DOCSLIB.ORG

The Surficial Geology and Pleistocene History of Vermont

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
The Surficial Geology and Pleistocene History of Vermont THE SURFICIAL GEOLOGY AND PLEISTOCENE HISTORY OF VERMONT By DAVII) P. STE\V\RT AND PATJL MAcCLINTOCK VERMONT GEOLOGICAL SURVEY ChARLES G. I)oIL, Slate Geologist 1)EPART lENT OF WATER RESOURCES MONTPELIER, VERMONT BULLETIN No. 31 1969 TABLE OF CONTENTS PAGE INTRODUCTION ...................... 15 Early Studies ...................... 15 The Scope of the Mapping Program ............ 19 Geomorphic and Tectonic Setting ............. 21 Acknowledgments .................... 23 SURFACE MATERIAL .................... 25 Till .......................... 25 Basal Till ...................... 26 Ablation Till ..................... 26 Glacio-Fluvial Deposits ................. 29 Kame Terraces .................... 29 Kame Moraines .................... 31 Eskers ........................ 31 Spillwav Gravel (Valley Trains) ............. 33 Lacustrine Sediment ................... 33 Local Origin I lvpothesis for the Lake Sediment....... 37 Marine Sediment . . . . . . . . . . . . . . . . . . . 39 GLACIAL AND GLACIO-FLUVIAL ERosIoN ........... 39 Glacial Erosion ..................... 39 Relative I lardness and Fabric of the Rock ........ 40 Major Topographic Features .............. 40 Erosional Topography ................. 40 Lake Basins ..................... 41 Mountain Gaps .................... 41 The Connecticut Valley ................ 41 The Vermont Valley .................. 42 Yellow I3og ...................... 12 Glacio-Fluvial Erosion .................. 42 Streams Beyond the Ice Margin . . . . . . . . . . . . 42 Subglacial, Englacial and Superglacial Streams ...... 13 Potholes ....................... 43 The Shattuck Mountain Channels ............ 43 PROBLEMS OF IDENTIFICATION AND CORREI.ATION OF l)RIFT SHEETS 44 Effects of Mountain Terrain ............... 44 Effects of Complex Bedrock ............... 45 Effects of Multiple Glaciation ............... 46 PAGE PAGE \ Conventional Field lethods that Proved Unsuccessful in Ver- Champlain Lowland ................... 111 ........................ 47 mont THE I3ITRLINGTON STAnK .................. 111 Physical Characteristics of the I)rift ........... 47 The Extent of the Burlington Glaciation .......... 113 Features Resulting from Glacial Erosion ......... 48 The Border of the Burlington Drift Sheet.......... 118 Features Resulting from Glacial Deposition ......... 48 Out\vash Deposits of the Burlington Stade ......... 125 Moraines ....................... 49 I linesburg Name Terraces ............... 125 Outwash Aprons . 49 Buck Hollow Name Terrace .............. 127 Boulder Trains and Indicator Fans ............ 49 Name Gravel of the Enoshurg Falls Quadrangle ...... 127 Organic Remains, I aleosol s, Interglacial Gravels and I3laek River Name Complex ............... 137 Weathering Profiles Between l)rift Sheets Name Deposits of the Newport Region ......... 137 TILL FAHRI(. ....................... 51 The Bristol-East Middleburv Name Terraces ....... 137 MULTIPLE GLAcI,TIox ................... Name Gravel in the Barre Area ............. 138 THE PLEISTOcENE SEIQI - ENCE IN Viiiox .......... 56 Name Terraces on the Green Mountain Slopes ...... 138 A lh)5SIHLE PEE-BENNINGTON GLAcI..L STADF ........ hIGH-LEVEL LAKES OF THE BURI.INGTON STADF ........ 139 THE BENNINGTON GLAcIAL STAnK .............. 61 high-Level Lakes of North Central Vermont ........ 139 Lake Bascom in the Bennington Region .......... 68 Stage I ....................... 143 THE \\E5T NORiVICH INTERSTAI)E .............. 70 lemphrcmagog Basin ................ 143 THE SIIELIIURNE GLAcIAL STADE .............. 70 Lamoille and Sto\ve Valleys ............. 143 Possibility of Two Northeast Tills ............. 79 Winooski \allev .................. 143 Alternate Interpretation I ............... 80 Stage II ....................... 