Pleistocene geology of the northeast Adirondack region, New York

Denny, Charles Storrow

doi:10.3133/pp786

Cited by 14 publications

(20 citation statements)

References 19 publications

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“…as a result of opening to marine waters. Similar drops of water-levels were also recognized further southwest along the Appalachian piedmont (Prichonnet, 1982a(Prichonnet, , 1982b(Prichonnet, , 1984aMcDonald, 1968) and at the foot of the Adirondacks (MacClintock and Terasmae, 1960;Denny, 1974;Clark and Karrow, 1984). The microfaunal record at Rivière Landry and the sudden fall of water levels suggest that glaciolacustrine waters were replaced by marine waters almost instantaneously, around 12 ka, in the Appalachian piedmont, southwest of Victoriaville.…”

Section: Champlain Sea Phase Ilmentioning

confidence: 79%

“…Lacustrine sediments of the Chambly Formation (LaSaIIe, 1981), which were deposited at altitudes (<40 m a.s.l.) well below those of previously recognized Fort Ann shoreline features in this region (Denny, 1974;Parrott and Stone, 1972), were probably deposited in this lake. The presence of clays containing Candona subtriangulata below marine clays in the lowlands between the St. Lawrence and Ottawa rivers suggests that the ice front may have retreated almost as far north as Ottawa during the life of this freshwater body (Anderson et al, 1985).…”

Section: Lake Candonamentioning

confidence: 98%

“…Around 12.5 ka, Lake Ontario basin was inundated by Lake Iroquois (MacClintock and Stewart, 1965;Denny, 1974;Fullerton, 1980;Clark and Karrow, 1984). High level of Lake Iroquois extended into the St. Lawrence Valley until the margin of the Laurentide Ice Sheet had retreated from highlands south of Covey Hill (Clark and Karrow, 1984).…”

Section: Deglaciation Of the Southern Appalachians Of Québec And Fortmentioning

confidence: 99%

“…difference between the latest glacial lacustrine shoreline features and upper marine shoreline features is on the order of 60 m. In order to determine whether glacial lake strandline features of the middle Saint-François Valley correspond to the Upper or to the Lower Fort Ann water plane of Clark and Karrow (1984), strandline features recorded in several published sources were compiled for the area extending between Granby (Québec) and St. Albans (Vermont), east and northeast of Lake Champlain (Appendices I and II). Features numbered #54 to 71 in Figure 7 belong to the well established Fort Ann strandline in New York Denny, 1974;Clark and Karrow, 1984) and those numbered #43 to 53 have been assigned to this phase in Vermont (Parrot and Stone, 1972;. Features that are located upstream of narrow valleys, however, were deleted, since they may have formed in small, local lake basins.…”

mentioning

confidence: 99%

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Late Wisconsinan Deglaciation and Champlain Sea Invasion in the St. Lawrence Valley, Québec

