Geology / Ecology Tour Guides

Al Donaldson,Dave Forsyth,

Chris Findlay & Bud Andress

Depart From: Mallorytown LandingDeparture Time: 9:00 AM

Conclusion: 4:30 PM

Field Trip Logistics Arranged ByJack Henry, Stewardship Coordinator

Chris Bellemore, Council VolunteerCliff Rogers, Council Volunteer

GRENVILLE LAND STEWARDSHIP COUNCIL

BOX LUNCH & REFRESHMENTS INCLUDED

TRANSPORTATIONSeaway Tour Boat – Captain Andy

~ ACKNOWLEDGEMENTS ~

On behalf of the Grenville Land Stewardship Council, we would like to acknowledge Al Donaldson, Chris Findlay and Dave Forsyth for the endless hours that they contributed to preparing this tour guide book. This guide illustrates the important geological and ecological history of the Thousand Islands Region and will continue to be an excellent resource for years to come.The Grenville Land Stewardship Council also gratefully acknowledges our co-sponsors, Parks Canada.

2

~ INDEX ~

A BRIEF GEOLOGICAL HISTORY OF THETHOUSAND ISLANDS REGION ………………….…….. 4

GEOLOGICAL OVERVIEW OF THE GEOTOUR ………… 9

CONCEPTS AND TERMS RELEVANT TO THIS EXCURSION ……… 11

TRIP LOG ………………………………………………… 12

GEOTOUR ITINERARY

Land Stop #1 (LS1) West Grenadier Park Dock. Up trail to stone Gazebo ………………………………………………………………. 15

Water Stop #1 (WS1) Around corner from Park dock, South East of Grenadier Island ………………………………………………. 16

WS2 Club Island ………………………………………………….. 16

WS3 Raft Narrows/Buck’s Bay ………………………….. 17

WS4 Darlingside ……………………………………………………… 17

WS5 Ash Island ……………………………………………………… 18

WS6 Mulcaster Island ……………………………………………… 18

LS2 Gordon Island …………………………………………………. 19

WS7 West of Melville (Hay) ……………………………………. 20

WS8 Southern Melville Island ……………………………… 21

REFERENCES ……………………………………………... 22

GEOLOGY / ECOLOGY TOUR MINI SURVEY ……… 23

3

4

A Brief Geological History of the Thousand Islands RegionIntroduction

The Thousand Islands occur where the St. Lawrence River crosses the Frontenac Axis, a topographic high on the Precambrian basement that links the Algonquin dome of Eastern Ontario to the Adirondack dome in New York State. Participants on Grenville Stewardship Council Geotours 2008 and 2009 will recall that the Precambrian landscapes of this region were formed is a result of the collision of ancient proto-continents over a billion years ago to form the supercontinent “Rodinia”.

The subsequent breakup of Rodinia and cycles of erosion and deposition of younger sedimentary rocks on the Precambrian surface produced the Paleozoic sandstones, limestones and dolostones on the eastern flank of the Frontenac Axis and on the Axis itself visited in Geotours 2008 and 2009. The great Wisconsin Ice Sheets (10.000 to 20,000 years before present) created the present distinctive glacial landforms that are in this region extensively mantled clay and silt deposits left by the Champlain Sea some 9,000 years ago.

During the Geotour 2010 “transect” of the Frontenac Axis, we will see evidence of the above processes in the rock types and tectonic and erosional features as they appear on the Islands in the St Lawrence River. Along the way, we will learn about some of the historical, cultural and ecological features that have contributed to the recognition of this special part of Ontario and New York. A recognition that led to, amongst other things, the establishment of Canada’s first National Park east of the Rockies in 1904 – St. Lawrence Islands National Park – as well as the more recent (2003) UNESCO – designated Frontenac Arch Biosphere Reserve.

The Precambrian Record (1 – 1.1 billion years ago)Although the story of the craton or core of North America – to become Laurentia –began some 2 billion years ago, the geological story of the Thousand Islands region part could begin at the plate tectonic merging of all the Earth’s landmasses to form the supercontinent Rodinia about 1100 million years ago. Though its exact size and configuration are only roughly known, it appears that Laurentia (brown core of North America) formed the heart of this super-continent with the east coast of North America adjacent to western South America and the west coast of North America next to Australia and Antarctica.