145 Alternate Interpretation II ............... 80 Memphremagog Basin ................ 146 Alternate Interpretation III .............. 80 Lamoille Valley ................... 146 \ loraincs (.omposcd of Shelburne Till ........... 80 Sto\ve Valley .................... 146 loraines of the St. Johnshurv Region .......... 81 Winooski Valley .................. 149 Shelburne Moraines of the Rutland Region ........ 85 Stage III ....................... 149 \ loraines of the \ lanchester-l3ennington Region ..... 85 Memphremagog Basin ................ 15 1 Outwash l)eposits of Shelburne Age ............ 88 The Lamoille and Sto\ve Valleys ........... 152 Name Gravel 1)eposits ................. 88 \\inooski Valley .................. 1 53 Eskers ........................ 89 Stage IV ....................... 151 The Connecticut Valley Eskers ............ 91 Memphremagog Basin ................ 154 The Passumpsic Valley Esker ............. 91 Lamoille, Stowe and \Vinooski Valleys ......... 155 High-Level Ice-Contact Lakes of Shelburne Age ....... 93 Stage V ....................... 157 I Ugh-Level Lakes of the Connecticut River Valley 93 \1emphremagog Basin ................ 157 I ugh-Level Lakes of the Manchester-Bennington Region 95 Lamoille, Stowe and Winooski Valleys ......... 158 Eastern Margin of the Shelburne Drift ........... 97 The End of the hugh-Level Lakes ............ 158 Origin of the Northeast Fahric Along the Eastern Margin.. 98 I high-Level Lakes of Southern Vermont ........... 159 Piggy-Back-Ride Hypothesis ............. 98 LAKE \ERMONT ...................... 160 \Iarginal Shear I lvpothesis .............. 101 The Calving Retreat of the Burlington Glacier ....... 160 THE LAKE IIITcHCOCK INTERSTADF ............. 101 The Quaker Springs Stage ................ 163 PAGE PAGE FIGURE 1. Index map showing the area of Bennington surface till and the The Coveville Lake Stage 169 Shelburne drift border ................. 60 ................... The Fort Ann Stage 174 2. Lake Bascom in Vermont ................ 69 POST LAKE \ERMONT EROSION INTERVAL ........... 177 3. Moraines of Shelburne age in the St. Johnsbury region 81 THE CHAMPLAIN SEA INTERVAL ............... 179 4. Moraines and high-level lakes of the Shaftsbury-Manchester POST-GLACIAL TILTING OF THE LAKE AND SEA SHORELINES 183 region 86 ......... CORRELATION OF THE \ERMONT 1LEISTOCENE 184 5. Lake Shaftsbury in Vermont ............... 96 Probable Correlation with the St. Lawrence Lowland and ....... 99 6. Probable eastern border of the Shelburne drift ................ 184 Southeastern Quebec 104 7. Profile plot of the littoral sediments of Lake Hitchcock ................... 185 Burlington Till 186 8. Crests of the Green Mountains and gaps through which Burl- Shelburne Till 110 ington ice advanced Bennington Till .................... 187 9. Index map showing the Burlington drift border in the Rutland Conclusions 187 and Lake St. Catherine regions 112 Correlation with Other Areas of New England 188 10. Index map showing the Burlington drift border in the Bethel- .................... 189 Bennington Till 114 Brandon region ... ................. Shelbume Till 189 11. Index map showing the Burlington drift border in the Mont- Middletown-Cambridge Readvance 189 pelier region 115 BII3LIOGRAPHY 239 12. Index map showing the Burlington drift border in the Hard- wick-Morrisville region ................. 116 Appendices PAGE 13. Index map showing the Burlington drift border in the APPENDIX Memphremagog region ................. 117 Field data and calculated vector mean of fabrics of the Benning- A. 140 14. High-level lakes of north-central Vermont—Stage I . ton till ......................... 191 15. High-level lakes of north-central Vermont—Stage II . 142 B. Field data and calculated vector mean of fabrics of the Shel- 16. High-level lakes of north-central Vermont—Stage III . 144 burne till 200 17. High-level lakes of north-central Vermont—Stage IV . 