Amabel or the Manitoulin Formations. The four small springs issuing from other aquifers are not included.

Feature Code NAmabel NManit. Explanation

Relict spring GR 1 0 Field evidence clearly indicates a spring but no evidence for recent discharge was observed.

Small spring G1 1 1 Discharge does not usually exceed 10 L/s. Large spring G2 2 0 Discharge usually exceeds10 L/s at least once annually.

Small perennial spring GP1 35 23 Almost always flowing and discharge does not usually exceed 10 L/s.

Large perennial spring GP2 7 2 Almost always flowing and discharge usually exceeds10 L/s at least once annually.

Small intermittent spring GI1 26 31 Discharge is intermittent and does not usually exceed 10 L/s.

Large intermittent spring GI2 2 0 Discharge is intermittent and usually exceeds 10 L/s at least once annually.

Small sinkpoint P1 4 0 Discrete point at which streamflow is lost at a doline or depression, or at a discrete point along a watercourse. The capacity is probably less than 20 L/s.

Large sinkpoint P2 3 0 Discrete point at which streamflow is lost at a doline or depression, or at a discrete point along a watercourse. The capacity is probably greater than 20 L/s.

Sinking stream with discrete sinkpoint SP 3 3 A watercourse that loses flow to the subsurface at a

discrete sinkpoint, typically at a doline.

Sinking stream that loses flow gradually along a losing reach

SL 3 24 A watercourse that loses flow to the subsurface by gradual infiltration along a “losing reach”. The infiltration likely occurs where the soil mantle is thin, then enters the underlying karst aquifer.

Dry valley SD 3 0 A relict fluvial valley that no longer has any surface flow, typically marked by dolines along its length.

Small suffosion doline DS1 6 7 Doline formed in the soil mantle with a surface area less than 20 m2 and less than 1.0 m deep.

Large suffosion doline DS2 13 1 Doline formed in the soil mantle with a surface area greater than 20 m2 and greater than 1.0 m deep.

Monitoring point (surface water) M 51 62

Location along a surface watercourse where discharge, temperature, electrical conductivity or fluorescence were measured.

Springs utilized for water supply (dug well, cistern) WS1 7 4

A dug well utilizing well tiles or a cistern designed to collect spring water for use as a drinking water supply or for livestock.

Other uses of springs (ponds, pipes) WS2 6 0

Either an artificial pond constructed at a spring, or the presence of a plastic or steel pipe at a spring suggesting former use as a water supply. The intended use is generally unknown.



Table C-2: Location and description of features inventoried during the field investigation

The location of each feature is identified by a unique site number (Site). Generally, the site numbers are listed from north to south. However, they are also grouped into several distinct geographic areas that are labeled within the table. These groups are arranged to facilitate finding features by their site number. Features are classified as to feature type (Type) and the codes for each feature type are explained in Table C-1. The UTM coordinates (Easting, Northing) are expressed in metres relative to NAD 1927. The elevation (Elev.) is indicated in metres above mean sea level. Many of the features are illustrated on Figure 1 using unique symbols for each feature type. The remaining features are illustrated on more detailed maps for selected areas (Figure 3, 13 and 17).

Site Type Easting (m)

Northing(m)

Elev.(m)

Description

Amabel plateau in the vicinity of Nottawasaga Lookout Provincial Park 1 DS2 559115 4917182 502 Broad, shallow suffosion doline that is 13 m in

diameter and 1.4 m deep located along the base of a broad, shallow valley. There is dolostone subcrop exposed a few metres to the west.

2 DS2 559159 4917180 502 Broad, shallow suffosion doline that is 20 m in diameter and 1.1 m deep located along the base of the broad, shallow valley.

3 DS2 559266 4917172 502 A cluster of several small suffosion dolines located within a broad, shallow depression. The largest of the dolines is 8 m long, 6 m wide and 1.0 m deep.

4 DS2 559313 4917134 503 Circular, cone-shaped suffosion doline that is 5 m in diameter and 1.0 m deep.

5 DS2 559349 4917066 503 Broad, shallow suffosion doline that is 16 m long, 8 m wide and 1.0 m deep located along the base of the broad, shallow valley.

6 P1 559639 4916793 505 The south end of a drainage ditch that appears to be excavated to drain a seasonally flooded area located to the northwest. The ditch ends here abruptly and gradually deepens towards this end. At this point, the ditch is 1.5 m deep. The seasonally flooded area may dry out completely during the summer and much of it has been reforested.

SW28 M 559693 4916347 500 Monitoring point located about 10 m upstream from the ephemeral pond that sinks into the karst. This was also the injection site for the groundwater trace.

7 P2 DS

559718 4916336 500 Ephemeral pond that sinks through the overburden into karst. It is fed by the SW28 watercourse flowing from the west. When runoff is high, the water level rises about 1.2 m and overflows the large depression. Most of the excess flow follows an overflow or flood channel to the Amabel escarpment, then continues down the escarpment slope past the SW27 springs. When in flood, the pond extends to the edge of the dolines at Sites 8 and 9 and these also flood. These may capture some of the flow as well. A bedrock ridge exposed about 18 m to the north of the lowest point in the pond suggests that overburden is thin.




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SW28A M 559754 4916346 501 Monitoring point located just downstream from the ephemeral pond. The watercourse here probably floods only briefly during the peak of spring runoff. From here to the escarpment, the land was once tilled and is now reforested in white pine, so the watercourse can only be traced when it is flowing. However, where the watercourse approaches the escarpment, the stream has incised 4 m into the overburden to expose the dolostone bedrock at the crest of the Amabel escarpment. The dolostone is buff-white with a distinctive gray-mottled pattern. It is thin- to medium-bedded and medium-crystalline.

8 DS1 559707 4916290 502 Suffosion doline situated a few metres to the west of the cluster of dolines at Site 9. The doline is 3.0 m long by 2.5 m wide and 1.0 m deep. It drains into a well developed soil pipe at the base, which is roughly 12 cm in diameter, at least 40 cm deep, and inclined at an angle of 20° from horizontal. Bedrock is not exposed. The overburden is primarily composed of clay and silt with some sand and a few small boulders.

9 DS 559715 4916289 502 A cluster of three closely-spaced and overlapping suffosion dolines with a maximum depth of 1.0 m. Bedrock is not exposed at the dolines. The overburden is clay-silt with minor sand and boulders. A few fieldstones have been dumped into all three dolines. These dolines may capture some of the flow from the adjacent ephemeral pond when it floods.

10 DS2 559729 4916307 501 A recently created suffosion doline that formed by the sudden collapse of the overburden into an underlying void sometime between April 24, 2004 and May 9, 2005. The surface opening is 1.5 m by 1.2 m. This opens into a void that is 1.9 m by 1.6 m with a depth of 1.8 m, with overhanging walls. The doline is located about 5 m within the flood limits of the ephemeral pond and likely takes some water when flooded.

11 GI1 WS2

559424 4915883 516 A small spring emerging from overburden at the edge of a hill composed of glacial sediment. There are several kettles located nearby. The closest is 60 m due south. It appears that the spring was once dug out to form a shallow pond about 8 m in diameter. However, the dam has since eroded and the pond is now largely drained and grassy. A small watercourse extends northward to the ditch along the south edge of 26/27 Sideroad.




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Description

SW9 watercourse 12 M 560418 4915415 509 SW9 watercourse about 23 m upstream from SW9.

This is the point where fluorescein dye was injected on April 23, 2005 for a groundwater trace. The watercourse can be traced about 65 m farther upstream to the beginning of an unevaluated wetland, then an additional 75 m into the wetland. The wetland is a low area that floods during the spring and that is forested primarily with eastern white cedar.

SW9 M 560440 4915421 509 JHL surface water monitoring point along the SW9 watercourse where it crosses the path.

13A M 560471 4915444 509 A low bedrock ridge outcrops on the north edge of the SW9 watercourse. This is the first bedrock exposed along the watercourse. The creek starts losing flow here where the overburden is thin. There is no indication that any flow is lost farther upstream. Much of the watercourse farther downstream from here is poorly defined and cannot be traced except when it is flowing.

13B M 560491 4915447 509 The SW9 watercourse was observed sinking here during moderately low flow. At the time, the stream was observed gradually sinking in the silt bed over a distance of 20 m. Dolostone outcrops adjacent to the channel here indicating that overburden is thin.

14A M 560531 4915469 509 The small tributary from Site 15 joins the SW9 watercourse just upstream from an ephemeral pond that is 30 m long, 15 m wide and up to 40 cm deep. This pond only forms briefly when flow is high in the watercourse.

14B M 560602 4915488 508 The SW9 watercourse about 20 m downstream from the ephemeral pond where flow is confined to a single channel. The channel is poorly defined and difficult to follow except when there is streamflow. A low bedrock ridge outcrops about 20 m to the south suggesting that the overburden is thin.

14C P1 560636 4915476 508 The SW9 watercourse where 6 L/s was observed sinking in a small isolated pool that was 7 m long, 2.5 m wide and 30 cm deep.

14D P1 560651 4915516 508 Final sinkpoint along the SW9 watercourse on April 25, 2005 during moderately high flow when 2 L/s sank at a small pool that was 5 m long by 4 m wide and 30 cm deep. The remaining 7 L/s sank along the previous reach, from Site 14C to 14D. About 20 m farther downstream, the watercourse enters an obvious ditch that continues for another 100 m out to the edge of a field. The watercourse was traced for an additional 150 m downstream from the ditch. However, this final reach has been tilled and the watercourse can only be traced when there is streamflow.




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Description

15 M 560490 4915322 509 A small ephemeral watercourse draining an unevaluated wetland located to the south. The wetland is a low area that floods in the spring and that is forested primarily with eastern white cedar. From there, the stream follows a poorly defined, braided channel towards the northeast. The watercourse loses flow by gradual infiltration through the overburden. About 2 L/s were observed during moderately high flow and all of this was lost before reaching the SW9 watercourse.

SW2 springs (expansion property) SW2B GI2 559295 4914917 522 Large ephemeral spring situated at the head of a small

flood channel that leads to the watercourse just downstream from the SW2A spring. The spring emerges from a small vertical-walled depression in overburden that is 1.4 m long, 0.8 m wide and 0.5 m deep. It is located between two dolostone ridges suggesting that the overburden is thin. The outflow channel is about 1.5 m wide and 0.3 m deep. Up to 22 L/s were observed issuing from the spring. However, the spring dries up quickly and it behaves like an overflow spring. The SW2A spring may be the underflow spring but this has not been determined. The elevation of the spring is about 522.3 m above mean sea level based on 1 m contours on the site plan (Figure 1-2, Jagger Hims Limited, 2005).

16 DS2 559262 4914854 520 A topographic depression that is roughly 40 m long and 15 m wide. It is located along the ephemeral watercourse about 50 m downstream from the spring at SW2B. Any flow entering the depression sinks slowly through the overburden causing the depression to flood. Even after the flow from SW2B stops, it takes several days for the depression to completely drain. When the capacity of the depression is exceeded, the depression overflows to the southwest forming a sizeable but mostly very shallow pond. The deepest point in the depression is at the west end where the depression floods to a maximum depth of 1.6 m. Although bedrock is not exposed within the depression, a low bedrock ridge is exposed on the north side indicating that overburden is thin.

17 DS1 559239 4914822 521 Suffosion doline that is 10 m long, 5 m wide and 50 cm deep. Some surface flow may sink here when the larger depression to the north overflows. Regardless, the overflow from the larger depression flows past this doline before entering a poorly defined channel extending across the field to the southwest. Some garbage has been dumped into the doline.




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Description

18 DS1 559120 4914785 520 A very shallow depression located in the open field that is 12 m long, 9 m wide and 40 cm deep. During spring 2005, there was fresh silt and clay alluvium deposited across much of the depression from spring runoff. There was also a tiny depression at the north end that is 60 cm in diameter and 25 cm deep. This appears to have formed by soil suffosion and probably acts as a minor sinkpoint for the pool that forms here during high flow. The depression is interpreted to be a suffosion doline that has likely been impacted by tilling. During peak spring runoff, the watercourse from SW2B extends past this depression following a very shallow gully across the field. Any channel that may have existed has likely been eradicated by tilling.

SW2A GP2 559071 4914672 515.7 Large, perennial spring emerging from a bedrock conduit and feeding a small pool. The pool is about 50 cm deep, with silt and sand sediment sloping upwards to the outlet channel. A well defined channel extends from the spring through a poorly drained area down to SW2 after crossing beneath Simcoe County Road 91. The elevation of the water surface at the spring pool during low flow is 515.7 m a.s.l., based on an elevation survey by Jagger Hims Limited in 2006. Amphipods collected here on November 17, 2005 by M. Buck were identified by Dr. John Holsinger as Gammarus lacustris, a widely distributed species commonly found in cold water habitats, including lakes, streams, wetlands and springs.

19 M 559066 4914673 517 Water samples from the SW2A spring were collected where the discharge crosses an obvious opening in the second control structure constructed at the outlet to the spring pool. The control structures are loose rocks placed across the stream channel. All groundwater tracing samples were collected here.

Duntroon Quarry DP1 DS1 559465 4914116 511.8 Recently formed depression located in the wetland to

the west of the quarry at a drivepoint piezometer installed by JHL (DP1). Apparently, the depression formed after the piezometer was installed. Since similar depressions were not found elsewhere along the south edge of the wetland, this suggests that the origin of the depression may be related in some way to the installation of the piezometer. The depression is 3 m long, 2.5 m wide and 0.6 m deep. The sides are overhanging in places indicating rapid subsidence/collapse of underlying sediment. The overburden is moist, black peat although there is one solutionally pitted dolostone boulder exposed in the wall. There are also numerous dolostone boulders situated on the gentle slope about 12 m to the south that are suggestive of underlying outcrop, but this is unclear. The depression clearly drains well and is tentatively interpreted to be a suffosion doline.




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Description

20 GP2 559455 4914433 502 In 2004, a large spring was observed issuing from fill at the base of the west wall of the quarry. Water discharged from the fill at three separate points over a width of 12 m. A water storage pond has since been constructed at the west end of the quarry to reduce or eliminate groundwater flow into the quarry at this location.

21 GP2 559595 4914335 508 In 2004, a large spring was observed issuing from the south wall of quarry at the second settling pond. In summer, much of the flow emerged from an inclined fracture (159/25SW) that terminated to the southwest at a prominent bedding plane. In high flow, an additional 5 L/s was observed emerging from the bedding plane about 20 m farther to the east. At the inclined fracture, the fracture aperture was variable but ranged up to 9 cm in width. By 2005, the spring had become buried in sediment and it is not known if it continues to flow.

22 GI1 559776 4914448 511 The largest of two springs located along the west-facing quarry wall below the asphalt plant. The spring was issuing roughly halfway up the quarry wall from several bedding planes over a width of about 20 m. The highest spring was about 11 m above the quarry floor. At the time, the springs were obvious because of dark green algae growing on the moist quarry wall beneath the springs. This quarry face was subsequently quarried in July 2004.

23 GI1 559782 4914433 507 A smaller spring located along the west-facing quarry wall beneath the asphalt plant, about 15 m south of the larger spring at Site 22. Water was observed discharging from a bedding plane about 7 m above the quarry floor. Dark green algae was present on the moist quarry wall beneath the spring. This quarry face was subsequently quarried in July 2004.

24 GI1 559870 4914430 510 A small spring located along the south-facing quarry wall beneath the asphalt plant. Water discharges from a prominent bedding plane about 10 m above the quarry floor. Dark green algae was present on the moist bedrock wall beneath the spring.

Amabel escarpment north of 26/27 Sideroad 25 GP1 558832 4917243 475 A small perennial spring issuing from talus about 40 m

up from the base of the talus slope. From here, the flow extends down the talus a short distance before sinking into the talus. From here, the flow must continue down the slope to resurge upstream from Site 28.




Northing(m)

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Description

26 GP1 558866 4917254 475 Small perennial springs located part way up the talus slope on the Amabel escarpment. The springs issue from the talus over a width of about 20 m. From here, several braided channels extend about 40 m down through the talus to where they converge at the head of the prominent gully cut deep into the glacial sediment. Other small springs were observed slightly to the west but their discharge was negligible.

27 GI1 558860 4917287 465 Small spring located at the base of the talus slope along the Amabel escarpment. The spring discharges from overburden at the base of the prominent gully, which is 50 m wide and 6 m deep. The gully extends an additional 25 m or more up the talus slope.

28 M 558838 4917304 462 Monitoring point located about 13 m downstream from the junction of the two spring-fed streams and just upstream from where the Bruce Trail side trail crosses the watercourse at a small footbridge. The flow here represents the combined discharge from the springs located farther up the slope at Sites 25 to 27.

29 GP1 558846 4917465 453 Spring emerging from overburden at the base of a 5 m high erosional escarpment at the top of the Manitoulin Formation. From here, a channel extends down the slope that is 2.5 m wide and 60 cm deep. There are numerous 5 to 50 cm diameter residual boulders in the channel indicating erosion of boulder till.

30 GP1 558887 4917503 455 Small spring issuing from overburden at the base of a 5 m high erosional escarpment formed at the top of the Manitoulin Formation. The discharge follows an obvious channel that is 2 to 3 m wide and 60 cm deep. It contains numerous small residual boulders from erosion of the till.

31 GP1 WS2

559065 4917424 482 Several small springs emerge over a width of about 50 m just up the slope from the base of the steep talus slope along the Amabel escarpment. The discharge from the springs converges farther down the slope into a single channel at the base of the escarpment slope. The presence of a 2 inch diameter steel pipe suggests that the spring was once utilized as a water supply.

32 M 559009 4917476 468 A monitoring point located about 75 m downstream from the springs at Site 31 where the watercourse reaches the lower edge of the dolostone rubble apron extending out from the Amabel escarpment slope. From here, the watercourse meanders across the Manitoulin bench.

33 M 558911 4917535 455 A second monitoring point located farther down the watercourse where it drops down a short, moderately steep slope. This 5 m high slope is the upper tier of the Manitoulin escarpment.




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Description

34 GP1 WS2

559133 4917539 475 A series of small springs emerging from the base of the talus slope along the Amabel escarpment. From there, the streamflow can be traced discontinuously through dolostone boulders for 70 m where it finally emerges from a prominent apron of dolostone boulders. The presence of a plastic pipe there suggests that this spring was once utilized as a water supply. It is not clear how the apron formed but the subangular shape of the dolostone boulders indicates some erosion and transport of the boulders, more than would be expected for talus. On May 13, 2005, the stream flowed an additional 100 m out across the Manitoulin bench before completely infiltrating into the overburden. However, the channel can be traced about 20 m farther across the gentling sloping surface.

35 GP1 559159 4917657 465 Small spring emerging from over a width of 20 m along the base of the same apron of dolostone boulders found below Site 34. From the spring, the stream flows across the Manitoulin bench for about 20 m to a wet area with shrubs and grass where the water infiltrates into the overburden. The Manitoulin bench here has a very gentle slope toward the north.

36 GP1 559206 4917667 464 Small spring emerging at the base of the prominent apron of dolostone boulders that extends 50 m out from the Amabel escarpment. On May 13, 2005 the watercourse starting at the spring meandered across the very gentle slope of the Manitoulin bench for about 100 m before finally sinking into the overburden next to the OFSC trail. The stream has incised very little and there is no defined channel.

37a 37b 37c 37d

GI1 GI1 GP1 GP1

559453 559468 559487 559497

4917572491756849175634917560

468 A series of four closely spaced springs discharging from overburden near the base of the Amabel escarpment. The discharge from each spring follows a small channel down the slope to where the streams sink into the overburden as they approach the Manitoulin bench, about 25 to 30 m from the springs. From west to east, the springs are identified as 37a, 37b 37c and 37d.

38 GI1 559537 4917565 467 Small spring issues from the base of the talus slope along the Amabel escarpment. A small channel extends down the slope about 35 m to the edge of the Manitoulin bench where the stream finally sinks into the overburden. The channel is 1.5 m wide and 30 cm deep. The Manitoulin bench is quite prominent here and has a slope of about 4 m per 100 m.




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39 GP1 559685 4917493 470 Small spring issuing from the base of the steep talus slope along the Amabel escarpment. An obvious gully leads down the slope from the spring that is 3 m wide and 70 cm deep. The channel is filled with small, residual gneiss boulders from fluvial erosion of the boulder till. The overburden here is dense, buff clay with numerous pebbles, cobbles and boulders. On May 13, 2005 the stream was observed sinking into the overburden about 125 m farther downstream at a wet grassy area that is about 20 m in diameter.

40 GI1 WS2

559721 4917167 483 Small spring located at the base of the Amabel escarpment. The spring is in the center of a 50 m wide embayment that extends 40 m back into the escarpment. The discharge immediately enters an artificial pond that is 40 m long and 25 m wide and about 1 m deep. The pond has an outlet at the east side. The outflow is minimal and sinks into the overburden within a few metres. There is a shallow gully extending about 130 m down the gradual slope to the east. The gully is about 10 m wide and 1 m deep.

41 GP1 559986 4916965 477 Small spring issues from the base of the steep talus slope along the Amabel escarpment. The spring discharges from the talus over a width of 10 m and the flow sinks into the overburden within 20 m at the edge of the Manitoulin bench.

42 GP1 560024 4916942 477 Small spring issuing from the base of the steep talus slope along the Amabel escarpment. The spring discharges from the talus over a width of about 25 m. On May 13, 2005 the surface flow followed a channel to the northeast across the Manitoulin bench and eventually sank in the overburden within 80 m.

43 GP1 560216 4916787 475 Small spring issuing from the base of the steep talus slope along the Amabel escarpment. The surface flow follows a channel across the Manitoulin bench and completely sinks in the overburden within 50 m of the spring.

44 GI1 560187 4916729 487 Small spring issuing from talus about 3 m below the 4 m high dolostone cliff that marks the crest of the Amabel escarpment. The discharge flows down the talus slope and immediately sinks into the overburden at the base.

