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hrust belt ens. wy. ciation of Late Quaternary deglaciation of the southwestern 1. '*logy Utah and St. Lawrence Lowland, and versity of I

DONALD L. PAIR Department of Geology, Univemiv of Dayton, Dayton, Ohio 45469-2364 CYRIL G. RODRIGUES Department of Geology, University of Windsor, Wdor,Ontario, Canada N9B 3P4

ABSTRACT treat from the St. Lawrence Lowland and SE'ITING surrounding regions (compare Karrow, The style of deglaciation and maximum ex- 1981; Clark and Karrow, 1984; Pair and The western St. Lawrence Lowland i: tent of earliest proglacial lakes have been re- others, 1988a; Gadd, 1980, 1981, 1987, bounded to the south by the northwesten constructed for the southwestern St. Lawrence 1988a, 1988b; Sharpe, 1988; Naldrett, , the lower Black Lowiand of New York and Ontario using ice- 1990, 1991; Rodrigues, 1991, 1992). Mod- River Valley, the promontory of the Tug Hi1 marginal sediments and landforms, strandline els for the area (Prest, 1970; Gadd, 1980) Plateau, and the adjacent Low feattuw, and the areal distribution ofCh&m differ substantially in (1) the duration of ice land (Fig. 1). Relief in the south rises from 7t subbiangrhlz-bearingrhythmites. An impor- cover in the Lowland, (2) mechanisms of m on the flat-lying Paleozoic sedimentaq tant recessional position, the Carthage-Harris- ice retreat, and (3) the sequence of lacus- rocks of the Lake Ontario plain to more thar ville ice border, fronted Iro- trine and marine (Champlain Sea) levels. 579 m on the upper Tug Hill Plateau anc quois in the eastern Lake Ontario Basin. These questions persist primarily because northwestern Adirondack slope. Subsequent ice retreat, probably earlier than of the absence of a detailed account of ice The northern boundary of the western 12,500 yr B.P., allowed Lake Iroquois to ex- retreat from the Adirondack Mountains Lowland is marked by the Madawaska High- pand along the northwestern flank of the Ad- and adjacent Lowlands. In addition, stud- lands in Ontario. The Frontenac Axis bridge5 irondackMountainsandintotheSt.Lawrence ies of the late-glacial water bodies have the south and north sides of the western Lowland. Contrasting styles of deglaciation, been hampered by discontinuous strand- St. Lawrence Lowland. It consists of low- controlled primarily by water depth, resulted line data, and a lack of objective indicators relief, northeast-southwest-trending, ridge- in a land-based ice margin which withdrew of lacustrine and marine conditions which and-valley topography resulting from differ- gradually off the northern slope of the Adiron- are independent of sedimentological inter- ential erosion of the Precambrian bedrock. dack Mountains, whiie the ice margin in the pretations. The timing of deglaciation and The rest of the Lowland is underlain by flat- western St. Lawrence Lowland retreated rap- the succession of water levels in the Low- lying sedimentary rocks. idly in the deep waters of Lake Iroquois. , land is of particular importance in view of The maximum extent of ice retreat during the recent emphasis on late Quaternary PREVIOUS STUDIES the early phases of Lake Iroquois has been es- events along the eastern margin of the timated on the basis of the distribution of the (Ruddiman and Fairchild (1907, 1919), Taylor (1924), and ostracode Cizdom subCriangulata in Lake Iro- Wright, 1987), and the proposed route and Coleman (1937) first discussed the spatial and quois and younger sediments in New York, timing of proglacial lake drainage to the temporal relationships between deglaciation, and by northward projl@ons of Iroquois North via the St. Lawrence proglacial water bodies, and the Champlain shoreline elevations to the region bounded by Lowland (Teller, 1988, 1990; Lewis and Sea in the western St. Lawrence Lowland. the Madawaska Highlands (Ontario). Results Anderson, 1989; Broecker and others, More recent work began with regional stud- indicate that the southwestern St. Lawrence 1989). ies by Stewart (1958), Muynech (1962), and Lowland was rapidly deglaciated during the The purpose of this paper is to evaluate MacClintock and Stewart (1%5) in the Lake highest phases of Lake Iroquois. The distlliu- the proposed models for the deglaciation Ontario Basin and St. Lawrence Lowland. tion and radiocarbon chronology of fossilifer- of the St. Lawrence Lowland. We present Subsequent research has resulted in the

cial lakes occupied the Lowland well before the posed fossiliferous lacustrine and marine land. The proglacial lake model of Prest Champlain Sea incursion. sediments in the southwestern St. (1970) depicted an ice front that retreated Lawrence Lowland. This information is from south to north, a style described as INTRODUCTION used to trace the retreat of the ice margin "windowblind" deglaciation by Gadd (1981, and associated expansion of proglacial p. 1393). In this model, ice retreat was ac- A great deal of controversy remains re- lakes from the Lake Ontario Basin into the companied by a series of proglacial lakes that garding the timing and style of glacial re- St. Lawrence Lowland. flooded the St. Lawrence Lowland. Subse-

Data Repository item 9321 contains additional material related to this article.

%logical Society of America Bulletin, v. 105, p. 1151-1164,9 figs., September 1993.

1151 PAIR AND RODRIGUES I

Figurr 1. Map of the southwestern St. Lawrence Lowland. Shaded area is below 200 m. north sedin quent incursion by the Champlain Sea was at Covey Hill was responsible for the degla- Pair and others, 1988b; Pair and Rod- New believed to have followed the last of these cia1 events, and concluded that "the 'win- rigues, 1989; Gurrieri and Musiker, 1990). Lacustrine water bodies (Henderson, 1967, dowblind' style of ice-marginal retreat re- These studies, however, did not address 1973; Denny, 1974; Kirkland and Coates, mains the most attractive and realistic the nature and timing of initial ice retreat 1977). interpretation of deglaciation for the St. out of the Ontario Basin. Gadd (1980, 1987, 1988a) proposed an al- Lawrence Lowland" (Clark and Karrow, Investigation of the age, origin, and depo- Se ternate hypothesis based on the mathemati- 1984, p. 813). Anderson and Lewis (1985) and sitional environments of the water bodies ginal =ally derived calving-bay model of Thomas Muller and Prest (1985) supported the con- considered in this study have been ap- tion ( '1977), which suggested that a calving-bay cept of progressive ice retreat during glacial proached through examination and radiocar- land .nigrated up the St. Lawrence Valley into the lake stages followed by the marine incursion. bon dating of the biota present in the glacio- differ lpper St. Lawrence and Valleys, al- Several studies along the southern mar- lacustrine and marine sediments. Anderson viron owing marine waters to encroach, while an gin of the former lacustrine and marine ba- and others (1985), and Anderson (1987,1988) and ce dam retained proglacial lakes in the Lake sins outlined the sequence and nature of proposed ages for events based on pollen Chee 3ntario Basin. Karrow (1981) pointed out the the regional water levels and discussed ice- zones. Rodrigues (1987,1988,1992) reported bidg€ )hysical difficultiesin maintaining such an ice marginal positions marking retreat from ages on invertebrate marine fossil assem- 19881 lam. Based on reconstructed lake levels in the flank of the Adirondack Mountains and blages and reconstructed the paleoenviron- (1 988 he region around Covey Hill, Clark and Kar- St. Lawrence Lowland (Clark and Street, ments of the glaciolacustrine and marine wa- Tine ow (1984) proposed that an active ice margin 1985; Clark and Davis, 1988; Street, 1988; ter bodies. Valle