147 Field data and calculated vector mean of fabrics of the Burling - C. 148 18. Iligh-level lakes of north-central Vermont—Stage V . ton till ......................... 215 D. Discussion of the glacial sequence in North America and New TABLE PAGE England. Reprinted from The Glacial Geology of Vermont 1. Field assistants that participated in the mapping program, the (Stewart, 1961) ..................... 224 year they worked and their present status 24 E. VECMAC program used to compute vector mean ...... 236 PLATE PAGE Illustrations I—Figure 1. FIGURE PAGE The crest of the Green Mountains in southern I. Index map showing the areas mapped by the participants in the Vermont. Hancock Mountain in foreground (Roches- mapping program 14 ter Quadrangle) ................ 20 2. Index map showing quadrangle names and locations . 17 Figure 2. 3. Index map showing the Physiographic Subdivisions of Vermont 18 The crest of the Green Mountains in the vicinity of 4. Stratigraphic units of the sections exposed along Stannard Mt. Snow (Mt. Pisgah). Picture taken looking north Brook 59 PLATE PAGE PLATE PAGE from the summit of Mt. Snow, elevation 3556 feet, VIII across the Somerset Reservoir (\Vilmington Quad- Fabrics of the Bennington till beyond the Shelburne rangle) 20 till border in the Wilmington-Brattleboro region . 65 11—Figure 1. Ix Slumping structure in lake sediment caused by the Fabrics of the Bennington till beyond the border of melting of ice in the underlying kame gravel. Two the Shelburne till in the Bennington area ...... 67 miles cast-southeast of Jericho Center (Camels X Hump Quadrangle) ............... 30 Northwest striae crossing northeast striae and Figure 2. earlier northwest striae. One-half mile west of The Four Varved and laminated lake sediment capped by Corners (Lyndonville
Load more

Recommended publications
  • Baseline Water Quality Inventory for the Southwest Alaska Inventory and Monitoring Network, Kenai Fjords National Park
    Baseline Water Quality Inventory for the Southwest Alaska Inventory and Monitoring Network, Kenai Fjords National Park Laurel A. Bennett National Park Service Southwest Alaska Inventory and Monitoring Network 240 W. 5th Avenue Anchorage, AK 99501 April 2005 Report Number: NPS/AKRSWAN/NRTR-2005/02 Funding Source: Southwest Alaska Network Inventory and Monitoring Program, National Park Service File Name: BennettL_2005_KEFJ_WQInventory_Final.doc Recommended Citation: Bennett, L. 2005. Baseline Water Quality Inventory for the Southwest Alaska Inventory and Monitoring Network, Kenai Fjords National Park. USDI National Park Service, Anchorage, AK Topic: Inventory Subtopic: Water Theme Keywords: Reports, inventory, freshwater, water quality, core parameters Placename Keywords: Alaska, Kenai Fjords National Park, Southwest Alaska Network, Aialik Bay, McCarty Fjord, Harrison Bay, Two Arm Bay, Northwestern Fjord, Nuka River, Delight Lake Kenai Fjords Water Quality Inventory - SWAN Abstract A reconnaissance level water quality inventory was conducted at Kenai Fjords National Park during May through July of 2004. This project was initiated as part of the National Park Service Vital Signs Inventory and Monitoring Program in an effort to collect water quality data in an area where little work had previously been done. The objectives were to collect baseline information on the physical and chemical characteristics of the water resources, and, where possible, relate basic water quality parameters to fish occurrence. Water temperatures in Kenai Fjords waters generally met the Alaska Department of Environmental Conservation (DEC) regulatory standards for both drinking water and growth and propagation of fish, shellfish, other aquatic life and wildlife. Water temperature standard are less than or equal to 13° C for spawning and egg and fry incubation, or less than or equal to 15° C for rearing and migration (DEC 2003).