5

A consensus view of reconstructions based on Paleomagnetic and geology data begins at 1100 Ma.

Laurentia lay not far from the Equator at that time. Between about 1.2 and 1 billion years ago it appears that a series of continental masses moved northwest, crushing the southeast margin of Laurentia like a giant vice. Older Precambrian sedimentary and volcanic rocks that had been deposited in shallow seas bordering Laurentia became caught up in this geological vice, were crumpled and forced deep into the earth’s crust, deformed by heat and pressure, invaded by granitic and related plutonic rocks and finally, thrown up above the sea to form a major mountain chain, probably not unlike the modern-day Himalayas. The Grenville Province was born. Over the next half-billion years the forces of erosion (wind, water, ice) planed down this Laurentian Mountain Belt to form a Precambrian surface with relatively gentle relief, variously estimated at between 30 and 100 metres and probably looking not much different than the landscape today ( Ambrose, 1964; Wynne-Edwards, 1967; Douglas, 1970; Johnson et. al., 1992).

The rocks forming the roots of this ancient mountain chain, called the Grenville Series or Grenville Supergroup, are exposed along a southwest-trending belt that stretches from the present day coast of Labrador through Quebec and Ontario and then disappears under younger rocks of central U.S.A They are a complex of sedimentary, volcanic and igneous rocks that have been converted by heat and pressure to a sequence of metamorphic rocks that include various gneisses (e.g. granitic gneiss, quartz-biotite-feldspar gneiss), migmatites (layered gneisses that have been invaded by narrow granitic bands parallel to the layering), quartzite and crystalline limestone. The part of the Grenville Supergroup that underlies the Thousand Island region is called the Central Metasedimentary Belt or CMB. As the name suggests, it is a belt of metamorphosed sediments representing a series of crustal fragments (now“Terranes” or Domains”) thrust to the northwest as the belt grew over time. Geotour

2010 is across the Frontenac Terrane. The characteristic structural fabric of the CMB strikes northeast and dips southeast. We will see examples of Frontenac Terrane rocks and theirdeformation on the islands (e.g. ductile folding, migmatite, granite gneiss).

6

Between about 800 million and 1 billion years ago, the rocks of the CMB were invaded by granite plutons and related igneous rocks. One example of this period of activity is the ubiquitous pink granite known as the Rockport granite. Examples are common in the Thousand Islands region. Three major episodes of continental glaciation took place towards the end of the Precambrian (Cryogenian Period, 850 to 630 million years ago; see http://www.palaeos.org/Cryogenian). Recent evidence suggests that at least one of these episodes may have resulted in almost complete coverage of the planet (oceans included) by a thick sheet of ice, leading to the designation “Snowball Earth” for this stage in Earth history. Evidence from all continents records an earlier, pre-Grenville glacial episode (~2.2 billion years ago) that also may have approached, the “Snowball Earth” stage. For more on the Snowball Earth hypothesis you might check out:

• http://www.palaeos.com/Proterozoic/Neoproterozoic/Cryogenian/Cryogenian.html• http://www.snowballearth.org/against.html

While all of the above was in progress, the Thousand Island area was punctuated by extensional episodes giving rise to two sets of narrow igneous bodies or dykes – thenorthwest trending “Kingston” swarm at 1160 Ma and the northeast tending “Rideau”swarm at about 575 Ma. We hope to see examples of the Rideau swarm exposed atDarlingside or at Ash Island. The Kingston swarm is exposed on the Admiralty Islands to the southwest.

The Frontenac Axis /ArchAs the geology map shows, the knobs and valleys of the Axis reflect the underlying

northeast geological structural tends and define the special nature of the Thousand Islands region. These basement structural trends extend continuously from southwest of Lake Ontario to western Quebec. Across this basement structure the northwest trending Frontenac Axis or Arch is a basement topographic high but is not currently defined by geological or tectonic structures. Debate continues as to whether and how thick subsequent sediment cover existed over the Axis and may have formed an “Arch”.

