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1 Recognising Glacial Features. Examine the Illustrations of Glacial Landforms That Are Shown on This Page and on the Next Page
1 Recognising glacial features. Examine the illustrations of glacial landforms that are shown on this C page and on the next page. In Column 1 of the grid provided write the names of the glacial D features that are labelled A–L. In Column 2 indicate whether B each feature is formed by glacial erosion of by glacial deposition. A In Column 3 indicate whether G each feature is more likely to be found in an upland or in a lowland area. E F 1 H K J 2 I 24 Chapter 6 L direction of boulder clay ice flow 3 Column 1 Column 2 Column 3 A Arête Erosion Upland B Tarn (cirque with tarn) Erosion Upland C Pyramidal peak Erosion Upland D Cirque Erosion Upland E Ribbon lake Erosion Upland F Glaciated valley Erosion Upland G Hanging valley Erosion Upland H Lateral moraine Deposition Lowland (upland also accepted) I Frontal moraine Deposition Lowland (upland also accepted) J Medial moraine Deposition Lowland (upland also accepted) K Fjord Erosion Upland L Drumlin Deposition Lowland 2 In the boxes provided, match each letter in Column X with the number of its pair in Column Y. One pair has been completed for you. COLUMN X COLUMN Y A Corrie 1 Narrow ridge between two corries A 4 B Arête 2 Glaciated valley overhanging main valley B 1 C Fjord 3 Hollow on valley floor scooped out by ice C 5 D Hanging valley 4 Steep-sided hollow sometimes containing a lake D 2 E Ribbon lake 5 Glaciated valley drowned by rising sea levels E 3 25 New Complete Geography Skills Book 3 (a) Landform of glacial erosion Name one feature of glacial erosion and with the aid of a diagram explain how it was formed. -
Landtype Associations (Ltas) of the Northern Highland Scale: 1:650,000 Wisconsin Transverse Mercator NAD83(91) Map NH3 - Ams
Landtype Associations (LTAs) of the Northern Highland Scale: 1:650,000 Wisconsin Transverse Mercator NAD83(91) Map NH3 - ams 212Xb03 212Xb03 212Xb04 212Xb05 212Xb06 212Xb01 212Xb02 212Xb02 212Xb01 212Xb03 212Xb05 212Xb03 212Xb02 212Xb 212Xb07 212Xb07 212Xb01 212Xb03 212Xb05 212Xb07 212Xb08 212Xb03 212Xb07 212Xb07 212Xb01 212Xb01 212Xb07 Landtype Associations 212Xb01 212Xb01 212Xb02 212Xb03 212Xb04 212Xb05 This map is based on the National Hierarchical Framework of Ecological Units 212Xb06 (NHFEU) (Cleland et al. 1997). 212Xb07 The ecological landscapes used in this handbook are based substantially on 212Xb08 Subsections of the NHFEU. Ecological landscapes use the same boundaries as NHFEU Sections or Subsections. However, some NHFEU Subsections were combined to reduce the number of geographical units in the state to a manageable Ecological Landscape number. LTA descriptions can be found on the back page of this map. County Boundaries 0 2.75 5.5 11 16.5 22 Miles Sections Kilometers Subsections 0 4 8 16 24 32 Ecological Landscapes of Wisconsin Handbook - 1805.1 WDNR, 2011 Landtype Association Descriptions for the Northern Highland Ecological Landscape 212Xb01 Northern Highland Outwash The characteristic landform pattern is undulating pitted and unpitted Plains outwash plain with swamps, bogs, and lakes common. Soils are predominantly well drained sandy loam over outwash. Common habitat types include forested lowland, ATM, TMC, PArVAa and AVVb. 212Xb02 Vilas-Oneida Sandy Hills The characteristic landform pattern is rolling collapsed outwash plain with bogs common. Soils are predominantly excessively drained loamy sand over outwash or acid loamy sand debris flow. Common habitat types include PArVAa, ArQV, forested lowland, AVVb and TMC. 212Xb03 Vilas-Oneida Outwash Plains The characteristic landform pattern is nearly level pitted and unpitted outwash plain with bogs and lakes common. -
Glacial Terminology