Geological Society of America Bulletin, September 1993 QUATERNARY DEGLACIATION, ST. LAWRENCE UlWLAND

cation of ice-marginal landforms through the western St. Lawrence Lowland. At tional sedimentologicstudy of recessional posits and analyses of elevations of drain thresholds, shoreline features, and rebor history have been reported elsewhere (I and others, 1988a, 1988b; Pair, 1991) and not discussed in this paper. Glacial features found in upland areas c sist of moraineesker complexes, associa outwash plains, and a series of welldefir ice-marginal channels (Denny, 1974; C1 and Street, 1985; Clark and Davis, 1988; F and others, 1988b; Street, 1988; Gunieri ; Musiker, 1990, Cadwell and Pair, 1991). 7 distribution of landforms and sediments ifi cates that the margins of northward-retrt ing lobes constructed with ice* tact slopes and deposited extensive outwi sediment on valley floors (Fig. 2A). I posures in ice-marginal landforms reveal p dominantly stratified icecontact and g ciofluvial sediments. Landform-sedimc associationsindicate a grounded, subaerial locally ponded ice margin, similar to ice-m ginal settings outlined by Gustawn a Boothroyd (1987) for Malaspina Glaci Alaska. Unlike the uplands, where ice-marginal c posits are restricted to bedrock valleys, , cessional sediments in the Lowland are d tributed mamly along broad bands align with bedrock highs and scarps (Cadwell a. Pair, 1991). Borrow pits expose sedimer exhibiting consistent proximal to distal faci changes hm cobble and boulder uni through largely ripple-drift sand, to laminat silt-clay sequences (Pair, 1991). These ha been mapped as subaqueous fans (Cadw Figure 2. (A) Landforms and sediments associated with a land-based ice margin along the and Pair, 1991) and were built along the i northwest flank of the Adirondack Mountains near Harrisville, New York. (B)Landforms and margin in proglacial lakes associated with i sediments associated with an ice margin terminating in near Rural Hill, retreat from the western St. Lawrence Lo. land (Fig. 2B). This ice-marginal setting consistent with other subaqueous depositic models described for the St. Lawrence Lo\ land (see Rust, 1988). These fan systems m, have been fed by subglacial meltwaters f Sedimentological analyses of ice-mar- ICE-MARGINAL AND LAKE-BASIN cused into bedrock valleys up-ice from be ginal sediments associated with deglacia- DEPOSITS rock scarps (Pair and Muller, 1990). E. ' tion of portions of the St. Lawrence Low- Henderson (1%7) and P. J. Henderson (198 land and yield significantly Recessional Deposits also suggested bedrock control of subglacl - different interpretations of depositional en- discharge near Kingston, Ontario. The dig vironments and late glacial events (Rust Interpretations of ice-marginal deposi- ment of ice-marginal materials in the westei and Romanelli, 1975; Rust, 1977, 1988; tional environments and water depths are St. Lawrence Lowland with bedrock higl Cheel and Rust, 1982; Naldrett, 1988; Bur- based on detailed surficial mapping (scale of and scarps may indicate that they acted i bidge and Rust, 1988; Sharpe, 1988; Gadd, 1:24,000) completed in association with the temporary pinning points along a retreatin, 1988b; Pair and others, 1988b). Gadd New York State Geological Survey's Sur- floating or at least buoyant, ice margin. She (1988b) continued to attribute a glacioma- ficial Geology Mapping Program-Adi- low water depths at bedrock highs woul rine origin to rhythmites in the Ottawa rondack Sheet (Cadwell and Pair, 1991). This have decreased iceeking rates and allowe regional mapping program permitted identifi- sediment to accumulate preferentially dow

Geological Society of America Bulletin, September 1993 115 PAIR AND RODRIGUES

75"

clude c The UP1 a shell 1 3. Iroquois and younger shorelines on the Ogdensburg map sheet (scale 1:250,000). Strandline numbers correspond to those listed in continut pendiv A. is conf blocky, this unit capped from bedrock highs. Crossen (1991) noted Sediments exposed along riverbanks near laminae. Clay inclusions are present in the silt ,irnilar relationship between subaqueous Ogdensburg, New York, and northwest of laminae of some of the couplets. WATElF msits and bedrock ridges studied in Canton, New York (Fig. 1) consist of diamic- Rhmtes overlying those of the lowest line. ton, rhythmites, and overlymg massive mud meter display micro-laminated silt beds, Form typical of the stratigraphy found at other lo- sharp contacts between silt and clay, and uni- from st] ythmites and Massive Silt and Clay cations in the St. Lawrence Lowland (Rod- form clay-bed thicknesses. Dropstones and ing crit rigues, 1992). Both sites are below the highest sediment clasts are rare. In places the beds ability): 3posures of rhythmically laminated silt marine shoreline in the region, and maximum are tilted, perhaps due to the slumping of the shorebll 1 clay underlain by till or ice-marginal ma- marine water depths exceeded 30 m. sediment as competent blocks. The upper channel ~alsare common in the western St. The lowest unit exposed at both sites is a rhythmites thin progressively to less than Shorelir wrence Lowland (Pair, 1991; Rodrigues, massive, stony diamictonwith striated clasts. 1-cm-thick laminae at their upper contact and ana 12). Deposition of these fine-grained sedi- Disconformably overiyng the diamicton are with the overlymg unit. Pair (19 nts occurred either in the deeper areas of silt and clay couplets consisting of altemat- The thin, uppermost couplets of the rhyth- Strandli lake basin or as part of the distal portions ing, finely laminated, green and gray silt/clay mites grade conformably into sediment re- Were prc ice-marginal subaqueous fans. Sharp con- couplets which are up to 2.5 cm thick at the ferred to here as the "transitional unit." It tain eql ts between silt and clay laminae and the base of the unit. In the lowest meter of the consists of -.5 m of thick, faintly laminated and 0th seneof trace fossils along some bedding rhythmites, silt laminae are graded, and lack clays with prominent, discontinuous silt nes suggest an annual cycle (that is, distinct boundaries between couplets. Drop beds, rare massive clay beds, and several L stones are common, and unlitMed sediment well-defined silt/clay couplets. Several of the 'GSA . ves), but deposition by sporadic under- data ~pp NS cannot be ruled out as a formative clasts that fell through the water column, per- contacts between the massive clays and silt/ Uments S, chanism for some of the rhythmites. haps as frozen debris, are embedded in silt clay couplets are distinctly erosional and in- co 80301

14 Geological Society of America Bulletin, September 1993 a QUATERNARY DEGLACIATION, ST. LAWRENCE LOWLAND

400 Shoreline data from Sites 83 Frontenac North of Lake Ontario Bellevlle X Iroquois - Watertown Phase A Trenton and Lake Glenfield Iroquois - Main Phase 300

-E IROQUOIS - WATERTOWN PHASE zz- P 5 200 y W

100

0 150 100 DISTANCE (km)

Fi4. Strandline diagram for Iroquois and younger water levels from Covey Hill, , to Rome, New York.