7

The origin and geological history of the Axis / Arch is sketchy but the changes inCambrian and Early Ordovician sandstones and limestones across the high show that the high influenced sedimentation in the period from about 520 to 460 Ma. On the other hand there is evidence that some of the older rocks in this sequence (e.g. Nepean sandstone) may have originally extended across the Arch. There are small lake basins along the interior of the Arch in which these older strata have been found although they do not appear on the surrounding Precambrian surface, apparently having been stripped off by erosion (Wynne-Edwards, 1962; 1967).

The question of whether the Frontenac Axis / Arch represents an actual arching ofthe Precambrian basement is problematic. It has been suggested by Wynne-Edwards(1962) that the Kingston dyke swarm along the crest of the Axis may have beenemplaced along tension fissures caused by upwarping of the basement. On the otherhand, unweighting of the land as the great ice-sheets retreated northwards may haveresulted in a much more recent uplift. The Axis also played a role in controlling theextent of post-glacial seas. Whatever the actual mechanism of origin of the Arch, it seems evident that over much of its lifetime it served as a bridge above sea-level and then, as now, played an important role in defining the landscape. The Precambrian metamorphic rocks of the CMB have been sculpted by time, erosion and ice to form the landscape of the present-day Thousand Islands.

The Paleozoic Record (450-550 million years ago)Following the formation of the Laurentian Mountain belt, 500 million years

passed before the geological record resumes. During this period the forces of erosionreduced the mountains to near sea level, setting the stage for the next major event in the geological history of the region. At the beginning of the Paleozoic (“dawn of life”) Era, much of the southern margin of Laurentia was flooded by seas that flowed into basins on either side of the Frontenac Axis. East of the Axis, the Ottawa-St Lawrence Lowland (Wilson, 1946) is underlain mainly by sandstone, limestone and dolomite (magnesium limestone) ranging in age from mid-Cambrian (520 million years) to late Ordovician (450 million years). To the west, similar but not exactly identical rocks were deposited, lapping on the flanks of the Arch north of the present-day Kingston area.

In the eastern Islands, these sedimentary rocks are present at only a few places,but on Gordon Island just east of Gananoque Narrows there are good exposures of astriking quartz pebble conglomerate along the west shores of the island. Acid test hereindicates a carbonate cement. At the south end of Gordon, the sandstone at the waterline shows no carbonate cement. According to the geological map (Wynne-Edwards 1962) this unit is part of an isolated outlier of Nepean (Potsdam) sandstone of Cambrian age that extends from Gordon Island to Melville and Huckleberry islands about 5 km to the west. Normally, sandstone and sandy dolomite of the March Formation overlie the Nepean sandstones but it has been noted that a pebble

8

conglomerate may be present where March formation strata rest directly on the Precambrain basement without the intervening Nepean Formation (e.g. Johnson et al, 1992). It is possible then that the Gordon Island conglomerate may be of March Formation age. Another possibility may be that the March/Nepean unconformity lies on Gordon Island. Other authors (e.g. Greggs and Gorman, 1976; Wynne-Edwards, 1962) have noted the presence of March Formation strata at (rare) localities on the west side of the Arch which suggests that at least up to about 450 million years ago the Arch may have been a “leaky” barrier to sedimentation across its axis.

The Quaternary Record (1.6 million years to present)Following the Paleozoic, the geological record for the next 400 million years or so is

sparse. A number of episodes of sea incursions took place but any record ofsedimentation has been erased by erosion. It is not until the Quaternary Period that the trail picks up again during Pleistocene (Late Quaternary) glaciation. The great ice-sheets of the Pleistocene Ice Age lay several kilometres thick over eastern Canada 20,000 years ago. Between about17,000 years and14,000 years B.P.(Before Present) theice began to meltback to the north. Byabout 12,500 yearsB.P. a large glaciallake known as LakeIroquois had formedto the west of theFrontenac Arch, an Early version of the later, smaller Lake Ontario. A few hundred years later, ice in southern Quebec had melted back to allow seawater of the Champlain Sea to flood most of the area of the present Gulf of St. Lawrence, the Ottawa and St. Lawrence river valleys, and the present Lake Champlain. During this time marine clays and silts were deposited in the Champlain Sea on top of sediments (till, sand, gravel, clay) laid down earlier by glacial meltwaters. At about the same time fresh water clays were deposited in glacial lakes formed along the front of the retreating ice sheets. The result was a complex mixture of fresh water and marine clays and silts that require lab studies of cores to distinguish.