    [Show full text]
  • A History of Connecticut's Long Island Sound Boundary
    The Catholic University of America, Columbus School of Law CUA Law Scholarship Repository Scholarly Articles and Other Contributions Faculty Scholarship 1972 A History of Connecticut's Long Island Sound Boundary Raymond B. Marcin The Catholic University of America, Columbus School of Law Follow this and additional works at: https://scholarship.law.edu/scholar Part of the Legal History Commons Recommended Citation Raymond B. Marcin, A History of Connecticut's Long Island Sound Boundary, 46 CONN. B.J. 506 (1972). This Article is brought to you for free and open access by the Faculty Scholarship at CUA Law Scholarship Repository. It has been accepted for inclusion in Scholarly Articles and Other Contributions by an authorized administrator of CUA Law Scholarship Repository. For more information, please contact [email protected]. 506 CONNECTICUT BAR JOURNAL [Vol. 46 A HISTORY OF CONNECTICUT'S LONG ISLAND SOUND BOUNDARY By RAYMOND B. MARciN* THE SCENEt Long before remembered time, ice fields blanketed central India, discharging floes into a sea covering the Plains of Punjab. The Argentine Pampas lay frozen and still beneath a crush of ice. Ice sheets were carving their presence into the highest mountains of Hawaii and New Guinea. On the western land mass, ice gutted what was, in pre-glacial time, a stream valley near the northeastern shore. In this alien epoch, when woolly mammoth and caribou roamed the North American tundra, the ice began to melt. Receding glaciers left an inland lake where the primeval stream valley had been. For a time the waters of the lake reposed in bo- real calm, until, with the melting of the polar cap, the level of the great salt ocean rose to the level of the lake.
    [Show full text]
  • Geography: Example Erosion
    The Physical and Human Causes of Erosion The Holderness Coast By The British Geographer Situation The Holderness coast is located on the east coast of England and is part of the East Riding of Yorkshire; a lowland agricultural region of England that lies between the chalk hills of the Wolds and the North Sea. Figure 1 The Holderness Coast is one of Europe's fastest eroding coastlines. The average annual rate of erosion is around 2 metres per year but in some sections of the coast, rates of loss are as high as 10 metres per year. The reason for such high rates of coastal erosion can be attributed to both physical and human causes. Physical Causes The main reason for coastal erosion at Holderness is geological. The bedrock is made up of till. This material was deposited by glaciers around 12,000 years ago and is unconsolidated. It is made up of mixture of bulldozed clays and erratics, which are loose rocks of varying type. This boulder clay sits on layer of seaward sloping chalk. The geology and topography of the coastal plain and chalk hills can be seen in figure 2. Figure 2 The boulder clay with erratics can be seen in figure 3. As we can see in figures 2 and 3, the Holderness Coast is a lowland coastal plain deposited by glaciers. The boulder clay is experiencing more rapid rates of erosion compared to the chalk. An outcrop of chalk can be seen to the north and forms the headland, Flamborough Head. The section of coastline is a 60 kilometre stretch from Flamborough Head in the north to Spurn Point in the south.