45 GP1 560181 4916517 482 Spring issuing from the base of the talus slope along the Amabel escarpment. The discharge flows eastward across the Manitoulin bench and gradually sinks into the overburden. However, the channel can be traced almost all the way to the Manitoulin escarpment.




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Description

SW27B GP1 560015 4916351 491 Small perennial spring located about 14 m down the slope from the Bruce Trail on the south edge of the SW28 watercourse. The spring discharges initially from the head of a small shallow channel cut into overburden situated about 2 m from the edge of the SW28 watercourse. In 2004, the water issued from a soil pipe in dense, medium-gray clay containing angular to subangular rock fragments (presumably till). Since then, soil collapse has covered the soil pipe with dolostone rubble. There is dolostone subcrop located about 1 m up the slope so the overburden here must be thin. There are numerous glacial boulders within the gully ranging up to 1 m across. These are primarily gneiss and may be residual but were just as likely dumped here from the fields above the escarpment.

SW27C GI1 560018 4916348 491 Small intermittent spring located along the south bank of the watercourse about 4 m southeast of SW27B and about 50 cm lower in elevation. The spring discharges from overburden about 2 m up the bank from the creek bed. A small channel extends down the bank to the creek bed.

SW27D GP1 560020 4916347 491 Small perennial spring located along the south bank of the watercourse about 6 m southeast of SW27B and about 1 m lower in elevation. The spring discharges from dolostone rubble about 3 m up the bank from the creek bed. A vague channel extends down the bank to the main watercourse.

SW27A GI1 560018 4916332 491 Intermittent spring issuing from a small soil pipe at the head of a well defined channel that is cut 1 m into the overburden. The spring is at the same elevation as the spring at SW27B. The spring is located about 9 m down the slope from the Bruce Trail. The overburden exposed in the channel is brown clay-silt-sand with about 10% rock fragments and may be glacial till.

SW27E GP1 560040 4916329 487 Small perennial spring issuing from clay-rich overburden over a width of about 12 m along the south bank of the creek. Although the discharge is somewhat dispersed, this was one of the two largest concentrations of flow. From here, the discharge flows about 6 m down the gully bank before entering a more defined channel.

SW27F GP1 560044 4916327 487 Small perennial spring issuing from clay-rich overburden over a width of about 12 m. Although the discharge is somewhat dispersed, this was one of the two largest concentrations of flow. From here, the discharge flows about 6 m down the gully bank before entering a more defined channel.




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Description

SW27G GI1 560035 4916313 491 Small spring emerging from a soil pipe in clay-rich overburden. The spring is at the same elevation as SW27A and SW27B. There is a small suffosion doline located 5 m to the south that is 2 m in diameter and 60 cm deep. Bedrock is not exposed at the spring or doline.

SW27H GR 560062 4916308 488 Small relict spring at the head of a gully that is 3 m wide, 50 cm deep, and extends down the slope towards the main watercourse. The spring is marked by a depression that is 3 m in diameter and 80 cm deep. There was no indication of recent flow.

46 M 560101 4916337 477 Stream monitoring point located about 10 m downstream from the junction of two tributaries from the various SW27 springs farther up the slope. The flow measured here represents the combined discharge from the SW27 springs. This was the initial location of the ISCO autosampler for the SW28 groundwater trace. Farther downstream, the gully is about 70 m wide and is cut 3.5 m deep. The graded channel is often braided with a width up to 10 m. There are numerous residual boulders of gneiss and dolostone from erosion of the till.

47 M 560138 4916336 473 Stream monitoring point located about 40 m farther downstream from location 46. This was the second location for the ISCO autosampler. It was moved to assure complete mixing of flow from the various tributaries farther upstream.

48 GI2 WS1

560002 4916172 495 Large intermittent spring located in the field not far north of 26/27 Sideroad. The discharge issues from the head of a fluvial gully eroded into the overburden at the elevation of the Amabel Formation. In 2004, a derelict concrete cistern indicated that this was once utilized as a water supply. A new well tile was installed here prior to May 9, 2005 for use by the newly constructed house located farther up the slope.

SW20 M 560051 4916170 490 Monitoring point along the watercourse at the Bruce Trail. The watercourse is fed by discharge from the spring at Site 48.

Manitoulin escarpment north of 26/27 Sideroad 49 GP1 559141 4917866 448 A small spring issues from overburden near the crest

of the Manitoulin escarpment. The stream has eroded into dense gray clay till. This is the first of a series of small springs at the head of a prominent gully cut into the escarpment.

50 GP1 559169 4917865 444 A small spring issues from overburden immediately below an outcrop of thinly bedded dolostone at the crest of the Manitoulin escarpment. There is a second smaller spring located 4 m to the east at the same elevation.

51 GP1 559213 4917840 444 A small spring issues from overburden just 3 m below an outcrop of thinly bedded dolostone at the crest of the Manitoulin escarpment.




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52 GP1 WS1

559261 4917845 448 A small spring issues from overburden about 15 m from the top of the Manitoulin escarpment. A steel cistern has been installed here to opportunistically utilize the spring discharge for a water supply.

53 M 559200 4917956 415 Monitoring point at the base of the Manitoulin escarpment where all of the small spring-fed tributaries converge into a single watercourse. The flow here represents the combined flow from the springs at Sites 49, 50, 51 and 52.

54 GI1 559295 4917844 444 A small spring issues from overburden near the top of the Manitoulin escarpment. There are several other small ephemeral springs nearby. The discharge from the springs between Sites 54 and 56 converges into a single watercourse farther down the slope.

55 GI1 559383 4917888 435 A small ephemeral spring issues from overburden along the Manitoulin escarpment.

56 GI1 559420 4917882 435 A small ephemeral spring issues from overburden at a subtle erosional bench below the Manitoulin escarpment. This bench can be traced for some distance and typically has a gentle slope and a width of about 5 to 10 m.

57 GI1 559479 4917835 452 A small ephemeral spring issuing from overburden about 8 m down the slope from an outcrop of thinly bedded dolostone at the crest of the Manitoulin escarpment. A small gully extends down the slope from the spring.

58 GI1 559551 4917836 452 A small ephemeral spring issuing from overburden about 8 m down the slope from an outcrop of thinly bedded dolostone at the crest of the Manitoulin escarpment.

59 GI1 559840 4917770 430 A series of small springs that issue from overburden along the lower tier of the Manitoulin escarpment over a width of about 100 m. The combined discharge from these springs converges into a single watercourse about 100 m farther down the slope. There are channels extending farther up the slope indicating that during peak flow there is discharge from near the crest of the escarpment. The spring discharge was not measured.




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60 GI1 559791 4917649 452 The first of at least three small springs that issue from overburden at the base of the upper tier of the Manitoulin escarpment. The upper tier of the escarpment is quite distinct with a relief of about 3 m, and thinly bedded dolostone often outcrops along its crest. Next to this, there is a distinct erosional bench that is nearly horizontal that extends to the crest of the lower tier of the Manitoulin escarpment. The discharge from the springs flows through vernal pools and poorly drained areas perched on the bench before converging into a single channel at the crest of the lower tier of the Manitoulin escarpment at Site 63. The bench narrows and eventually disappears about 100 m to the northwest where the upper and lower tiers join into a single escarpment slope.

61 GP1 559815 4917626 452 A second small spring issuing from overburden at the base of the upper tier of the Manitoulin escarpment. Thin-bedded dolostone outcrops about 5 m up the slope.

62 GP1 559851 4916618 452 A third small spring issuing from overburden at the base of the upper tier of the Manitoulin escarpment, which has a relief of about 4 m at this site.

63 M 559870 4917672 450 Monitoring point where the watercourse reaches the crest of the lower tier of the Manitoulin escarpment. From here, the stream cascades down the escarpment face along a sloping waterfall. This is a convenient location to measure the combined discharge from the springs between Sites 60 and 62.

64 GP1 559927 4917574 452 A small spring issuing from overburden at the base of the upper tier of the Manitoulin escarpment. During low flow, most of the discharge issues from overburden farther down the slope at Site 66. The streams issuing from the spring group at Sites 64 to 68 have carved a substantial gully into the glacial deposits covering the escarpment slope. Their combined discharge converges into a single channel about 100 m farther down the slope.

65 GP1 559988 4917565 452 A small spring issuing from overburden at the base of the upper tier of the Manitoulin escarpment. There is a second smaller spring located just to the west at the same elevation. V. Smidor (property owner) indicated that these springs flow quite well early each spring.

66 M 560047 4917611 437 Monitoring point along a prominent gully extending down the lower tier of the Manitoulin escarpment. The flow here is fed by spring discharge near the crest of the escarpment (from Site 64 65) as well as from farther down the gully.

67 GP1 560100 4917554 432 Several small springs issue from overburden at this elevation. The largest of these is located at the base of the steepest part of the slope at the head of a small gully that is 3 m wide and 1 m deep. However, during high flow much of the discharge emerges farther up the slope.




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Description

68 GI1 560111 4917506 448 Spring issuing from overburden just below the crest of the lower tier of the Manitoulin escarpment at the head of an obvious gully. Here, the Manitoulin escarpment has two distinct tiers. The upper tier starts abruptly and has a moderate slope with a total relief of about 6 m. Thinly bedded dolostone commonly outcrops near the crest. Between the two tiers, there is a 25 m wide erosional bench with a very gentle slope where the overburden appears to be thin. The second tier starts abruptly and descends at a moderate slope.

69 M 560904 4917860 380 Monitoring point along a watercourse about 1.3 km downstream from its source at the Manitoulin springs between Site 59 and Site 68. During low flow, much of the flow originates at these springs.

70 GI1 560266 4917258 445 Small spring located at the head of an obvious gully that has cut through a low moraine situated just northeast of the upper tier of the Manitoulin escarpment. The water discharges from the overburden for some distance along the gully. The gully rapidly increases in size to about 30 m wide and 4 m deep and contains numerous cobbles and boulders ranging from 5 to 50 cm in diameter. The channel is 1.5 to 2 m wide suggesting that it occasionally has flows up to 30 L/s or more. Transported branches and leaf litter caught up on obstacles indicate greater flow earlier in 2005, also suggesting more substantial flows during the peak of spring runoff. Upstream from the spring, a very subtle gully extends westward to the Manitoulin escarpment. This gully is 40 m wide and 2.5 m deep. There is no defined channel in the gully but it may have been eradicated by tilling. This valley would be the natural surface outlet for the topographic depression that lies between the Manitoulin escarpment and the nearby moraine. The Manitoulin escarpment here is quite distinct. It has a relief of about 7 m and dolostone commonly outcrops at its crest.

71 GI1 560345 4917003 452 A series of small springs that issue from overburden at the base of the Manitoulin escarpment over a width of about 30 m. The discharge from the springs sinks within 10 m along the valley that lies between the escarpment and the moraine. The moraine is a broad, gentle ridge with only a few metres of relief at most. It is set back from the Manitoulin escarpment about 80 m and extends for at least 600 m parallel to the escarpment. It is similar to the moraine located to the south of 26/27 Sideroad and is at the same elevation.




Northing(m)

Elev.(m)

Description

72 GI1 560368 4916909 456 Small spring issuing from overburden about half way up the Manitoulin escarpment. The spring is 6 m down the slope from an outcrop of thin-bedded dolostone (roughly 2 m lower in elevation). The water flows down the slope and sinks in the shallow valley that lies between the escarpment and the adjacent moraine, about 50 m downstream from the spring.

73 GI1 560406 4916850 450 Small spring issuing from overburden at the base of the Manitoulin escarpment. The escarpment here distinct, with a vertical height of about 7 m. The discharge feeds an elongated area that is poorly drained

74 GI1 560368 4916785 459 Small spring issuing from overburden at the base of the Manitoulin escarpment. The escarpment here is nothing more than a moderate slope that rises vertically about 5 m. There are other very small springs nearby but with negligible flow. The discharge feeds a narrow area that is poorly drained without an obvious outlet. Presumably the flow normally infiltrates into the overburden.

75 GP1 560362 4916650 457 A poorly drained area extending for about 200 m along the base of the Manitoulin escarpment where the ground is saturated. There is no open water but much of the ground remains quite damp throughout the year and the vegetation is open forest with shrubs and other water-loving plants. Most of the area of saturated ground is about 20 m wide except near the centre where it extends down the slope about 60 m. It appears to be fed by widespread discharge from the Manitoulin escarpment.

76n 76s

M 560273 4916317 457 Monitoring point at the junction of two tributaries. The north tributary (76n) is fed by discharge from the SW27 springs. The south tributary (76s) is fed by discharge from the spring at Site 48. The Manitoulin Formation is exposed along the base of the gully to a point about 40 m farther up the north tributary.




Northing(m)

Elev.(m)

Description

Amabel and Manitoulin escarpments south of 26/27 Sideroad 77 GP1

WS2 560123 4916051 493 Small spring issuing from a bedrock conduit located

along of the Amabel escarpment. The actual outcrop is quite small. However, there are small exposures of bedrock about 10 m farther up the slope. At the spring, the stream has cut 1.2 m through the overburden. Just downstream from the spring, the overburden was excavated and an earth dam was built about 14 m downstream to create a pond. The earth dam is 80 cm high and up to 3 m wide. However, the stream has since cut through the earth dam and it has largely drained via a new channel that continues down the slope. Nevertheless, the relict pond contains a few cattails suggesting that wet conditions persist throughout much of the year. There is one length of 4.4 cm O.D. steel pipe lying at the spring pool suggesting that the spring was once utilized as a water supply. From the spring, a stream was observed flowing down a small, poorly defined channel for 180 m down the slope when flow was relatively high. During low flow, the stream was observed sinking much farther up the slope and it is clear that the stream gradually looses flow all along the channel by gradual infiltration into the overburden.

78 GP1 560354 4916195 460 Small spring issuing from overburden over a width of 15 m at the head of a gully that is generally 15 m wide and 1.3 m deep. The spring is roughly at the elevation of the Manitoulin Formation. The position of the spring suggests that some of its recharge may be from the loosing stream located farther up the slope. The spring discharge was measured farther down the watercourse at Site 79.

79 M 560390 4916241 450 Monitoring point located downstream from the spring at Site 78 where the watercourse enters the ditch along the south edge of 26/27 Sideroad. All of the discharge from the spring is confined to a single channel at the ditch.

80a 80b 80c

GP1 560458 560471 560475

491613049161174916099

460 A series of three closely spaced springs discharging from the overburden at the elevation of the Manitoulin Formation. The three springs are spread out over a distance of about 50 m. The overburden is light brown, dense silt-clay till with 10-20% angular rock fragments. Each of the springs was monitored separately and identified as 80n (northern spring), 80c (central spring) and 80s (southern spring). Their combined discharge was measured farther downstream at Site 82n.




Northing(m)

Elev.(m)

Description

81 GP1 560544 4916105 461 Spring issuing from dolostone rubble at the base of the 4 m high dolostone cliff at the crest of the Manitoulin escarpment. A water supply system was installed just down the slope at SW24A. The Manitoulin dolostone was quarried here but it appears that the quarrying was quite limited along the exposed face. The discharge is easier to measure downstream at SW24A or at location 82s.

SW24A M WS1

560544 4916123 455 Water supply system installed about 18 m down the slope from the Manitoulin spring on the former F. Sestito property. It uses a barrel to collect water from the spring.

82w 82s

M 560559 4916162 446 Monitoring point at the junction of two tributaries. The north branch (82n) is fed by spring discharge from Site 80. The south branch (82s) is fed by spring discharge from Site 81.

83 M 560665 4916148 447 Monitoring point along a watercourse about 55 m upstream from SW24 and the pond. The watercourse is fed by spring discharge at Site 84.

84w 84c 84e

GI1 560693 560706 560718

491613249161254916116

448 A series of small springs discharging from the base of the talus slope beneath the Manitoulin escarpment. All of these likely derive much of their recharge from the surface stream that sinks just downstream from SW21C, located on the Manitoulin bench. Their combined discharge follows a defined channel to the west past Site 83 to the pond at SW24. The three springs from west to east are identified as 84w, 84c and 84e. Measurements were not made at the springs but one measurement was made of their combined discharge at Site 83 and there are numerous measurements at SW24.

85w 85e

GP1 560746 560764

49161104916107

448 Two small springs discharging from the base of the talus slope beneath the Manitoulin escarpment. Both likely derive much of their recharge from the surface stream that sinks just downstream from SW21C, located on the Manitoulin bench. Their combined discharge follows a poorly defined channel eastward to Site 87 where it joins another spring fed tributary flowing from the east. The west spring is 85w and the east spring is 85e. Measurements were not made here but one measurement was made farther downstream at 87w during springtime. The springs are presumed to be perennial since SW21C has flow extending throughout the summer.

86 GP2 560601 4915941 485 Spring discharging from the base of the prominent talus slope along the Amabel escarpment. From here, braided channels extend down the gradual slope roughly following the edge of the forest to SW21C. The braided channels form a single channel at SW21C.




Northing(m)

Elev.(m)

Description

SW21C M WS1

560698 4916023 469 JHL stream monitoring point where the farm road crosses the watercourse. H. Franks has installed a water supply system here. In low flow, all of the flow is captured in the water supply system. However, a poorly defined channel extends to the crest of the Manitoulin escarpment. In high flow, the stream sinks towards the escarpment. There are some vague channels farther down the talus slope suggesting that the stream may occasionally flow over the escarpment.

87w 87e

M 560851 4916084 446 Stream monitoring point at the junction of two tributaries. The west branch (87w) is fed by discharge from springs at Site 85. The east branch (87e) continues upstream to SW21D and is fed by spring discharge from Sites 88, 90 and just east of SW21D. Red shale of the Queenston Formation is exposed along the channel at this site.

88 GI1 560866 4915970 455 Uppermost spring issuing from talus along the Manitoulin escarpment. There is additional discharge all the way down the slope, including at the well at Site 89.

89 WS1 560886 4915982 451 Dug water well located towards the base of the Manitoulin escarpment. This well opportunistically utilizes the spring discharge from the Manitoulin escarpment. The well is a round concrete tile 113 cm in diameter and extending 70 cm above the ground with a flat iron cover.

90 GI1 560880 4915951 458 A small ephemeral spring that briefly issues from talus just down the slope below the dolostone cliff at the crest of the Manitoulin escarpment. The spring is at the edge of a farm road that angles up the escarpment.

SW21D M 560948 4915931 448 JHL stream monitoring point at the steel culvert where a farm road crosses over the watercourse. On the upstream side, there is a pond that is roughly 60 m long, 25 m wide and 50 cm deep. Its volume was estimated to be roughly 75 m3 when the flow at the culvert was 2 L/s. Based on observed flows, it is clear that the pond must be spring fed.

Manitoulin escarpment primarily north of Simcoe County Road 91 227w GI1 561034 4915837 458 The first of four closely spaced springs, all located

about 10 m from the base of the talus slope. This intermittent spring issues from overburden at the west end of the watercourse leading to Franks Pond. The spring is located in cedar forest and there is no defined channel leading downstream. The flow from the spring is partially concealed by fallen branches and deadfall from cedar trees.

SW11D GP1 561038 4915831 458 JHL monitoring point at a perennial spring located at the head of a small gully that is 2 m wide and 50 cm deep. The spring issues from overburden between a few boulders at the head of the small gully.




Northing(m)

Elev.(m)

Description

SW11C GI1 561040 4915829 458 An intermittent spring monitored monthly by JHL. Apparently, this is located next to SW11D. This spring was not noted during the karst investigation.

227e GI1 561043 4915827 458 An intermittent spring discharging along a shallow gully that is 2 m wide and 60 cm deep.

227 M 561047 4915831 458 Monitoring point where the combined flow from sites 227w, SW11D, SW11C and 227e was measured. There is a small defined channel at this point.

SW11B GP2 561062 4915815 457 JHL monitoring point at a perennial spring with a well defined spring run that extends 5 m to the main creek. The spring issues from overburden at the head of the 1.2 m wide channel, about 15 m from the base of the talus slope. The overburden is light brown, dense clay till. The channel bed is sand and gravel with a few small boulders.

228 GP1 561067 4915813 457 Perennial spring discharges along a small, poorly defined gully that extends about 4 m south of the main creek. This small inconspicuous spring issues from overburden about 15 m from the base of the talus slope.

SW11Aw SW11Ae SW11A

GP2 GP1

561083 561084

49158054915804

457 JHL monitoring point that measures the combined discharge from two adjacent perennial springs (SW11B) at the head of a well defined channel that extends 6 m to the main watercourse. The overburden is light brown clay till. The channel bed is silt with small angular rubble. The west spring (SW11Bw) emerges from beneath the roots of a tree and the east spring (SW11Be) discharges from beneath a pile of rotting wood. The springs emerge about 25 m from the base of the main talus slope, although there are a few boulders extending down the slope as far as the springs.

91 GI1 561105 4915793 457 JHL monitoring point that measures the discharge from an intermittent spring issuing from overburden along the south bank of the main creek just upstream from the 60 cm diameter steel culvert. The discharge flows across a wide channel with small subangular boulders covered with moss.

SW11 M 561120 4915791 456 JHL monitoring point located along the watercourse about 10 m downstream from the culvert beneath the trail.

92w 92c 92e 92

GP1

561119 561128 561133 561137

4915785491578049157764915780

456 Small, inconspicuous springs issuing from overburden over a distance of about 20 m along the south bank of the main watercourse. The perennial flow follows a small rut for over 30 m before entering the main watercourse. Groundwater tracing samples were collected just downstream from the springs where the flow converged into a single channel (92). The west spring (92w), central spring (92c) and east spring (92e) were all monitored separately on some occasions.




Northing(m)

Elev.(m)

Description

93 GI1 561174 4915751 456 A small ephemeral spring that issues from overburden at the edge of the farm road. The discharge flows down the ruts along the farm road.

SW11E M 561211 4915760 443 JHL stream monitoring point located about 15 m upstream from the pond along the main watercourse. The channel here descends at a slope of 0.14 and is a 3 m wide braided or graded channel. The bed is cobbles covered with moss and other vegetation.