9

Glacial deposits blanket the landscape east and west of the Frontenac Axis (e.g. Owen, 1951) but over the Axis itself the southwest direction of movement is evident in the distinct roche moutonnée profiles of many islands. The north sides rise gently fromshoals while the south, down-ice sides are steep and form steep, irregular shorelines due to the ice freezing to the bedrock and dislodging or plucking blocks along joints. By about 6,000 years B.P. the present configuration of the Great Lakes and the St. Lawrence and Ottawa rivers had been established (Prest, 1970). The spectacular landscape of the Thousand Islands had arrived.

GEOLOGICAL OVERVIEW OF THE GEOTOURThis trip has been designed to provide an overview of the impressive geodiversity

within Grenville and Leeds Counties, and to demonstrate earth-science principles tothose with little or no previous geological training. The varied landscapes within thisregion are dictated by the three basic components of the underlying geology notedabove (Geological History) that were formed during parts of three Eras (latePrecambrian, early Paleozoic and late Cenozoic). The oldest component, an extensionof the Canadian Shield that is exposed mainly within the Frontenac Axis and alongparts of the St. Lawrence River shoreline and offshore islands, comprises Precambrianrocks of the Canadian Shield. This complex of ancient rocks belongs to the GrenvilleStructural Province, which extends southward to link with the Adirondacks of NewYork State (Fig. 1). These rocks comprise metamorphic and intrusive igneous rocks ofthe Precambrian Grenville Series, more than one billion years old.

The second component includes all of the overlying unmetamorphosed andpredominantly flat-lying sedimentary rocks (sandstone, limestone and dolostone beds,shale and minor conglomerate) that range in age from 400 to 500 million years.These strata were deposited during Cambrian and Ordovician time (the twolowermost Periods of the Paleozoic Era).

The third component includes the unconsolidated cover deposits lying on thePrecambrian and Paleozoic bedrock. Glacial till, an unsorted mix of particles rangingfrom clay through sand and gravel to giant boulders, was deposited during theWisconsin advance of a continental blanket of ice, up to 3 km thick, during thePleistocene Ice Age (late Cenozoic).

Although some Wisconsin glacial deposits in eastern Ontario (the latest of fourmajor episodes of Pleistocene glaciation) are no more than 17,000 years old, the oldestadvance, as recorded in several places elsewhere in North America, began almost 2million years ago. How many similar events have reduced the surface of the land inthis region since the Paleozoic sedimentary strata were deposited and lithified is notknown. During the melting of the last ice sheet, vast volumes of sand and gravel weredeposited as outwash in front of the retreating ice. Melt-back of the ice also allowedthe Atlantic Ocean to invade low areas, creating the Champlain Sea within whichthick accumulations of clay, silt and sand were deposited 13,000 to 9,000 years ago.

10

Fig. 1 Regional Map of theFrontenac Axis adapted from the Atlas of Canada (http://atlas.nrcan.gc.ca). Along the Frontenac Axis rocks represent geological Eras from the Cenozoic –present ~ 65M (Pleistoceneglacial and later Holocene deposits), Paleozoic 250 to 540 Ma (Cambrian to Ordovician) sandstones andoverlying carbonates(dolostones and limestones) and Neoproterozoic or timebefore ~ 540 Ma (the crystalline basement). Mesozoic age (65 to ~ 250 Ma) rocks in the form of Jurassic dykes occur in Prince Edward County.

Fig. 2 Route map for Geology / Ecology Tour, Sunday, October 17, 2010.