NRE 430 / EEB 489 D.R. Zak 2003 Lab 1 Glacial Terminology The last glacial advance in Michigan is known as the Wisconsin advance. The late Wisconsin period occurred between 25,000 and 10,000 years ago. Virtually all of Michigan's present surface landforms were shaped during this time. A. Glacial Materials Glacial Drift: material transported and deposited by glacial action. Note that most glacial features are recessional, i.e., they are formed by retreating ice. Materials deposited during glacial advance are usually overridden and destroyed or buried before the glacier has reached its maximum. Till: unstratified drift (e.g., material not organized into distinct layers), ice-transported, highly variable, may consist of any range of particles from clay to boulders. Ice-deposited material is indicated by random assemblage of particle sizes, such as clay, sand and cobbles mixed together. Ice-worked material is indicated by sharp-edged or irregular shaped pebbles and cobbles, formed by the coarse grinding action of the ice. Outwash: stratified drift (e.g., material organized into distinct horizontal layers or bands), water-transported, consists mainly of sand (fine to coarse) and gravel rounded in shape. Meltwater streams flowing away from glacier as it recedes carries particles that are sorted by size on deposition dependent upon the water flow velocity – larger particles are deposited in faster moving water. Water-deposited material is indicated by stratified layers of different sized sand particles and smooth rounded pebbles, consistent in size within each band. Water-worked material is indicated by smooth, rounded particles, formed by the fine grinding action of particles moved by water. -
Geologic Site of the Month: Maine's Glacial Moraines: Living on the Edge
Maine's Glacial Moraines: Living on the Edge Maine Geological Survey Maine Geologic Facts and Localities January, 2000 Maine's Glacial Moraines: Living on the Edge Text by Woodrow Thompson Maine Geological Survey, Department of Agriculture, Conservation & Forestry 1 Maine's Glacial Moraines: Living on the Edge Maine Geological Survey Introduction Toward the end of the "Ice Age," a glacier of vast proportions covered Maine. This was the Laurentide Ice Sheet, which advanced southward out of Canada about 25,000 years ago and remained here for nearly 15,000 years. The slowly flowing ice was thick enough to cover Maine's highest mountains. It swept away much of the evidence of earlier glaciations, eroding both the bedrock and previously existing sediment cover. Many glacial features that we see today were actually left behind during the final northward retreat of the ice sheet, when the pulverized rock debris was released from the melting ice. Even as the ice margin withdrew, internal flow within the glacier continued to transport its sediment load southward toward the edge of the ice sheet. Through a variety of processes, this dirty material was either released directly from the ice, forming a stony deposit called "till," or washed out of the glacier in meltwater streams. The water-laid sediments were deposited as layered accumulations in river valleys, lake basins, and Maine's coastal lowland. They include the majority of our sand and gravel deposits, and the finer silts and clays commonly found near the coast. Maine Geological Survey, Department of Agriculture, Conservation & Forestry 2 Maine's Glacial Moraines: Living on the Edge Maine Geological Survey Introduction The clearest markers of glacial retreat are ridges of sediment called "end moraines," which will be referred to here as simply "moraines" (Figure 1). -
Kettle Moraine State Forest T Glenbeulah Northern Unit Glen Rd
to Elkhart Lake CCC C C P Kettle Moraine State Forest T Glenbeulah Northern Unit Glen Rd. Camp Evelyn Rd. Sugarbush Rd. Designated Trails and Public Use Areas Old Wade House State Historic Site 23 A . d R S e g d i P . R Rd to Center Rd. nk Pla Fond du Lac Greenbush 23 23 to Plymouth G . r T D Spring Valley Rd. e n i a r A o M . e l d t t R e Mullet Creek K Greenbush Outdoor e g State Group Camp id R Wildlife Area Hill Top Rd. Z Greenbush Greenbush T Trail Area Kettle U ZZ Summit Rd. 5 Graham T Corners Mullet Lk. A to Plymouth Forest Dr. 67 S Watercress Rd. G Dog Training Area (field) U Armstrong 67 Woodside Rd. U V Parnell 4 Trail B Johnson Area Log Cabin Rd. Cabin Log Hill Parnell Tower Glacier Rd. Glacier Clems Rd. Kettle View Rd. Rd. Lane Cedar SHEBOYGAN CO. SHEBOYGAN FOND DU LAC CO. LAC DU FOND Conner Rd. Shamrock Garriety Hill Hill N Scenic Dr. A Chinatown Lakeview Rd. Nichols Creek State Wildlife Mc Mullen Hill Areas Long V Deer Rd. V is ta Lk. Rd. Division Ash Rd. D r . 67 Long Lake Spruce Recreation Parnell Lk. Area Rd. Slatts Rd. Hughview V S . r D Butler P d Butler Lk. R a n d. d. rne to a l l t R Lk. l R d r d. o po A Cascade o ir A Dr. Scenic W Mud Lk. Butler Lake Trail Area Pine Rd. -