94 GI1 561200 4915740 446 Small ephemeral spring emerges from overburden along the south bank of the farm road. The discharge initially follows the road then descends the slope along a defined channel extending to the pond. Groundwater tracing samples were collected about 12 m downstream from the spring.

95n 95s 95

GI1 561220 561225

49157334915726

445 Two small ephemeral springs issuing from overburden along the south bank of the farm road. The discharge from the north spring (95n) and south spring (95s) converges along the road then descends the slope along a poorly defined channel extending to the pond. Groundwater tracing samples were collected just downstream from the springs where the flows converged (95).

96 GI1 561239 4915720 443 Intermittent spring issuing from overburden at the head of an obvious gully or spring run. The gully is about 3 m wide and 70 cm deep and extends 12 m to the edge of the pond. There are a few residual boulders exposed along the base of the gully.

97 GP1 561247 4915708 442 Small perennial spring issuing from overburden along a gully or spring run that extends to the edge of the pond. The gully is 3 m wide and 80 cm deep. There are a few moss-covered, residual boulders along the base of the gully.

98 GI1 561245 4915693 446 Small intermittent spring issuing from overburden along the south bank of the farm road. The discharge initially follows the road then descends the slope towards the pond.

99 GI1 561210 4915633 464 Spring issuing from dolostone talus just below a small bedrock scarp where the Manitoulin Formation is exposed. The elevation of the spring is 5.6 m below the top of the bedrock scarp. The discharge flows down the slope beneath talus for 13 m before finally emerging at the head of a poorly defined channel that extends down the talus slope to the springs at Site 101. The channel bed is dolostone rubble partly covered with moss.

100 GI1 561220 4915649 456 Intermittent spring issuing from talus about half way down the talus slope along the Manitoulin escarpment. The spring is located at the head of a fairly obvious channel. The bed of the channel consists of moss-covered dolostone boulders and cobbles.




Northing(m)

Elev.(m)

Description

100A GI1 561212 4915660 455 Ephemeral spring issues from talus about half way down the talus slope along the Manitoulin escarpment. The spring is located at the head of a poorly defined channel.

101n 101c 101s 101

GI1

561248 561250 561251 561249

4915683491568049156774915686

446 Small intermittent springs issuing from overburden along the south bank of the farm road. The discharge crosses the road then descends the slope towards the pond. The springs are located roughly at the base of the talus slope below a poorly defined channel in the talus. The north (101n), central (101c) and south (101s) springs were monitored separately. Their combined flow was measured at the edge of the farm road (101).

102 M 561258 4915676 445 Stream monitoring point at the downstream end of a 26 cm diameter steel culvert where an intermittent watercourse crosses beneath the farm road. The watercourse extends down the talus slope from the intermittent spring at Site 100. Near the farm road, the watercourse has a defined channel that is about 1 m wide and 50 cm deep.

103 GP1 561264 4915686 442 Small perennial spring located about 12 m downstream from Site 102. The spring issues from overburden about 20 m from the base of the talus slope at the head of an obvious shallow gully or spring run that extends 8 m to the main watercourse just upstream from SW12.

104 GP1 561270 4915677 442 Small spring issuing from overburden about 20 m from the base of the talus slope along the Amabel-Manitoulin escarpment. A spring run extends 9 m northeast to the main watercourse about 20 m upstream from SW12. The gully at the spring is about 4 m wide and 1 m deep.

105 M 561282 4915683 441 Stream monitoring location along the main watercourse, about 25 m upstream from SW12 and 2 m upstream from the spring run from Site 104.

106 GP1 561346 4915591 443 Spring issuing from overburden over a width of about 25 m along the southwest bank of the watercourse. This was not monitored during summer or early fall but is presumed to be a perennial spring.

107 M 561454 4915449 451 Culvert near B. Frank's shed. The small watercourse here is fed by discharge from various small springs located along the base of the talus slope below the Manitoulin escarpment.

SW12A M 561471 4915441 450 JHL monitoring point along a watercourse about 320 m upstream from SW12.

108 M 561470 4915433 451 Stream monitoring point near the southeast corner of B. Frank's shed at a small watercourse that is fed by spring discharge from the base of the Manitoulin escarpment. This stream is tributary to the main watercourse about 10 m to the east.

109 M 561480 4915437 451 Monitoring point near the head of the small watercourse about 110 m from Simcoe County Road 91.




Northing(m)

Elev.(m)

Description

110 GI1 561451 4915342 465 Spring issuing from dolostone rubble at the base of the 2.5 m high bedrock wall of a small quarry in the Manitoulin Formation. The quarry was excavated about 10 m into the Manitoulin Formation immediately north of Simcoe Country Road 91. From the spring, the stream flows across the quarry floor then flows down the steep talus or rubble slope to Site 111.

111 M 561472 4915360 455 Stream monitoring location at the base of the talus/rubble slope that lies beneath the Manitoulin escarpment. The stream originates up the slope at a bedrock spring at Site 110. The total discharge from the springs is better measured at this site.

112 GI1 561495 4915210 462 Spring located along the Manitoulin escarpment issuing from dolostone rubble excavated from the adjacent, abandoned quarry. Since the quarry is dry, the flow almost certainly discharges from a bedrock spring. Flow was measured about 15 m farther downstream (to the north) in a well defined but small channel. Farther downstream, some of the flow infiltrates into the overburden where it crosses the field, but the remainder flows south to where it enters a poorly drained forested area before crossing Concession 10 at Site 191. There is additional groundwater seepage into the forested area along the base of the Manitoulin escarpment. However, the largest of the springs observed was at Site 112.

Amabel escarpment north of Simcoe County Road 91 113 GI1 561086 4915711 473 Small intermittent spring that issues from the base of

the talus slope along the Amabel escarpment. There is a distinct erosional bench on top of the Manitoulin Formation that is about 15 m wide with a slope of about 0.1. The discharge from the spring was observed flowing part way across the bench before sinking into overburden about 5 m from the top of the Manitoulin escarpment.

114 GI1 561165 4915625 475 Small intermittent spring discharging from the base of the talus slope along the Amabel escarpment. The flow immediately enters a small intermittent pond that is 5 m long and 3 m wide. The pond contains black, organic-rich sediment. A small channel extends northeast across the Manitoulin bench and the stream gradually sinks into the overburden along the length of the channel. During high flow the stream was observed flowing about 20 m to just 5 m short of the top of the Manitoulin escarpment.

115 GI1 561164 4915604 475 Small intermittent spring issuing from the base of the talus slope. The discharge sinks almost immediately into overburden at the edge of the Manitoulin bench.




Northing(m)

Elev.(m)

Description

116 GP1 DS1

561163 4915593 475 Small perennial spring situated at the base of the talus slope along the Amabel escarpment. The discharge enters a small ephemeral pool where there is black organic-rich sediment. There is a small suffosion doline situated 2 m south of the spring at the edge of the talus slope that is 1.5 m in diameter and 0.6 m deep. The suffosion doline stays dry even though it is at a lower elevation than the adjacent spring indicating that it is well drained.

117 GI1 561168 4915580 475 Small intermittent spring located at the base of the talus slope along the Amabel escarpment. During high flow, the discharge enters an intermittent pool located just downstream then flows along a poorly defined watercourse across the Manitoulin bench most of the way to the Manitoulin escarpment. The flow gradually sinks into the overburden and no flow was observed reaching the lower escarpment. The pool is in a very shallow depression that is partly filled with wet, black organic-rich sediment.

118 GP1 561172 4915573 475 Small perennial spring located at the base of the talus slope along the Amabel escarpment. During high flow, the discharge enters the same intermittent pool that is also fed by spring discharge from Site 117.

119 GI1 561171 4915566 475 Small intermittent spring located at the base of the talus slope. The discharge flows 6 m east where it sinks into a doline at Site 120.

120 DS1 561176 4915568 475 Suffosion doline that is 5 m long, 4 m wide and 0.4 m deep, containing wet, black organic-rich sediment.

121 GI1 561176 4915553 475 Ephemeral spring issuing from the base of the talus along the Amabel escarpment. A small channel, 2.5 m wide and 0.5 m deep, extends 6 m east to the suffosion doline at Site 122.

122 DS1 DS1

561183 4915554 475 Suffosion doline that is 7 m long, 4 m wide and 0.8 m deep, situated 5 m from the base of talus slope. The doline contains two fieldstones that were probably dumped there. The overburden is silt with some clay and sand. There is a second suffosion doline, 3 m long, 3 m wide and 0.7 m deep, located 5 m to the south. It has a small soil pipe at the base that is 3 cm in diameter.

123 DS2 561186 4915518 475 Suffosion doline located 4 m from the base of the talus slope along the Amabel escarpment. The doline is 5 m long, 5 m wide and 1.0 m deep and contains more than 30 fieldstones. A small gully enters from the south but no flow was ever observed there. There probably was a spring there that is now relict or only active during very high flow.

SW10n GP1 561182 4915421 479 One of two closely spaced springs that feed the small watercourse flowing past SW10. The stream from the north spring joins the stream from SW10s about 5 m upstream from SW10. During spring, some water issues from the talus at least 30 m farther up the talus slope.




Northing(m)

Elev.(m)

Description

SW10s GP1 561174 4915414 478 The second of two closely spaced springs that flow to SW10. The spring issues from the base of the talus slope. During spring, discharge issues from the talus at least 30 m farther up the talus slope.

SW10 M WS1

561192 4915418 477 JHL monitoring point along the watercourse about 5 m upstream from B. Frank's well tile catchment. The water supply system consists of three well tiles buried in gravel in the small pool, each about 90 cm in diameter. The overflow from the pool either sinks into overburden along the channel to the east or sinks in the suffosion doline at Site 124 during high flow. While conducting the SW9 watercourse groundwater trace, water samples were collected about 2 m downstream from the well tiles. A second, simultaneous trace was conducted here by injecting Phloxine B fluorescent dye just downstream from the well tiles.

124 DS1 561211 4915421 476 Suffosion doline that is 5 m long, 3 m wide and 1.1 m deep, partly filled with large fieldstones. The doline drains into an obvious, 20 cm diameter soil pipe at its base. This is the sinkpoint for the stream from the two springs at SW10n and SW10s. There is currently no indication of any channel or gully extending eastward across the cultivated field that extends across most of the Manitoulin bench.

125 DS1 561213 4915412 476 Suffosion doline that is 10 m long, 5 m wide and 90 cm deep containing numerous fieldstones. A small channel extending from springs to the doline may still be active but no flow was observed during the study.

126 GI1 561178 4915382 478 Small spring located at the base of the talus slope along the Amabel escarpment. A small channel extends 15 m to the east and the spring discharge gradually sinks into the overburden along this channel.

127 GP1 561167 4915356 478 Small spring issuing from the base of the talus slope along the Amabel escarpment. A channel extends down the slope to the edge of the cultivated field but there is no indication that surface flow continues across the field. The stream was observed sinking into overburden at the edge of the field.

128 M 561196 4915360 476 Monitoring point located along the watercourse 30 m downstream from the spring at Site 127. The spring discharge was better measured here.

129 GI1 WS2

561112 4915285 486 Small spring located at the base of the talus slope along the Amabel escarpment. A small channel extends 10 m down the slope to a junction with the channel from Site 130. There is one length of 2" O.D. steel pipe at the spring suggesting that the spring was once utilized as a water supply.

130 GI1 561094 4915281 488 Small spring located at the base of the talus slope along the Amabel escarpment. Dolostone bedrock is exposed at the 4 m high cliff at the top of the talus slope, about 25 m to the west. A small channel extends down the slope to the east.




Northing(m)

Elev.(m)

Description

131 M 561152 4915272 479 Stream monitoring point located about 15 m downstream from the junction of the two spring-fed tributaries, about 10 m upstream from the edge of the cultivated field. This was a convenient location to monitor the combined flow from the two springs at Sites 129 and 130. A well defined channel continues eastward to the cultivated field. Although the stream was observed flowing as much as 50 m across the cultivated field before completely infiltrating into overburden, the channel is largely eradicated by tilling. However, a very subtle, shallow drainage swale extends across the Manitoulin bench all the way to the Manitoulin escarpment.

132 Lime Kiln

561112 4915248 487 Well preserved lime kiln. The inner chamber is about 2 m in diameter, 3.5 m high and is lined by small gneiss boulders ranging up to 40 cm in diameter. The top is open but covered with decaying logs and vines (quite hazardous for anyone unaware of the kiln!). The lateral opening at the base of the kiln has collapsed slightly and the metal door has been placed inside the chamber. The lateral opening extends through to the outside surface of the wall, which is planar, roughly vertical and built from slabs of Manitoulin dolostone. The surrounding ground is covered in a blanket of periwinkle.

Amabel escarpment south of Simcoe County Road 91 133 GP1 561041 4915092 492 Perennial spring issuing from coarse talus about 6 m

from a prominent cliff where the Amabel Formation is exposed. A poorly defined channel extends down to the base of the talus slope. From there, a more defined channel extends southward through the forest eventually leading to the cultivated field where the channel has been eradicated by tilling. The spring discharge is better measured farther down the watercourse at Site 134.

134 M 561064 4915065 486 Monitoring point along a watercourse located about 40 m downstream from the spring at Site 133. Just downstream, the gully is 25 m wide and 2.5 m deep.

135 DS1 561152 4914806 469 Suffosion doline located in the middle of the field that is 6 m long, 3 m wide and 40 cm deep. A small channel leads to this doline indicating that it was an active sinkpoint when streamflow was moderately high. On April 22, 2005 the stream was observed finally sinking through the overburden about 10 m upstream from this doline. The doline suggests that the underlying Manitoulin Formation may be karstic. On a return visit on November 20, 2005 the doline had been completely filled in by tilling.




Northing(m)

Elev.(m)

Description

136 GP1 561026 4914913 480 Spring issuing from the base of the talus slope along the Amabel escarpment. An obvious channel extends out into the nearby field. During high flow, the stream presumably continues flowing south across the cultivated field.

SW22A GP1 560950 4914876 483 A spring discharging from the base of the talus slope along the Amabel escarpment at the head of a small gully that is 6 m wide and 1.3 m deep. A well defined natural channel extends for about 90 m to where it has been excavated to improve drainage. The ditch extends from there all the way to Site 144. The JHL monitoring point is located about 15 m downstream from the spring. Some of the discharge emerges from a 30 cm diameter soil pipe formed in the overburden along the bank of the gully. There is a dolostone cliff located about 70 m up the slope to the northwest.

137 GI1 560918 4914863 485 Small spring issuing from talus along the Amabel escarpment. The discharge from the spring initially flows through talus before following a poorly defined channel to where it joins the flow from the SW22A spring.

138 GP1 560912 4914846 483 Small spring issuing from overburden beneath the talus slope along the Amabel escarpment. A poorly defined channel extends about 60 m down the slope to where it joins the watercourse from the SW22A spring.

139 M 560923 4914784 475 Point along the ditch where the tributary from Site 138 enters the larger watercourse from SW22A.

140 GP2 560824 4914801 488 Spring issuing from a prominent talus apron located below the Amabel escarpment. Dolostone cliffs about 12 m high are located about 25 m to the northwest. The spring is about 5 m below the elevation of the base of the cliff. The discharge disperses widely down the talus apron but eventually emerges from the talus at three separate watercourses, all leading to the large wetland feature located to the southeast. The discharge is difficult to estimate within the talus but can be measured farther downstream at the three individual watercourses.

141e 141c 141w

M 560866 560835 560811

491477949147664914759

480 480 480

Three poorly defined watercourses were observed extending out from the talus apron. Presumably, these are all fed by springs discharging from Site 140. From east to west, these are identified as 141e, 141c and 141w. They were all monitored immediately upstream from the wetland feature (an area that is forested in cedar, birch and ash with damp ground, also with some open grassy areas with cattails).

142 GP1 560706 4914718 490 Small spring issuing from overburden at the head of an obvious gully cut into the Amabel escarpment slope. The gully is about 30 m wide and is incised about 5 m deep. About 50 m down the slope, the flow from the spring enters the wetland feature that is forested with cedar and tamarack.




Northing(m)

Elev.(m)

Description

143 GP1 560751 4914644 480 Small spring issuing from overburden at the base of the Amabel escarpment. This provides some recharge to the adjacent wetland feature that is forested with tamarack.

144n 144w

M 560944 4914661 470 A monitoring point located about 35 m upstream from SW22C at the junction of two tributaries: The west tributary (144w) follows the north edge of the adjacent unevaluated wetland and much of the flow from this wetland drains via this channel. This wetland is fed by springs at Sites 140, 144 and 145. The north tributary (144n) is a ditch that extends up to the springs at SW22A and Sites 137 and 138.

145n 145s

M 560957 4914650 470 A monitoring point located at the junction of two tributaries about 17 m upstream from SW22C. The west tributary (145w) represents the combined flow from two tributaries that join at Site 144, about 17 m farther upstream. The south tributary (145s) has a very small channel that drains part of the adjacent wetland.

SW22C M 560971 4914641 470 A monitoring point where various spring fed tributaries have joined to form a single watercourse. The watercourse crosses beneath a trail in a culvert. The flow at this site represents the combined flow from springs at Sites SW22A, 137, 138, 140, 142 and 143. The unevaluated wetland located to the west remains damp throughout the year because of the perennial discharge from these springs. The northwest portion of the wetland is forested, typically with a mix of cedar, birch, tamarack, ash and various shrubs. The southeast portion is more open marsh dominated by cattails but with a few trees, especially around the perimeter.




Northing(m)

Elev.(m)

Description

SW22 GP2 560636 4914429 493 Large perennial spring issuing from overburden over a width of 2.5 m near the base of the Amabel escarpment. The spring is at the head of an obvious fluvial gully and a well defined channel extends down the slope. The JHL monitoring point (SW22) is located about 16 m downstream from the spring at the steel culvert that extends beneath the ski trail. The escarpment slope above the spring appears to be boulder till since there are frequent, subangular to subrounded boulders on the ground, primarily of dolostone but also of gneiss. Bedrock is not exposed farther up the slope. At the east edge of the existing Duntroon Quarry, the dolostone bedrock surface is about 15 to 20 m lower compared to farther north and south along the Niagara Escarpment. This suggests that there is a prominent erosional embayment in the Niagara Escarpment that is largely filled with glacial sediment. If so, then the spring may be fed by this overburden aquifer. However, the concentration of flow issuing at a discrete point and the elevation of the spring roughly at the elevation of the base of the Amabel Formation suggest that it is more likely a karst spring issuing from a bedrock conduit.

146 GI1 560717 4914332 495 Small spring issuing from overburden about 10 m up from the base of the Amabel escarpment slope. The overburden appears to be a thick deposit of glacial till. The discharge flows down a poorly defined channel and sinks into the overburden only a short distance down the slope. This spring is interpreted to be discharging from the glacial sediment and not the Amabel aquifer.

147 GP1 WS1

560807 4914279 490 Water well located opportunistically at a spring that discharges from overburden along the Amabel escarpment slope. The round concrete cistern is 1.06 m in diameter and protrudes 70 cm above the ground. The cistern contains gravel. A plastic pipe extends down the slope from the cistern. The spring may still be in active use. A graded channel extends down the slope and additional groundwater discharges into this channel for some distance.

148 M 560854 4914313 480 Monitoring point along the watercourse about 50 m downstream from the spring at Site 147. This is a better location to monitor the total spring discharge, especially where the flow is confined to a narrow channel.

149 GI1 560989 4914037 488 A small spring issuing from overburden part way up the Amabel escarpment slope. The spring is located in a small forested area within the golf course grounds.




Northing(m)

Elev.(m)

Description

150 M 561031 4914054 477 Monitoring point at a culvert that forms the outlet for a 5 m diameter pond located at the base of the Amabel escarpment. The pond is fed in part by discharge from a small gully located next to a small building. The function of the building is unknown, although it could house a water supply well. Therefore, it is not clear if a natural spring is located here or if the discharge is from a water well. The flow from the spring at Site 150 also contributes to the flow at this monitoring point.

151 GI1 WS1

561993 4914024 486 Water well located opportunistically at a spring along the Amabel escarpment. The round concrete cistern is 1.1 m in diameter and protrudes 60 cm above the ground. The cistern is about 3 m deep. The amount of discharge observed at this spring was minimal. The well is located within the same small forested area as the spring at Site 150.

152n 152s 152

GP1 M

561204 4913750 478 Small spring (152n) discharges at the base of the talus slope beneath the Amabel escarpment. The discharge seeps from the talus directly into the ditch immediately north of the steel culvert. The discharge immediately joins the stream flowing in the ditch that comes from the south. The combined flow continues eastward through the steel culvert and continues down the slope about 40 m to a small pond. The flow in the ditch to the south of the culvert was also monitored (152s). The ditch follows the west edge of the golf course and was probably designed to capture discharge from all along the base of the talus slope. It also captures some of the flow from the spring at Site 153. The combined flow from 152n and 152s was measured at the east end of the culvert (152).

153 GP2 561200 4913673 487 Small spring issuing from talus about 30 m up the slope from the base of the Amabel escarpment. From there, the discharge flows down the slope through the talus in a poorly defined channel. Most of the flow continues straight down the slope to the watercourse at Site 155. However, some flow is captured by the ditch and goes to the culvert at Site 152.

154 GP1 561237 4913679 479 Small spring issuing from talus along the Amabel escarpment.

155 M 561300 4913702 472 Monitoring point located along the watercourse just upstream from a small artificial pond at the edge of the golf course. The watercourse is fed by various springs located on the talus slope but primarily at Sites 153 and 154.

156 GI1 561241 4913668 479 Two closely spaced springs issuing from talus about 20 m up from the base of the talus apron along the Amabel escarpment. From here, water flows through the talus down to the Manitoulin bench. Measurements were made of the combined discharge from both springs.




Northing(m)

Elev.(m)

Description

157 GI1 561285 4913653 475 Small spring issuing from overburden at the base of the Amabel escarpment.

158 M 561313 4913692 472 Monitoring point located along the grassy watercourse adjacent to the fenceline. This watercourse is fed by springs at Sites 157 and 158.