We will visit 8 sites that collectively illustrate the major geological components of the region (Fig. 2): igneous Grenville rocks of the Precambrian Shield; unmetamorphosed basal Paleozoic quartz sandstone and overlying beds of limestone and dolostone; and unconsolidated Late Cenozoic deposits of Pleistocene glacial till, sand and gravel that in most places blanket the older consolidated rocks. At each stop we will discuss the rock types present, stressing significant geological features (such as contact relationships between different rock types, primary sedimentary structures, and the trace fossils) that serve to reveal many details about geological history.

11

CONCEPTS AND TERMS RELEVANT TO THIS EXCURSION

Geological time scaleActualism, Steno’s principlesAge relationships, truncationsUnconformityCrystalline texture of igneous and metamorphic rocksClastic texture of sedimentary rocksMassive, crystalline, sparryMinerals: feldspar, quartz, mica, amphibole, pyroxene, calcite,

dolomite, clay minerals, sulphides, iron oxidesStructure, joint, fault, fold, fold axis, anticline, synclineFoliation, lineation, gneissosity, schistosity, cleavage, En echelon fracturesGneiss, schist, amphibolite, marble, basalt, dioriteIntrusions: plutonic rock, dyke, vein, pegmatite, aplite, xenolithExtrusions: lava, volcanic rock, ash, tephraAlteration, reaction rimsMechanical weathering, chemical weathering, regolith, paleosolClastic sediments, chemical sediments, recrystallized sedimentsBlock, boulder, cobble, pebble, sand, silt, clayRoundness, sphericityPrimary structure, secondary structureStrata, stratigraphy, depositional environmentLithification, cement, matrixBedding, lamination, crossbedding, angle of reposeRipple mark (symmetric, asymmetric), interference ripple markDesiccation crack, syneresis structureRip-up clast, intraclastStyloliteDewatering structure, fluid-escape structureSolution-cavity, geopetal structureFossil, microfossilTrace fossil, biogenic structure, bioturbationBiofilm, stromatolite, thromboliteSolution cavity, evaporite castContinental glaciation, deglaciationGlacial striation, chatter markHydraulic scouring, potholeGlacial till, glacial erratic, outwash, roche moutonnée, drumlin, moraineLeda clay, varve

12

TRIP LOGThroughout our trip today, we will make a marine transect of Frontenac Terrane,

the southernmost crustal addition to the Frontenac Axis (Fig.1). Like the St. Lawrence itself, we will be sailing approximately along strike or nearly parallel to the structural trends of the geology.

From the start, our cruise passes many rocky islands and shoals that show the power oferosive action by the of glaciers ice that is inferred to have attained a thickness of several kilometres as it moved across the region.

Fig. 2. Roche moutonnée glacial form.

Fig. 1Geotour 2010

13

For thousands of years the continental ice sheet relentlessly scoured, grooved and polished the bedrock, locally marking the rock surfaces with distinct parallel striae that provide direct evidence of the sense of ice movement over the bedrock. In addition, the southwest direction of movement is locally recorded by distinct roche moutonnée profiles, well illustrated in some islands and shoals, where the up-ice profile is gently curved, and the down-ice profile is blocky to irregular, due to the tendency of the ice to freeze to the bedrock, dislodge blocks along orthogonal joints, and pluck the bocks away in the down-ice (south) direction (Fig. 7).Shoreline exposures of bedrock provide excellent views of the principal rock types within the Frontenac Axis, and bring home the relationship between the continuous rocky upper surface of the lithosphere and the unconsolidated overburden that was deposited during the last Ice Age in patches over the low parts of the bedrock. The overburden comprises glacial till scoured from the bedrock during glaciation, sand and gravel outwash deposited by rivers, and silt and clay that settled into the Champlain Sea that inundated this region during the waning stages of glaciation (Fig. 6).

Fig. 3. Champlain Sea ~9000 years ago. This arm of the Atlantic Ocean wasformed by the melting of the continental ice sheet, before significant rebound of thecrust that had been depressed beneath the glacial ice for thousands of years.

The most abundant rocks within the Frontenac Axis are foliated (layered) metamorphic rocks, deformed in a ductile state (Fig. 2) and massive (unlayered and uniformly textured) plutonic rocks (Fig. 3) that were intruded (injected as hot liquid magmas) into the older gneissic structure.