    [Show full text]
  • An Esker Group South of Dayton, Ohio 231 JACKSON—Notes on the Aphididae 243 New Books 250 Natural History Survey 250
    The Ohio Naturalist, PUBLISHED BY The Biological Club of the Ohio State University. Volume VIII. JANUARY. 1908. No. 3 TABLE OF CONTENTS. SCHEPFEL—An Esker Group South of Dayton, Ohio 231 JACKSON—Notes on the Aphididae 243 New Books 250 Natural History Survey 250 AN ESKER GROUP SOUTH OF DAYTON, OHIO.1 EARL R. SCHEFFEL Contents. Introduction. General Discussion of Eskers. Preliminary Description of Region. Bearing on Archaeology. Topographic Relations. Theories of Origin. Detailed Description of Eskers. Kame Area to the West of Eskers. Studies. Proximity of Eskers. Altitude of These Deposits. Height of Eskers. Composition of Eskers. Reticulation. Rock Weathering. Knolls. Crest-Lines. Economic Importance. Area to the East. Conclusion and Summary. Introduction. This paper has for its object the discussion of an esker group2 south of Dayton, Ohio;3 which group constitutes a part of the first or outer moraine of the Miami Lobe of the Late Wisconsin ice where it forms the east bluff of the Great Miami River south of Dayton.4 1. Given before the Ohio Academy of Science, Nov. 30, 1907, at Oxford, O., repre- senting work performed under the direction of Professor Frank Carney as partial requirement for the Master's Degree. 2. F: G. Clapp, Jour, of Geol., Vol. XII, (1904), pp. 203-210. 3. The writer's attention was first called to the group the past year under the name "Morainic Ridges," by Professor W. B. Werthner, of Steele High School, located in the city mentioned. Professor Werthner stated that Professor August P. Foerste of the same school and himself had spent some time together in the study of this region, but that the field was still clear for inves- tigation and publication.
    [Show full text]
  • Champlain Valley (Why Are Clay Soils Where They Are?)
    Geomorphic history of the Champlain Valley (why are clay soils where they are?) part 1) How did landscape evolve and where do “clay” minerals come from? part 2) How were they deposited in Lake Vermont/ Champlain Sea? part 3) Can we predict the distribution of “clay” thickness? (…can we compare prediction with what people observe) 500,000,000 years Today ~500,000,000 years: Sediments of “Champlain Valley Sequence” deposited on shoreline of ancient ocean Monkton quartzite + Taconic Slates Limestones + Marbles ~460,000,000 years: Collision of island arc causes thrusting + metamorphism Champlain Thrust Fault Champlain Thrust: -Exposed at Snake Mtn + Mt. Philo -delineates boundary between “low” and “mid” grade metamorphic rocks -Marbles pf middlebury syncline folded along back of thrust -Topography of Addison County reflects erodibility of bedrock: T1: lower surface: “low grade” sedimentary rocks below thrust (e.g. shale) T2: upper surface: “mid grade” meta-sedimentary rocks above thrust (e.g. marble) Green Mountains= “high grade” metamorphic rocks (e.g. schist and gneiss) T1 T2 Green Mtn gneiss Geologic map of Addison County Taconics Part 2: How were clays deposited in Lake Vermont and the Champlain Sea? 500,000,000 years Today ~96,000 - 20,000 years (i.e. yesterday…): Champlain Valley sat below 1-3 km of ice Soils and clay minerals from previous inter-glacial cycles were stripped by advancing glaciers Rocks were ground into “clay size fraction” and trapped under ice retreating glacial ice withdrew from Champlain Valley between ~14-13 kyr Many depositional features in Champlain Valley record ice retreat -Layers of “basal till” deposited beneath ice sheets (coarse, angular, poorly sorted debris) -Meltwater streams flow between glacier and hillslopes -Sedimentary deposits accumulate, leaving ‘kame terraces’ when glacier retreats Lake Vermont had 2+ stages: Coveville: Ice dammed in So.