159 GP1 WS1

561263 4913554 486 A spring issuing from overburden and talus along the Amabel escarpment. There is a concrete cistern located 9 m below the escarpment crest and about 10 m above the base of the escarpment. The cistern is square with a width of 90 cm and height of about 80 cm. It collects water from the spring and allows the sediment to settle. The cistern feeds a pipe and hose that are utilized as a water supply. Additional discharge issues from talus just above the cistern as well as all the way down the steep slope. There is a 2 m high dolostone cliff exposed near the crest of the escarpment and the overlying overburden appears to be about 2 m thick at most.

160 M 561340 4913585 474 Monitoring point located about 80 m downstream from the spring at Site 159 at a point where the stream crosses beneath the new ski trail via a small culvert.

161 M 561375 4913800 468 The junction of two watercourses, both fed by the group of distributary springs issuing from the Amabel escarpment at Sites 152, 153, 154, 156, 157 and 159. The flow could not be readily monitored at this location because it is in the middle of an active golf course. Instead, the flow here was calculated as the sum of the flow measurements at Sites 152, 155, 158, and either 160 or 159 (depending on where flow was measured at any given time).

162 M 561598 4913448 476 Monitoring point at a small watercourse where it enters the ditch along the south side of 21/22 Sideroad. This may be fed by a nearby spring but this was not investigated.

163 M 561746 4913498 474 Monitoring point at a 60 cm diameter steel culvert that crosses beneath 21/22 Sideroad. The culvert drains the wetland to the south, a low marshy area with some shrubs that is flooded in wet weather.

164 DS2 560840 4913232 512 Suffosion doline that is 25 m long, 11 m wide and 1.2 m deep. The bottom has three low points and is largely filled with fieldstones and numerous pitted dolostone boulders covered with moss. The doline is situated along a very subtle drainage swale that is roughly 25 m wide and less than 50 cm deep.

165 DS2 560905 4913261 509 Suffosion doline that is 6 m long, 5 m wide and 1.0 m deep that contains numerous dolostone boulders up to 1 m long that are quite pitted, as well as a few gneiss boulders. There is no bedrock exposed at the doline.




Northing(m)

Elev.(m)

Description

166 DS2 560918 4913263 508 Suffosion doline that is 7 m long, 6 m wide and 1.0 m deep with 3 minor low points. It contains a few small dolostone boulders up to 40 cm long. There is no bedrock exposed. The doline is situated near the head of the shallow gully that can be readily traced for 60 m to where the topographic slope lessens noticeably. From there, the drainage swale is very subtle but appears to continue to the top of the steep Amabel escarpment. Where it approaches the escarpment, an obvious fluvial gully has incised into the overburden. Upstream from the doline there is a very shallow drainage swale but this ends within 20 m and there is no clear indication that this doline may have acted as an overflow sink for the SW26 doline.

SW26A M 560745 4913095 512 JHL monitoring point near the twin steel culverts along the Camarthen Wetland Tributary where it crosses beneath a wide trail.

SW26 P2 DS2

560780 4913080 511 A large suffosion doline that is roughly 22 m in diameter and 4.0 m deep with moderately steep sides. The doline is the sinkpoint for the Camarthen Wetland Tributary. The overburden is primarily silt with sand, clay and a few boulders. The boulders appear to be residual from erosion of the glacial overburden. There is no bedrock exposed. Several fieldstones were dumped into the watercourse where it enters the doline. Streamflow infiltrates into the fill at the bottom of the doline, which consisting of leaf litter and silt. There are a few small, irregular soil pipes in this fill. The gully just upstream from the doline is 9 m wide and 2.2 m deep, with 1 to 20 cm gravel or cobbles and no fines. The slope of the channel there is about 0.03. The coarse residual sediment with lack of fines indicates rapid flow velocities during peak flow. There is no clear indication of an overflow channel extending beyond the doline. Going upstream, the watercourse can be traced for about 200 m to where it is fed by the outflow from the Camarthen Wetland. At the south end, the unevaluated wetland is forested with a mix of balsam fir, elm, white cedar, ash, walnut, white birch and red maple. There is no indication that any flow is lost along the watercourse until within a few metres of the large suffosion doline.

167 DS1 560853 4913034 512 Suffosion doline that is 4 m long, 3.5 m wide and 1.2 m deep with fairly steep sides. Bedrock is not exposed and there is only one 5 cm cobble in the doline.

168 DS2 560863 4913033 512 Suffosion doline that is 5 m in diameter and 1.2 m deep. There is no bedrock exposed and no associated runoff channels.




Northing(m)

Elev.(m)

Description

169 DS2 560879 4913033 512 Suffosion doline that is 10 m long, 5 m wide and 1.4 m deep with steep sides. There is no bedrock exposed and there are no associated runoff channels. It is situated along a topographic valley that appears to rise at least 1 m higher than the doline in the downslope direction.

Stream monitoring points around the perimeter of the karst study area SW1 M 559102 4914051 513 JHL monitoring point at the twin steel culverts at Grey

County Road 31. 170 M 559195 4913574 514 Culvert beneath Grey County Road 31.

SW25 M 559424 4912208 507 JHL monitoring point at the outlet for Edward Lake at a culvert on the west side of County Road 31.

172 M 559520 4911771 506 Culvert beneath Grey County Road 31 that drains a watercourse flowing eastward.

173 P2 559634 4911681 505 During spring runoff, the stream creates a shallow pool about 20 m wide just upstream from here and this sinks through the overburden. This is the farthest point that the stream reached during 2005 before completely sinking. No discrete sinkpoints or soil pipes were observed in the gully, although this field is tilled so any small dolines would be eradicated.

174 G2 559591 4911560 504 Spring emerging from a small depression at the edge of a low ridge of glacial sediment. This is the likely resurgence for the sinking stream at Site 173. From here, the flow enters a damp, grassy area adjacent to Grey County Road 31.

175 P1 559560 4911270 503 Outlet for a culvert beneath County Road 31. From here, the stream flows west along a ditch. The ditch was excavated for a distance of about 80 m through a low ridge of glacial sediment to a depth of at least 1.5 m. Presumably the ditch was excavated to prevent seasonal flooding of the road and adjacent fields. On May 16, 2005, there was 4 L/s flowing through the culvert and all of this infiltrated into the overburden about 10 m to the west.

176 M 559719 4910523 494 The Mad River at the Highway 126 bridge crossing. 177 M 560558 4910939 486 The Mad River at Ewing Road, which is at the first

bridge downstream from Highway 126. The river enters a canyon there and the gradient increases.

178 G2 562558 4912002 486 Spring issuing from the base of the talus slope on the north side of Highway 126. A 3 m high cliff of Amabel dolostone is visible at the top of the talus slope about 25 m up the slope from the road. The spring-fed stream crosses beneath the road through a culvert.




Northing(m)

Elev.(m)

Description

179 G1 WS1

562584 4912041 486 Spring issuing from the base of the talus slope on the north side of Highway 126. The setting is very similar to that at the spring at Site 178. From the spring, the stream crosses beneath the road through a culvert. The spring appears to be utilized as a water supply since there is a concrete box cistern located here. The cistern is 155 cm by 155 cm and 60 cm high and has a locked hatch and a vent. The spring is 5 m from the Bruce Trail. The watercourses from both springs extend down the slope to a pond.

180 M 562774 4911926 461 Small watercourse at the rim of the Mad River Gorge. There is a prominent erosional bench at this elevation that is at the top of the Manitoulin Formation. This watercourse is fed by a nearby pond that may be spring-fed.

181 G1 562935 4912159 461 Spring located in a steep ravine on the south side of Highway 126. The spring issues from rubble at the elevation of the Manitoulin Formation. The Manitoulin dolostone outcrops at this site.

182 M 563560 4911503 373 Mad River at a bridge crossing beside Devils Glen Country Club, next to the ski hill parking lot.

183 M 563688 4911870 414 Small watercourse crosses beneath road. 184 M 563666 4912168 430 Watercourse crosses beneath Highway 126 in a

culvert. 185 M 563806 4912206 425 Watercourse crosses beneath Highway 126 in a



culvert. 188 M 564673 4912668 400 Small watercourse crosses beneath Highway 126. 189 M 564661 4913179 405 Watercourse crosses beneath Highway 126. 190 M 564607 4913495 400 Watercourse crosses beneath Highway 126. 191 M 564502 4914084 383 Watercourse crosses beneath Highway 126 in a

culvert. 192 M 563678 4914111 398 Watercourse crosses beneath 21/22 Sideroad in a

1.5 m diameter culvert. 193 M 563207 4913957 407 Watercourse crosses beneath 21/22 Sideroad in a

1.5 m diameter culvert. 194 M 562452 4913717 430 Watercourse crosses beneath 21/22 Sideroad in a

culvert. 195 M 561873 4914012 435 Watercourse crosses beneath Concession 10 in a 2 m

diameter culvert. 196 M

WS1 561723 4914851 450 A pond fed by groundwater discharge on the former

Sampson property drains beneath Concession 10 through a steel culvert. There is a concrete tile in the pond that was presumably utilized as a water supply.

197 M 561690 4915050 452 Small watercourse crosses beneath Concession 10 in a small steel culvert. This watercourse drains various small springs located along the Manitoulin escarpment, the largest of which is at Site 112.




Northing(m)

Elev.(m)

Description

SW14 M 561524 4916025 415 Watercourse crosses beneath Concession 10 in a 1.0 m diameter culvert.

SW15 M 561494 4916203 420 Watercourse crosses beneath Concession 10 in a culvert.

SW18 M 561395 4916788 390 Watercourse crosses beneath Concession 10 in a box culvert that is 2.8 m wide and 1.0 m high.

198 M 561295 4917426 385 Watercourse crosses beneath Concession 10 in a 1.0 m diameter culvert.

199 M 561238 4917691 367 Watercourse crosses beneath Concession 10 in a steel culvert that is 2.0 m wide and 1.5 m high.

200 M 561005 4918923 299 Small watercourse draining a small pond at the junction of Concession 10 and 30/31 Sideroad.

201 M 560773 4918872 305 Small watercourse crosses beneath 30/31 Sideroad at a small culvert.

202 M 560386 4918749 316 Gully crosses 30/31 Sideroad. 203 M 559690 4918531 349 Watercourse crosses 30/31 Sideroad through two

steel culverts, each about 80 cm in diameter. 204 GP1 559206 4918410 370 The road skirts around the head of a prominent gully

with several small springs visible down the slope to the north. The springs were not investigated (permission was not obtained to access property). However, they are located well below the elevation of the Manitoulin Formation.

205 GP1 559160 4918400 373 There appears to be another spring located about 40 m north of the road, to the west of the springs at Site 204. This was not investigated (permission was not obtained to access property). However, it is located well below the elevation of the Manitoulin Fm.

206 M 558573 4918181 387 Small watercourse crosses beneath 30/31 Sideroad. 207 M 558384 4918126 371 Small watercourse crosses beneath 30/31 Sideroad in

a 40 cm diameter culvert just west of the junction with a gravel road going north.

208s 208

M 558052 4918002 357 A large watercourse crosses 30/31 Sideroad at twin 90 cm diameter steel culverts. Two tributaries join on the south side of the road before crossing through the culverts. Measurements were made of the combined flow at the culvert (208) and at the larger tributary (208s) immediately upstream of the junction. This tributary comes down the escarpment slope from the southeast. Flow in the smaller tributary was measured about 70 m farther upstream at Site 209, located to the west along the south side of 30/31 Sideroad.

209 M 557991 4917987 360 A small watercourse comes down the escarpment slope to 30/31 Sideroad then flows eastward along the ditch to join the larger stream at Site 208 before crossing the road there.

210 M 557392 491801 370 Small watercourse crosses beneath 30/31 Sideroad in a 60 cm diameter steel culvert.




Northing(m)

Elev.(m)

Description

211e 211w 211

M 557068 4917666 358 Two small tributaries join here into a single watercourse. From here, the watercourse extends about 25 m downstream to the 30/31 Sideroad where it crosses through a 1.85 m diameter steel culvert. In addition to the combined flow (211), flow was also measured at both the east and west tributaries (211w and 211e).

212 M 556971 4917671 355 Watercourse crosses 30/31 Sideroad in a 2.3 m diameter steel culvert.

213 M 556686 4917582 365 Small watercourse crosses 30/31 Sideroad in a 45 cm diameter culvert.

214 M 556380 4917483 355 Large watercourse crosses 30/31 Sideroad in a 1.4 m diameter steel culvert.

215 M 556260 4917449 357 Small watercourse crosses 30/31 Sideroad in a 60 cm diameter steel culvert.

216 M 556184 4917418 360 Small watercourse crosses 30/31 Sideroad in a 60 cm diameter steel culvert.

217 M 555815 4917303 356 Small watercourse crosses 30/31 Sideroad in an 80 cm diameter steel culvert located just east of the junction with Pretty River Road (County Road 31).

218 M 555323 4917159 360 Small watercourse crosses County Road 31 in a 60 cm diameter steel culvert. The stream appears to come from the Manitoulin escarpment that is visible up the slope.

219 M 555068 4917070 365 Small watercourse crosses Pretty River Road at the prominent bend in the road in a 60 cm diameter steel culvert.

220 M 554985 4916638 392 Small watercourse crosses Pretty River Road in an 80 cm diameter steel culvert.

221 M 555030 4916187 412 Large watercourse crosses Pretty River Road in a 1.35 m diameter steel culvert.

222 M 555079 4915964 417 Large watercourse crosses Pretty River Road flowing eastward in a 1.2 m diameter steel culvert.

223e 223s 223

M 555095 4915712 421 Large watercourse crosses Pretty River Road flowing westward. Two tributaries join here. The largest crosses the road through the culvert from the east (223e). The second is the ditch following the west edge of Pretty River Road approaching from the south (223w). This ditch continues upstream along the west edge of the road for about 210 m. There, a small culvert emerges from the base of a 5 m high slope. The culvert is the outlet for a small artificial pond located just above the steep slope. The combined flow from the ditch and the culvert is reported as 223.

224 224w 224s 224e

M 555170 4914739 461 Three small tributaries join on the south side of 12 Line Road before crossing beneath the road in a culvert at location 224. Flow was monitored in each of the tributaries: the ditch following the edge of the road flowing from the east (224e), the small stream coming from the south (224s), and the ditch following the edge of the road coming from the west (224w).




Northing(m)

Elev.(m)

Description

225 M 555615 4914890 475 Watercourse crosses beneath 12 Line Road in a 90 cm diameter steel culvert.

SW6A M 555282 4912472 495 Large watercourse crosses Osprey Sideroad 30 at twin steel culverts that are 1.6 m wide and 1.0 m high.

226 M 558787 4915862 511 Small culvert beneath Grey County Road 31. This culvert allows drainage between poorly drained areas on either side of the road with flow observed towards the west.

SW3A M 558805 4915721 511 Single culvert located under Grey County Road 31 just south of the intersection with 26/27 Sideroad.

SW3 M 558882 4915342 510 Small watercourse crosses Grey County Road 31 in a 60 cm diameter steel culvert.



Table C-3: Incidental observations of groundwater use at springs

Use indicates whether a spring is actively utilized (A), no longer utilized (X) or the use is unknown (?). A more detailed description and the location of each site can be found in Table C-2.

Type Aquifer Site Use Description

48 A A well tile was recently installed at an Amabel spring to replace a derelict cistern. The well tile is currently utilized as water supply for the nearby house.

SW21C A Well tiles buried in gravel in the bed of a watercourse fed by discharge from an Amabel spring at Site 86. Currently utilized by H. Franks as a water supply for a house.

SW10 A Three concrete well tiles buried in gravel in the bed of a watercourse fed by nearby springs discharging from the Amabel Formation. Currently utilized as a water supply by W. Franks at a nearby house.

147 ? A round concrete well tile buried where a small perennial spring discharges from the Amabel escarpment slope. The cistern is 1.06 m in diameter and protrudes 70 cm above the ground surface and contains gravel. A plastic pipe extends down the slope from the well.

151 ? A round concrete well tile buried where a small spring discharges from the Amabel escarpment slope. The tile is 1.1 m in diameter and 3 m deep with about 60 cm protruding above the ground surface.

159 ? A square concrete cistern that is 90 cm across and 80 cm high. The cistern was formed in place and collects water from a small perennial spring discharging just up the slope along the Amabel escarpment. A hose extends down the slope from the cistern.

Amabel

179 ? A concrete cistern that is 1.5 m square protruding 60 cm above the talus with a locked hatch and vent. The cistern collects discharge from a spring where it issues from the base of the talus slope beneath the Amabel escarpment.

52 ? A small round steel well tile buried where a small perennial spring discharges 15 m below the crest of the Manitoulin escarpment.

SW24A A A cistern constructed 18 m downstream from a small perennial spring discharging from below the crest of the Manitoulin escarpment. One pipe extends up to the spring to collect water and another delivers the water to the nearby house located farther down the slope.

89 ? A concrete well tile buried in the bed of a watercourse fed by discharge from a Manitoulin spring about 20 m farther up the slope. The round well tile is 1.1 m in diameter and protrudes about 70 cm above the ground surface.

Dug well or cistern

Manitoulin

196 ? A concrete well tile buried at the edge of a spring-fed pond. The groundwater discharge may be from the Manitoulin dolostone.



Type Aquifer Site Use Description

31 X A section of steel pipe is located next to a watercourse just downstream from a series of small springs along the Amabel escarpment. The pipe suggests a makeshift attempt to use the spring as a water supply.

34 X A plastic pipe located along a watercourse fed by discharge from a series of small springs along the Amabel escarpment. The pipe suggests a makeshift attempt to use the spring as a water supply.

40 X An earth dam was constructed downstream from a small spring issuing from the base of the Amabel escarpment to create a pond that is 40 m long, 25 m wide and 1 m deep. Although still holding water, the pond does not currently appear to be utilized.

77 X An earth dam was constructed 14 m downstream from a small spring to create a pond. The spring issues from a conduit in dolostone bedrock towards the crest of the Amabel escarpment. The earth dam is 80 cm high and up to 3 m wide. However, the stream has since cut through the earth dam and drained the pond. A small section of steel pipe is located next to the spring.

Amabel

129 X A section of steel pipe is located at a spring near the base of the Amabel escarpment. The pipe suggests a makeshift attempt to use the spring as a water supply.

Other uses of springs.

Overburden 11 X An excavation and an earth dam were constructed to create a shallow pond about 8 m in diameter at a small spring. The earth dam has since eroded and the pond is now drained. The groundwater is interpreted to be discharging from glacial sediment.


Marcus J. Buck Karst Solutions Appendix D, Page 146 Worthington Groundwater

Appendix D: Surface Water Data Contents Page Table D-1: Surface water data measured during the field investigation of karst....................147

Table D-2: Measurements utilized for calculating a rating curve for the SW2A spring ..........162



Table D-1: Surface water data measured during the field investigation of karst

The location of the surface water monitoring sites (Site) are identified by specific alphanumeric codes. These are described in Table C-1 and are illustrated on Figure 1,.3, 13 and 17. Some of the monitoring locations correspond to Jagger Hims Limited monitoring sites and these are identified using their codes. Electrical conductivity (EC) and temperature (Temp) data were measured using a WTB conductivity meter (model Cond 340i) using non-linear temperature compensation corrected to a reference temperature of 25° C. Accuracy reported by the manufacturer is 0.5% of the value for conductivity and 0.1° C for temperature. Streamflow (Q) was measured using one of several methods (Method), and in a few cases an estimate of error (Error) was made in the field. The methods used to measure streamflow are indicated by codes and these are described as follows:

E: Visual estimate (very approximate) M1: Rough measurement of cross-sectional area and velocity using floating objects (± 40%) M2: Careful measurement of cross-sectional area and mean velocity using floating objects (± 30%) M3: Careful measurement of cross-sectional area and mean velocity using a flow meter (± 20%) MV: Measured volumetrically using a bucket (± 5 to 25%) C1: Calculated using electrical conductivity data and streamflow measurements at other sites C2: Calculated by addition or subtraction of data from other sites

SDG: Measured by salt-dilution gauging using the slug injection method (± 15%)

Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

Amabel plateau in the vicinity of Nottawasaga Lookout Provincial Park SW28 04/24/04 15:06 4. E 381 14.6 05/09/05 13:08 7.5 M1 373 15.9 05/09/05 16:24 372 17.4 05/10/05 6:00 6. M1 381 9.3 At time of tracer injection. 05/11/05 9:00 5.4 M2 05/12/05 7:50 3. M1 05/13/05 18:45 3. E 05/14/05 12:09 11. M1 373 11.4 Pond level was up again

because of recent rainfall. SW28A 04/22/05 19:06 10. E Overflow from the

ephemeral pond. 11 04/14/05 11:26 0.3 M1 468 9.9

SW9 watercourse SW9 04/23/04 14:45 6. M2 414 9.0 04/23/05 7:08 30. M1 361 4.7 Measured during

groundwater tracing. 04/25/05 8:56 39. M2 320 2.0 13A 04/25/05 9:34 39. M2 13B 04/23/04 14:50 4. E The remaining 4 L/s sank

here and the channel was dry farther downstream.

14A 04/25/05 9:43 32. E 14B 04/25/05 10:00 19. M2 14C 04/25/05 10:02 15. M1 Of the total of 15 L/s, 6

L/s was sinking in a small isolated pond in a shallow depression.



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

14D 04/25/05 10:10 2. M1 About 2 L/s was sinking in a small pool, which was the furthest point that the stream reached at the time. The remaining 7 L/s sank between Sites 14C and 14D.

15 04/25/05 8:50 2. E All of the flow (2 L/s) sank gradually into the overburden over the next 80 m along the watercourse.

SW2 Springs SW2B 04/23/04 14:06 0. E 467 5.8 The water level in the

spring pool was 10 cm below the elevation of the outlet.