14

Fig. 4. Foliated (layered) granite gneiss, slightly folded while ductile, south Grenadier Is.

Fig. 5. Granitic texture: Potassium feldspar (pink), quartz (glassy) and amphiboles (black)

Radiometric dating of the rocks has yielded precise ages for several successive intrusive events, thus confirming the validity of the relative age relationships established by successive cross-cutting relationships (Fig. 6.), and providing additional direct evidence of the long geologic history that created the underpinnings for this lithospheric component of our planet

15

Fig. 6. Aplite (lightpink) dykes cross cut

already deformedgranite (grey)

On Grenadier Island, the gazebo shelter foundation wall (Fig. 7) shows blocks of felsic (light coloured, rich in iron-poor minerals such as feldspar) and mafic (dark coloured due to iron-rich minerals) igneous and metamorphic rocks, some cut by granitic dykes with shiny black tourmaline.

Fig. 7. Gazebo wall on Grenadier Island

16

Just south of Grenadier Island, the end of Tar Island features a Rideau swarm diabase emplaced in granite turned white from being “baked” by the intrusion (Fig. 8). The exposure suggests the intrusive body dips gently to the north along the shoreline. The sub-horizontal form of the body may indicate an irregularly shaped semi-horizontal intrusive body or “sill” structure.

Fig. 8. Tar Island, diabase dyke (blk) intrudes (baked) granitic host rock.

The sudden cooling of the diabase induced stresses to form brittle fractures – a featureexploited by the landowner who has easily picked the black blocks to construct animpressive seriesof walls.

On the northshore of ClubIsland, a newfront lawnexhibits quartziteand foliatedgranite intrudedby dykes ofyounger granitepegmatite(coarse-grainedtexture) andaplite (finegrainedtexture).

Fig. 9. ClubIsland quartziteand graniticcomplex.

17

East of statue of St. Lawrence at Raft Narrows/Buck’s Bay, the granite gneiss is cut by aplitic (fine-grained) dykes of pink granite. View looking northward. Note that the dykes cut across the foliation that dips gently to the west (left).

Fig. 10. Raft Narrows/Buck’s Bay, Aplite dykes (pink) cutting gneiss

Behind the historic post office complex at Darlingside on north shore of St. LawrenceRiver, a large mafic dyke of the 575 Ma Rideau swarm intrudes granite. The browncoloration on joint surfaces is due to weathering of iron-rich minerals in the maficdyke.

At the south end of Ash Island, another of the Rideau swarm dykes intruded into massive to slightly foliated pink granite (high rounded part of outcrop, right side Fig. 12) at the west

Fig. 11. Darlingside, Rideau swarm dyke in granite.

18

end of Ash Island. In turn, the mafic dyke has been later intruded by small irregular dykes of younger pink granite. Prominent joints within the mafic dyke are both parallel and normal to the contacts.

Fig. 12. Ash Island mafic dykes intruded by pink granitic dykes.

Passing the south side of Mulcaster Island, steeply dipping foliation in migmatiticgneiss is cut by irregular dykes of pink granite (Fig. 13).

During the most westerly part of our cruise, some of the sedimentary cover rocks (Figure 14) that overlie the Precambrian basement (general term for older

Fig. 13. Mulcaster Island, irregular pink dykes intrude deformed gneiss.

rocks of the Canadian Shield) are exposed. Although the actual contact between the Shield and the cover rocks is not directly exposed along our route, the contact is exposed on land both north and south of the River.

On Gordon Island (Fig. 14), Paleozoic conglomerate is overlain by sandstone at Parks Canada dock. The multi-tonne Grenville-age boulder (erratic) to the right of the ramp was probably plucked from the Frontenac Axis to the northeast, and dropped from an iceberg calved from the tidewater front of the continental ice sheet at the time when this area was inundated by the Champlain Sea.

19

Fig.14. Erratic, eroded conglomerate layer beneath sandstone, Gordon Is.