    [Show full text]
  • THE HISTORY and LAW of VERMONT TOWN ROADS (11.3.14 Version)
    THE HISTORY AND LAW OF VERMONT TOWN ROADS (11.3.14 version) Author: Paul S. Gillies Montpelier, Vermont This article is made available to the Vermont Agency of Transportation Mapping Section website courtesy of the author - November 2014 The History and Law of Vermont Town Roads THE HISTORY AND LAW OF VERMONT TOWN ROADS (11.3.14 version) 1. Introduction In the beginning there was the landscape, crushed and folded and drained. The valleys and the mountains and the waters determined how people moved on that landscape, by foot or horse or canoe, for thousands of years. Animal paths became foot paths for human traffic, and horses. When settlers arrived, the paths grew into trails, which became town roads. The road network is a town’s history carved in dirt and gravel. There is no more permanent monument to the first settlers. Buildings collapse, are abandoned or replaced. Landscapes change from open to wooded in a few years. But highways rarely change. They may stray from their original beds, as sharp corners get rounded and wet spots are avoided, but they leave deep creases on the face of the town. Until something happens, we take roads for granted. When a bridge goes out, a stretch of gravel road is swept away in a flood, the snow accumulates in high drifts, when the roadbed is deep with mud or ribbed for our jostling pleasure, only then do we think about these ribbons of public property. In law, they are called public easements or public rights-of-way. Other than schools, the most important function of local government is maintenance of highways.
    [Show full text]
  • LESSON PLAN #2: Creating the Driftless: a Study in Glacial Movement
    LESSON PLAN #2: Creating the Driftless: A Study in Glacial Movement Overview: Glaciers are moving mountains of ice. They move like slow rivers and actually flow. Gravity and the sheer weight of the ice mass are the causes of glacial motion. Ice is softer than rock so is easily deformed by the pressure of its own weight. Movement at the underside of a glacier is slower than movement along the top. Glaciers retreat and advance, depending on snow accumulation, evaporation, or ice melt. Glaciers transport materials as they move. They also sculpt and carve the land beneath them. A glacier’s weight combined with gradual movement, reshapes the land over hundreds to thousands of years. The ice erodes the land surface and carries broken rock and soil debris far from their original places, resulting in some interesting glacial landforms. Due to the nature of land formations, some areas in northwest Illinois along with southwest Wisconsin, southeast Minnesota, and northeast Iowa were missed by the four glaciers that at different times covered the rest of these states. This area not covered by glaciers and the resulting glacial drift is called “The Driftless Area.” This Driftless Area is rich with historic and geological information free from glacial impact. Duration: 30 minutes Subject Areas: Earth Science, Physical Science, Geography Standards Addressed: 4-PS3-1 4-PS3-4 5-ESS3-1 MS-ESS3-1 MS-ESS2-5 MS-ESS2-3 MS-ESS1-C MS-PS2-4 Objectives: Gain an understanding of how glaciers move Understand the types of landforms created from glacial movement and glacial scraping Define what is meant by The Driftless Area Teacher Background: Glaciers are made up of fallen snow that, over many years, compresses into large, thickened ice masses.
    [Show full text]
  • The Geology of the Saddleback Mountain Area, Northwood Quadrangle, Southeastern New Hampshire
    University of New Hampshire University of New Hampshire Scholars' Repository New England Intercollegiate Geological NEIGC Trips Excursion Collection 1-1-1984 The geology of the Saddleback Mountain Area, Northwood quadrangle, southeastern New Hampshire Whitaker, Laura R. Follow this and additional works at: https://scholars.unh.edu/neigc_trips Recommended Citation Whitaker, Laura R., "The geology of the Saddleback Mountain Area, Northwood quadrangle, southeastern New Hampshire" (1984). NEIGC Trips. 352. https://scholars.unh.edu/neigc_trips/352 This Text is brought to you for free and open access by the New England Intercollegiate Geological Excursion Collection at University of New Hampshire Scholars' Repository. It has been accepted for inclusion in NEIGC Trips by an authorized administrator of University of New Hampshire Scholars' Repository. For more information, please contact [email protected]. B6-1 207 THE GEOLOGY OF THE SADDLEBACK MOUNTAIN AREA, NORTHWOOD QUADRANGLE, SOUTHEASTERN NEW HAMPSHIRE Laura R. Whitaker Department of Geology The College of Charleston Charleston. SC 2942^ Introduction Saddleback Mountain is a four-peaked saddle-shapped mountain located 39 km west of Portsmouth, NH (Figure 1). The mountain lies along the boundary between the New England Uplands and the Seaboard Lowlands Sections of the New England Physiographic Province of Fenneman (1938). It also lies adjacent to the western boundary of the Massabesic Gneiss Complex as designated by Anderson (1978). Figure 2 of this text is a generalized Geologic Map of Southeastern New Hampshire compiled from Billings (1956) and later workers cited in the references from Figure 1. Portions of Figure 2 show that the Saddleback Mountain area is on strike with two convergent fault zones which are postulated to be of regional tectonic significance: the Nurambego of southern Maine (Hussey and Pankiwskyj, 1976; Hussey and Newberg, 1978), and the Pinnacle-Campbell-Hill-Hall Mountain Faults mapped by Camein (1976).
