Journal articles: 'Geology – Vermont – Champlain Valley'

1

Parent, Michel, and Serge Occhietti. "Late Wisconsinan Deglaciation and Champlain Sea Invasion in the St. Lawrence Valley, Québec." Géographie physique et Quaternaire 42, no. 3 (December 18, 2007): 215–46. http://dx.doi.org/10.7202/032734ar.

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ABSTRACT 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.

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2

Waite, Carl E., Donald H. DeHayes, Terry L. Turner, David J. Brynn, and William A. Baron. "Black Walnut Seed Sources for Planting in Vermont." Northern Journal of Applied Forestry 5, no. 1 (March 1, 1988): 40–45. http://dx.doi.org/10.1093/njaf/5.1.40.

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Abstract The growth, phenology, and susceptibility to winter injury of 82 black walnut provenances were compared in a northwestern Vermont provenance test plantation. After seven growing seasons, provenances from MI, central OH, northern IN, and PA exhibit the best combination of growth, budbreak, and winter hardiness characteristics and are recommended for planting in Vermont's Champlain and Connecticut river valleys. Provenances from MI appear to be particularly well-suited to the environment of Vermont's Champlain Valley, as exemplified by a provenance from Volinia, MI which is 26% taller than the plantation average and among the latest to begin growth in spring. Despite fast growth, provenances from KY, IL, and VA do not appear suitable for planting in Vermont because of their relatively early budbreak and high susceptibility to winter injury. Provenances from the Great Plains are not recommended for planting in Vermont due to their relatively slow growth rate and early budbreak. North. J. Appl. For. 5:40-45, March 1988

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3

Murray, Helena F., and Anthony W. D'Amato. "Stand Dynamics and Structure of Two Primary Champlain Valley Clayplain Forests, Vermont." Northeastern Naturalist 26, no. 1 (March 1, 2019): 95. http://dx.doi.org/10.1656/045.026.0103.

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4

Sullivan, S. M. P., and M. C. Watzin. "Stream-floodplain connectivity and fish assemblage diversity in the Champlain Valley, Vermont, U.S.A." Journal of Fish Biology 74, no. 7 (May 2009): 1394–418. http://dx.doi.org/10.1111/j.1095-8649.2009.02205.x.

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5

Hugenholtz, Chris H., and Denis Lacelle. "Geomorphic Controls on Landslide Activity in Champlain Sea Clays along Green’s Creek, Eastern Ontario, Canada." Géographie physique et Quaternaire 58, no. 1 (June 26, 2006): 9–23. http://dx.doi.org/10.7202/013108ar.

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AbstractLandslides in Champlain Sea clays have played an important role in shaping Eastern Ontario’s landscape. Despite extensive research, there is a limited understanding of the relations between landslide activity, climatic controls, and the geomorphic evolution of river valleys in Champlain Sea clay deposits. With these issues in mind, a study was undertaken to determine the controls on the spatio-temporal distribution of contemporary landslide activity in valley slopes composed of Champlain Sea clay. The study area was the Green’s Creek valley located in the east end of Ottawa, Ontario. Observations and measurements indicate that landslide activity is closely related to valley development. An inventory of landslide activity from 73 years of aerial photographs revealed that landslides occurred preferentially in slopes located on the outside of meander bends, and that they often recurred in the same slope after a period of ripening. The largest and highest density of landslides occurred along a major tributary valley where geomorphic features such as knickpoints, V-shaped valley profiles and bedrock depth-to-slope height ratios reflect an unstable phase of valley development. A small number of landslides incurred successive failures along the slopes of the backscarp for several years-to-decades after the initial failure. Correlation analysis showed that the temporal distribution of landslide activity has fluctuated in response to decadal-scale changes in the amount of precipitation.

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Zika, Peter F. "Contributions to the Flora of the Lake Champlain Valley, New York and Vermont, II." Bulletin of the Torrey Botanical Club 115, no. 3 (July 1988): 218. http://dx.doi.org/10.2307/2995958.