04/14/05 14:55 22. M1 437 5.7 05/09/05 9:25 0. 0. 477 5.8 Level logger was 10 cm

above the water level. There was still about 30 cm of water in the spring pool.

SW2A 04/23/04 13:46 8. M1 491 5.5 07/28/04 12:47 1. M1 09/16/04 18:00 0.2 M1 561 10.1 04/14/05 15:14 35. 14. M1 451 4.9 04/14/05 15:14 444 5.0 Discharge emerging from

the adjacent rock pile at the north corner of the spring pool. The flow was not measured but was probably less than 2 L/s.

05/09/05 11:43 17.2 0.9 SDG 506 5.7 05/12/05 14:20 05/12/05 16:50 13.6 0.7 SDG 05/12/05 17:46 12. 3. M2 512 5.7 05/17/05 16:53 12. 5. M1 524 5.9 05/26/05 16:24 8.1 0.4 SDG 538 6.0 10/04/05 11:20 0.32 0.05 MV 11/17/05 16:26 0.15 0.07 M1 684 8.1 07/08/06 8:30 2. 0.4 M2 566 7.9 SW2 04/14/05 13:52 60. M1 294 4.9 Roughly 25 L/s were

flowing overland from the spring at SW2B and the remainder of the flow was issuing from the spring at SW2A.

SW2 05/09/05 10:51 17. M2 513 6.9 05/12/05 16:36 518 7.1 05/26/05 16:30 6. M1



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

Duntroon Quarry 20 04/23/04 9:50 30. M1 562 4.5 21 04/24/04 11:10 15. E 565 4.6 07/27/04 17:00 15. E 772 8.6 Conductivity was similar

to several measurements in the wetland located to the west made later that afternoon (e.g., 798, 803 µS/cm)

22 04/24/04 10:39 0.5 M1 778 6.2 23 04/24/04 10:31 0.1 M1 621 6.3 24 04/24/04 10:22 0.05 E 687 5.1

Amabel escarpment north of 26/27 Sideroad 25 07/08/06 10:30 0.1 E 26 05/14/05 16:17 6. E 481 7.0 11/19/05 13:53 0.05 E 517 6.8 The measurement was

made at one of several small springs located over a width of about 20 m.

27 05/14/05 16:14 3. E 473 7.5 11/19/05 13:45 trace 477 5.0 28 05/14/05 16:08 9. M1 470 8.1 11/19/05 13:41 0.3 MV 471 4.0 07/08/06 10:40 2. E 29 05/14/05 15:44 1.5 M1 449 6.2 11/19/05 14:14 0.05 E 484 7.9 30 05/13/05 17:02 1.7 M1 423 5.9 11/19/05 14:20 0.25 MV 474 6.6 Flow was measured 20 m

downstream. 31 05/13/05 16:26 7. E 402 6.7 Flow was measured

downstream where the discharge converges into a single channel.

11/19/05 14:59 0.1 E 477 6.3 32 11/19/05 16:48 0.6 0.15 M1 442 2.8 33 05/14/05 16:50 7. M1 Measured about 80 m

farther upstream. 11/19/05 14:35 0.6 MV 432 2.3 34 05/13/05 16:13 2.5 M1 377 4.8 Flow measured 45 m

downstream in a single channel.

11/19/05 15:12 0.35 MV 457 6.0 Flow measured 65 m downstream in a single channel.

35 05/13/05 15:53 0.5 E 395 6.2 11/19/05 15:28 0.03 M1 459 5.6 36 05/13/05 15:42 1. M1 398 6.0 11/19/05 15:34 0.05 M1 465 6.2 37a 05/13/05 15:24 0.3 E 384 2.4 37b 05/13/05 15:21 0.3 E 381 3.6 37c 05/13/05 15:17 0.3 E 380 4.6



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

37c 11/19/05 9:51 0.03 E 393 4.1 This may be snow melt from farther up the slope.

37d 05/13/05 15:14 0.4 E 385 3.1 11/19/05 9:55 0.02 E 397 5.0 This may be snow melt

from farther up the slope. 38 05/13/05 15:04 0.5 E 391 4.5 11/19/05 9:40 0. E Dry 39 05/13/05 14:45 0.7 M1 382 4.1 11/19/05 9:34 0.1 M1 422 5.2 40 05/10/05 13:28 0.3 E 452 8.9 11/19/05 10:14 0. E 356 1.3 The adjacent pond was

full. 41 05/10/05 13:15 0.3 M1 382 5.2 11/19/05 10:23 0.05 E 409 2.2 42 05/10/05 13:01 0.5 E 378 5.4 11/19/05 10:31 0.25 MV 381 6.6 43 05/09/05 15:40 1. E 395 7.0 All of the flow sank within

50 m downstream. 05/10/05 8:57 0.8 E 399 6.7 05/17/05 15:08 0.3 M1 396 8.4 11/19/05 10:43 0.02 E 415 2.4 44 05/09/05 15:50 1.5 E 408 6.7 05/10/05 8:45 2. MV 413 6.9 05/17/05 15:03 0.3 M1 420 7.0 11/19/05 11:00 dry 45 05/09/05 15:13 1. M1 430 5.9 05/10/05 8:39 430 6.3 05/17/05 14:57 0.3 M1 422 8.1 11/19/05 11:03 0.02 E 432 3.5 SW27A 04/24/04 14:39 1. E 379 6.1 07/28/04 10:05 0.2 E 476 6.9 09/16/04 18:39 0.05 E 497 7.5 05/09/05 14:07 2. E 383 6.3 05/10/05 6:23 3. E 387 6.3 11/19/05 11:15 0.015 MV 487 6.9 SW27B 04/24/04 14:47 10. E 370 5.7 The combined flow from

the three adjacent springs.

07/28/04 9:45 1.3 M1 488 6.9 The combined flow from the three adjacent springs.

09/16/04 18:43 495 7.5 The combined flow from the three adjacent springs.

05/09/05 13:54 3. E 371 6.0 05/10/05 6:19 3. E 375 6.0 11/19/05 11:10 0.04 MV 504 6.9 07/08/06 9:30 0.05 E SW27C 05/09/05 13:57 0.6 E 373 6.2 05/10/05 6:20 1.5 E 377 6.2 11/19/05 11:10 0. E Dry 07/08/06 9:30 0. E Dry



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

SW27D 05/09/05 14:00 1.4 E 374 6.3 05/10/05 6:21 1.5 E 379 6.2 11/19/05 11:15 0.015 MV 487 6.9 07/08/06 9:30 0.05 E SW27E 05/09/05 14:18 0.5 E 404 6.5 05/10/05 6:25 1. E 409 6.5 07/08/06 9:30 trace E SW27F 07/28/04 10:20 505 7.2 05/09/05 14:21 0.6 E 408 6.4 05/10/05 6:26 1.5 E 411 6.3 07/08/06 9:30 trace E SW27G 05/09/05 14:23 1.5 E 412 6.3 05/10/05 6:27 2. E 416 6.3 11/19/05 11:20 0. E Dry 07/08/06 9:30 0. E Dry 46 07/28/04 10:20 3. M1 481 9.0 05/09/05 14:33 25. M1 379 8.7 05/10/05 6:32 23. M1 386 6.5 05/14/05 11:00 22. M1 401 8.0 It rained during the

previous night. 05/16/05 14:50 18. M1 404 7.6 11/19/05 11:25 1.1 0.2 MV 492 4.8 48 04/24/04 14:25 432 6.1 07/28/04 13:21 1. E 500 7.5 05/09/05 14:53 454 6.2 11/19/05 11:30 0. E Dry SW20 05/09/05 14:46 11. M1 435 11.9 05/10/05 6:54 12. M2 452 6.4 05/17/05 15:20 8. M1 464 8.1 11/19/05 11:30 0. E Channel was dry.

Manitoulin escarpment north of 26/27 Sideroad 49 05/15/05 19:28 2. M1 390 5.7 11/19/05 15:43 0.05 M1 392 8.5 50 05/15/05 19:21 2. M1 399 5.5 Combined flow from two

closely spaced springs. 11/19/05 3:52 0.15 MV 333 8.4 51 05/15/05 19:16 1.5 M1 402 5.1 11/19/05 15:56 0.1 M1 494 9.0 52 05/15/05 19:08 3.5 M1 389 5.5 11/19/05 16:00 * 521 8.8 * Any flow was captured

in the plastic pipe that forms the outlet for the water supply system.

53 11/19/05 16:28 0.6 0.1 MV 452 3.9 54 05/15/05 19:01 0.1 M1 401 5.8 11/19/05 16:15 0. E Dry 55 05/15/05 18:56 0.2 M1 431 6.3 11/19/05 16:15 0. E Dry 56 05/15/05 18:50 0.2 M1 449 6.4 11/19/05 16:15 0. E Dry



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

57 05/15/05 18:45 < 0.1 M1 11/19/05 16:15 0. E Dry 58 05/15/05 18:40 0.2 M1 11/19/05 16:15 0. E Dry 61 05/15/05 18:02 2. M1 502 5.4 11/18/05 12:40 0.05 E 495 4.8 62 11/18/05 12:38 0.3 E 521 8.8 63 05/15/05 17:52 6. M1 467 6.6 11/18/05 12:24 1.1 0.3 MV 513 4.6 64 11/18/05 12:20 trace 65 11/18/05 12:12 0.05 E 525 4.1 66 05/15/05 17:40 1. M1 434 6.0 67 05/15/05 17:34 0.5 M1 420 7.6 Flow was only measured

at the largest spring. 11/18/05 11:50 0.05 E 512 8.5 Flow was measured at the

largest spring and the other springs located farther up the slope were dry.

68 05/15/05 17:28 0.5 M1 431 5.2 11/18/05 11:50 0. E 69 11/18/05 11:25 2. E 532 0.3 70 05/15/05 17:04 0.6 M1 426 5.9 11/19/05 9:00 0. E Dry 71 05/15/05 16:52 0.2 M1 391 6.2 Flow was only measured

at the largest spring since the flow at the other springs was negligible.

11/19/05 8:57 0.1 E 474 7.1 The combined flow from three small springs.

72 05/15/05 16:41 0.5 M1 407 6.1 The flow was measured farther downstream.

11/19/05 8:42 0. E 455 6.1 The channel was damp but there was no flow.

73 05/15/05 16:29 0.3 E 414 7.3 11/19/05 8:40 0. E Dry 74 05/15/05 16:19 0.3 E 409 6.3 11/19/05 8:33 0. E 434 4.1 Damp but not flowing. 76n 07/28/04 10:44 3. M1 461 9.6 04/23/05 13:48 45. M1 327 4.4 76s 07/28/04 10:40 0.3 M1 432 13.4 04/23/05 13:50 16. M1 384 3.1

Amabel and Manitoulin escarpments south of 26/27 Sideroad 77 07/28/04 13:37 0.2 M1 487 8.5 04/22/05 19:15 1.5 M1 330 4.9 04/23/05 18:54 1.5 E 350 4.9 05/10/05 7:16 1. M1 412 5.2 05/17/05 15:25 0.4 M1 412 5.7 11/19/05 11:37 0.02 0.004 MV 455 9.3



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

79 04/23/05 14:12 7. M1 363 2.6 11/19/05 8:10 0.03 0.006 MV 485 3.3 80b 07/28/04 14:20 0.3 E 574 7.1 81 07/28/04 14:40 0.5 E 583 6.8 82w 04/23/05 14:22 5.5 M1 367 3.1 82s 04/23/05 14:23 8. M1 426 5.3 83 04/23/05 14:34 9. M1 357 3.4 86 07/28/04 15:14 0.3 * E 448 8.5 * The discharge at the

spring is underestimated. 07/28/04 15:24 1.7 M1 442 10.1 Measurement about 50 m

farther down the slope. This provided a better estimate of total spring discharge.

SW21C 04/23/04 16:32 3. E 384 7.6 04/23/05 13:31 9. M1 378 4.9 87w 04/23/05 9:06 4. E 04/23/05 14:44 6.5 M1 334 2.0 87e 04/23/05 9:06 5. E 04/23/05 14:44 10. M1 313 1.9 89 04/23/05 15:16 4. E 341 3.3 11/17/05 15:00 0. E Water level was 84 cm

below the top of the well. 90 04/23/05 10:00 2.5 M1 SW21D 04/23/05 13:22 2. M1 248 3.9 11/17/05 14:45 0. E There was some water in

the shallow pond to the south.

Manitoulin Escarpment primarily north of Simcoe County Road 91 227w 04/18/05 8:11 2.6 M1 332 2.2 04/23/05 15:30 1. E 340 2.3 11/17/05 14:35 0.1 E 07/07/06 13:00 0. E Damp but no flow. SW11D 04/18/05 8:16 6. M1 314 3.7 04/23/05 15:32 4. E 346 4.1 07/07/06 14:35 0.1 E 07/07/06 13:00 0.05 M1 227e 04/18/05 8:26 1.5 M1 312 3.9 04/23/05 15:33 2. E 345 4.2 11/17/05 14:35 0. E 07/07/06 13:00 0. E Damp but no flow. 227 07/07/06 14:35 0.2 M1 444 5.4 SW11B 07/29/04 14:27 0.3 E 518 7.6 04/18/05 8:44 5. M1 314 3.8 04/23/05 15:34 6. E 342 4.0 07/07/06 13:30 0.3 M1 228 04/18/05 8:48 4. M1 313 4.0 04/23/05 15:36 0.6 E 346 4.3 07/07/06 13:30 0.05 M1 SW11Aw 04/18/05 8:56 2. M1 313 4.0 SW11Ae 04/18/05 8:56 7. M1 313 4.1



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

SW11A 04/18/05 8:56 9. C2 313 4.1 04/23/05 15:37 4. E 348 4.4 11/17/05 14:29 0.1 0.03 M1 475 7.4 07/07/06 13:30 0.05 M1 91 04/18/05 9:12 5. M1 313 4.1 04/23/05 15:39 2. E 348 4.4 07/07/06 13:30 0. E Wet but no measurable

flow. 92w 04/18/05 9:26 2.5 M1 313 4.4 92c 04/18/05 9:27 1.5 M1 311 4.5 92e 04/18/05 9:27 3. M1 308 4.1 92 04/18/05 9:28 8. M1 309 4.4 04/23/05 15:43 3. E 336 3.9 07/07/06 14:00 0.1 M1 93 04/18/05 9:47 2. M1 306 4.4 07/07/06 14:00 0. E Dry SW11E 04/23/05 11:32 70. M1 04/24/05 19:46 70. E 316 3.9 04/25/05 12:46 56. M1 319 4.6 11/17/05 14:23 0.6 0.2 MV 450 3.6 94 04/18/05 9:59 2. M1 310 4.7 07/07/06 14:00 0. E Dry 95n 04/18/05 10:17 3. M1 304 3.9 95s 04/18/05 10:19 1. M1 302 3.8 95 04/18/05 10:18 4.5 M1 303 4.6 07/07/06 14:00 0. E Dry 96 04/18/05 10:28 1. M1 316 4.2 07/07/06 14:00 0. E Damp but no flow. 97 07/29/04 14:40 0.15 M1 503 10.6 04/18/05 10:29 4. M1 314 4.5 04/19/05 13:42 1.5 M1 311 4.8 04/23/05 19:30 2. E 328 4.8 07/07/06 12:30 0.08 M1 98 04/18/05 10:35 2. M1 311 4.8 04/19/05 13:39 2. M1 305 5.7 07/07/06 14:00 0. E Dry 99 04/18/05 11:18 7. M1 314 5.4 04/19/05 13:59 2. E 305 5.5 07/07/06 14:00 0. E Dry 100A 04/19/05 13:49 3.8 M1 306 6.6 07/07/06 14:00 0. E Dry 100 04/23/04 16:01 1. E 360 5.4 04/19/05 13:49 9. M1 306 5.7 07/07/06 14:00 0. E Dry 101 04/18/05 10:55 2. M1 307 6.9 07/07/06 14:00 0. E Dry 102 04/18/05 10:50 4.5 M1 312 6.8 102 04/19/05 13:35 5.5 M1 307 7.2 04/23/05 19:34 4. E 328 4.8 07/07/06 14:00 0. E Dry



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

103 07/29/04 14:46 0.1 E 446 9.0 07/07/06 12:30 0.04 M1 104 07/29/04 14:55 0.02 E 04/18/05 18:00 1. M1 361 6.1 07/07/06 12:30 0.01 E 105 04/18/05 18:05 23. M1 520 10.4 04/23/05 19:32 20. E 513 3.1 11/17/05 14:17 0.2 E 686 2.7 07/07/06 14:00 1. E There must have been

groundwater discharge upstream from here along the creek, perhaps at Site 106, since the watercourse was dry at SW12A.

106 04/18/05 18:15 2. E 416 6.2 107 04/18/05 18:17 3. E 359 5.9 07/07/06 14:00 0. E Dry 108 04/18/05 18:18 1.5 M1 441 7.8 07/07/06 14:00 0. E Dry 109 04/18/05 18:21 5. M1 1034 10.5 The conductivity is

elevated suggesting that the discharge is contaminated with road salt from County Road 91.

07/07/06 14:00 0. E Dry 110 04/18/05 19:06 1. M1 381 6.4 04/25/05 7:36 518 6.3 Discharge at north side of

small quarry at the cliff. 04/25/05 7:36 616 6.5 Discharge at south side of

small quarry at the cliff. 04/25/05 7:36 697 6.0 Discharge measured 9 m

farther south than previous reading. There appears to be increasing contamination by road salt to the south.

111 04/18/05 18:29 1. M1 444 7.0 04/25/05 7:41 1.6 M1 567 6.2 07/07/06 14:00 0. E Dry 112 04/18/05 18:37 4. M1 557 7.4 04/25/05 7:49 3.5 M1 517 6.1 11/17/05 15:08 0.06 0.02 MV 752 7.0 The spring discharge

sank within 15 m downstream.

07/07/06 14:00 0. E Damp but no flow. Amabel escarpment north of Simcoe County Road 91

113 04/18/05 11:41 1. E 304 4.3 114 04/18/05 11:50 5. M1 317 5.4 114 04/19/05 14:03 6. M1 305 5.5 07/07/06 14:00 0. E Damp but no flow. 115 04/19/05 14:12 0.2 M1 310 5.9



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

116 07/29/04 13:06 0.01 E 510 11.6 Discharge sank through overburden within 10 m.

04/18/05 12:00 5.5 M1 317 5.9 04/19/05 14:15 5. M1 313 6.0 07/07/06 14:00 0.01 E The spring discharge

infiltrated into overburden within 12 m.

117 04/19/05 14:21 0.5 M1 310 6.3 118 07/29/04 12:52 0.01 E 496 12.8 04/19/05 14:24 1. MV 305 5.1 07/07/06 14:00 0.01 E The spring discharge

sank in overburden within 15 m.

119 07/29/04 12:40 0. E The doline to the east was damp but there was no measurable flow.

SW10 04/23/04 15:32 0.2 E 413 7.1 04/19/05 14:37 4. MV 339 7.9 04/23/05 7:35 1.7 M1 363 5.9 SW10n 04/19/05 14:40 3. E 341 6.7 07/29/04 12:04 0.05 E 584 19.0 04/23/04 15:36 0.2 E 423 6.4 SW10s 07/29/04 12:02 0.05 E 578 14.0 04/19/05 14:41 1. E 319 7.2 127 07/29/04 11:51 0.02 E 582 14.9 128 04/19/05 14:45 1.5 E 338 8.7 04/22/05 15:30 0.6 E 130 07/29/04 11:30 0.05 E 569 13.5 131 08/29/04 0. E Dry 04/19/05 14:50 7. M1 340 7.9 04/22/05 15:40 1.8 E

Amabel escarpment south of Simcoe County Road 91 133 04/22/05 8:47 0.01 E 643 4.4 134 04/22/05 17:16 5. M1 11/20/05 8:50 0.02 E 616 3.1 07/07/06 16:00 0.02 E 136 04/22/05 17:05 3. M1 11/20/05 9:02 0.01 E 668 4.0 07/07/06 16:00 0. E Dry SW22A 04/24/05 14:15 8. M1 528 5.2 11/20/05 9:07 0.27 0.03 MV 926 5.9 137 04/24/05 16:01 1. E 536 5.2 11/20/05 9:30 0. E Dry 138 04/25/05 15:57 1.5 E 520 3.2 11/20/05 9:25 0.1 0.03 MV 992 6.4



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

140 04/24/05 15:35 15. E 545 6.0 11/20/05 9:50 0.03 * E 881 5.1 * Flow measured here in

the talus is an underestimate of the total spring discharge. The flow measured at Site 141c farther downstream probably provided a better estimate of total discharge from the spring.

141e 11/20/05 9:35 0. E Damp but no measurable flow.

141c 11/20/05 9:45 0.1 E 858 5.1 141w 11/20/05 9:55 0. E Dry 142 04/24/05 15:22 3. E 478 7.0 11/20/05 10:06 0.05 * E 558 7.2 * Flow measured here is

an underestimate of the total spring discharge.

11/20/05 10:03 0.1 0.03 MV 524 3.6 Flow measured 50 m farther down the gully. This should be representative of the total spring discharge.

143 11/22/05 10:15 0.03 MV 549 7.5 144n 04/22/05 16:55 6. E 11/20/05 10:42 0.6 0.2 MV 926 4.0 144w 04/22/05 16:55 11. E 11/20/05 10:40 0.8 0.2 MV 737 4.5 145n 04/24/05 14:39 23. M1 432 4.2 145s 04/24/05 14:45 8. M1 324 3.1 11/20/05 10:36 0.4 0.1 MV 484 4.1 SW22C 04/22/05 16:27 17. M1 04/24/05 14:45 31. C2 Calculated from

measurements at 145n, s SW22 04/24/04 13:32 2. E 494 6.4 04/22/05 16:47 24. M1 04/24/05 15:00 15. E 449 6.7 05/15/05 12:25 8. M1 524 6.6 11/17/05 12:53 0.37 0.04 MV 543 7.6 146 05/15/05 12:11 0.3 E 487 7.3 11/17/05 0. E 147 05/15/05 11:16 1.5 M1 483 6.8 11/17/05 12:30 0.6 MV 516 8.3 148 05/15/05 11:43 4. M1 464 7.9 149 05/15/05 10:42 0.5 M1 443 7.2 11/17/05 12:00 0. E Spring and watercourse

were dry. 150 11/17/05 12:08 0.25 0.02 MV 513 6.5 152n 05/15/05 9:59 0.2 M1 384 6.5 11/17/05 11:32 0.11 0.01 C1 488 3.8 Discharge was calculated

from discharge at 152.