Parent¹,

Occhietti²

2007

gpq

116

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Champlain Sea history is directly linked to Late Wisconsinan deglacial episodes. Champlain Sea Phase I (Charlesbourg Phase) began in the Québec area at about 12.4 ka. It represented a western extension of the Goldthwait Sea between remnant Appalachian ice masses and the Laurentide Ice Sheet. Further south, at about the same time, in the Appalachian uplands and piedmont, high-level glacial lakes were impounded by the ice-front during glacial retreat toward NNW: lakes Vermont, Memphrémagog and Mégantic. Lowlands of the Upper St. Lawrence and Lake Champlain valleys were progressively deglaciated and inundated by Lake Iroquois and Lake Vermont. At about 12.1 ka, these two lakes coalesced and formed a single water-body, here referred to as Lake Candona. After the Ulverton-Tingwick Moraine was constructed, this lake extended northeastward onto the Appalachian piedmont where varved sediments containing Candona subtriangulata underlie marine clays. Current data and interpretations bring into question the former concept of the Highland Front Moraine System. The invasion of the main basin, or Champlain Sea Phase II, began around 12 ka. Replacement of Lake Candona by the sea resulted in a fall of about 60 m in water levels. Champlain Sea Phase III began at the end of the Saint-Narcisse episode, at about 10.8 ka. At this time marine waters were able to enter valleys of the Laurentian Highlands where brackish or fresh paramarine basins developed.L'histoire de la Mer de Champlain est directement liée à la déglaciation du Wisconsinien supérieur. La phase I de la Mer de Champlain (Phase de Charlesbourg) débute dans la région de Québec vers 12,4 ka. Elle représente le prolongement de la Mer de Goldthwait entre l'Inlandsis laurentidien et les glaces résiduelles appalachiennes. Plus au sud et approximativement en même temps, le retrait glaciaire vers le NNW sur les plateaux et le piémont appalachiens est marqué par des moraines et les lacs proglaciaires Vermont, Memphrémagog et Mégantic; les terres basses du haut Saint-Laurent et du lac Champlain étaient progressivement déglacées et inondées par les lacs Iroquois et Vermont. Vers 12,1 ka, ces deux lacs forment par coalescence Ie Lac Candona. Après l'épisode de la Moraine d'Ulverton-Tingwick, ce lac inondait le piémont appalachien vers le NE, où des varves à Candona subtriangulata reposent sous les argiles marines. Ces données remettent en question le concept de Highland Front Moraine System. L'invasion du bassin principal (Phase II de la Mer de Champlain) débute vers 12 ka. Le remplacement du Lac Candona par la mer provoque une chute d'environ 60 m du niveau du plan d'eau. La Phase III de la Mer de Champlain commence à la fin de l'épisode de Saint-Narcisse, vers 10,8 ka; les eaux marines pénètrent dans les vallées des Laurentides et sont coalescentes à des bassins paramarins saumâtres ou non salés.Die Geschichte des Meeres von Champlain ist direkt mit Enteisungs-Episoden im spàten Wisconsin verknùpft. Die Phase I des Champlains-Meeres (Charlesbourg Phase) began im Gebiet von Québec...

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Section: Champlain Sea Phase Ilmentioning

confidence: 79%

Section: Lake Candonamentioning

confidence: 98%

Section: Deglaciation Of the Southern Appalachians Of Québec And Fortmentioning

confidence: 99%

mentioning

confidence: 99%

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Late Wisconsinan Deglaciation and Champlain Sea Invasion in the St. Lawrence Valley, Québec

Parent¹,

Occhietti²

2007

gpq

116

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“…L'éventail d'orientations dans les trames de till n'est ainsi pas le fait de la seule topographie ou d'écoulements radiaires issus d'un même lobe glaciaire comme l'ont suggéré Denny (1974), Kirkland et Coates (1977), Fullerton (1980) ainsi que Clark et Karrow (1983).…”

Section: Discussionunclassified

Façonnement du modelé drumlinoïde par deux écoulements glaciaires successifs au sud-ouest de Montréal