clude clay rip-up clasts in the silt laminae. these profiles permits direct evaluation of high-level strandlines on the north shore of The upper contact at both sites is defined by shoreline data from both the southern and Lake Ontario (Appendix A). These shore- a shell bed lying directly above the last dis- northern margins of the former water bod- lines are found on the high ground on the continuous silt stringer. The transitional unit ies and is the basis for recognition of six north shore of Lake Ontario and may corre- is conformably overlain by fossiliferous, distinct water levels (Fig. 4). The gradients late with the Watertown phase (A, B, C, and blocky, massive gray clay. The upper part of of the Iroquois and post-Iroquois Fronte- D in Figs. 4,5). this unit has thin red and gray laminae and is nac water planes increase exponentially to capped by faintly laminated silt. the northeast, but shorter segments used in Main Lake haquois Phase this study are essentially linear. I WATER LEVELS The shoreline of the Main Lake Iroquois Watertown Phase of Lake Iroquois phase (gradient 0.9 rnlkm), the next lowest Former water levels were reconstructed water plane on the strandline diagram from strandline evidence using the follow- The highest water plane identified on the (Fig. 4), is marked by a series of deltas and ing criteria (in order of decreasing reli- strandline diagram is related to an early level beaches (Figs. 3, 4) extending from the ability): glaciolacustrine deltas; beaches, of Lake Iroquois in the Ontario Basin re- Covey Hill region to the Ontario Basin (Clark shorebluffs, or terraces; drainage cols or ferred to here as the "Watertown phase." It and Karrow, 1984, Pair, 1986; this study). channels; and subaqueous sand plains. is identified from shoreline features that can The Main Lake Iroquois shoreline can be Shoreline characteristics, isobase trends, be traced from Watertown southward along traced south of the study area and is approx- and analysis methods were described by the eastern Lake Ontario shoreline toward imately parallel to the present shoreline of Pair (1986) and Pair and others (1988a). the Rome region (Figs. 3,4). Correlative with Lake Ontario. Muller and Prest (1985) re- th- Strandline data (Fig. 3 and Appendix A') this phase are strandlines northeast of Wa- ported strandlines and projected lake-level re- were projected onto curved profiles to ob- tertown and in the lowermost portion of the elevations extending as far north as Cloyne, It tain equidistant diagrams (compare Pair Black River Valley that are equivalent to the Ontario. The shore features they reported fall ed and others, 1988a). The orientation of lowest levels of Lake Glenfield (Strandlines generally on the Main Lake Iroquois water silt 3-5 in Fig. 3). The Watertown phase repre- plane reconstructed from strandlines on the ral sents an early stabilized level of Lake Iro- southern margin of the Lowland. Shore fea- 'GSA Data Reposito~yitem 9321, strandline- .he data ~~~~~di~,is on request from D~~- The gradient of this water plane is tures on the north shore of Lake Ontario may ,ild uments Secretary, GSA, P.O. Box 9140, Boulder, -1.1 m/km. Coleman (1937), mech also be correlative with the Main Lake Iro- in- (1962), and Sly and Prior (1984) identified quois level.

Geological Society of America Bulletin, September wes Figure 5. Shorelines, isobase trends, occurrences of C&M subbiangrrlata assemblages in the study area, and occurrences of marine fossils on war* the Ogdensburg map sheet (scale 1:250,000). Shorelines dashed where insufficient data prevent exact location from being indicated. Regional isobase F trends from Muller and Prest (1985), Pair (1986), and Parent and Occhietti (1988). Curved profiles for strandline diagram (Fig. 4) were dram the perpendicular to isobases. meIi ern i Lak 1991 1 Post-Iroquois Phases ing to the Frontenac level at Flinton, On- DEGLACIATION, PALEOGEOGRAPHY, "Ca tario (F1 in Figs. 4,5), which also appears AND DEPOSITIONAL ENVIRONMENTS an ir Shorelines from the southern margin of to correspond to the Frontenac level. the I the Lowland related to the post-Iroquois Pair (1986) and Pair and others (1988a) dis- Ice-Marginal History and Lake Iroquois into Frontenac level plot as a distinct lowerwa- cussed post-Iroquois (Belleville and Trenton) w ter plane (gradient 0.9 &) below the levels. The next lower water level in the St. We have identified a number of former ice Posir Main Lake Iroquois level (Figs. 3, 4). The Lawrence Lowland, the highest marine borders in the Adirondack Mountains and Wate northern margin of the Frontenac water shoreline, falls below the Belleville and Tren- adjacent St. Lawrence Lowlands from ice- body is represented by terraces and beach ton levels in Figure 4. There are no interme- marginal materials, landforms, and channels featu gravels at elevations well below the Main diate shoreline features between the Trenton (Fig. 6). Recession of the ice margin to the Harr Lake Iroquois strandlines (Figs. 3, 4). water plane and the highest marine shoreline base of the Tug Hill Scarp opened spillways gin ir Henderson (1967) identified a delta belong- (Fig. 4). for glacial Lake Glenfield in the Black River outvv

Geological Society of America Bulletin, September 1993 QUATERNARY DEGLACIATION, ST. LAWRENCE LOWLAND FIGURE 5 LEGEND Basin was ice free (compare Fairchild 17 I 1919; Dyke and Prest, 1987). I ) Fossil Sites Shorelines- North Shore Lake Ontario The next prominent recessional posi tions are represented by the ~eferiet-~ortl 1 - BREWERTON A - OAK LAKE Wilna and Philadelphia-Antwerp : 2 - CAUGHDENOY B - OAK LAKE (Fig. 6B). The proximity of these moraines tc 3 - WESTWOOD CORNERS C - PANCAKE HlLL bedrock highs (Cadwell and Pair, 1991) sug 4 - SPRAGUEVILLE D - PANCAKE HlLL gests that they were constructed when tht 5 - GOUVERNEUR E- CLOYNE 6 - CLAYTON F - NORTH BROOK retreating ice margin was temporarily stabi 7 -ALEXANDRIA BAY G - COOPER lized. Northward retreat of the ice margin tc 8 -BLACK LAKE H - MADOC these positions allowed Lake Iroquois to ex 9 - MORRISTOWN I- ROUND LAKE pand into the St. Lawrence Lowland anc 10 -SPARROWHAWK POINT J - OAK LAKE along the northwest flank of the Adirondack 11 -BUCKS BRIDGE K - OAK LAKE Mountains. Water depth in front of these ice 12 -LAMBS POND CORE L- BRIGHTON margins was at least 91 m. I 13 - MERRICKVILLE M - OAK LAKE Deglaciation of the western St. Lawrence 14 -TWIN ELM N - OAK LAKE 15 - BRAZEAU PIT 0 - PRESQUILE Lowland continued until the ice margin be- 1 16 -FOSTER SAND PIT F1 - FLINTON came stabilized again by a bedrock scarp at 17 - MER BLEUE BORE HOLE Ba, - MADOC LaFargeville (Fig. 6C). Deposition at the ice 1 18 - BEARBROOK margin built subaqueous fans in about 90 m of Ba, HAZZARDS CORNERS , 19 - CASSELMAN BORE HOLE - water. A beach associated with the Belleville , 20 - CASSELMAN water plane is developed on the crest of these features at 136 m (Fig. 6C), indicating that ice A Candona subtriangulata Above Highest Marine Shoreline had retreated from the southwestern St. Lawrence Lowland before the post-Iroquois Belleville and Trenton phases. Candona subtriangulata (Not overlain by marine sediments) The Role of the Rome Outlet Below Hiahest Marine Shoreline I Candona subtriangulata The relationship of the outlet at Rome 111 1 (Overlain by Marine Sediments) (Figs. 1, 5) to the levels of Lake Iroquois is poorly understood. The elevation of the sill, Marine Fossils [only sites on Ogdensburg map sheet (1:250,000) are shown] wmmonly quoted as being at 140 m, has not been re-examined since it was first proposed by early workers. Fullerton (1980) ques- Valley. The location of these spillways pro- Glenfield level in the Black River Valley tioned the role of the Rome Outlet in control- vides a means of identlfylng the position of (Cadwell and Pair, 1991). Along the Carthage ling Lake Iroquois water levels. He inferred the ice margin along the northwest Adiron- portion of the ice border, the glacial lake in that the threshold may not have been at dack flank and northern scarp of the Tug Hill. front of the ice margin was 40m deep. The Rome, but east down the Iromohawk River Water carried by these spillways drained ice margin was grounded, and hummocky to- (in the Mohawk River Valley) at the bedrock west along or under the ice margin into north- pography dominates the landscape. Ice-mar- sill near Little Fak (as first suggested by wardencroaching Lake Iroquois (Fig. 6A). ginal sediments associated with the western- Brigham, 1898). The sill at Little Falls may Following retreat from the Tug Hill scarp, most edge of the Carthage-Harrisville ice have controlled initial water levels and down- the ice margin stabiied and deposited sedi- border were deposited in the deeper waters of cutting of the Rome outlet. The present ele- ments that can be traced from the northwest- northeastwardencroaching Lake Iroquois. vation of the Little Falls sill is estimated here ern flank of the Adirondack Mountains to the The western edge of the ice border was in to be about 155 m. The position of this sill on Lake Ontario Lowland (Cadwell and Pair, water about 90 to 120 m deep, and deposition the equidistant diagram (Fig. 4) and the wn- 1991). This position, referred to as the along the margin was in the form of subaq- vergence of the water levels suggest that it "Carthage-Harrisville ice border," provides ueous fans built into Lake Iroquois (Figs. 2B, indeed may have influenced Iroquois water