VACATION LAND the National Forests in Oregon
VACATION LAND The National Forests in Oregon High up in the mountains, where the timber is scarce and stunted and the only means of transportation is by horseback United States Department of Agriculture::Forest Service 1919 WELCOME TO THE ATIONAL PORESTS U.S.DEPARTVENT OFAGRICULTURE FOREST SIEIRVICE UNITED STATES DEPARTMENT OF AGRICULTURE DEPARTMENT CIRCULAR 4 Contribution from the Forest Service HENRY S. GRAVES. Forester DIRECTORY OF NATIONAL FORESTS IN OREGON. George H. Cecil, District Forester. District Office, Post Office Building, Portland, Oreg. NATIONAL FOREST. FOREST SUPERVISOR. HEADQUARTERS. Cascade C. R. Seitz Eugene, Oreg. 2- Crater H B Rankin Medford, Oreg. Deschutes N. G. Jacobson Bend, Oreg. H Fremont...... Gilbert D. Brown Lakeview, Oreg. -Maiheur Cy J. Bingham John Day, Oreg. L-Milaam R. M. Evans.... Baker, Oreg. - Ochoco.. V. V. Harpham Prineville, Oreg. Oregon H. Sherrard...... Portland, Oreg. Santiam C. C. Hall.. Albany, Oreg. -Siskiyou.... N. F. Macduff Grants Pass, Oreg. Siuslaw R. S. Shelley Eugene, Oreg. \-Umati1la W. W. Cryder Pendleton, Oreg. 13 .Umpqua C. Bartrum Roseburg, Oreg. j Wallowa H. W. Harris Wallowa, Oreg. S'Wenaha J. C. Kulins Walla Walla, Wash. l,Whitman R. M. Evans.... Baker, Oreg. The view on page s of the cover is a reprodtction from a photograph of Mount Jefferson, Sautiam National Forest, showing forest and snow peak. THE NATIONAL VACATION 1 ANDESTS IN OREGON AN IDEAL VACATION LAND HEN, tired of the daily grind, you say to yourself, "I need a vacation," your first thought is to get away from civili- zation and its trammels.Your next is to find interest- ing and health-giving recreation.In the National For- ests in Oregon you may find both, and much besides. -
Glaciers and Glacial Erosional Landforms
GLACIERS AND GLACIAL EROSIONAL LANDFORMS Dr. NANDINI CHATTERJEE Associate Professor Department of Geography Taki Govt College Taki, North 24 Parganas, West Bengal Part I Geography Honours Paper I Group B -Geomorphology Topic 5- Development of Landforms GLACIER AND ICE CAPS Glacier is an extended mass of ice formed from snow falling and accumulating over the years and moving very slowly, either descending from high mountains, as in valley glaciers, or moving outward from centers of accumulation, as in continental glaciers. • Ice Cap - less than 50,000 km2. • Ice Sheet - cover major portion of a continent. • Ice thicker than topography. • Ice flows in direction of slope of the glacier. • Greenland and Antarctica - 3000 to 4000 m thick (10 - 13 thousand feet or 1.5 to 2 miles!) FORMATION AND MOVEMENT OF GLACIERS • Glaciers begin to form when snow remains Once the glacier becomes heavy enough, it in the same area year-round, where starts to move. There are two types of enough snow accumulates to transform glacial movement, and most glacial into ice. Each year, new layers of snow bury movement is a mixture of both: and compress the previous layers. This Internal deformation, or strain, in glacier compression forces the snow to re- ice is a response to shear stresses arising crystallize, forming grains similar in size and from the weight of the ice (ice thickness) shape to grains of sugar. Gradually the and the degree of slope of the glacier grains grow larger and the air pockets surface. This is the slow creep of ice due to between the grains get smaller, causing the slippage within and between the ice snow to slowly compact and increase in crystals. -
Glaciers of the Canadian Rockies