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Zika, Peter F., and Everett J. Marshall. "Contributions to the Flora of the Lake Champlain Valley, New York and Vermont, III." Bulletin of the Torrey Botanical Club 118, no. 1 (January 1991): 58. http://dx.doi.org/10.2307/2996976.

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8

Brett, Kevin D., and Stephen R. Westrop. "Trilobites of the Lower Ordovician (Ibexian) Fort Cassin Formation, Champlain Valley region, New York State and Vermont." Journal of Paleontology 70, no. 3 (May 1996): 408–27. http://dx.doi.org/10.1017/s0022336000038348.

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The Lower Ordovician (Ibexian) Fort Cassin Formation of New York State and Vermont consists mainly of carbonates that were deposited in a subtidal storm-influenced setting. The low diversity trilobite fauna is dominated overwhelmingly by the isoteline, Isoteloides. Eleven species representing at least nine genera are described; Acidiphorus whittingtoni is new. The bathyurine genus Goniotelina Whittington and Ross is regarded as paraphyletic and is synonymized with Acidiphorus Raymond. The presence of Isoteloides canalis (Whitfield; = I. latimarginatus Fortey), I. peri Fortey and Bathyurellus platypus Fortey indicates a correlation of the Fort Cassin with the Strigigenalis caudata Zone of the Catoche Formation of western Newfoundland.

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9

Munroe, Jeffrey S., Zachary M. Perzan, and William H. Amidon. "Cave sediments constrain the latest Pleistocene advance of the Laurentide Ice Sheet in the Champlain Valley, Vermont, USA." Journal of Quaternary Science 31, no. 8 (November 2016): e2913. http://dx.doi.org/10.1002/jqs.2913.

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10

Brakenridge, G. Robert, Peter A. Thomas, Laura E. Conkey, and Jane C. Schiferle. "Fluvial Sedimentation in Response to Postglacial Uplift and Environmental Change, Missisquoi River, Vermont." Quaternary Research 30, no. 2 (September 1988): 190–203. http://dx.doi.org/10.1016/0033-5894(88)90023-3.

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Three lithologically distinct alluvial units of Holocene age can be distinguished along trenched cross sections of the Missisquoi valley bottom. The oldest is of early Holocene age, and the associated floodplain had aggraded to nearly its present level by 8000 14C yr B.P. At that time, early Archaic projectile points were deposited in a fire hearth 50 cm below the surface. Abandonment of this floodplain was followed by the development of an A-E-Bt soil profile. Accumulation of a younger floodplain had begun by 6400 14C yr B.P. and local sedimentation persisted to ca. 500 14C yr B.P., as indicated by radiocarbon dates of buried woody debris (including large logs) and of charcoal. Alluvium of the modern floodplain began accreting after A.D. 1860 and contains machine-cut square nails, whiteware ceramics, and coal clinker. Previous locations of the river channel can be reconstructed from relict surfaces marked by paleosols, the preserved depositional stratigraphy, and the radiocarbon samples. Immediately after regression of the Champlain Sea from this part of the valley, and before 8000 14C yr B.P., the river incised late Fleistocene marine silts and clays at an average rate of at least 1 m/100 yr. After the interval of downcutting, episodic lateral migration became the dominant process, with the rate varying between 0 and 4 m/100 yr. The early Holocene incision was most likely a lagged response to postglacial crustal rebound, whereas strong soil development and floodplain stability between 8000 and 6400 14C yr B.P. may reflect an independently documented warmer, and perhaps drier, climate in New England at this time. Finally, the post-A.D. 1860 period of active floodplain sedimentation may have been a response to timber clear-cutting, row crop agriculture, and cattle and sheep grazing in the watershed.