Geological Society of America Bulletin, September 1993 1157 Geological Society of America Bulletin, September 1993

- -.. I QUATERNARY DEGLACIATION, ST. LAWRENCE LOWLAND Foraminifers Ostracodes levels, representing significant drops in re- gional water levels controlled by outlets in the lower Champlain Valley of New York. The 20-m difference in elevation, and parallel trend of the Belleville and Trenton water planes (both -.9 mAun) (Fig. 4), indicate that these levels were close in time. The absence of intermediate shoreline features between the Trenton water plane and the highest ma- rine shoreline (Fig. 4) indicates that the drop to sea level was rapid. Pair and others (1988a) showed that the highest shoreline of the Champlain Sea on the southern shore of the basin exceeded the elevation of the Lake On- tario threshold and was, therefore, confluent with Early Lake Ontario. Sediments at the Sparrowhawk Point and Bucks Bridge sites (nos. 10 and 11; Figs. 5,7, and 8) illustrate the succession of water bod- ies and depositional environments. Rhyth- C 10-25 mites overlying the glacial diamicton were deposited in a glacial lake preceding the ma- rine transgression. Graded transitions from silt to clay beds indicate surgedeposit origin for some of the couplets. These graded beds are particularly common at the base of the unit and at the upper contact with the over- lying marine sediments. The majority of the rhythmites, however, display sharp contacts between silt and clay beds and consistent clay thicknesses. The number of couplets (-60) present at both sections may provide an es- timate of the duration of the last lake level in this area preceding the Champlain Sea. The alternating massive and laminated fine-grained sediment which overlies the rhythmites represents the transition from la- custrine to marine conditions. The change @ Massive silt and clay v Present from thin couplets to clays with irregular @ITransitional intelval <8% banding is probably related to mixing of ma- @Rhythmically laminated silt and clay o 400 tests or valves per rine and fresh water during the early stages of 100 g of sediment @stony diamicton (Fort Covington Till] the marine transgression. Sporadic under- flows may account for the occasional siWclay Figure 7. Stratigraphyand invertebrate fossils at Sparrowhawk Point Site (no. 10 in Fig. 5). couplets at the base of the transitional zone. As marine conditions developed, suspension and fiocculation dominated sedimentation, Barnett (1986, oral commun.) north of Ma- Main Lake Iroquois persisted until drain- resulting in deposition of the overlying mas- sive clays. Underflows in the marine envi- ronment require sigmficant fluctuations in the Adirondack phase are well developed on the southern meltwater output and sediment load to main- descriied by Clark and Karrow (1984), margin of the former lake basin (Fig. 5). The tain density stratification, conditions that are 1986), Pair and others (1988a), and this water plane of the Frontenac phase falls at usually associated with an ice-proximal set- .These data were plotted on the strand- least 6 m below the elevation given for the ting (Mackiewicz and others, 1984; Domack, maximum area Rome Outlet (140 m) (Fig. 4). 1984; Stevens, 1985, 1986). The absence of glaciomarine deposits at these sites (Figs. 7, rn edge of the St. Lawrence Lowland. Bekville, Trenton Phases, and the 8) indicates that the marine sediments were reconstructions indicate that the north- Champlain Sea deposited some distance from the retreating ice margin. The few rhythmically laminated beds intercalatedwith massive marine clay of the transitional zone may be related to surge PAIR AND RODRIGUES

from <1% in Ecozone B to between 1% and 25% in Ecowne C. Anderson and others (1985), Naldrett (1988), and Rodrigues (1984, 1987, 1988, 1W) also reported the succession from rh~~laminated silt and clay to Cham- plain Sea sediments in the Ottawa Valley north of the St. Lawrence River (sites 14-19, Fig. 5). They concluded that the Candona subaiangzhta assemblages in the rmtes are evidence for a proglacial lake extending from Lake Ontario into the Ottawa Valley preceding the Champlain Sea. Gadd (1987, 1988a, 1988b) and Sharpe (1988), however, (Fresh water) proposed that the rhythmites in the Ottawa Valley were deposited in a glaciomarine environment. C&na subtriangukzta lives in the at depths ranging from 8 to 363 m and in temperatures ranging from 2.6 to 19.2 "C, and can tolerate high turbidity @elorme, 1970,1978,1989; Westgate and others, 1987). The species has been reported from Holo- @ Massive silt and clay v Present cene lacustrine deposits in @Transitional interval <8% (Colman and others, 1990), and from late @Rhythmically laminated silt and clay o 400tests or valves per glaciolacustrine deposits in the 100 g of sediment @Stony diamicton (Fort Covington Till) Metro-Toronto region of southern Ontario (Westgate and others, 1987). The presence of 8. Stn-phy and invertebrate fossils at Bucks Bridge Site (no. 11 in Fig. 5). Candona subtriangulata in rhythmites above 1 the Frontenac level, south of the eastern end of the Lake Ontario Basin (sites 1 and 2; Fig. 5), and between the Frontenac and deposits triggered by episodic slumping or above the highest shoreline of the Champlain younger Belleville levels east of the Lake On- debris flows. The drop to sea level was a min- Sea, whereas sites 6-9 are below. tario Basin (sites 3-5) shows that the rhyth- imum of 18 to 37 m and may well have initi- The rhythrmcally laminated silt and clay to mites overlain by marine sediments and char- ated such mass movements in the basin. Mas- massive clay successions at the Spar- acterized by Candona subtriangulata at sites sive silt and clay in the upper parts of the two rowhawk Point and Bucks Bridge sites in the western St. Lawrence Lowland (sites sections (Figs. 7, 8) represent establishment (nos. 10 and 11; Fig. 5) are divided into three 10, 11, 14-19) were deposited in a glaciola- of marine conditions in the study area. ewzones on the basis of ostracode and fo- custrine environment. Rodrigues (1988) wn- raminiferal assemblages (Figs. 7 and 8). cluded that Candona subtriangukzta mi- DISTRIBUTION AND SIGNIFICANCE OF Monospecific Candona subtriangulata as- grated from the Lake Ontario Basin into the INVERTEBRATE FOSSILS semblages are present in ewzone A. The Ottawa Valley before the marine transgres- foraminifer E@idium excavahun clavata We sampled exposures of rhythmically and Candona subtriangulata characterize laminated and massive silt and clay for fo- Ecozone B. Ecozone C is characterized by raminiferal and ostracode analyses to inter- EIphiakm excavahrm clavata-dominant pret paleoenvironmental conditions during assemblages. Figure 9. Possible configuration of the ice deposition of the fine-grained sediments. The The Candona subtriangulata assemblages margin during deglaciation of the southd- results reported here are part of a regional of Ecozone A at Sparrowhawk Point and ern St. Lawrence Lowland. Ice-margin psi- study (Rodrigues, 1992) based on a total of Bucks Bridge are identical to those from tion, in part, after Dyke and Prest (1987). h 166 samples from 10 sites within both the rhythmically laminated silt and clay at sites rows indicate discharge routes of glacial lakes. western and central St. Lawrence Lowland. 1-9 (Fig. 5). The rhythmites at sites 1-5 Occurrences of CMdom sub- assem- Ice-marginal deposits or diamicton are over- (Fig. 5) were deposited in glacial lakes asso- blages indicated by solid circles, square, and lain by rhythmically laminated silt and clay at ciated with the Iroquois and Frontenac lev- triim&s. (A) Carthage-Hamsville ice border sites 1-9 (Fig. 5). Trace fossils were observed els, and those of Ecozone A at Sparrowhawk and Watertown Phase of Lake Iroquois. (B) along parting planes in the rhythmtes at some Point and Bucks Bridge (sites 10 and 11) are LaFargeville ice border and Main Phase of sites. Monospecific ostracode assemblages related to the Belleville and Trenton levels. Lake Iroquois. (C) Frontenac and Fort Ann Lake pb.(D) Lake St. Lamence. (E)Higb' 6 consisting of 125 valves of Candona subhi- Ecozone B at sites 10 and 11 represents a '* angulata per 100 g of sediment are present in transition from glaciolacustrine to marine est level of the Champlain Sea and Early the fine-grained sediments. Sites 1-5 are conditions. Bottom-water salinity ranged Ontario.