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

152s 05/15/05 10:01 4. M1 271 6.4 11/17/05 11:28 0.44 0.04 C1 443 6.6 Discharge was calculated

from discharge at 152. 152 11/17/05 11:32 0.55 0.05 MV 452 5.1 153 05/15/05 9:30 10. E 266 5.7 11/17/05 11:16 0.5 E 445 7.1 154 05/15/05 9:23 1. E 266 5.9 11/17/05 11:13 0.7 0.1 MV 446 6.5 155 05/15/05 9:48 28. M1 266 6.3 11/17/05 11:18 0.86 0.09 MV 455 4.7 156 05/15/05 9:14 7. E 269 5.7 11/17/05 11:15 0. E 157 05/15/05 9:04 5. M1 274 5.6 11/17/05 11:10 0. E 552 5.2 Measurements were

made in a puddle at the spring.

158 05/15/05 10:15 9. M1 275 6.5 11/17/05 11:20 0.25 0.1 M1 494 3.7 Flow was difficult to

measure accurately because of thick grass growing in the small channel.

159 07/29/04 10:19 0.19 0.01 MV 570 7.9 Measured the outflow from the concrete cistern.

05/15/05 8:51 3. E 334 5.9 Measured 2.5 m upstream from the cistern.

05/15/05 8:45 6. M1 369 6.5 Measured at the base of the steep slope, about 15 m downstream from the spring.

11/17/05 10:50 0.07 MV 583 8.3 Measured the outflow from the concrete cistern.

11/17/05 10:45 0.3 E 514 4.5 Measured at the base of the steep slope, about 15 m downstream from the spring.

160 11/17/05 11:00 0.5 0.15 M1 514 3.7 161 05/15/05 10:00 47. 19. C2 282 Calculated combined flow

from spring group. 11/17/05 11:20 2.2 0.4 C2 473 Calculated combined flow

from spring group. 162 05/15/05 13:03 3. E 478 7.3 11/17/05 13:36 0.1 E 480 2.8 Flow was measured 80 m

farther downstream at the steel culvert crossing beneath 21/22 Sideroad.

163 05/15/05 13:14 12. M1 411 10.8 11/17/05 13:40 4. M1 445 4.3 SW26A 07/29/04 9:00 0.3 M1 327 14.3



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

SW26 04/23/04 11:23 170 5.7 The stream was sinking at the base of the doline and the water was about 30 cm deep.

07/29/04 9:10 0.3 E 340 15.0 05/15/05 13:39 25. M1 195 7.3 11/17/05 10:00 0.35 0.07 MV 270 1.0 The stream was sinking at

the upstream edge of the doline.

Stream monitoring points around the perimeter of the karst study area SW1 04/23/04 13:30 588 8.9 07/28/04 12:26 45. E 803 17.6 05/16/05 14:38 43. M1 634 10.9 170 05/16/05 14:48 0. 171 SW25

05/16/05 14:55 32. M1 383 11.4 Presumably, all of the flow sank before reaching Site 172, which was dry.

11/20/05 13:18 3. M1 359 2.6 172 04/14/05 11:00 54. M1 All of the flow sank before

reaching Site 173. 05/16/05 15:00 0. 174 05/16/05 15:28 14. M1 471 6.3 175 05/16/05 15:41 4. M1 420 10.6 All of the flow sank about

10 m west at a pool. 176 05/16/05 15:54 426 9.9 177 10/26/04 310. M3 05/16/05 16:04 4000 * E 432 9.6 * Difficult to measure flow

accurately. 178 05/16/05 16:18 5.2 MV 507 7.6 179 05/16/05 16:22 1. MV 506 7.8 180 05/16/05 ? No data. The

watercourse was not investigated.

181 05/16/05 16:39 1. E 600 6.1 182 10/26/04 367. M3 05/16/05 17:03 3000 * E 432 9.5 * Difficult to measure flow

accurately. 183 05/16/05 * * Watercourse was dry or

flow was negligible. 184 05/16/05 16:51 3.8 MV 460 9.6 185 05/16/05 16:58 0.

186 05/16/05 * * Watercourse was dry or

flow was negligible. 187 05/16/05 17:39 5. M1 437 12.1 188 05/16/05 * * Watercourse was dry or

flow was negligible. 189 05/16/05 * * Watercourse was dry or

flow was negligible. 190 05/16/05 * * Watercourse was dry or

flow was negligible. 191 05/16/05 17:49 5. MV 519 8.8 192 05/16/05 17:55 12. MV 447 9.9



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

193 05/16/05 18:00 30. 6. MV 439 9.0 194 05/16/05 18:09 4.4 MV 496 9.7 195 10/26/04 9. M3 05/16/05 18:17 85. 17. M2 395 8.5 196 05/15/05 14:50 2. E 560 8.2 05/16/05 18:36 3.5 MV 563 8.2 197 04/18/05 19:20 10. M1 618 12.9 05/16/05 18:42 0.3 M1 714 12.1 11/17/05 15:20 0. E Dry SW14A 10/26/04 0.7 MV 05/16/05 18:48 21. 5. MV 416 8.9 SW15 05/16/05 18:57 1.8 MV 460 11.8 SW18 10/26/04 1.8 MV 05/16/05 19:03 62. M1 414 9.0 198 10/26/04 0.03 MV 05/16/05 19:16 5.5 MV 460 9.0 199 10/26/04 0.7 MV 05/16/05 19:23 29. M1 454 9.1 200 05/16/05 19:41 3.1 MV 453 11.2 201 05/16/05 19:54 0.6 M1 457 10.3 202 05/16/05 20:00 0. 203 10/26/04 0.8 MV 05/16/05 20:06 17. MV 428 7.8 204 10/26/04 0.4 MV 05/16/05 20:14 2. E Private property, flow

estimated from the road. 205 05/16/05 20:14 1. E Private property, flow

estimated from the road. 206 05/16/05 20:22 0.8 M1 511 8.7 207 05/17/05 8:37 2.2 MV 499 6.8 208s 05/17/05 9:11 53.5 C2 434 5.9 208 10/26/04 4.3 MV 05/17/05 8:46 58. M2 437 5.9 Combined flow from two

tributaries (202s + 203) 209 05/17/05 9:04 4.5 MV 456 6.6 210 05/17/05 9:19 4.4 MV 451 6.4 211e 05/17/05 9:38 6. C2 457 6.5 211w 05/17/05 9:37 3.5 C2 455 6.7 211 10/26/04 0.79 MV 05/17/05 9:32 9.5 MV 460 6.6 Combined flow for both

tributaries (205e + 205w) 212 10/26/04 0.93 MV 05/17/05 9:45 10. MV 430 6.8 213 05/17/05 9:58 7.5 MV 448 7.5 214 10/26/04 5.9 MV 05/17/05 10:04 86. M2 453 7.7 215 05/17/05 10:25 1.4 M1 469 9.6 216 05/17/05 10:32 3.8 MV 450 7.9 217 05/17/05 10:41 3.6 MV 469 8.0 218 05/17/05 10:48 3.3 MV 488 9.2 219 05/17/05 10:55 2. MV 496 8.5



Site

Date mm/dd/yy

Time hr:min

Q L/s

Error L/s

Method

EC µS/cm

Temp °C

Comments

220 05/17/05 11:02 3.9 MV 506 7.8 221 10/26/04 68. M3 05/17/05 11:10 198. M2 506 7.8 222 05/17/05 11:54 216. M1 457 8.6 223e 05/17/05 12:35 161. C2 471 8.9 Calculated from

measurements at Sites 217 and 217w.

223w 05/17/05 12:35 10. M1 477 11.8 223 05/17/05 12:20 171. M1 471 9.1 Combined flow for both

tributaries (217e + 217w). 224e 05/17/05 13:06 6. M1 508 7.7 224s 05/17/05 13:11 18. M1 486 8.2 224w 05/17/05 13:04 7. M1 507 8.6 224 05/17/05 13:16 31. M1 498 8.2 225 05/17/05 13:29 15. MV 457 9.8 SW6A 05/17/05 13:41 270. M1 462 9.2 SW3 05/17/05 14:02 2.2 M1 390 8.9 226 05/17/05 14:10 2.5 M1 319 9.6



Table D-2: Measurements utilized for calculating a rating curve for the SW2A spring

Error is an estimate of the total error in the discharge measurement. The Method used for measuring flow is described in Table D-1. The rating curve was calculated from the water elevations measured relative to Gauge A. The elevation of Gauge A is 516.596 metres above sea level based on an elevation survey by Jagger Hims Limited on November 16, 2006. The rating curve was used to convert water elevation data to discharge data for the SW2A spring.

Water Level Relative to

Each Gauge

Date mm/dd/yy

Time hr:min

Discharge L/s

Error L/s

Method

Gauge A 1 metres

Gauge B 2 metres

Elevation metres a.s.l.

04/14/05 15:14 35. 14. M1 -0.680 0.174 515.916 05/09/05 11:43 17.2 0.9 SDG -0.760 0.095 515.836 05/12/05 16:50 13.6 0.7 SDG -0.773 515.823 05/12/05 17:46 12. 3. M2 -0.774 0.082 515.822 05/17/05 16:53 12. 5. M1 -0.784 0.071 515.812 05/26/05 16:24 8.1 0.4 SDG -0.803 0.053 515.793 10/04/05 11:20 0.32 0.05 MV -0.888 -0.045 3 515.708 11/17/05 16:26 0.15 0.07 M1 -0.871 -0.011 3 515.725 07/08/06 8:30 2. 0.4 M2 -0.859 -0.003 3 515.737

1 Gauge A is the top of the steel pipe inserted vertically into the spring pool next to the spring orifice.

2 Gauge B is an “X” scratched on the bedrock surface exposed beneath the spring pool. These redundant measurements were recorded in case the steel pipe was moved.

3 Three measurements relative to Gauge B were estimated because the water had drained below the “X” on the bedrock surface.


Marcus J. Buck Karst Solutions Appendix E, Page 163 Worthington Groundwater

Appendix E: Groundwater Tracing Data Contents Page Table E-1: Calculation of tracer velocities for the eight groundwater traces..........................164

Table E-2: Groundwater tracing results for an injection at Site 114 on April 19, 2005...........165

Table E-3: Groundwater tracing results for injections at the SW9 watercourse and at SW10 on April 23, 2005......................................................................................169

Table E-4: Groundwater tracing results for the injection at SW28 on May 10, 2005 .............180

Table E-5: Groundwater tracing results for injections at four wells near the SW2A spring....185



Table E-1: Calculation of tracer velocities for the eight groundwater traces

Tracer velocities calculated here consider the length of the flow paths along surface streams and through talus in addition to the straight-line flow path through bedrock. The velocities are calculated from the time to peak concentration. For some traces, the velocities indicated are significantly higher than the mean velocities because of the high dispersion that occurs for those streams sinking through the overburden mantle.

Estimated Length of Flow Path (m)

Details of Groundwater Trace InjectionSite

SamplingSite

Streama

Bedrockb

Talusc

Sum a+b+c

Time to Peak Concentration

(hours)

Tracer Velocity

(m/hr) 97 11 25 86 122 1.6 7698 11 25 75 111 2.2 51

101 11 33 72 116 4.2 28Small sinking stream on Manitoulin bench ● 3.25 g uranine: 9:05 am, April 19, 2005 114

102 11 33 71 115 0.8 14789 178 557 13 748 53 1490 178 530 10 718 53 14

SW21D 208 432 125 765 103 7SW11E 318 485 108 911 8.1 113

105 288 690 70 1048 12 90114 178 540 43 761 12 64

SW9 watercourse on Amabel plateau ● 99.3 g uranine: 7:08 am, April 23, 2005 12

116 178 530 43 751 12 63SW11E 143 370 63 576 14.0 41Small sinking stream on Manitoulin bench

● 8.7 g phloxine B: 7:32 am, April 23, 2005 SW10 105 115 162 70 347 11 31

SW27 144 300 2 446 22.7 20Sinking stream on Amabel plateau ● 24.75 g uranine: 6:00 am, May 10, 2005 SW28

BH03-9 5 17 0 22 0.45 49TW04-1 5 18 0 23 * not recovered * <0.2TW04-2 5 35 0 40 9.88 4

Four wells to the SW2A spring (May 12, 2005)● BH03-9: 2.34 g uranine at 2:15 pm ● TW04-1: 10.83 g phloxine B at 5:55 pm ● TW04-2: 12.3 g uranine at 6:07 pm ● TW04-3: 12.82 g phloxine B at 2:51 pm TW04-3

19 (SW2A)

5 24 0 29 0.39 75

* Although a spike was detected at 15 hours after injection, this does not have the characteristic shape of a breakthrough curve. Therefore, there was no clear indication of tracer recovery even 119 hours after injection and the tracer velocity was less than 0.2 m/hr.



Table E-2: Groundwater tracing results for an injection at Site 114 on April 19, 2005

3.25 g of uranine was injected into the stream at Site 114 at 9:05 am on April 19, 2005. The injection site is immediately downstream from the spring and at the time the stream flowed for 16 m before completely sinking into overburden. Water samples were collected at 20 sites. The Time Elapsed is the number of hours elapsed after the injection. Note that sampling started prior to the injection at most sites to determine background fluorescence and therefore the elapsed time for these samples is negative. [UR] is the measured fluorescence expressed as ppb uranine and this includes the background fluorescence.

Water Sample Collection Results Site Date

(mm/dd/yy) Time

(hr:min:sec) Time Elapsed

(hr) [UR] (ppb)

227 04/19/05 9:49:20 0.739 0.876 04/19/05 10:26:00 1.350 0.858 04/19/05 11:48:30 2.725 0.954 04/19/05 15:27:30 6.375 1.279

SW11B 04/19/05 8:27:40 -0.622 0.571 04/19/05 9:48:40 0.728 0.676 04/19/05 10:25:20 1.339 0.615 04/19/05 11:47:40 2.711 0.720 04/19/05 15:26:40 6.361 0.650

228 04/19/05 8:27:00 -0.633 0.557 04/19/05 9:48:00 0.717 0.579 04/19/05 10:24:40 1.328 0.640 04/19/05 11:47:10 2.703 0.656 04/19/05 15:26:10 6.353 0.603

SW11A 04/19/05 8:25:30 -0.658 0.605 04/19/05 9:47:00 0.700 0.589 04/19/05 10:23:30 1.308 0.666 04/19/05 11:46:10 2.686 0.621 04/19/05 15:25:00 6.333 0.660

91 04/19/05 8:24:10 -0.681 0.585 04/19/05 9:46:10 0.686 0.494 04/19/05 10:22:50 1.297 0.654 04/19/05 11:45:10 2.669 0.617 04/19/05 15:23:20 6.306 0.688

92 04/19/05 8:23:10 -0.697 0.470 04/19/05 9:45:20 0.672 0.454 04/19/05 10:21:40 1.278 0.504 04/19/05 11:44:00 2.650 0.478 04/19/05 15:22:30 6.292 0.537

93 04/19/05 8:21:20 -0.728 0.571 04/19/05 9:30:00 0.417 0.547 04/19/05 9:44:00 0.650 0.595 04/19/05 10:06:20 1.022 0.634 04/19/05 10:20:10 1.253 0.551 04/19/05 10:45:00 1.667 0.575




(mm/dd/yy) Time


(hr) [UR] (ppb)

93 04/19/05 11:42:40 2.628 0.555 04/19/05 15:21:00 6.267 0.478

94 04/19/05 8:20:00 -0.750 0.551 04/19/05 9:21:20 0.272 0.504 04/19/05 9:31:50 0.447 0.571 04/19/05 9:43:00 0.633 0.591 04/19/05 10:05:00 1.000 0.559 04/19/05 10:19:20 1.239 0.589 04/19/05 10:44:00 1.650 0.621 04/19/05 11:42:00 2.617 0.591 04/19/05 15:20:00 6.250 0.630

95 04/19/05 8:19:00 -0.767 0.551 04/19/05 9:20:40 0.261 0.613 04/19/05 9:31:00 0.433 0.632 04/19/05 9:42:20 0.622 0.654 04/19/05 10:04:30 0.992 0.593 04/19/05 10:18:30 1.225 0.613 04/19/05 10:43:10 1.636 0.626 04/19/05 11:41:00 2.600 0.630 04/19/05 15:19:10 6.236 0.674

96 04/19/05 8:18:00 -0.783 0.258 04/19/05 9:20:00 0.250 0.325 04/19/05 9:30:30 0.425 0.305 04/19/05 9:41:30 0.608 0.343 04/19/05 10:04:00 0.983 0.301 04/19/05 10:17:50 1.214 0.321 04/19/05 10:42:40 1.628 0.349 04/19/05 11:40:00 2.583 0.424 04/19/05 15:18:30 6.225 0.559

97 04/19/05 8:17:20 -0.794 0.470 04/19/05 9:19:10 0.236 0.549 04/19/05 9:29:50 0.414 0.496 04/19/05 9:42:00 0.617 0.452 04/19/05 10:03:20 0.972 1.862 04/19/05 10:17:10 1.203 5.287 04/19/05 10:41:40 1.611 6.987 04/19/05 11:16:30 2.192 6.475 04/19/05 11:39:30 2.575 5.969 04/19/05 12:27:40 3.378 4.986 04/19/05 13:20:00 4.250 4.249 04/19/05 15:17:30 6.208 3.279

98 04/19/05 8:16:00 -0.817 0.452




(mm/dd/yy) Time


(hr) [UR] (ppb)

98 04/19/05 9:18:10 0.219 0.587 04/19/05 9:29:00 0.400 0.539 04/19/05 9:39:50 0.581 0.601 04/19/05 10:02:30 0.958 4.078 04/19/05 10:16:20 1.189 10.097 04/19/05 10:41:00 1.600 12.887 04/19/05 11:15:30 2.175 12.934 04/19/05 11:38:50 2.564 10.876 04/19/05 12:26:50 3.364 8.579 04/19/05 13:18:40 4.228 6.927 04/19/05 15:16:40 6.194 4.736

99 04/19/05 13:59:00 4.900 1.342100 04/19/05 13:48:00 4.717 1.469

100A 04/19/05 13:48:00 4.717 1.487101 04/19/05 8:15:20 -0.828 0.406

04/19/05 9:17:40 0.211 0.416 04/19/05 9:28:20 0.389 0.498 04/19/05 9:39:20 0.572 0.426 04/19/05 10:01:40 0.944 0.745 04/19/05 10:15:50 1.181 0.936 04/19/05 10:40:00 1.583 1.277 04/19/05 11:14:30 2.158 1.273 04/19/05 11:37:20 2.539 1.386 04/19/05 12:25:40 3.344 1.336 04/19/05 13:18:00 4.217 1.431 04/19/05 15:16:00 6.183 1.293

102 04/19/05 8:11:20 -0.894 0.502 04/19/05 9:17:20 0.206 0.527 04/19/05 9:25:00 0.333 0.488 04/19/05 9:27:40 0.378 0.502 04/19/05 9:38:30 0.558 2.559 04/19/05 9:52:00 0.783 6.366 04/19/05 9:58:30 0.892 6.227 04/19/05 10:10:40 1.094 5.668 04/19/05 10:34:40 1.494 4.270 04/19/05 11:14:00 2.150 3.123 04/19/05 11:36:50 2.531 2.676 04/19/05 12:21:40 3.278 2.090 04/19/05 13:16:00 4.183 1.661 04/19/05 15:15:20 6.172 1.328

104 04/19/05 8:09:00 -0.933 0.172 04/19/05 9:16:00 0.183 0.125




(mm/dd/yy) Time


(hr) [UR] (ppb)

104 04/19/05 9:26:50 0.364 0.174 04/19/05 9:37:50 0.547 0.224 04/19/05 9:57:40 0.878 0.276 04/19/05 10:09:50 1.081 0.206 04/19/05 10:33:50 1.481 0.250 04/19/05 11:36:00 2.517 0.258 04/19/05 15:14:30 6.158 0.218

105 04/19/05 8:07:40 -0.956 0.577 04/19/05 9:14:30 0.158 0.482 04/19/05 9:26:00 0.350 0.450 04/19/05 9:37:10 0.536 0.426 04/19/05 9:57:00 0.867 0.575 04/19/05 10:09:10 1.069 0.531 04/19/05 10:33:00 1.467 0.555 04/19/05 11:35:10 2.503 0.543 04/19/05 15:13:30 6.142 0.650

114 1 04/19/05 14:01:00 4.933 0.843

1 The sample collected for Site 114 was collected from the sinking stream about 15 metres downstream from the injection site.



Table E-3: Groundwater tracing results for injections at the SW9 watercourse and at SW10 on April 23, 2005

Two injections were conducted on April 23, 2005:

1) 98 g of uranine was injected into the SW9 watercourse at Site 12 at 7:08 am. The injection site is about 23 m upstream from SW9 where Jagger Hims Limited conducts monthly flow measurements. At the time, the SW9 watercourse probably flowed an additional 250 m before completely sinking into the overburden. A series of measurements on April 25, 2005 indicated gradual loss of flow all along the watercourse downstream from Site 13A, located 60 m downstream from the injection site.

2) 10 g of phloxine B were injected just downstream from the water supply system at SW10 at 7:32 am. At the time, the stream sank into overburden within a few metres before reaching the doline at Site 124.

Water samples were collected at 55 sites. The Time Elapsed is the number of hours elapsed after each injection. [UR] and [PB] are the measured fluorescence expressed as ppb uranine and ppb phloxine B and these include background fluorescence.