    [Show full text]
  • Trip F the PINNACLE HILLS and the MENDON KAME AREA: CONTRASTING MORAINAL DEPOSITS by Robert A
    F-1 Trip F THE PINNACLE HILLS AND THE MENDON KAME AREA: CONTRASTING MORAINAL DEPOSITS by Robert A. Sanders Department of Geosciences Monroe Community College INTRODUCTION The Pinnacle Hills, fortunately, were voluminously described with many excellent photographs by Fairchild, (1923). In 1973 the Range still stands as a conspicuous east-west ridge extending from the town of Brighton, at about Hillside Avenue, four miles to the Genesee River at the University of Rochester campus, referred to as Oak Hill. But, for over thirty years the Range was butchered for sand and gravel, which was both a crime and blessing from the geological point of view (plates I-VI). First, it destroyed the original land form shapes which were subsequently covered with man-made structures drawing the shade on its original beauty. Secondly, it allowed study of its structure by a man with a brilliantly analytical mind, Herman L. Fair­ child. It is an excellent example of morainal deposition at an ice front in a state of dynamic equilibrium, except for minor fluctuations. The Mendon Kame area on the other hand, represents the result of a block of stagnant ice, probably detached and draped over drumlins and drumloidal hills, melting away with tunnels, crevasses, and per­ foration deposits spilling or squirting their included debris over a more or less square area leaving topographically high kames and esker F-2 segments with many kettles and a large central area of impounded drainage. There appears to be several wave-cut levels at around the + 700 1 Lake Dana level, (Fairchild, 1923). The author in no way pretends to be a Pleistocene expert, but an attempt is made to give a few possible interpretations of the many diverse forms found in the Mendon Kames area.
    [Show full text]
  • The Character of Vermont : Twentieth-Anniversary Reflections Michael Sherman
    University of Vermont ScholarWorks @ UVM Center for Research on Vermont Occasional Papers Research Centers and Institutes 1996 The character of Vermont : twentieth-anniversary reflections Michael Sherman Jennie G. Versteeg Samuel B. Hand Paul S. Gillies Follow this and additional works at: https://scholarworks.uvm.edu/crvocc Recommended Citation Sherman, Michael; Versteeg, Jennie G.; Hand, Samuel B.; and Gillies, Paul S., "The character of Vermont : twentieth-anniversary reflections" (1996). Center for Research on Vermont Occasional Papers. 5. https://scholarworks.uvm.edu/crvocc/5 This Article is brought to you for free and open access by the Research Centers and Institutes at ScholarWorks @ UVM. It has been accepted for inclusion in Center for Research on Vermont Occasional Papers by an authorized administrator of ScholarWorks @ UVM. For more information, please contact [email protected]. OCCASIONAL PAPER #19 CENTER FOR RESEARCH ON VERMONT UNIVERSITY OF VERMONT BURLINGTON, VERMONT . ... : . ~.._ - - THE CHARACTER OF VERMONT Twentieth-Anniversary Reflections By MICHAEL SHERMAN and JENNIE VERSTEEG SAMUEL B. HAND and PAUL GILLIES WILB F ,Sfen 19'/b ~ ./ © 1996 by the University of Vermont. All rights reserved ISBN 0-944277-34-9 The Center for Research on Vermont University of Vermont Burlington, VT 05401-3439 802/656-43 89 email: [email protected] ...Wil!Ul CuONiVITi"iT LU CTIO yN J Of V!l!AONT l1 81A!T Contents Foreword Paul Eschholz . v11 Part 1 The Character of Vermont: Then and Now The Character of Vermont: Then and Now Michael Sherman and Jennie Versteeg . 1 Appendix 1. Taylor's "Sample" of Vermonters .............. ... ...... 35 Appendix 2. Taylor's Respondents ...........