Delage

Gangloff

2010

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La morphologie et les dépôts de la plaine au sud-ouest de Montréal révèlent une dynamique glaciaire complexe. Des formes allongées (drumlinoïdes) subparallèles à l’axe du Saint-Laurent sont constituées d’un corps de till d’accrétion fissile et compact parfois recouvert d’un till de fusion ou d’un matériel grossier d’origine littorale, probablement glacielle. Ce modelé sous-glaciaire a d’abord été façonné par un important écoulement glaciaire du nord-est qui remontait les basses terres du Saint-Laurent en direction sud-ouest. Ceci est démontré par la présence de traceurs pétrographiques d’origine appalachienne, ainsi que par les trames de till et les microformes orientées dans ce même axe NE-SO. La genèse initiale de ce modelé s’apparente donc plus à celle des drumlins qu’à celle des formes transverses à l’écoulement, telles les moraines de Rogen ou côtelées. Ce sont avant tout des formes d’accumulation, mais la forte correspondance entre la plus grande partie des constituants du till et la lithologie locale, et l’excellent état de conservation des morceaux de lit glaciaire polis et striés montrent que la source de ces matériaux était proche. Ces drumlinoïdes fraîchement forgés ont été chevauchés par un second écoulement glaciaire, du nord-ouest ou du nord celui-là, sans qu’il y ait eu déglaciation. Bien qu’il ait laissé ses traces un peu partout sur le territoire, ce second flux glaciaire a peu transformé le modelé initial du nord-est. Toute la partie glaciaire des drumlinoïdes appartient à un seul et même épisode glaciaire du Wisconsinien supérieur. Les tills d’accrétion formant leur noyau sont corrélables entre eux, mais aussi à la presque totalité des tills les plus récents trouvés dans la région.Landforms and deposits of Huntingdon plain, southwest of Montréal, reveal a complex glacial history. Of that glacial heritage, we have considered elongated landforms nearly parallel to the St. Lawrence River axis. The core of these drumklin-like (drumlinoids) forms is a fissile and compact lodgement till, occasionally covered by a melt-out till or by coarse littoral material of probable drift ice (ice-rafted) origin. These subglacial landforms were first moulded by an important ice flow from the northeast moving up St. Lawrence Lowlands south-westwards. This is shown by indicator stones of appalachian origin, but also by till fabrics and microforms of glacial erosion both oriented northeast-southwest. Thus, the initial part of their genesis makes the drumlinoids more similar to drumlins than to subglacial transverse landforms like Rogen or ribbed moraines. Characteristics of the lodgement till indicate than the drumlinoids were constructed by accumulation processes, but that erosion processes responsible for an important fraction of the till were in action near by. The first ice flow from the northeast was followed by a second one from the northwest or the north without deglaciation. Even if this second ice flow let its traces all over the studied area, the initial glacial morphology was only slightly modified. The en...

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The developmental history of Adirondack (N.Y.) lakes

et al. 1989

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We utilized paleoecological techniques to reconstruct long-term changes in lake-water chemistry, lake trophic state, and watershed vegetation and soils for three lakes located on an elevational gradient (661-1150 m) in the High Peaks region of the Adirondack Mountains of New York State (U.S.A.). Diatoms were used to reconstruct pH and trophic state. Sedimentary chrysophytes, chlorophylls and carotenoids supplied corroborating evidence. Pollen, plant macrofossils, and metals provided information on watershed vegetation, soils, and biogeochemical processes. All three lakes were slightly alkaline pH 7-8) and more productive in the late-glacial. They acidified and became less productive at the end of the late-glacial and in the early Holocene. pH stabilized 8000-9000 yr B.P. at the two higher sites and by 6000 yr B.P. at the lowest. An elevational gradient in pH existed throughout the Holocene. The highest site had a mean Holocene pH close to or below 5; the lowest site fluctuated around a mean of 6. The higher pH and trophic state of the late-glacial was controlled by leaching of base cations from fresh unweathered till, a process accelerated by the development of histosols in the watersheds as sprucedominated woodlands replaced tundra. An apparent pulse of lake productivity at the late-glacialHolocene boundary is correlated with a transient, but significant, expansion of alder (Alnus crispa) populations. The alder phase had a significant impact on watershed (and hence lake) biogeochemistry. The limnological changes of the Holocene and the differences between lakes were a function of an elevational gradient in temperature, hydrology (higher precipitation and lower evapotranspiration at higher elevation), soil thickness (thinner tills at higher elevation), soil type (histosols at higher elevation), vegetation (northern hardwoods at lower elevation, spruce-fir at higher), and different Holocene vegetational sequences in the three watersheds.

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Pleistocene geology of the northeast Adirondack region, New York

Cited by 14 publications

References 19 publications

Late Wisconsinan Deglaciation and Champlain Sea Invasion in the St. Lawrence Valley, Québec

Late Wisconsinan Deglaciation and Champlain Sea Invasion in the St. Lawrence Valley, Québec

Façonnement du modelé drumlinoïde par deux écoulements glaciaires successifs au sud-ouest de Montréal

The developmental history of Adirondack (N.Y.) lakes

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