Sample Collection Uranine Results Phloxine B Results Site Date

(mm/dd/yy) Time

(hr:min) Time Elapsed

(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

76n 04/23/05 8:34 1.433 0.173 1.033 -0.348 04/23/05 9:37 2.483 0.202 2.083 -0.032 04/23/05 10:27 3.317 0.120 2.917 0.237 04/23/05 11:18 4.167 0.136 3.767 -0.237 04/23/05 12:29 5.350 0.157 4.950 -0.063 04/23/05 13:47 6.650 0.226 6.250 0.300 04/23/05 19:00 11.867 0.141 11.467 0.142 04/24/05 10:26 27.300 0.246 26.900 0.032 04/25/05 12:10 53.033 0.193 52.633 0.11176s 04/23/05 8:34 1.433 0.204 1.033 -0.111 04/23/05 9:37 2.483 0.196 2.083 -0.095 04/23/05 10:27 3.317 0.147 2.917 -0.142 04/23/05 11:18 4.167 0.161 3.767 -0.095 04/23/05 12:29 5.350 0.198 4.950 0.095 04/23/05 13:47 6.650 0.277 6.250 0.996 04/23/05 19:01 11.883 0.333 11.483 0.696 04/24/05 10:27 27.317 0.290 26.917 0.522 04/25/05 12:11 53.050 0.246 52.650 0.64877 04/23/05 18:55 11.783 0.088 11.383 -0.221 04/24/05 10:20 27.200 0.035 26.800 -0.41179 04/23/05 8:44 1.600 0.244 1.200 0.348 04/23/05 9:45 2.617 0.216 2.217 -0.095 04/23/05 10:30 3.367 0.210 2.967 -0.190 04/23/05 11:21 4.217 0.214 3.817 0.016 04/23/05 12:33 5.417 0.206 5.017 0.000 04/23/05 14:11 7.050 0.218 6.650 -0.07979 04/23/05 19:05 11.950 0.279 11.550 0.348 04/24/05 10:30 27.367 0.222 26.967 0.111 04/25/05 12:15 53.117 0.189 52.717 0.206




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

82n 04/23/05 8:23 1.250 0.031 0.850 -0.364 04/23/05 8:52 1.733 0.261 1.333 0.348 04/23/05 9:48 2.667 0.206 2.267 0.348 04/23/05 10:33 3.417 0.208 3.017 0.379 04/23/05 11:25 4.283 0.204 3.883 0.348 04/23/05 12:37 5.483 0.271 5.083 0.506 04/23/05 14:19 7.183 0.240 6.783 0.664 04/23/05 19:10 12.033 0.367 11.633 1.597 04/24/05 10:35 27.450 0.230 27.050 1.312 04/25/05 12:18 53.167 0.328 52.767 0.63282s 04/23/05 8:18 1.167 0.216 0.767 0.158 04/23/05 8:52 1.733 0.248 1.333 0.285 04/23/05 9:49 2.683 0.265 2.283 0.364 04/23/05 10:33 3.417 0.228 3.017 0.285 04/23/05 11:25 4.283 0.279 3.883 0.348 04/23/05 12:37 5.483 0.214 5.083 0.364 04/23/05 14:19 7.183 0.251 6.783 0.237 04/23/05 19:00 11.867 0.263 11.467 0.617 04/24/05 10:36 27.467 0.216 27.067 0.364 04/25/05 12:18 53.167 0.436 52.767 0.33283 04/23/05 8:55 1.783 0.318 1.383 0.285 04/23/05 9:54 2.767 0.385 2.367 0.569 04/23/05 10:40 3.533 0.373 3.133 0.696 04/23/05 11:27 4.317 0.338 3.917 0.332 04/23/05 12:39 5.517 0.330 5.117 0.379 04/23/05 14:31 7.383 0.346 6.983 0.411 04/23/05 19:12 12.067 0.436 11.667 1.075 04/24/05 10:38 27.500 0.409 27.100 0.917 04/25/05 12:22 53.233 0.385 52.833 0.522SW21C 04/23/05 8:12 1.067 0.308 0.667 0.648 04/23/05 9:29 2.350 0.265 1.950 0.964 04/23/05 10:17 3.150 0.268 2.750 -0.032 04/23/05 11:08 4.000 0.270 3.600 0.095 04/23/05 12:18 5.167 0.230 4.767 -0.079 04/23/05 13:30 6.367 0.289 5.967 0.063 04/23/05 18:32 11.400 0.434 11.000 0.364 04/24/05 10:05 26.950 0.470 26.550 0.474 04/25/05 12:00 52.867 0.308 52.467 0.300 04/27/05 14:00 102.867 0.375 102.467 0.474 04/29/05 * 136.867 0.306 136.467 0.28587w 04/23/05 9:06 1.967 0.297 1.567 0.775 04/23/05 9:59 2.850 0.330 2.450 0.522




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

87w 04/23/05 10:46 3.633 0.350 3.233 0.427 04/23/05 11:31 4.383 0.344 3.983 0.158 04/23/05 12:43 5.583 0.363 5.183 0.427 04/23/05 14:41 7.550 0.314 7.150 0.253 04/23/05 19:18 12.167 0.501 11.767 1.107 04/24/05 10:44 27.600 0.450 27.200 1.059 04/25/05 12:28 53.333 0.409 52.933 0.47487e 04/23/05 9:06 1.967 0.955 1.567 1.265 04/23/05 10:00 2.867 0.959 2.467 1.122 04/23/05 10:46 3.633 0.978 3.233 1.423 04/23/05 11:31 4.383 0.935 3.983 1.138 04/23/05 12:44 5.600 0.952 5.200 1.565 04/23/05 14:41 7.550 0.956 7.150 1.470 04/23/05 19:18 12.167 1.077 11.767 2.466 04/24/05 10:44 27.600 1.131 27.200 2.324 04/25/05 12:28 53.333 1.143 52.933 1.50289 04/24/05 10:47 27.650 1.603 27.250 2.181 04/25/05 12:30 53.367 2.031 52.967 1.391 04/27/05 * 88.867 1.801 88.467 1.818 04/29/05 * 136.867 1.252 136.467 1.10790 04/24/05 10:00 26.867 1.711 26.467 2.023 04/25/05 11:58 52.833 1.732 52.433 1.201 04/27/05 * 88.867 1.473 88.467 1.138 04/29/05 * 136.867 1.115 136.467 0.632SW21D 04/23/05 8:07 0.983 1.120 0.583 1.770 04/23/05 9:14 2.100 1.073 1.700 1.897 04/23/05 9:24 2.267 1.096 1.867 1.865 04/23/05 10:11 3.050 1.264 2.650 1.280 04/23/05 11:04 3.933 1.203 3.533 1.328 04/23/05 12:13 5.083 1.203 4.683 1.201 04/23/05 13:19 6.183 1.205 5.783 1.581 04/23/05 15:11 8.050 1.239 7.650 1.375 04/23/05 18:26 11.300 1.203 10.900 1.359 04/24/05 9:55 26.783 1.492 26.383 2.071 04/25/05 11:50 52.700 1.401 52.300 1.707 04/27/05 13:40 102.533 1.540 102.133 2.245 04/29/05 * 136.867 1.315 136.467 1.691227w 04/23/05 19:04 11.933 5.165 11.533 1.597 04/24/05 10:58 27.833 2.098 27.433 1.660 04/25/05 12:35 53.450 1.324 53.050 0.869




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

SW11D 04/23/05 19:03 11.917 13.721 11.517 2.102 04/24/05 10:58 27.833 4.234 27.433 1.201 04/25/05 12:35 53.450 2.020 53.050 0.933227e 04/23/05 19:02 11.900 11.562 11.500 1.628 04/24/05 10:54 27.767 4.548 27.367 0.948 04/25/05 12:35 53.450 2.122 53.050 0.490227 04/23/05 7:57 0.817 0.774 0.417 0.696SW11B 04/23/05 19:00 11.867 12.607 11.467 1.391 04/24/05 11:03 27.917 3.864 27.517 0.854 04/25/05 12:38 53.500 1.994 53.100 0.537228 04/23/05 18:59 11.850 14.116 11.450 1.960 04/24/05 11:04 27.933 3.870 27.533 0.617 04/25/05 12:38 53.500 2.026 53.100 0.474SW11A 04/23/05 18:58 11.833 16.255 11.433 2.213 04/24/05 11:05 27.950 3.967 27.550 0.648 04/25/05 12:39 53.517 1.990 53.117 0.71191 04/23/05 18:58 11.833 16.964 11.433 2.940 04/24/05 11:07 27.983 3.784 27.583 1.549 04/25/05 12:40 53.533 1.990 53.133 1.26592 04/23/05 18:57 11.817 8.411 11.417 1.423 04/24/05 11:09 28.017 3.045 27.617 0.775 04/25/05 12:41 53.550 1.823 53.150 0.72793 04/23/05 18:56 11.800 4.519 11.400 0.980 04/24/05 11:11 28.050 3.118 27.650 0.996 04/25/05 12:42 53.567 1.790 53.167 0.506SW11E 04/23/05 7:51 0.717 0.648 0.317 1.107 04/23/05 8:26 1.300 0.682 0.900 1.107 04/23/05 8:31 1.383 0.662 0.983 0.648 04/23/05 8:40 1.533 0.654 1.133 1.170 04/23/05 8:46 1.633 0.692 1.233 1.644 04/23/05 9:01 1.883 0.684 1.483 1.201 04/23/05 9:08 2.000 0.709 1.600 0.775 04/23/05 9:16 2.133 0.684 1.733 1.122 04/23/05 9:31 2.383 0.707 1.983 1.344 04/23/05 9:46 2.633 0.723 2.233 1.012 04/23/05 9:55 2.783 0.688 2.383 0.885 04/23/05 10:01 2.883 0.703 2.483 0.585 04/23/05 10:16 3.133 0.684 2.733 0.395 04/23/05 10:31 3.383 0.707 2.983 0.727 04/23/05 10:46 3.633 0.788 3.233 0.696 04/23/05 11:01 3.883 0.963 3.483 0.711 04/23/05 11:16 4.133 1.328 3.733 0.696




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

SW11E 04/23/05 11:31 4.383 2.104 3.983 0.522 04/23/05 11:46 4.633 3.006 4.233 1.439 04/23/05 12:01 4.883 4.008 4.483 1.075 04/23/05 12:16 5.133 5.128 4.733 1.107 04/23/05 12:24 5.267 6.075 4.867 0.996 04/23/05 12:31 5.383 6.124 4.983 1.249 04/23/05 12:46 5.633 7.067 5.233 1.486 04/23/05 12:51 5.717 7.902 5.317 1.201 04/23/05 13:01 5.883 7.904 5.483 1.265 04/23/05 13:16 6.133 8.666 5.733 1.612 04/23/05 13:31 6.383 9.375 5.983 1.628 04/23/05 13:46 6.633 9.894 6.233 5.691 04/23/05 14:01 6.883 10.356 6.483 1.644 04/23/05 14:11 7.050 10.986 6.650 1.865 04/23/05 14:16 7.133 10.672 6.733 1.676 04/23/05 14:50 7.700 11.866 7.300 1.723 04/23/05 15:12 8.067 12.084 7.667 2.071 04/23/05 15:32 8.400 11.821 8.000 2.245 04/23/05 16:32 9.400 12.008 9.000 2.292 04/23/05 17:32 10.400 11.678 10.000 2.513 04/23/05 18:32 11.400 11.393 11.000 2.308 04/23/05 18:51 11.717 11.560 11.317 2.371 04/23/05 19:32 12.400 10.733 12.000 2.656 04/23/05 20:32 13.400 10.004 13.000 2.766 04/23/05 21:32 14.400 9.322 14.000 2.877 04/23/05 22:32 15.400 8.587 15.000 2.719 04/23/05 23:32 16.400 7.955 16.000 2.466 04/24/05 0:32 17.400 7.438 17.000 2.213 04/24/05 1:32 18.400 6.792 18.000 2.102 04/24/05 2:32 19.400 6.130 19.000 2.308 04/24/05 3:32 20.400 5.527 20.000 2.197 04/24/05 4:32 21.400 5.069 21.000 2.482 04/24/05 5:32 22.400 4.672 22.000 2.687 04/24/05 6:32 23.400 4.220 23.000 2.482 04/24/05 7:32 24.400 3.892 24.000 1.818 04/24/05 8:32 25.400 3.723 25.000 2.055 04/24/05 9:32 26.400 3.591 26.000 1.897 04/24/05 10:32 27.400 3.432 27.000 1.612 04/24/05 11:13 28.083 3.279 27.683 1.375 04/24/05 11:32 28.400 3.275 28.000 1.597 04/24/05 12:32 29.400 3.106 29.000 1.265 04/24/05 13:32 30.400 3.067 30.000 1.612




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

SW11E 04/24/05 14:32 31.400 2.762 31.000 1.944 04/24/05 19:42 36.567 2.507 36.167 1.296 04/24/05 21:42 38.567 2.461 38.167 1.170 04/25/05 0:42 41.567 2.294 41.167 1.059 04/25/05 3:42 44.567 2.168 44.167 1.075 04/25/05 6:42 47.567 2.061 47.167 0.711 04/25/05 9:32 50.400 1.930 50.000 0.964 04/25/05 12:42 53.567 1.875 53.167 0.854 04/27/05 13:20 102.200 1.165 101.800 0.948 04/29/05 * 136.867 0.672 136.467 0.94894 04/23/05 10:44 3.600 0.523 3.200 0.585 04/23/05 18:50 11.700 1.426 11.300 1.502 04/24/05 11:12 28.067 2.244 27.667 1.328 04/25/05 13:00 53.867 1.477 53.467 1.17095 04/23/05 10:44 3.600 0.609 3.200 1.091 04/23/05 18:50 11.700 2.970 11.300 1.043 04/24/05 11:24 28.267 2.605 27.867 1.233 04/25/05 13:00 53.867 1.631 53.467 0.96496 04/23/05 18:49 11.683 0.472 11.283 0.617 04/24/05 11:26 28.300 0.772 27.900 0.664 04/25/05 13:01 53.883 0.667 53.483 0.53797 04/23/05 10:41 3.550 0.517 3.150 0.316 04/23/05 18:46 11.633 0.859 11.233 0.885 04/24/05 11:30 28.367 1.206 27.967 0.980 04/25/05 13:01 53.883 0.992 53.483 0.96498 04/24/05 11:37 28.483 1.658 28.083 1.043 04/25/05 13:04 53.933 1.246 53.533 1.249101 04/24/05 11:38 28.500 1.334 28.100 0.743 04/25/05 13:04 53.933 1.018 53.533 0.696102 04/23/05 7:50 0.700 0.695 0.300 0.854 04/23/05 8:01 0.883 0.527 0.483 0.569 04/23/05 8:24 1.267 0.546 0.867 0.348 04/23/05 8:42 1.567 0.554 1.167 0.490 04/23/05 9:05 1.950 0.546 1.550 0.711 04/23/05 9:20 2.200 0.574 1.800 0.790 04/23/05 9:52 2.733 0.560 2.333 0.427 04/23/05 10:07 2.983 0.536 2.583 0.458 04/23/05 10:38 3.500 0.542 3.100 0.585 04/23/05 10:48 3.667 0.642 3.267 0.743 04/23/05 11:44 4.600 0.611 4.200 0.854 04/23/05 12:21 5.217 0.546 4.817 0.664 04/23/05 12:48 5.667 0.556 5.267 0.427




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

102 04/23/05 13:26 6.300 0.558 5.900 0.648 04/23/05 14:08 7.000 0.686 6.600 0.237 04/23/05 14:47 7.650 0.800 7.250 0.490 04/23/05 18:42 11.567 1.607 11.167 1.138 04/24/05 11:39 28.517 1.582 28.117 0.996 04/25/05 13:05 53.950 1.141 53.550 1.091104 04/24/05 11:40 28.533 0.312 28.133 0.822 04/25/05 13:06 53.967 0.244 53.567 0.332105 04/23/05 7:47 0.650 0.666 0.250 0.901 04/23/05 8:38 1.500 0.633 1.100 0.964 04/23/05 9:06 1.967 0.631 1.567 1.241 04/23/05 9:19 2.183 0.617 1.783 1.043 04/23/05 9:53 2.750 0.637 2.350 0.972 04/23/05 10:06 2.967 0.690 2.567 2.474 04/23/05 10:39 3.517 0.633 3.117 0.972 04/23/05 11:46 4.633 0.672 4.233 1.241 04/23/05 12:22 5.233 0.597 4.833 0.980 04/23/05 12:49 5.683 0.665 5.283 2.324 04/23/05 13:27 6.317 0.583 5.917 1.249 04/23/05 14:09 7.017 0.585 6.617 1.146 04/23/05 14:48 7.667 0.577 7.267 1.043 04/23/05 18:44 11.600 0.938 11.200 7.556 04/24/05 11:41 28.550 0.708 28.150 3.794 04/25/05 13:06 53.967 0.599 53.567 1.589107 04/24/05 11:53 28.750 0.316 28.350 0.063 04/25/05 13:36 54.467 0.257 54.067 0.285SW12A 04/23/05 8:46 1.633 0.629 1.233 0.474 04/23/05 9:25 2.283 0.650 1.883 0.443 04/23/05 9:49 2.683 0.656 2.283 0.601 04/23/05 10:11 3.050 0.646 2.650 0.885 04/23/05 10:35 3.450 0.609 3.050 0.790 04/23/05 12:16 5.133 0.662 4.733 0.458 04/23/05 12:44 5.600 0.587 5.200 0.490 04/23/05 13:22 6.233 0.593 5.833 0.506 04/23/05 14:40 7.533 0.556 7.133 0.664 04/23/05 19:21 12.217 0.792 11.817 1.518 04/24/05 11:53 28.750 0.582 28.350 0.822 04/25/05 13:37 54.483 0.491 54.083 0.790108 04/24/05 11:56 28.800 0.409 28.400 1.265 04/25/05 13:38 54.500 0.348 54.100 1.122109 04/24/05 11:56 28.800 0.782 28.400 1.992 04/25/05 13:38 54.500 0.717 54.100 1.660




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

110 04/24/05 12:00 28.867 0.310 28.467 0.601 04/25/05 7:40 48.533 0.192 48.133 0.253 04/27/05 * 88.867 0.352 88.467 0.395 04/29/05 * 136.867 0.310 136.467 0.522111 04/24/05 11:59 28.850 0.342 28.450 1.344112 04/24/05 12:04 28.933 0.230 28.533 0.601 04/25/05 7:49 48.683 0.212 48.283 0.506114 04/23/05 7:40 0.533 0.527 0.133 0.079 04/23/05 8:42 1.567 0.564 1.167 0.316 04/23/05 9:37 2.483 0.460 2.083 0.190 04/23/05 10:35 3.450 0.525 3.050 0.221 04/23/05 11:49 4.683 0.491 4.283 0.000 04/23/05 13:08 6.000 0.542 5.600 0.190 04/23/05 14:48 7.667 1.240 7.267 0.032 04/23/05 19:07 11.983 4.609 11.583 0.759 04/24/05 9:39 26.517 2.798 26.117 0.775 04/25/05 12:44 53.600 1.399 53.200 0.427116 04/23/05 7:42 0.567 0.468 0.167 -0.221 04/23/05 8:44 1.600 0.483 1.200 0.190 04/23/05 9:40 2.533 0.440 2.133 -0.206 04/23/05 10:37 3.483 0.438 3.083 0.063 04/23/05 11:51 4.717 0.729 4.317 0.759 04/23/05 13:10 6.033 2.623 5.633 0.300 04/23/05 14:50 7.700 5.218 7.300 0.474 04/23/05 19:08 12.000 6.312 11.600 1.075 04/24/05 9:41 26.550 2.527 26.150 0.664 04/25/05 12:46 53.633 1.312 53.233 0.348SW10 04/23/05 7:46 0.633 0.426 0.233 0.142 04/23/05 8:46 1.633 0.393 1.233 -0.221 04/23/05 9:44 2.600 0.418 2.200 -0.016 04/23/05 10:40 3.533 0.369 3.133 -0.047 04/23/05 11:53 4.750 0.363 4.350 -0.126 04/23/05 13:13 6.083 0.383 5.683 0.032 04/23/05 14:55 7.783 0.328 7.383 0.079 04/23/05 19:13 12.083 0.497 11.683 0.458 04/24/05 9:46 26.633 0.552 26.233 0.253 04/25/05 12:51 53.717 0.515 53.317 0.221128 04/23/05 7:48 0.667 0.572 0.267 0.206 04/23/05 8:48 1.667 0.538 1.267 0.285 04/23/05 9:46 2.633 0.493 2.233 0.206 04/23/05 10:42 3.567 0.477 3.167 -0.158 04/23/05 11:56 4.800 0.501 4.400 0.206