    [Show full text]
  • Newtown Linford Village Design Statement 2008
    Newtown Linford Village Design Statement 2008 Newtown Linford Village Design Statement 2008 Contents Title Page Executive summary 2-6 The Purpose of this Village Design Statement 7 1. Introduction 8 The purpose and use of this document. Aims and objectives 2. The Village Context 9-10 Geographical and historical background The village today and its people Economics and future development 3. The Landscape Setting Visual character of the surrounding countryside 11-12 Relationship between the surrounding countryside and the village periphery Landscape features Buildings in the landscape 4. Settlement Pattern and character 13-15 Overall pattern of the village Character of the streets and roads through the village Character and pattern of open spaces 5. Buildings & Materials in the Village 16-26 1. The challenge of good design 2. Harmony, the street scene 3. Proportions 4. Materials 5. Craftsmanship 6. Boundaries 7. Local Businesses 8. Building guidelines 6. Highways and Traffic 27-29 Characteristics of the roads and Footpaths Street furniture, utilities and services 7. Wildlife and Biodiversity 30-32 8. Acknowledgments 33 9. Appendix 1 Map of Village Conservation Area 34 Listed Buildings in the Village 35 10. Appendix 2 Map of the SSSI & Local Wildlife Sites 36 Key to the SSSI & Local Wildlife Sites 37-38 “Newtown Linford is a charming place with thatched and timbered dwellings, an inviting inn and a much restored medieval church in a peaceful setting by the stream - nor is this all, for the village is the doorstep to Bradgate Park, one of Leicestershire’s loveliest pleasure grounds,... … … with the ruins of the home of the ill fated nine days queen Lady Jane Grey” Arthur Mee - “Leicestershire” - Hodder and Stoughton.
    [Show full text]
  • Bedrock Valleys of the New England Coast As Related to Fluctuations of Sea Level
    Bedrock Valleys of the New England Coast as Related to Fluctuations of Sea Level By JOSEPH E. UPSON and CHARLES W. SPENCER SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY GEOLOGICAL SURVEY PROFESSIONAL PAPER 454-M Depths to bedrock in coastal valleys of New England, and nature of sedimentary Jill resulting from sea-level fluctuations in Pleistocene and Recent time UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1964 UNITED STATES DEPARTMENT OF THE INTERIOR STEWART L. UDALL, Secretary GEOLOGICAL SURVEY Thomas B. Nolan, Director The U.S. Geological Survey Library has cataloged this publication, as follows: Upson, Joseph Edwin, 1910- Bedrock valleys of the New England coast as related to fluctuations of sea level, by Joseph E. Upson and Charles W. Spencer. Washington, U.S. Govt. Print. Off., 1964. iv, 42 p. illus., maps, diagrs., tables. 29 cm. (U.S. Geological Survey. Professional paper 454-M) Shorter contributions to general geology. Bibliography: p. 39-41. (Continued on next card) Upson, Joseph Edwin, 1910- Bedrock valleys of the New England coast as related to fluctuations of sea level. 1964. (Card 2) l.Geology, Stratigraphic Pleistocene. 2.Geology, Stratigraphic Recent. S.Geology New England. I.Spencer, Charles Winthrop, 1930-joint author. ILTitle. (Series) For sale by the Superintendent of Documents, U.S. Government Printing Office Washington, D.C. 20402 CONTENTS Page Configuration and depth of bedrock valleys, etc. Con. Page Abstract.__________________________________________ Ml Buried valleys of the Boston area. _ _______________
    [Show full text]