Glaciers of North America— GLACIERS OF CANADA GLACIERS OF THE CANADIAN ROCKIES By C. SIMON L. OMMANNEY SATELLITE IMAGE ATLAS OF GLACIERS OF THE WORLD Edited by RICHARD S. WILLIAMS, Jr., and JANE G. FERRIGNO U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1386–J–1 The Rocky Mountains of Canada include four distinct ranges from the U.S. border to northern British Columbia: Border, Continental, Hart, and Muskwa Ranges. They cover about 170,000 km2, are about 150 km wide, and have an estimated glacierized area of 38,613 km2. Mount Robson, at 3,954 m, is the highest peak. Glaciers range in size from ice fields, with major outlet glaciers, to glacierets. Small mountain-type glaciers in cirques, niches, and ice aprons are scattered throughout the ranges. Ice-cored moraines and rock glaciers are also common CONTENTS Page Abstract ---------------------------------------------------------------------------- J199 Introduction----------------------------------------------------------------------- 199 FIGURE 1. Mountain ranges of the southern Rocky Mountains------------ 201 2. Mountain ranges of the northern Rocky Mountains ------------ 202 3. Oblique aerial photograph of Mount Assiniboine, Banff National Park, Rocky Mountains----------------------------- 203 4. Sketch map showing glaciers of the Canadian Rocky Mountains -------------------------------------------- 204 5. Photograph of the Victoria Glacier, Rocky Mountains, Alberta, in August 1973 -------------------------------------- 209 TABLE 1. Named glaciers of the Rocky Mountains cited in the chapter -
GLACIATION in SNOWDONIA by Paul Sheppard
GeoActiveGeoActive 350 OnlineOnline GLACIATION IN SNOWDONIA by Paul Sheppard This unit can be used These remnants of formerly much higher mountains have since been independently or in Conwy conjunction with OS 1:50,000 eroded into what is seen today. The Bangor mountains of Snowdonia have map sheet 115. N Caernarfon Llanrwst been changed as a result of aerial Llanberis Capel Curig Snowdon Betws y Coed (climatic) and fluvial (water) HE SNOWDONIA OR ERYRI (Yr Wyddfa) Beddgelert Blaenau erosion that always act upon a NATIONAL PARK, established Ffestiniog T Porthmadog landscape, but in more recent SNOWDONIA Y Bala in 1951, was the third National NATIONAL Harlech geological times the effects of ice PARK Park to be established in England have had a major impact upon the and Wales following the 1949 Barmouth Abermaw Dolgellau actual land surface. National Parks and Access to the Cadair Countryside Act (Figure 1). It Idris Tywyn 2 Machynlleth Glaciation covers an area of 2,171 km (838 Aberdyfi 0 25 km square miles) of North Wales and Ice ages have been common in the British Isles and northern Europe, encompasses the Carneddau and Figure 1: Snowdonia National Park Glyderau mountain ranges. It also with 40 having been identified by includes the highest mountain in important to look first at the geologists and geomorphologists. England and Wales, with Mount geological origins of the area, as The most recent of these saw Snowdon (Yr Wyddfa in Welsh) this provides the foundation upon Snowdonia covered with ice as reaching a height of 1,085 metres which ice can act. -
Submarine Glacial Landforms in Southeast Greenland Fjords Reveal Contrasting Outlet-Glacier Behaviour Since the Last Glacial Maximum C
EGU2020: Sharing Geoscience Online Submarine glacial landforms in Southeast Greenland fjords reveal contrasting outlet-glacier behaviour since the Last Glacial Maximum C. L. Batchelor 1,2 J. A. Dowdeswell2, E. Rignot3,4, R. Millan3 1 2 3 4 Email: [email protected] 1. We use bathymetric data to investigate the deglacial history of SE Greenland • The SE Greenland margin (Fig. 1), (a) (b) (c) which includes the Julianehåb Ice Cap (JIC), is suggested to have been sensitive to past climatic changes (Bjørk et al., 2012). • Mountainous terrain and a lack of ice-free areas have hitherto largely prevented analysis of the deglacial and Holocene behaviour of SE Greenland’s marine-terminating outlet glaciers. • We use bathymetric data, from NASA’s Oceans Melting Greenland (OMG) mission and from gravity inversion derived from Operation Fig. 1. (a) Map of SE Greenland and major ocean currents. (b) and (c) Maps of the SE Greenland margin Icebridge gravity data (Millan et al., and the Julianehåb Ice Cap (JIC), respectively, showing OMG bathymetric data and the distribution of 2018), to map the distribution of submarine moraines. Background is IBCAO bathymetry (Jakobsson et al., 2012). Yellow circles are submarine moraines (Fig. 1). published 10Be and 14C deglacial ages (Bennike and Björck, 2002; Weidick et al., 2004; Roberts et al., 2008; Larsen et al., 2011; Dyke et al., 2014; Winsor et al., 2014). Adapted from Batchelor et al. (2019). 2. Inner-fjord moraines exist in many SE Greenland fjords (a) b • Major moraine ridges exist in an inner‐fjord (landward third of the fjord length) setting for 26 (~65%) of the surveyed fjords of SE Greenland, including beyond the JIC (Fig. -