The cobble conglomerate exhibitsangular to sub-angular quartziteclasts (nearby source), the cobblesare fractured along joints and thecement is contains calcite andweathers recessively – the cobblesare harder and stand out from thesand matrix (Fig. 15). All thesefeatures are not common toconglomerate layers in the Nepean sandstone onshore. Theconglomerate may be part of The Early Ordovician Theresa(previously March) formation.

Fig.15. Cobble conglomerate,Gordon Island.

20

A thicker section of sandstone beds is found in a block along southern Melville Island (Fig 16). The exposed face displays crossbedding at several levels within the concave-up beds that may be the foreset beds within a large subaqueous dune. The lower image details conglomerate beds, crossbedding and an eroded section of a dewatering cylinder.

Fig.16. Sandstoneblock withconglomerate andcross beds; de-watering cylinder at right edge of block.

~ THE END ~

Thank you for joining us!

21

References

Ambrose, J.W. 1964. Exhumed paleoplains of the Precambrian Shield of NorthAmerica. Am. J. Sci. vol 262, pp 817 – 857.

Douglas, R.J.W. 1970. (Sci. ed.) Geology and Economic Minerals of Canada. Geol.Surv. Can. Economic Geology Report No. 1, 838 p.

Greggs, R.D. and W.A. Gorman. 1976. Geology of the Thousand Islands. ParksCanada. Island Insights No. 2, 53 p.

Ian W. D. Dalziel, Sharon Mosher, and Lisa M. Gahagan. 2000. Laurentia KalahariCollision and the Assembly of Rodinia. The Journal of Geology. 108, Issue 5, pp 499–513.

Johnson, M.D., Armstrong, D.K., Sanford,B.V., Telford, P.G. and M.A. Rutka. 1992.Paleozoic and Mesozoic Geology of Ontario. Chapter 20 in Geology of Ontario, (eds.)P.C. Thurston, H.R. Williams, R.H. Sutcliffe and G.M. Scott. Ont. Geol. Surv. SpecialVolume 4, Part 2, pp 907 – 1008.

Owen, E.B. 1951. Pleistocene and Recent Deposits of the Cornwall – Cardinal Area,Stormont, Dundas and Grenville Counties, Ontario. Geol. Surv. Can. Paper 51-12., 24 p.

Poster: Glacial History of Lake Ontario – Miller Museum, Queens University atKingston.

Prest, V.K. 1970. Quaternary Geology; Chapter XII in Geology and Economic Mineralsof Canada. (Sci. ed.) R.J.W. Douglas. Geol. Surv. Can. Economic Geology Report No. 1,pp 675 – 764.

Wilson, Alice E. 1964 (reprinted 1970) Geology of the Ottawa – St. Lawrence Lowland, Ontario and Quebec. Geol. Surv. Can. Memoir 241, 66 p.

Wynne-Edwards, H.R. 1962. Geology Gananoque Ontario. Geol. Surv. Can. Map 27-1962. 1”=1mi.

1963. Geology, Brockville - Mallorytown Area Ontario. Geol.Surv. Can. Map 7 – 1963. 1”=1 mi.

1967. Westport Map – Area, Ontario, with Special Emphasison the Precambrain Rocks. Geo. Surv. Can. Memoir 346. 142 p.

22

~ GEOTOUR MINI SURVEY ~

• Were the Tour Boat, PA System, and facilities to your satisfaction?

• Were you satisfied with the Tour Guides? Were they able to answer all your questions?

• Did you find the Tour "too long" or "too short", "rushed" or "slow" to be able to take in all the information?

• Was the Tour content more or less information than you had anticipated it would be?

• Did you find the Tour, Lunch and Refreshments were of good value for what was offered?

• Should the Tour be available again next year in another County, would you be interested in attending or recommending the Tour to friends and family?

• If the Tour was available at the same price or slightly more, and it was “Bring Your Own Lunch”, how likely would you have participated?

• What impressed you the most about the Tour (from registration to disembarking)?

• What suggestions would you recommend to improve the Tour?

• On a scale of 1 to 10 (1 = Low, 10 = High), how would you rate the Tour overall?

• Additional Comments: (use reverse if required)

Thank you for completing our survey. Your comments are certainly appreciated and it will help us make our

Tour better next year!