1160 Geological Society of America Bulletin, September 1993

I PAIR AND RODRIGUES sion. The presence of monospcitic Candona outlets, while the eastern Lake Ontario and tent of water bodies in the region (Fig. 9). 199; subtriangulata assemblages in rhythmites southwestern St. Lawrence Lowlands were Ice-margin positions in Ontario are based on Law above the highest Champlain Sea shoreline in rapidly evacuated of ice by calving retreat in the distribution of pre-Champlain Sea glaci- cia1 New York and the succession from C. sub- the deep waters of Lake Iroquois. olacustrine deposits summarized by Rod- than triangulata-bearing rhythmites to marine rigues (1992). The configuration of -the i& bodj sediments in New York and Ontario confirm Chronology of Deglaciation and Water lobe in the Lake Ontario Basin is adapted imw the migration route proposed by Rodrigues Bodies from Dyke and Prest (1987). Pending detailed cedi. (1988). glaciological reconstructions which are be- from, Basal organic material from the bottom of yond the scope of this study, the actual ge ing < a kettle lake adjacent to the Carthage-Hams- ometry of this lobe must be considered rine ville ice border (Fig. 6A) yielded a radiocar- speculative. (1W. Ice-Marginal Controls on Deglacial History bon age of 12,500 + 140 yr B.P. (GSC-4370) The Watertown phase of Lake Iroquois Lakc and provides a minimum age for deglaciation corresponded to the Carthage-Harrisville ice oritj I The results of our study suggest that water of the northwestern Adirondack flank and border in New York and to a position north of GI depths along the retreating ice margin in the subsequent incursion by Lake Iroquois (Pair high-level strandlines on thk Lake Ontario plain / St. Lawrence Lowland controlled the mode and others, 1988b). We correlate the Car- shoreline in Ontario. Such a position may assel of ice-marginal deposition. Previous ice-mar- thage-Harrisville ice border with the Star correspond to the Dummer Moraine in On- the 2 ginal correlations (for example, Taylor, lW, Lake moraine to the east, where a radiocar- tario as indicated by Dyke and Prest (1987), Char MacClintock and Stewart, 1965) were based bon age of 12,640 + 430 yr B.P. (GX-13278) or if this feature is subglacial in origin as sug- wate on morphologic evidence between "mo- was obtained from organic material in the gested by Shulrneister (1989) and Shaw and into raines" in the Lowlands and those on the bottom of another in the others (1991), this region of till and hum- lath 1 northwestern slop of the Adirondack Moun- south of the Star Lake Moraine (Clark and mocky topography (Barnett and others, 1991) (his ( 1 tains. These correlations imply time-equiva- Davis, 1988). may be unrelated to the ice border. The pa- Karr. 1 lency between moraine segments, without The age of the lacustrine-marine transition leogeography of Watertown phase, however, Mulk 1 recognition that the ice margin may have re- indicates that considerable time separated the indicates that a sigmficant portion of the Lake (1% sponded differently along various portions of northeastward expansion of Lake Iroquois Ontario Basin was ice free (Fig. 9A). Lake the ice border. Our model for the region is into the western St. Lawrence Lowland and The ice margin then retreated to La- Thou I based on the distribution and characteristics incursion of the Champlain Sea. Pollen anal- Fargeville, where it stabilized at a bedrock 1988~ of ice-marginal sediments, and estimated wa- yses of a core at Mer Bleue near Ottawa, On- high (Fig. 9B). Ice-marginal sediments were em ( ter depths in front of the ice margin. Thus, the tario, and of sediment at Sparrowhawk Point deposited in a series of subaqueous fans into wate: causes of ice-marginal stabilization may have (sites 17 and 10, Fig. 5) identified the rise in Main Lake Iroquois in about 90 m of water. and 1 differed between the uplands of the Adiron- Picea across the contact between the lacus- If calving rates at the ice margin were high, of m dack Mountains and the St. Lawrence trine and marine sediments (Anderson, 1987, the remaining ice in the Lake Ontario Basin New Lowland. 1988). This same rise in Picea was dated at may have been removed very quickly. Cor- We propose that the land-based margin of 11,200 k 190 yr B.P. (GSC-3429) at Boyd relation of the best available shoreline data SUM the ice sheet retreated slowly by backwasting Pond, New York. Thus, Anderson (1987, from the area north of Lake Ontario with the off the Adirondack slope with ice-marginal 1988) concluded that marine waters arrived in Main Lake Iroquois strandline along the In + sediments accumulating during climatically the western part of the basin between about northwest ~dirondackflank has established the s and/or topographically controlled stillstands. 11,000 to 11,500 yr B.P. Rodrigues (1992) the maximum extent of lacustrine water bod- New At the same time, the ice sheet retreated rap- used radiocarbon ages to determine the ar- ies on the northern edge of the St. Lawrence of de idly out of the Lake Ontario Basin by actively rival of the salt-water wedge in the central St. Lowland. Results of this reconstruction show Glaci calving in the deep water of Glacial Lake Iro- Lawrence Lowland and placed the beginning that the northern margin of Lake Iroquois Lowl. quois. Consequently, the retreat of the ice of the Champlain Sea between 11,400 and may have reached the edge of the Mada- lakes margin in the Lowland would have paused 11,600 yr B.P. Both of these estimates are waska Highlands at elevations as high as 300 The d only when calving rates slowed in the shallow consistent with the sequence of water levels m while drainage continued through the Iro- custri water near bedrock highs. and estimates on the age of the conlluence mohawk River system east of Rome, New used Discussions of regional ice-border geome- between the westernmost Champlain Sea in York. Ex, try and deglacial history (for example, Clark the St. Lawrence Lowland and Early Lake Ice retreat uncovered a lower outlet on deten and Karrow, 1984, Gadd, 1988a) for this re- Ontario in the Ontario Basin by Anderson Covey Hill, and Main Lake Iroquois drainage deglac gion should consider these different controls. and Lewis (1985). was through the Covey Hill gap and into a Lawn The concept of "windowblind ice retreat," Fort Ann level in the Champlain Valley em TI with straight ice margins extending for great Mqjor Ice Borders and Paleogeography of (Fig. 9C). Deep water in front of the retreat- dack ! distances, should be re-evaluated using the Water Bodies ing ice margin may have resulted in rapid re- allawc details of ice retreat reconstructed from stud- treat and a relatively straight ice margin. Ex- north ies in the southwestern St. Lawrence Low- Ice-marginal features and shorelines in pansion of Lake Iroquois from the Lake into tl land. We suggest that a topographically con- New York (Cadwell and Pair, 1991), and lo- Ontario Basin allowed the migration of Can- Ward trolled and slowly retreating land-based ice cations of Candona subtriangulata in the dona subtriangulata into the western St. quois, margin pinned against the northern slope of western and central St. Lawrence Lowland Lawrence Lowland (Figs. 5, 9A, 9B). The enced the Adirondack Mountains at Covey Hill re- (Rodrigues, 1992) were used to reconstruct presence of this ostracode in the lacustrine An tained high water levels by blocking lower former ice borders and the sequence and ex- sediments throughout the region (Rodrig~es, Carth