Rogen Moraine: an Example of Glacial Reshaping of Pre-Existing Landforms
ARTICLE IN PRESS Quaternary Science Reviews 25 (2006) 362–389 Rogen moraine: an example of glacial reshaping of pre-existing landforms Per Mo¨llerà GeoBiosphere Science Centre/Quaternary Sciences, Lund University, So¨lvegatan 12, SE-22362 Lund, Sweden Received 23 May 2004; accepted 19 January 2005 Abstract Rogen moraine is widely distributed in the core areas of the former Scandinavian and Laurentide ice sheets. It is generally agreed upon that these gently arched, ice-flow transverse ridges can be used in reconstructions of paleo-ice-flow patterns and that they indicate a melted-bed or poly-thermal basal ice regime. However, the processes of ridge generation have been contentious. This study proposes a two-stage formation of Rogen moraine, based on detailed sedimentological and structural investigations in excavated trenches in a Rogen moraine landscape in the province of Dalarna, central Sweden. Field data suggest that Rogen moraine ridges are the reshaped remains of pre-existing transverse moraine ridges, originally deposited from ice-cored moraines in an ice-marginal zone. Due to back- and down-wasting of ice-cores, inter-ridge troughs were filled with debris flow and fluvial deposits, which after landscape inversion were transformed to areas of transverse and hummocky moraines. It is proposed that this primary landscape formation occurred during an Early Weichselian deglaciation. This relict landscape was later preserved beneath cold-based Mid- to Late-Weichselian ice sheet(s), which turned wet-based during the Preboreal deglaciation phase and re-moulded the precursor landforms into Rogen moraine. r 2005 Elsevier Ltd. All rights reserved. 1. Introduction transition to drumlins (Lundqvist, 1969, 1989), some- times with streamlined moraine hummocks in between Rogen moraine forms one of the most conspicuous the end-member landforms. -
Glacial Features Explained
John Muir, Earth - Planet, Universe: Pupil Activity Support Notes Glacial features explained Glaciers The snow which forms temperate glaciers is subject to repeated freezing and thawing, which changes it into a form of granular ice called névé. Under the pressure of the layers of ice and snow above it, this granular ice fuses into denser firn. Over a period of years, layers of firn undergo further compaction and become glacial ice. The lower layers of glacial ice flow and deform plastically under the pressure, allowing the glacier as a whole to move slowly like a viscous fluid. Glaciers usually flow down a slope, although they do not need a surface slope to flow, as they can be driven by the continuing accumulation of new snow at their source, creating thicker ice and a surface slope. The upper layers of glaciers are more brittle, and often form deep cracks known as crevasses as they move. Erosion Rocks and sediments are added to glaciers through various processes. Glaciers erode the terrain principally through two methods: abrasion and plucking. As the glacier flows over the bedrock's fractured surface, it softens and lifts blocks of rock that are brought into the ice. This process is known as plucking, and it is produced when sub-glacial water penetrates the fractures and the subsequent freezing expansion separates them from the bedrock. When the water expands, it acts as a lever that loosens the rock by lifting it. This way, sediments of all sizes become part of the glacier's load. Abrasion occurs when the ice and the load of rock fragments slide over the bedrock and function as sandpaper that smooths and polishes the surface situated below.