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

128 04/23/05 13:15 6.117 0.519 5.717 0.126 04/23/05 14:58 7.833 0.635 7.433 0.285 04/23/05 19:16 12.133 0.564 11.733 -0.032 04/24/05 9:49 26.683 0.599 26.283 0.316 04/25/05 12:53 53.750 0.574 53.350 0.506131 04/23/05 7:50 0.700 0.517 0.300 0.111 04/23/05 8:50 1.700 0.519 1.300 0.269 04/23/05 9:48 2.667 0.481 2.267 0.253 04/23/05 10:44 3.600 0.525 3.200 0.569 04/23/05 11:58 4.833 0.511 4.433 0.253 04/23/05 13:19 6.183 0.454 5.783 0.190 04/23/05 15:07 7.983 0.660 7.583 0.237 04/23/05 19:18 12.167 0.597 11.767 0.727 04/24/05 9:51 26.717 0.517 26.317 0.364 04/25/05 12:55 53.783 0.546 53.383 0.348134 04/23/05 7:57 0.817 0.299 0.417 0.490 04/23/05 8:57 1.817 0.273 1.417 0.332 04/23/05 9:53 2.750 0.297 2.350 0.095 04/23/05 11:00 3.867 0.297 3.467 0.095 04/23/05 12:16 5.133 0.291 4.733 0.759 04/23/05 13:50 6.700 0.274 6.300 0.285 04/23/05 15:31 8.383 0.331 7.983 0.032 04/23/05 18:16 11.133 0.341 10.733 0.348 04/24/05 10:01 26.883 0.392 26.483 0.379 04/24/05 14:00 30.867 0.468 30.467 0.585 04/25/05 7:33 48.417 0.350 48.017 0.364 04/25/05 12:02 52.900 0.381 52.500 0.332 04/29/05 * 136.867 0.320 136.467 -0.142136 04/23/05 8:02 0.900 0.719 0.500 0.664 04/23/05 8:59 1.850 0.721 1.450 0.617 04/23/05 9:57 2.817 0.707 2.417 0.838 04/23/05 11:03 3.917 0.676 3.517 0.269 04/23/05 12:21 5.217 0.709 4.817 0.427 04/23/05 13:56 6.800 0.718 6.400 -0.063 04/23/05 15:37 8.483 0.737 8.083 0.269 04/23/05 18:19 11.183 0.737 10.783 0.253 04/24/05 10:06 26.967 1.110 26.567 0.980 04/24/05 14:04 30.933 1.034 30.533 0.901 04/24/05 16:09 33.017 1.144 32.617 1.233 04/25/05 7:37 48.483 0.908 48.083 0.743 04/25/05 13:34 54.433 0.862 54.033 0.822 04/27/05 * 88.867 1.024 88.467 1.122




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

136 04/29/05 * 136.867 0.919 136.467 1.122SW22A 04/24/05 14:12 31.067 0.687 30.667 0.348 04/24/05 16:03 32.917 0.851 32.517 0.696 04/25/05 7:40 48.533 0.567 48.133 0.379 04/25/05 13:09 54.017 0.449 53.617 0.221 04/27/05 * 88.867 0.632 88.467 0.285SW22A 04/29/05 * 136.867 0.339 136.467 0.190140 04/24/05 15:39 32.517 0.525 32.117 1.043142 04/24/05 15:22 32.233 0.110 31.833 -0.269144w 04/24/05 14:36 31.467 0.763 31.067 0.964 04/27/05 * 88.867 0.919 88.467 1.249 04/29/05 * 136.867 0.638 136.467 0.601145n 04/24/05 14:43 31.583 0.813 31.183 0.901 04/27/05 * 88.867 0.912 88.467 0.869 04/29/05 * 136.867 0.933 136.467 1.059SW22C 04/23/05 8:07 0.983 0.772 0.583 1.075 04/23/05 9:05 1.950 0.749 1.550 0.680 04/23/05 10:02 2.900 0.701 2.500 1.122 04/23/05 11:10 4.033 0.649 3.633 0.664 04/23/05 12:29 5.350 0.683 4.950 0.711 04/23/05 14:03 6.917 0.678 6.517 0.490 04/23/05 15:44 8.600 0.710 8.200 0.885 04/23/05 18:26 11.300 0.813 10.900 0.980 04/24/05 10:14 27.100 0.862 26.700 0.838 04/25/05 13:14 54.100 0.773 53.700 0.917 04/27/05 * 88.867 0.910 88.467 1.328 04/29/05 * 136.867 0.777 136.467 0.838SW22 04/23/05 8:14 1.100 0.159 0.700 -0.206 04/23/05 9:11 2.050 0.065 1.650 -0.190 04/23/05 10:11 3.050 0.065 2.650 -0.047 04/23/05 11:17 4.150 0.073 3.750 -0.285 04/23/05 12:36 5.467 0.031 5.067 -0.174 04/23/05 14:12 7.067 0.065 6.667 0.032 04/23/05 15:53 8.750 0.063 8.350 0.379 04/23/05 18:35 11.450 0.033 11.050 0.095 04/24/05 10:26 27.300 0.088 26.900 -0.269 04/25/05 15:00 55.867 0.049 55.467 0.063 04/25/05 13:22 54.233 0.026 53.833 -0.142197 04/23/05 8:57 1.817 0.430 1.417 0.680 04/23/05 10:55 3.783 0.464 3.383 0.601 04/23/05 12:37 5.483 0.466 5.083 0.727 04/23/05 13:45 6.617 0.434 6.217 0.696




(mm/dd/yy) Time


(hr) [UR] (ppb)

Time Elapsed (hr)

[PB] (ppb)

197 04/23/05 15:53 8.750 0.475 8.350 0.743 04/23/05 18:35 11.450 0.597 11.050 1.280 04/24/05 12:13 29.083 0.491 28.683 0.901 04/25/05 11:35 52.450 0.442 52.050 1.312

* Samples collected by Jagger Hims Limited. The exact time of sample collection was not recorded.



Table E-4: Groundwater tracing results for the injection at SW28 on May 10, 2005

24.8 g of uranine was injected into the SW28 watercourse at Site SW28 at 6:00 am on May 10, 2005. The injection site is about 10 m upstream from the ephemeral pond at Site 7. At the time, all of the flow sank into the overburden beneath the pond. Water samples were collected at 14 sites. The Time Elapsed is the number of hours elapsed after the injection. [UR] is the measured fluorescence expressed as ppb uranine and this includes the background fluorescence.

Sample Collection Uranine Site Date

(mm/dd/yy) Time


(hr) [UR] (ppb)

7 * 05/12/05 8:00 50.000 0.956 05/13/05 18:45 84.750 0.92443 05/10/05 9:00 3.000 0.234 05/10/05 12:44 6.733 0.272 05/10/05 16:21 10.350 0.305 05/10/05 19:10 13.167 0.295 05/11/05 10:03 28.050 0.264 05/11/05 20:30 38.500 0.276 05/12/05 7:18 49.300 0.252 05/12/05 20:43 62.717 0.248 05/13/05 14:15 80.250 0.315 05/14/05 10:45 100.750 0.363 05/15/05 20:12 134.200 0.295 05/17/05 15:06 177.100 0.32944 05/10/05 8:50 2.833 0.107 05/10/05 12:42 6.700 0.129 05/10/05 16:18 10.300 0.137 05/10/05 19:08 13.133 0.139 05/11/05 10:00 28.000 0.149 05/11/05 20:28 38.467 0.192 05/12/05 7:15 49.250 0.165 05/12/05 20:41 62.683 0.161 05/13/05 14:11 80.183 0.153 05/14/05 10:47 100.783 0.147 05/15/05 20:16 134.267 0.107 05/17/05 15:01 177.017 0.16545 05/10/05 8:37 2.617 0.234 05/10/05 12:38 6.633 0.339 05/10/05 16:14 10.233 0.355 05/10/05 19:04 13.067 0.371 05/11/05 9:56 27.933 0.222 05/11/05 20:25 38.417 0.224 05/12/05 7:11 49.183 0.252 05/12/05 20:37 62.617 0.313 05/13/05 14:08 80.133 0.293 05/14/05 10:40 100.667 0.309




(mm/dd/yy) Time


(hr) [UR] (ppb)

45 05/15/05 20:22 134.367 0.284 05/17/05 14:56 176.933 0.351SW27B 05/10/05 15:29 9.483 0.514 05/10/05 16:49 10.817 0.648 05/10/05 19:24 13.400 0.829 05/11/05 9:15 27.250 0.787 05/11/05 20:43 38.717 0.853 05/12/05 7:32 49.533 0.815SW27C 05/10/05 15:29 9.483 0.468 05/10/05 16:49 10.817 0.571 05/10/05 19:29 13.483 0.718 05/11/05 9:15 27.250 0.708 05/11/05 20:43 38.717 0.775 05/12/05 7:32 49.533 0.710SW27D 05/10/05 15:28 9.467 0.414 05/10/05 16:49 10.817 0.512 05/10/05 19:29 13.483 0.656 05/11/05 9:15 27.250 0.674 05/11/05 20:43 38.717 0.682 05/12/05 7:32 49.533 0.690SW27A 05/10/05 15:27 9.450 0.359 05/10/05 16:47 10.783 0.422 05/10/05 19:28 13.467 0.547 05/11/05 9:23 27.383 0.565 05/11/05 20:42 38.700 0.569 05/12/05 7:30 49.500 0.521SW27E 05/10/05 15:26 9.433 0.089 05/10/05 16:46 10.767 0.073 05/10/05 19:26 13.433 0.030 05/11/05 9:25 27.417 0.081 05/11/05 20:39 38.650 0.052 05/12/05 7:25 49.417 0.059SW27F 05/10/05 15:26 9.433 0.042 05/10/05 16:46 10.767 0.085 05/10/05 19:26 13.433 0.032 05/11/05 9:26 27.433 0.091 05/11/05 20:39 38.650 0.032 05/12/05 7:25 49.417 0.097SW27G 05/10/05 15:24 9.400 0.048 05/10/05 16:45 10.750 0.052 05/10/05 19:24 13.400 0.089 05/11/05 9:26 27.433 0.107




(mm/dd/yy) Time


(hr) [UR] (ppb)

SW27G 05/11/05 20:39 38.650 0.065 05/12/05 7:25 49.417 0.06546 05/10/05 6:34 0.567 0.278 05/10/05 6:47 0.783 0.256 05/10/05 7:00 1.000 0.334 05/10/05 7:20 1.333 0.301 05/10/05 7:40 1.667 0.307 05/10/05 8:00 2.000 0.310 05/10/05 8:20 2.333 0.296 05/10/05 8:40 2.667 0.332 05/10/05 9:00 3.000 0.341 05/10/05 9:20 3.333 0.328 05/10/05 9:40 3.667 0.341 05/10/05 10:00 4.000 0.372 05/10/05 10:20 4.333 0.359 05/10/05 10:40 4.667 0.348 05/10/05 11:10 5.167 0.348 05/10/05 11:40 5.667 0.384 05/10/05 12:10 6.167 0.368 05/10/05 12:25 6.417 0.337 05/10/05 12:40 6.667 0.287 05/10/05 13:10 7.167 0.292 05/10/05 13:40 7.667 0.325 05/10/05 14:10 8.167 0.337 05/10/05 14:40 8.667 0.325 05/10/05 14:44 8.733 0.372 05/10/05 15:10 9.167 0.381 05/10/05 15:20 9.333 0.350 05/10/05 16:00 10.000 0.399 05/10/05 16:40 10.667 0.431 05/10/05 17:20 11.333 0.460 05/10/05 18:00 12.000 0.447 05/10/05 18:40 12.667 0.525 05/10/05 19:20 13.333 0.498 05/10/05 20:00 14.000 0.560 05/10/05 20:40 14.667 0.564 05/10/05 21:20 15.333 0.607 05/10/05 22:00 16.000 0.638 05/10/05 22:40 16.667 0.632 05/10/05 23:20 17.333 0.618 05/11/05 0:00 18.000 0.632 05/11/05 0:40 18.667 0.640




(mm/dd/yy) Time


(hr) [UR] (ppb)

46 05/11/05 1:20 19.333 0.597 05/11/05 2:00 20.000 0.595 05/11/05 2:40 20.667 0.600 05/11/05 3:20 21.333 0.617 05/11/05 4:00 22.000 0.645 05/11/05 4:40 22.667 0.658 05/11/05 5:20 23.333 0.645 05/11/05 6:00 24.000 0.651 05/11/05 6:40 24.667 0.628 05/11/05 10:15 28.250 0.618 05/11/05 20:22 38.367 0.625 05/12/05 7:08 49.133 0.603 05/12/05 20:33 62.550 0.558 05/13/05 14:04 80.067 0.533 05/14/05 10:37 100.617 0.469 05/15/05 20:26 134.433 0.435 05/17/05 14:52 176.867 0.404SW20 05/10/05 6:50 0.833 0.161 05/10/05 7:25 1.417 0.180 05/10/05 7:55 1.917 0.178 05/10/05 8:15 2.250 0.192 05/10/05 9:10 3.167 0.232 05/10/05 9:59 3.983 0.240 05/10/05 10:42 4.700 0.198 05/10/05 11:55 5.917 0.202 05/10/05 12:21 6.350 0.244 05/10/05 14:11 8.183 0.212 05/10/05 15:59 9.983 0.200 05/10/05 17:40 11.667 0.254 05/10/05 19:34 13.567 0.176 05/11/05 8:51 26.850 0.192 05/11/05 20:45 38.750 0.192 05/12/05 8:01 50.017 0.198 05/12/05 20:56 62.933 0.194 05/13/05 14:02 80.033 0.204 05/14/05 11:05 101.083 0.210 05/15/05 20:30 134.500 0.212 05/17/05 15:20 177.333 0.20477 05/10/05 7:17 1.283 0.089 05/10/05 7:47 1.783 0.063 05/10/05 10:53 4.883 0.067 05/10/05 14:20 8.333 0.095




(mm/dd/yy) Time


(hr) [UR] (ppb)

77 05/10/05 17:44 11.733 0.038 05/10/05 19:37 13.617 0.056 05/11/05 8:35 26.583 0.089 05/11/05 20:50 38.833 0.059 05/12/05 8:04 50.067 0.079 05/12/05 21:00 63.000 0.040 05/13/05 13:53 79.883 0.059 05/14/05 10:31 100.517 0.061 05/15/05 20:35 134.583 0.054 05/17/05 15:25 177.417 0.052

* Two samples were collected roughly in the center of the ephemeral pond located just downstream from SW28 to determine residual tracer concentrations.



Table E-5: Groundwater tracing results for injections at four wells near the SW2A spring

Injections were conducted at each of the following four wells on May 12, 2005:

Trace 1) 2.34 g of uranine was injected into BH03-9 at 14:15 hours.

Trace 2) 12.82 g of phloxine B was injected into TW04-03 at 14:51 hours.

Trace 3) 10.83 g of phloxine B was injected into TW04-01 at 17:55 hours.

Trace 4) 12.3 g of uranine was injected into TW04-02 at 18:07 hours.

After each injection the wells were flushed with 80 litres of water. All water samples were collected just downstream from the SW2A spring pool at Site 19. [UR] and [PB] are the measured fluorescence expressed as ppb uranine and ppb phloxine B and these were both corrected for the initial background fluorescence measured prior to each injection.

Sample Collection Elapsed Time after each Injection (hours) Results Date

(mm/dd/yy) Time

(hr:min) Trace 1

UR, BH03-9 Trace 2

PB, TW04-3 Trace 3

PB, TW04-1 Trace 4

UR, TW04-2 [UR] (ppb)

[PB] (ppb)

05/12/05 14:15 0.000 0.589 * 05/12/05 14:20 0.083 0.111 * 05/12/05 14:24 0.150 0.041 * 05/12/05 14:28 0.217 0.016 * 05/12/05 14:32 0.283 0.630 * 05/12/05 14:34 0.317 6.818 * 05/12/05 14:36 0.350 7.227 * 05/12/05 14:38 0.383 8.500 * 05/12/05 14:40 0.417 9.182 * 05/12/05 14:42 0.450 9.523 * 05/12/05 14:44 0.483 8.364 * 05/12/05 14:46 0.517 7.432 * 05/12/05 14:48 0.550 6.909 * 05/12/05 14:50 0.583 5.955 * 05/12/05 14:52 0.617 0.023 5.227 * 05/12/05 14:54 0.650 0.056 4.693 * 05/12/05 14:56 0.683 0.089 4.489 * 05/12/05 14:58 0.717 0.123 4.045 0.27605/12/05 15:00 0.750 0.156 3.909 1.15805/12/05 15:04 0.817 0.223 3.414 0.49605/12/05 15:06 0.850 0.256 3.105 14.33805/12/05 15:08 0.883 0.289 * 244.66905/12/05 15:10 0.917 0.323 * 1144.66905/12/05 15:12 0.950 0.356 * 1977.75705/12/05 15:14 0.983 0.389 * 2297.79405/12/05 15:16 1.017 0.423 * 1754.96305/12/05 15:18 1.050 0.456 * 1403.67605/12/05 15:20 1.083 0.489 * 1089.33805/12/05 15:25 1.167 0.573 2.480 606.61805/12/05 15:31 1.267 0.673 1.952 230.515




(mm/dd/yy) Time

(hr:min) Trace 1

UR, BH03-9 Trace 2

PB, TW04-3 Trace 3

PB, TW04-1 Trace 4


[PB] (ppb)

05/12/05 15:37 1.367 0.773 1.577 141.54405/12/05 15:43 1.467 0.873 2.084 288.05105/12/05 15:53 1.633 1.039 1.277 83.08805/12/05 16:03 1.800 1.206 0.893 42.27905/12/05 16:13 1.967 1.373 0.891 30.14705/12/05 16:23 2.133 1.539 0.830 18.78705/12/05 16:33 2.300 1.706 0.618 12.29805/12/05 16:43 2.467 1.873 0.507 10.47805/12/05 16:53 2.633 2.039 0.364 6.71005/12/05 17:03 2.800 2.206 0.386 5.57005/12/05 17:13 2.967 2.373 0.245 3.80505/12/05 17:23 3.133 2.539 0.227 4.87105/12/05 17:33 3.300 2.706 0.152 3.08805/12/05 17:43 3.467 2.873 0.305 2.50005/12/05 17:53 3.633 3.039 0.170 2.61005/12/05 18:00 3.750 3.156 0.083 0.091 1.47105/12/05 18:10 3.917 3.323 0.250 0.050 0.118 1.36005/12/05 18:30 4.250 3.656 0.583 0.383 0.080 1.34205/12/05 19:00 4.750 4.156 1.083 0.883 0.102 0.82705/12/05 20:00 5.750 5.156 2.083 1.883 0.086 2.11405/12/05 20:30 6.250 5.656 2.583 2.383 0.095 1.34205/12/05 20:40 6.417 5.823 2.750 2.550 0.125 0.77205/12/05 20:50 6.583 5.989 2.917 2.717 0.157 0.97405/12/05 21:00 6.750 6.156 3.083 2.883 0.300 1.43405/12/05 21:10 6.917 6.323 3.250 3.050 0.414 1.39705/12/05 21:20 7.083 6.489 3.417 3.217 0.550 0.99305/12/05 21:30 7.250 6.656 3.583 3.383 0.586 1.04805/12/05 21:40 7.417 6.823 3.750 3.550 0.795 0.75405/12/05 22:00 7.750 7.156 4.083 3.883 0.898 0.51505/12/05 22:20 8.083 7.489 4.417 4.217 1.173 0.11005/12/05 22:40 8.417 7.823 4.750 4.550 1.320 2.16905/12/05 23:00 8.750 8.156 5.083 4.883 1.598 1.32405/12/05 23:30 9.250 8.656 5.583 5.383 1.800 1.06605/13/05 0:00 9.750 9.156 6.083 5.883 2.291 0.84605/13/05 0:30 10.250 9.656 6.583 6.383 2.530 1.10305/13/05 1:00 10.750 10.156 7.083 6.883 2.436 1.04805/13/05 1:30 11.250 10.656 7.583 7.383 2.918 1.02905/13/05 2:00 11.750 11.156 8.083 7.883 3.189 1.47105/13/05 3:00 12.750 12.156 9.083 8.883 3.543 1.52605/13/05 3:30 13.250 12.656 9.583 9.383 3.341 1.61805/13/05 4:00 13.750 13.156 10.083 9.883 4.130 1.47105/13/05 4:30 14.250 13.656 10.583 10.383 4.127 1.14005/13/05 5:00 14.750 14.156 11.083 10.883 3.557 0.809




(mm/dd/yy) Time

(hr:min) Trace 1

UR, BH03-9 Trace 2

PB, TW04-3 Trace 3

PB, TW04-1 Trace 4


[PB] (ppb)

05/13/05 6:00 15.750 15.156 12.083 11.883 3.227 1.50705/13/05 7:00 16.750 16.156 13.083 12.883 3.614 1.21305/13/05 7:30 17.250 16.656 13.583 13.383 3.245 1.32405/13/05 8:00 17.750 17.156 14.083 13.883 3.152 4.76105/13/05 8:30 18.250 17.656 14.583 14.383 3.257 10.23905/13/05 9:00 18.750 18.156 15.083 14.883 2.823 10.82705/13/05 9:30 19.250 18.656 15.583 15.383 2.736 7.13205/13/05 10:01 19.767 19.173 16.100 15.900 3.168 1.30505/13/05 12:01 21.767 21.173 18.100 17.900 3.025 1.59905/13/05 14:00 23.750 23.156 20.083 19.883 3.155 1.89305/13/05 16:00 25.750 25.156 22.083 21.883 2.916 0.88205/13/05 18:00 27.750 27.156 24.083 23.883 2.595 0.71705/13/05 20:00 29.750 29.156 26.083 25.883 3.305 0.91905/13/05 22:00 31.750 31.156 28.083 27.883 2.741 0.69905/14/05 2:00 35.750 35.156 32.083 31.883 2.452 0.47805/14/05 6:00 39.750 39.156 36.083 35.883 2.775 1.10305/14/05 10:00 43.750 43.156 40.083 39.883 1.957 0.90105/14/05 14:10 47.917 47.323 44.250 44.050 2.030 1.69105/14/05 18:10 51.917 51.323 48.250 48.050 1.818 1.37905/15/05 2:10 59.917 59.323 56.250 56.050 2.273 1.80105/15/05 10:00 67.917 67.323 64.250 64.050 1.784 1.39705/15/05 18:10 75.917 75.323 72.250 72.050 1.784 2.05905/16/05 2:10 83.917 83.323 80.250 80.050 1.786 1.56305/16/05 10:10 91.917 91.323 88.250 88.050 1.234 1.30505/16/05 18:10 99.917 99.323 96.250 96.050 1.166 1.58105/17/05 2:10 107.917 107.323 104.250 104.050 0.982 1.08505/17/05 10:10 115.917 115.323 112.250 112.050 0.923 1.61805/17/05 16:54 122.650 122.050 118.983 118.783 0.334 0.699

* Not measured

karst investigation of the duntroon quarry expansion lands€¦ · 4.1 regional karst geomorphology...

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