1162 Geological Society of America Bulletin, September 1993 QUATERNARY DEGLACIATION, ST. LAWRENCE LOWLAND

1992) indicates that water bodies in the St. identified. The western margin of this ice bor- versity, New York State Geological Sur Lawrence Lowland were extensions of gla- der terminated in Glacial Lake Iroquois, and Honorarium Program, and the Universit). cial lakes in the Lake Ontario Basin rather subsequent recession, perhaps as early as Dayton Research Institute. Support of I than discontinuous, locally ponded, water 12,500 yr B.P., allowed Lake Iroquois to ex- work through the New York State Geolog! bodies as stated by Gadd (1988a). The max- pand along the northwestern flank of the Survey's Surficial Mapping Program, un imum northern extent of the glacial lake pre- Adirondack Mountains and into the St. the direction of D. H. Cadwell, is gratefi ceding the Champlain Sea was determined Lawrence Lowland. Contrasting styles of acknowledged. Support to Rodrigues c from the distribution of rhythmites contain- deglaciation, controlled primarily by water provided by an operating grant from the r\ ing Candona subtriangulata overlain by ma- depth at the ice margin, resulted in a land- ural Sciences and Engineering Resea rine sediments (Figs. 5 and 9D). Rodrigues based ice margin pinned against the northern Council of Canada. (1992) pointed out that the name "Glacial slope of the Adirondack Mountains, which Lake St. Lawrence" (Upham, 1895) has pri- maintained high-water levels of Lake Iro- REFERENCES CITED ority over other names. quois while Covey Hill was covered by ice. Anderson, T. W., 1981. Tenstrial environments and age ot Glacial lakes were followed by the Cham- Simultaneously, an actively calving ice front Champlain Sea based on pollen stratigraphy of the 0t1 ton north of Valley-Lake Ontario region, in Fulton, R. I., ed., Quater ke Ontario plain Sea (Fig. 9E). The absence of marine in the deep waters of Lake Iroquois was rap- geology of the Ottawa region, Ontario and Quebec: Gel ical Survey of Canada Paper 86-23, p. 31-42. Isition may assemblages in the extreme western part of idly evacuating the western St. Lawrence Anderson, T. W., 1988, Late Quaternary @en stratigraphy o tine in On- the area (Figs. 5 and 9E) submerged by the Lowland of ice. Ottawa Valley-Lake Ontario region and its application in ing the Champlain Sea, in Gadd, N. R., ed., The late ( rest (1987), Champlain Sea is probably related to fresh- The early deglaciation of the southwestern ternary development of the Champlain Sea Basin: Geolo, Assdlation of Canada Special Paper 35, p. 20-zl.1. igin as sug- water outflow from the Lake Ontario Basin St. Lawrence Lowland has been supported Anderson, T. W., and Lewis, C.F.M., 1%. Postglacial water-I into the western Champlain Sea. Such a re- by field evidence, including shoreline fea- histoq of the Lake Ontario Basin, in Kamnv, P. F., Shaw and Calkin, P. E.. eds., Quaternary evolution of the Gnat La lationship was described by Fairchild (1907) tures and lacustrine sediments characterized Geological Association of Canada Special Paper and hum- p. 231-253. hers, 1991) (his Gilbert Gulf) and discussed by Clark and by the ostracode Candorm subtriangulata, Anderson, T. W., Mott, R. I., and Delorme, L. D., I%, Evidc Karrow (1984), Anderson and Lewis (1985), which indicates the maximum extent of pre- for a prc-Champlain Sea glacial lake phase in Ottawa Va I :r. The pa- Ontario, and its implications: Current Research, Part A, Muller and Prest (1985), and Pair and others Champlain Sea lakes (Rodrigues, 1992). Doc- ological Survey of Canada Paper &1A, p. 239-245. ,however, Barnett, P. J., Cowan, W. R., and Henry, A. P., 1991, Quater 3f the Lake (1988a). Drainage of fresh water from Early umentation of the maximum extent of the geology of Ontario, southern sheet: Ontario Geolog~cal vey, Map 2556, scale 1:1,000,000. 'A). Lake Ontario through a narrow strait at the highest lakes in the Lowland and the distri- Brigham, A. P., 1898, T-aphy and glacial deposits of the Thousand Islands (Fig. 9E) (Pair and others, bution of the fossiliferous sediments relating hawk Valley: Geological Society of America Bulletin, \ XI to La- p. 183-210. a bedrock 1988a) diluted marine water in the southwest- to the lower post-Iroquois levels were used to Bruecker, W. S., Kemek J. P., Flower, B. P., Teller, J. T., Tr bore, S., Bonani, G., and WoUli, W., 1989, Routing of n lents were em Champlain Sea. The presence of fresh reconstruct the paleogeography of proglacial water from the Lawentide Ice Sheet during the Your water to the west of the Sparrowhawk Point lakes that occupied the St. Lawrence Low- Dryas mld episak: Nature, v. 341, p. 31&321. IS fans into Buddiion. A. F.. 1934. Geolw and mineral rmunxs of 1 and Bucks Bridge sites prevented migration land prior to the Champlain Sea incursion. %ammond, ~ntw&p,and mequadrangles: New \r of water. State Museum Bulletin 2%, 255 p. were high, of marine organisms beyond Ogdensburg, Models requiring contemporaneous lacus- Burbidge, G. H., and Rust, B. R., 1988, A Champlain Sea suh New York. trine and marine events in the western St. fan at St. Lazare, Quebec, in Gadd, N. R., ed., The late C rario Basin ternary dmlopnent of the aumplah Sea Basin:GeoIq Lawrence Lowland are considered improba- Association of Canada Special Paper 35. p. 47-62. ckly. Cor- Cadwell, D. H.,and Pair, D. L., 1991, Surfidalgedogic mapof I' reline data SUMMARY ble in light of the ove~whelmingevidence for Yo*: Adirondack sheet: Albany, New York State Muse, Gcdogic Sutny Map and M Series No. 40,l sheet, s< io with the extensive pre-Champlain Sea glacial lakes. 1:250,000. In this paper, we have used new data from Low-salinity assemblages from the Spar- Cheel, R. I., and Rust, B. R., 1982, Coarsc grained fades of gl along the Omarme deposits near Ottawa, Canada, in Davidson-Am stablished the southwestern St. Lawrence Lowland of rowhawk Point and Bucks Bridge sections R.. Nicklip& W., and Fahey, B: D., &., Rcscarch ingla, glaci,ohd, and glaaohmne systems: Norwich, < water bod- New York and Ontario to determine the style and the absence of marine fossils west of Og- napcut, Gexhoks. p. 279-295. of deglaciation, timing of the expansion of densburg establish that fresh-water outflow Gnne, N. E.. 1979, Gladal Lake kaqu& in central New Yg Lawrence Northeastern Geobgy: v. 1, p. 6%105. xion show Glacial Lake Iroquois into the St. Lawrence from Early Lake Ontario resulted in very low Clark, P., 1980, Late Quaternary histoty of the Malonc area, P York p.Sc. thesis]: Waterloo, Ontario, Univmity of ' 3 Iroquois Lowland, and the extent of the proglacial salinities in the southwestern Champlain Sea terloo. 188 p. lakes preceding the marine transgression. basin. Clark, P., and Karrow, P. F., 1984, Late Pleistocene water bo~ he Mada- in the St. Lawrence Md,New Yo& and regional I The distniution of shoreline features and la- relatiom: Geological Society of America Bulletin, v. tigh as 300 p. -813. $I the Iro- custrine and marine faunal assemblages were ACKNOWLEDGMENTS Clark, P. U., and Davis, P. T., 1988, Degladal duadogv of dwestern Adinnulack Mountaim Gcdogical Wen )me, New used to delimit these water bodies. America Abstrads with Pmgram, v. 20, p. 12. Extremes in bedrock relief appear to have The authors thank E. A. Romanowicx and Clark, P. U., and Street, J. S., 1985, Deglaciation of the northu Adkmiack Mountains and mrthward emoadumnt of L determined the character and orientation of T. A. Payne for assistance with field work. Iroquois: Geological Sodety of America Abstracts with I grams, v. 17. p. 11. deglacial ice borders in the southwestern St. Helpful discussions and unpublished infor- Coleman, A. P., 1937. Lake Iroquois OntarioDcpartment of MI Lawrence Lowland. Ice retreat off the north- mation were provided by T. W. Anderson, 45th Annual Report. pt. 2.. p. 1-36. Colman. S. M.. Jones. G. A.. Fomtm. R. M.. and Foster. D. ern Tug W scarp, the northwestern Adiron- P. J. Barnett, P. U. Clark, and J. S. Street. 1990, ~dmn;palmclimatic &dena'and sedhncnta! rates from a core in southwestem Lakc Michigan: Journa dack slope, and out of the Black River Valley Comments by E. H. Muller and H. T. Mul- Paleoihn~,v. 4, p. 269-284. allowed Glacial Lake Iroquois to expand lins, and thorough reviews by P. U. Clark, aosseRKJ.. 1991.S~mnholddepositionbyPkistocc tidewater , Gulf of Maim, in Andemon, J. B., northeastward from the Lake Ontario Basin P. J. Fleisher, D. R. Sharpe, and an anony- Ashley, G. M., cds., Glacial marine xdimcntation; Paleo matic sidcaar: GeoloeicalWetv of America Seal into the St. Lawrence Lowland. With north- mous reviewer led to significant improve- per 261:~. 127-135. - ward encroachment of Glacial Lake Iro- ments in this manuscript. Funding to the first Delome, L. D., 1970, Freshwater araamdes of Canada. Part 8 Family Candonidae: Canadii Joumal of Zodogy, v. quois, ice-border morphology was also influ- author was provided by grants from the Ge- o.larnl27. Dclonhe, L. D., 1978. DistributionoffrcJhwatcrostracodesinL enced by deep water at the ice margin. ological Society of America, Senate Re- Erie: Journal of Gmt lhResearch, v. 4, p. 216-220. An important recessional position, the search Committee of Syacuse University, Delomx, L. D., 1989, MethDds in Ouaternarv ccdonv 7-Fre water ose;acodes: Gascience b. 16, p~&?-90. Carthage-Hanisville ice border has been the Department of Geology of Syracuse Uni- Dcmy, C. S., 1974, Pleistocene gedogy of the nonheast Adirc