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11

Mazzola, M., and D. R. Bergdahl. "The phenology and spore dissemination patterns of Uredinopsismirabilis on Abiesbalsamea and Onocleasensibilis." Canadian Journal of Forest Research 19, no. 1 (January 1, 1989): 88–95. http://dx.doi.org/10.1139/x89-012.

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Phenology and spore dissemination patterns of Uredinopsismirabilis (Peck) Magnus were monitored from 1982 to 1984 in the Champlain Valley and north central Vermont. Teliospore germination began as early as May 5 and basidiospore dissemination continued as late as the week of June 17. Maximum basidiospore dissemination occurred after measurable precipitation. Infection of Abiesbalsamea (L.) Mill, occurred between May 19 and 30. Pycnia were apparent on current-year needles of A. balsamea by the week of June 17. Aeciospore development was observed by the week of June 24 and dissemination of aeciospores was completed about July 29. Aeciospores were trapped at highest concentrations during precipitation events. During dry periods, aeciospore dissemination showed a diurnal periodicity, with most spores trapped in the late morning hours. Uredia were formed on Onocleasensibilis L. as early as July 28 and urediniospores were trapped as late as October 4. Teliospores were formed in host tissues as early as July 7.

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12

Allen, David, Benjamin Borgmann-Winter, Laura Bashor, and Jeremy Ward. "The Density of the Lyme Disease Vector Ixodes scapularis (Blacklegged Tick) Differs between the Champlain Valley and Green Mountains, Vermont." Northeastern Naturalist 26, no. 3 (July 24, 2019): 545. http://dx.doi.org/10.1656/045.026.0307.

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13

Keller, Erin L., Samantha T. Connolly, Josef H. Görres, and Jos J. Schall. "Genetic diversity of an invasive earthworm, Lumbricus terrestris, at a long-term trading crossroad, the Champlain Valley of Vermont, USA." Biological Invasions 22, no. 5 (February 12, 2020): 1723–35. http://dx.doi.org/10.1007/s10530-020-02215-7.

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14

Laird, Neil F., Jared Desrochers, and Melissa Payer. "Climatology of Lake-Effect Precipitation Events over Lake Champlain." Journal of Applied Meteorology and Climatology 48, no. 2 (February 1, 2009): 232–50. http://dx.doi.org/10.1175/2008jamc1923.1.

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Abstract This study provides the first long-term climatological analysis of lake-effect precipitation events that developed in relation to a small lake (having a surface area of ≤1500 km2). The frequency and environmental conditions favorable for Lake Champlain lake-effect precipitation were examined for the nine winters (October–March) from 1997/98 through 2005/06. Weather Surveillance Radar-1988 Doppler (WSR-88D) data from Burlington, Vermont, were used to identify 67 lake-effect events. Events occurred as 1) well-defined, isolated lake-effect bands over and downwind of the lake, independent of larger-scale precipitating systems (LC events), 2) quasi-stationary lake-effect bands over the lake embedded within extensive regional precipitation from a synoptic weather system (SYNOP events), or 3) a transition from SYNOP and LC lake-effect precipitation. The LC events were found to occur under either a northerly or a southerly wind regime. An examination of the characteristics of these lake-effect events provides several unique findings that are useful for comparison with known lake-effect environments for larger lakes. January was the most active month with an average of nearly four lake-effect events per winter, and approximately one of every four LC events occurred with southerly winds. Event initiation and dissipation occurred on a diurnal time scale with an average duration of 12.1 h. In general, Lake Champlain lake-effect events 1) typically yielded snowfall, with surface air temperatures rarely above 0°C, 2) frequently had an overlake mesolow present with a sea level pressure departure of 3–5 hPa, 3) occurred in a very stable environment with a surface inversion frequently present outside the Lake Champlain Valley, and 4) averaged a surface lake–air temperature difference of 14.4°C and a lake–850-hPa temperature difference of 18.2°C. Lake Champlain lake-effect events occur within a limited range of wind and temperature conditions, thus providing events that are more sensitive to small changes in environmental conditions than are large-lake lake-effect events and offering a more responsive system for subsequent investigation of connections between mesoscale processes and climate variability.