Geological Society of America Bulletin, September 1993

- PAIR AND RODRIGUES

dack region, New Yo& U.S. Goological Survey Profescional mmts in Muir Wet, AlasLa: Marine Geobgy, v. 57, of North Amctica, Volume K-3:Boulder, Cobrado, Geolog. Paper 786,50 p. p. 113-147. ical~tyofAmerica,501D. ,ma&, E. W.. 1984, RhytMdy bedded gkdanarine sedi- Mhyncch, E.. 1962, Pkis~xwegedogy of the TrenmCampbeP Rusl. B. R., l*, Mass Bow d&ts in a Quaternary swcesio,, I Dic ments on Whidbey Island, Washington: Journal of Sedimen- fordmaparea, 0ntariom.D. thesis]: Tomnto, Canada, UN- ncar Ottawa, Gnada: Dmpxuc criteria for subaqucousout. tary Peaology, v. 54, p. 589-602 wmity of Tomnto, 176 p. warh: Can& Joumal of Earth Scienm, v. 14.0. 175-184 ~en~a; ke, A. S.. and Rtsf V. K, 1981. Late Wiiand Hob Muller, E. H., and Piest, V. K,1985, Glacial lakes in the Ontario Rust, B. R., 1988 la-orcodmal deoosits of the Cha&Iain-~ - .- -. -ant &eat of the Laurcntid; laSheet: Gcdogical Survey ~inKarrow,P.F.,andW,P.E.,&.Quatemary vxlth G-, marOnn;d, Canada, in add; N. R. ed., of Canada Map 17CW scak 15,000,000. evdution dthe Great lakes: Oeological Asmiation of Can- 7hc lak Ouamdd-nt of the fhmdain Sd Ba- ~rchdd.H. L.. 1907, Gilbert Gulf: Gdozical Smctv of America ada Speial Paper 30, p. 213229. sin: Gcdogical A&ciatio;l of Canada Spd4 Paper 35, tin, v. 17, p. 712-718. Naldnn, D. L.. 1968, The late glacial-cprly glacianarim transition 0.37-46. irchild, H. L., 1919, Pleistocenemarine subme'gena of the Hud- in the Ottawa Valley: Evidcna for a glacial lake?: Gaogra- Rust, B. R., and Raaanelli, R., 1975, Late Quatenmy subaqu- son. Cham-, and St. Lawrena Valleys: New Yak Slate phie phy~+ et Quatermkc, v. 42, p. 171-179. outwash deposits near Ottawa, Canada, in Jopling, A. V., Museum e'ulktin 209-210.76 p. Naldrnt D. L. 1990. Lnccmotion and f& Uaca in Charnolain and Md)ooald,B. C., eds.. GlacioRwialand glaci-hine ,rster. S. W.. 1971, Pl&tOCCK gedogy of the Canhage 15' quad- S;a s&que& outwash deposia near--a, Canada: Ca- sedimentation: Society of Eamomic Paleontdogists and &e 1Ph.D. th&l: Syracuse, New York, Syrawe Uni- nadian ~wmnlof Earth Fences, v. n, p. 1495-lm. Mine- Special Publication 23, p. 111-192. Naldren, D. L,1991. LaamWm~and feeding traces in Champlain Sharpc, D. R., 1988. Glacioavim fan deposition in the Chmplain .Uerton, d..S., i980, &Iicanlation of post-Erie Inkr- Sea subaqueous outwash depoeits near ORaWa, Canada: Re- Sea, in Gadd, N. R.. cd., The late Quaternary development evcnts (16.000-10.000 radiocarbon years kfore ply: Canndian loumal of Eanh Sdenm v. 28, p. 833-834. of the Cbmplah Sea Bash Geological Associatan of Can- present), cenwl'and eastern Great Lakes & and Hud- Pair. D.. 1986. Raonsmrcbon and histcw of ice retrcat. prolJadal ada WalPaon 35. D. 682. son, Champlain, and St. Lawrena Lcnuknds, United States I&, ddthe ChqAain Sea, c&tnl St. ~-&-Lcnu- Shaw, I., ~hdrnt,D.. and~rceh,W., 1991, The late glacial and and Canada: U.S. Geologital Sumy Rofess~Paper lands, New York m.k. thesis]: Walerbo, Onlano, Univcr- post-&A cmhnmmt of the Kingston area: The CaMdian 1089.52 p. sitv of Waterloo. a1D. +sociation of Gccgmphen field 6,10 p. ddd. N. R.. 1980, Late-glacial regbd ice flow patterns in eastern pair. D..L.. 1991. ate ~~~istoanc hrstory and maptic Shulmusta. 1.. 1989, A cnrepualmodel for the deposition of the Ontario: Canadian Joumal of Earth Sciences, v. 17, chrawsedtlgraphy. westan Aduoodack bordhd, New Dunrmcr Moraine, southern Ontario: Gcrnno~phology,v. f n. 1439-1453. Yo* IPh.D. thesisl: Svracusc. New Yo& SyraCuSe U&r- p. 385-3% 3dd.k.-R, 1981; Late-glacial re@ ice flow patterns in eastern Sly, P. G., and Ra,J. W.. 1984, Late glacial and post glacial Iat Ontario: Renk Canadian Joumal of Earth Scienas. v. 18, Pair, DYL~-&~MUU~,E. H., 1990, Regional flow patterns and gdo&v in the lake Ontario Basin: CanadianJournal of Earth Andes p. 13%[email protected] ~~Macialccmditioas ofthe St. Lawrura-Lake Ontario ice Sdcmrs. v. 21.D.802821. add, N. R., 1987, Geological setting and Quaternary deposits of lobey western ~dbondaclrbordcrknd, New Yo* Gcologtcal Spenar, J. ~..~184ihclmquok shore north ofthe Adirondadrs: PI- the Ottawa region, in Fultm R. J., ed., Quaternary geology Society of America Abstracts with Rograms, v. 22, p. 61. Gcokgical Society of America Bulletin, v. 3, p. 488-491. of the Ottawa region, Ontario and Quebec: Geological Survey Pair, D. L., and Rodr@m, C. G., 1989, Late &ternary deglad- Stevcns, R., 1985. Gladomarine vams in Late-Pkistoccnc clavs fault S of Canada Paper 86-23, p. 3-9. ation of the southwestern St. Lawrence Lowland, NY: Gc- near Gotcbosg, southvestern Sweden: Boreas, v. f4, n in-112 Eaulttcl .add. N. R.. 1988a.The basin. the ice, the C3a~lainWin Gadd, oloaical Society of America Abstracls with m,v. 21, r. -- --- 'N. R.; ed., 'he late &ternary devc.