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15

Elson, John A. "West-southwest glacial dispersal of pillow-lava boulders, Philipsburg–Sutton region, Eastern Townships, Quebec." Canadian Journal of Earth Sciences 24, no. 5 (May 1, 1987): 985–91. http://dx.doi.org/10.1139/e87-095.

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Pillow-lava boulders, probably from Place Mountain in the Bolton valley east of the Sutton Mountains, occur in a narrow belt or fan 43 km long trending west-southwest (azimuth about 248°) from 10 km southwest of Place Mountains to Rosenberg, near Philipsburg, Quebec. Glacial striations with this direction are uncommon; the general glacial movement indicated by abundant striations and indicator erratics is southeastward. A southwestward flow in the axial part of the St. Lawrence Lowlands near Montréal is apparently the youngest direction there, of late Wisconsinan age. In the Eastern Townships of Quebec east and northeast of the study area and in adjoining northern Vermont there is evidence of a southwestward flow of mid-Wisconsinan age. Local southwestward flow in the study area at the beginning and end of a glacial cycle may have resulted from a mobile bed in the flooded St. Lawrence – Champlain lowland, but a hypothesis of flow from a major mid-Wisconsinan axis of accumulation in the northern Appalachians farther to the east is supported by much published field evidence.

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16

Naldrett, Dana L. "The Late Glacial-Early Glaciomarine Transition in the Ottawa Valley: Evidence for a Glacial Lake?" Géographie physique et Quaternaire 42, no. 2 (December 18, 2007): 171–79. http://dx.doi.org/10.7202/032723ar.

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ABSTRACT Rhythmites overlying either cross-bedded sand or diamicton are found throughout the Ottawa Valley. Previously thought to be restricted glacial lake sediments, they are now known to be widespread, and represent a large proglacial lake which preceded the Champlain Sea. The rhythmites consist of thin silt and clay laminae which fine upwards and contain slump, flame, shear (ice-contact?) and fluid escape structures. Ice-rafted material is common. The ostracode Candona cf. C. subtriangulata occurs in low numbers and indicates a freshwater body with depth of approximately 200 m. The alternation of silt and clay rhythmite laminae is characteristic of deposition by underflow and overflow currents, respectively. To produce underflows with typical glacial outwash concentrations may require discharge into fresh rather than marine water. This evidence and the widespread occurrence of rhythmites throughout the Ottawa Valley and the Rideau Lakes area suggests a large proglacial lake as the sedimentary basin. The lake is tentatively correlated with the Belleville Phase of Glacial Lake Iroquois and the Ft. Ann Phase of Glacial Lake Vermont. These phases occurred at depths consistent with the requirements for Candona survival. The water body which existed in the Ottawa area is here called Lake Rideau after the type locality where rhythmites were first observed. Generation of such a lake favours the more conventional "window blind" model for déglaciation rather than the calving bay concept.

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17

BRITZKE, ERIC R., ALAN C. HICKS, SUSANNA L. VON OETTINGEN, and SCOTT R. DARLING. "Description of Spring Roost Trees Used by Female Indiana Bats (Myotis sodalis) in the Lake Champlain Valley of Vermont and New York." American Midland Naturalist 155, no. 1 (January 2006): 181–87. http://dx.doi.org/10.1674/0003-0031(2006)155[0181:dosrtu]2.0.co;2.

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18

Carrera, Marco L., John R. Gyakum, and Charles A. Lin. "Observational Study of Wind Channeling within the St. Lawrence River Valley." Journal of Applied Meteorology and Climatology 48, no. 11 (November 1, 2009): 2341–61. http://dx.doi.org/10.1175/2009jamc2061.1.