*nt of the Cham- p. 55. Stevens, R., 1986, Gfaciomarincvan~~ and the character of d+ m plain Sea Basin: Geological Assoaabon of Canada Special Pair, D. L., Karrow, P. F., and Qark. P. U., 196% Histoly of the ciation, sa\sanvalky,sarlhwestem Sweden: v. 15, Paper 35, p. 15-24. Changlain*intheanwlSt.L.awren~Lowl~,N~ n- ---ZRLXS --- . shear $add,N. R., 19883, Lithofacies relationshipsin freshwater-marine York and ~tsrelationshiu to Lake Ontano water Ievcls, m Stew- D. P., 1!X7,ThePle&oane gedogy of the Watertown and transition of the Champlain Sea,in Gadd, N. R., ed., The late add; N. R., ed. Gte 0wmw-y development of the Sackcts Harbor quadrangles, New York: New York State ern pa Quaternary development of the Champlain Sea Basin: Gco Champlam Sea B-: Gcdogical- Assoaahcm of Canada Spe- Museum Bulletin 369,79 p. CreEac logical Association of Canada Spedal Paper 35, p. em., cial piper 35, p. 107-124. Street. J. S., 1988. Glacial meltwater channels associated with dc- iurrieri, I. T., and Musiker, L. B., 1990, Late WisconEman rce Pair, D. L., Mulla, E. H., and Aodmon, T. W., 19883, Glacial dcdogical society of ~mericaAbstractswith F'm cies, c margins and recssional events in the nonhcenwl Adiron- mopims&at&aphic relamiship and ice recession on thc gramn,v. 20, p. 285. mne. dack mountains, New Yak: Northeastern Geology, v. 12, northwest Adirondack slo~eand adiaant I&&, New Sutton, R. G., Lcwip, T. L., and Woodrow, D. L., 1972. Pat- p. 185-197. York: Geological Society bf hr& Abstxacts with Pro, lroqucis lake nags and shoreline sedimentation in &tern dudik >ustavson,T. C., and Boothmyd, J. C., 1987, A depqsitional meel grams, V. m, p. 60. Ontario Basin: Joumal of Gdogy, v. 80, p. 34E-356. faoutwash, sediment sources, and bydrolog~ccharactens- Parent, M., and Occhietti, S., 1988, Late Wisconsinan deglaciation Taylor, F. B., 1924,Morainesofthe St. LawenceLowland: Jwmal ceolr9: tics, Malaspina , Alaska: A modem analog of the andChamplainSeainvasion in the St. Lawrena Valky, Quc- southeastern margin of the Lawentide Ice Sheet: Geobgrcal bec: -hie physique et Quaremaire, v. 42, p. 21S246. Teller, J. ~.,&%;~ake&Land itsconmbuoon to flow through amorF Society of America Bdetin, v. 99, p. 187-200. Rest, V. K., 1970, Quaternq gmlogy of Canada, in Douglas, the Ortawa-Sl. Lawrence system, m Gadd, N. R.. ed., Qua. amphi Henderson, E. P., 1%7, Shcial gedogy north of the St. Lawrence R.J.W., ed., Geology and economic minerals of Canada: Ge- ternary evolution of the Champlam Sea Basin: Geological As- River, Kingston to hcscon,in Guidebmk, Geology of parts oloaical S- of Canada Economic Geology Report l (5th sociation of Canada SpdPaper 35, p. 281-290. the er of and western Quebec Geological Associ- edih), p. 67c764. Teller, J. T.. 1990, Volume andmtmgoflakglaaal runoffhum the fonwr ation of Canada, p. 1W208. Rodrigues, C. G., 19W, Faunal successionsin late Pleistocene sed- soulhem Lawentide Ice Sheet: Quaternary Research, v. 34, Henderson, E. P., 1973, Surficial gdogy of the Kingston (north- iments of the OttawG3t. Lawrence Lmvlands: 1984 Cana- r.n --17-73 -. Tb4 half) map area, Ontario: Geological Swey of Canada Pa- dian Paleontology and Biostrati~Seminar Progam with Thomas, R. H., 1977, C+ing bay dynamicsand ice sheet retreat up per 72-48.6 p. Abstracts, p. 7. the St. Lamnce Valley system: Geographic physique et placen Henderson, P. J., 19% Sedimentationinanesker systeminfluenced Rodrigues, C. G., 1987, Late Pleistocene invertebrate macrofossb, Quaternaire, v. 31, p. 347-356. by bedrock t-phy near Kingston, Ontario: Canadian minofossils, and depositional environments of the western Upham, W., 1895, Late glaaal or Champlain subsidence and reel- opma Journal of Earth Sciences, v. 25, p. 987-999. basin of the Champlain Sea, in Fultcm, R. J., ed., Quaternary evation of the St. Lawrence River basin: hrimJournal of the kx ~amm,P F., 1981, Late-glanal re~onh~ce-flow pattern m at- geology of the Ottawa region, Ontario and Quebec: Geolog- Science, v. 49, p. 1-18. ern Ontmo: D~uuum:Canad~an Joumal of Eanh Sacnces, ical Survey of Canada Paper 86-23, p. 16-23. Westgate, J. A,, Chen, F. J., and Delonne, L. D., 1987, Laastrine was b v. 18, p. 1W1390. Rodrigues, C. G., 1988, Late Quaternary invenebrate faunal asx~ osuacodes in the late Pleistocene Sunnvbtuok diamicton of Kirkland, J. T., and Coates, D. R., 1977, lle Champlain Sea and ciations and chronology of the western Champlain Sea Basin, southern Ontario, Canada: Canadian J&rnal of Earth Sci- was p. Quaternary deposits in the St. Lawrence Lowland. New in Gadd, N. R., ed., Thc late Quaternary development of the enas, v. 24, p. 233W2335. ponen York. in Newman. W. S., and Sahven, B., eds., Amerinds Champlain Sea Basin: GeologicalAssociation of Canada Spe- Wright, F. M., lPn, The Pleistocene and Recent geology of the and theu paleoemronments m North Amenca: New York cial Paper 35, p. 15S176. Oneida-Rome district, New York 1Ph.D. thesis]: Syracuse. magm Academy of Sclences Annals. v. 288. p. 7W89. Rodrigues, C. G., 1991, humofion and feeding traces in Cham- New York, Syracuse University, 181 p. Ims. C.F M.. and Andenon, T. W., 1989, Osallduons of lcvels plain Sea subaqueous ounvash deposits near Ottawa, Can- Brit and cool phases of the Laurentian Great Lakes caused by ada: Discussion: Canadian Joumal of Earth Sciences, v. 28, of the inffows from glacial Lakes Agassiz and BarIowQibway: p. 831-832. Journal of Paleolimndogy, v. 2, p. W146. Rodrigues, C. G., 1992, Suocessiofis of invertebrate microfossils sidm MacClintock, P., and Stewart, D. P., 1%5, Pleistocene geology of and the late Quaternary deglaciation of the central St. the St. Lawrence Lowland: New York State Museum Bul- Lawrence Lowland, Canada and United States: Quaternary en& letin 394, 152 p. Science Reviews, v. 11, p. 5G3-534. fabric Mackiewia, N. E., Powell, R. D., Carlson, R. P., and Molnia, Ruddiman, W. F., and Wright, H. E., eds., 1987, North America B. F., 1984, Interlaminated iceproximal glacimarine sedi- and adjacentoceans during the last degladation: meGeology forma placem tle sini

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