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Abstract The presence of orography can lead to thermally and dynamically induced mesoscale wind fields. The phenomenon of channeling refers to the tendency for the winds within a valley to blow more or less parallel to the valley axis for a variety of wind directions above ridge height. Channeling of surface winds has been observed in several regions of the world, including the upper Rhine Valley of Germany, the mountainous terrain near Basel, Switzerland, and the Tennessee and Hudson River Valleys in the United States. The St. Lawrence River valley (SLRV) is a primary topographic feature of eastern Canada, extending in a southwest–northeast direction from Lake Ontario, past Montreal (YUL) and Quebec City (YQB), and terminating in the Gulf of St. Lawrence. In this study the authors examine the long-term surface wind climatology of the SLRV and Lake Champlain Valley (LCV) as represented by hourly surface winds at Montreal, Quebec City, and Burlington, Vermont (BTV). Surface wind channeling is found to be prominent at all three locations with strong bidirectionalities that vary seasonally. To assess the importance of the various channeling mechanisms the authors compared the joint frequency distributions of surface wind directions versus 925-hPa geostrophic wind directions with those obtained from conceptual models. At YUL, downward momentum transport is important for geostrophic wind directions ranging from 240° to 340°. Pressure-driven channeling is the dominant mechanism producing northeasterly surface winds at YUL. These northeasterlies are most prominent in the winter, spring, and autumn seasons. At YQB, pressure-driven channeling is the dominant physical mechanism producing channeling of surface winds throughout all seasons. Of particular importance, both YUL and YQB exhibit countercurrents whereby the velocity component of the wind within the valley is opposite to the component above the valley. Forced channeling was found to be prominent at BTV, with evidence of diurnal thermal forcing during the summer season. Reasons for the predominance of pressure-driven channeling at YUL and YQB and forced channeling at BTV are discussed.

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19

Sullivan, S. Mažeika P., and Mary C. Watzin. "Relating stream physical habitat condition and concordance of biotic productivity across multiple taxa." Canadian Journal of Fisheries and Aquatic Sciences 65, no. 12 (December 2008): 2667–77. http://dx.doi.org/10.1139/f08-165.

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To explore the potential of assessments of stream geomorphic condition and habitat quality in evaluating lotic productivity, we investigated concordance of stream biotic productivity (aquatic macroinvertebrates, crayfish, fish, and belted kingfishers ( Ceryle alcyon )) and their physical habitat correlates in 18 streams in the Champlain Valley, Vermont, USA. Pearson correlation analysis indicated significant concordance between macroinvertebrate density and fish biomass (r = 0.76), between the density of macroinvertebrates in the orders Ephemeroptera, Plecoptera, and Trichoptera and fish biomass (r = 0.81), and between fish biomass and kingfisher brood weight (r = 0.54). We used principal component analysis followed by linear regression to investigate relationships between physical habitat condition and biotic productivity and to identify key components of physical habitat condition assessments. Our analysis supported the combined use of geomorphic and habitat assessments as a comprehensive indicator of stream physical habitat condition. We found relationships between habitat assessment scores and productivity measures of all taxa except crayfish, suggesting similar responses to physical condition across trophic levels. Our results encourage the use of additional taxa, in addition to widely used macroinvertebrate metrics, as indicators of the composite effects of physical habitat impairment in stream ecosystems.

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20

Lefebvre, Guy. "Slope instability and valley formation in Canadian soft clay deposits." Canadian Geotechnical Journal 23, no. 3 (August 1, 1986): 261–70. http://dx.doi.org/10.1139/t86-039.

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The purposes of the paper are to examine the deepening of valleys in clay deposits of Eastern Canada and in particular to look at the changes in the groundwater regime and slope stability conditions during valley formation. Field observations and laboratory testing indicate that the rate of valley deepening in Champlain clay deposits is of the order of only a few millimetres a year, owing to the low erodibility of the intact clay. The clay banks are, however, more erodible, owing to alteration and fissuration.The stratigraphy of Eastern Canadian clay deposits can be simplified by considering it to be a stratum of low permeabilityconfined between two boundary layers of relatively high permeability, which are the till layer at the base and a weathered crust or coarse-grained layer at the top. As the valley bottom get closer to the bottom till layer, the groundwater regime, and consequently the stability conditions, are modified. During the process of valley formation, the groundwater regime passes through astage where the conditions are rather detrimental to slope stability as it evolves toward conditions that enhance bank stability. Those changes in stability conditions happen over geological time more rapidly or less, depending on clay erodibility. Key words: soft clay, valley formation, slope stability, groundwater, erosion, erodibility.

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21

Görres, Josef H., Korkmaz Bellitürk, and Ryan D. S. Melnichuk. "Temperature and moisture variables affecting the earthworms of genus Amynthas Kinberg, 1867 (Oligachaeta: Megascolecidae) in a hardwood forest in the Champlain Valley, Vermont, USA." Applied Soil Ecology 104 (August 2016): 111–15. http://dx.doi.org/10.1016/j.apsoil.2015.10.001.

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22

Cao, Y. L., and K. T. Law. "Energy dissipation and dynamic behaviour of clay under cyclic loading." Canadian Geotechnical Journal 29, no. 1 (February 1, 1992): 103–11. http://dx.doi.org/10.1139/t92-011.

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A laboratory study has been conducted to investigate the dynamic behaviour of Champlain Sea clay from two locations in the Ottawa River valley region. The test program includes cyclic triaxial tests and resonant-column tests. The soil samples were consolidated at a range of pressures before the dynamic shear in order to cover the dynamic behaviour under both the overconsolidated and the normally consolidated states. An energy concept is introduced to interpret the test results. Mathematical relationships have been established for describing the various aspects of dynamic behaviour. These aspects include excess pore pressure, dynamic strength, dynamic shear modulus, and plastic strain. The study shows that the energy concept provides a promising way to analyze dynamic soil behaviour. Key words : energy, dynamic behaviour, clay, cyclic test, earthquake, excess pore pressure, shear modulus, strength.

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23

Masse, Roger J., Allan M. Strong, and Noah G. Perlut. "The Potential of Uncut Patches to Increase the Nesting Success of Grassland Songbirds in Intensively Managed Hayfields: A Preliminary Study From the Champlain Valley of Vermont." Northeastern Naturalist 15, no. 3 (September 2008): 445–52. http://dx.doi.org/10.1656/1092-6194-15.3.445.

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24

Munroe, Jeffrey S. "Testing the ‘Vineyard Geologic Identity’ concept in Marquette-producing vineyards in the Champlain Valley, Vermont, USA." Journal of Wine Research, November 30, 2022, 1–21. http://dx.doi.org/10.1080/09571264.2022.2151993.

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25

Allmendinger, Richard W., and Paul Karabinos. "Illuminating geology in areas of limited exposure using texture shading of lidar digital terrain models." Geosphere, November 17, 2022. http://dx.doi.org/10.1130/ges02531.1.

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Regions of sparse exposure challenge geologic mappers because of limited information available on the underlying structure and continuity of the map units. We introduce here a little-known technique for post-processing bare earth digital terrain models (DTMs) that can dramatically improve knowledge of the underlying structure in covered areas. Texture shading enhances changes in slope and does not suffer from limitations introduced by artificial illumination required in hillshade or shaded relief images. When this technique is applied to lidar DTMs, layers of rock units with variable resistance to erosion can be clearly imaged, even in areas with limited outcrop. This technique enables one to collect comprehensive orientation data in areas of deformed sedimentary strata, assess the continuity of metamorphic and igneous rock units, and depict basement fracture sets. We demonstrate the use of texture shading in the Valley and Ridge of northern Pennsylvania, metamorphic rocks in the Berkshire Hills of western Massachusetts and Green Mountains of Vermont, and glacial deposits in the Finger Lakes region of upstate New York (northeastern United States).

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Journal articles on the topic 'Geology – Vermont – Champlain Valley'

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