Glacial Landforms of the Puget Lowland
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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). -
Disappearing Kettle Ponds Reveal a Drying Kenai Peninsula by Ed Berg
Refuge Notebook • Vol. 3, No. 38 • October 12, 2001 Disappearing kettle ponds reveal a drying Kenai Peninsula by Ed Berg A typical transect starts at the forest edge, passes through a grass (Calamagrostis) zone, into Sphagnum peat moss, and then into wet sedges, sometimes with pools of standing water, and then back through these same zones on the other side of the kettle. Three of the four kettles we surveyed this summer were quite wet in the middle (especially after the July rains), and we had to wear hip boots. These plots can be resurveyed in future decades and, if I am correct, they will show a succession of drier and drier plants as the water table drops lower and lower, due to warmer summers and increased evap- Photo of a kettle pond by the National Park Service. otranspiration. If I am wrong, and the climate trend turns around toward cooler and wetter, these plots will When the glaciers left the Soldotna-Sterling area be under water again, as they were on the old aerial some 14,000 years ago, the glacier fronts didn’t re- photos. cede smoothly like their modern descendants, such as By far the most striking feature that we have Portage or Skilak glaciers. observed in the kettles is a band of young spruce Rather, the flat-lying ice sheets broke up into nu- seedlings popping up in the grass zones. These merous blocks, which became partially buried in hilly seedlings can form a halo around the perimeter of a moraines and flat outwash plains. In time these gi- kettle. -
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. -
Impacts of Glacial Meltwater on Geochemistry and Discharge of Alpine Proglacial Streams in the Wind River Range, Wyoming, USA
Brigham Young University BYU ScholarsArchive Theses and Dissertations 2019-07-01 Impacts of Glacial Meltwater on Geochemistry and Discharge of Alpine Proglacial Streams in the Wind River Range, Wyoming, USA Natalie Shepherd Barkdull Brigham Young University Follow this and additional works at: https://scholarsarchive.byu.edu/etd BYU ScholarsArchive Citation Barkdull, Natalie Shepherd, "Impacts of Glacial Meltwater on Geochemistry and Discharge of Alpine Proglacial Streams in the Wind River Range, Wyoming, USA" (2019). Theses and Dissertations. 8590. https://scholarsarchive.byu.edu/etd/8590 This Thesis is brought to you for free and open access by BYU ScholarsArchive. It has been accepted for inclusion in Theses and Dissertations by an authorized administrator of BYU ScholarsArchive. For more information, please contact [email protected], [email protected]. Impacts of Glacial Meltwater on Geochemistry and Discharge of Alpine Proglacial Streams in the Wind River Range, Wyoming, USA Natalie Shepherd Barkdull A thesis submitted to the faculty of Brigham Young University in partial fulfillment of the requirements for the degree of Master of Science Gregory T. Carling, Chair Barry R. Bickmore Stephen T. Nelson Department of Geological Sciences Brigham Young University Copyright © 2019 Natalie Shepherd Barkdull All Rights Reserved ABSTRACT Impacts of Glacial Meltwater on Geochemistry and Discharge of Alpine Proglacial Streams in the Wind River Range, Wyoming, USA Natalie Shepherd Barkdull Department of Geological Sciences, BYU Master of Science Shrinking alpine glaciers alter the geochemistry of sensitive mountain streams by exposing reactive freshly-weathered bedrock and releasing decades of atmospherically-deposited trace elements from glacier ice. Changes in the timing and quantity of glacial melt also affect discharge and temperature of alpine streams. -
Quarrernary GEOLOGY of MINNESOTA and PARTS of ADJACENT STATES
UNITED STATES DEPARTMENT OF THE INTERIOR Ray Lyman ,Wilbur, Secretary GEOLOGICAL SURVEY W. C. Mendenhall, Director P~ofessional Paper 161 . QUArrERNARY GEOLOGY OF MINNESOTA AND PARTS OF ADJACENT STATES BY FRANK LEVERETT WITH CONTRIBUTIONS BY FREDERICK w. SARDE;30N Investigations made in cooperation with the MINNESOTA GEOLOGICAL SURVEY UNITED STATES GOVERNMENT PRINTING OFFICE WASHINGTON: 1932 ·For sale by the Superintendent of Documents, Washington, D. C. CONTENTS Page Page Abstract ________________________________________ _ 1 Wisconsin red drift-Continued. Introduction _____________________________________ _ 1 Weak moraines, etc.-Continued. Scope of field work ____________________________ _ 1 Beroun moraine _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ 47 Earlier reports ________________________________ _ .2 Location__________ _ __ ____ _ _ __ ___ ______ 47 Glacial gathering grounds and ice lobes _________ _ 3 Topography___________________________ 47 Outline of the Pleistocene series of glacial deposits_ 3 Constitution of the drift in relation to rock The oldest or Nebraskan drift ______________ _ 5 outcrops____________________________ 48 Aftonian soil and Nebraskan gumbotiL ______ _ 5 Striae _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ 48 Kansan drift _____________________________ _ 5 Ground moraine inside of Beroun moraine_ 48 Yarmouth beds and Kansan gumbotiL ______ _ 5 Mille Lacs morainic system_____________________ 48 Pre-Illinoian loess (Loveland loess) __________ _ 6 Location__________________________________ -
Hogback Trail Greenfield State Park Greenfield, New Hampshire
Hogback Trail Greenfield State Park Greenfield, New Hampshire Self-Guided Hike 1. The Hogback Trail is 1.2 miles long and relatively flat. It will take you approximately 45 minutes to go around the pond. As you walk, keep an eye out for the abundant wildlife and unique plants that are in this secluded area of the park. Throughout the trail, there are numbered stations that correspond to this guide and benches to rest upon. Practice “Leave No Trace” on your hike; Take only photographs, leave only footprints. 2. Hogback Pond is a glacial kettle pond formed when massive chunks of Stop #5: ridge is an example of glacial esker ice were buried in the sand, then slowly melted leaving a huge depression in the landscape that eventually filled with water. Kettle ponds generally have no streams running into them or out of them, resulting in a still body of water. Water in the pond is replenished by rain and is acidic, prohibiting many common wetland species from flourishing. 3. The blueberry bushes around Hogback Pond and throughout Greenfield State Park are two species; low-bush and high-bush. Many animals such as Black Bear and several species of birds seek out these berries as an important summer food source. Between Stops #2 & 3: example of unique vegetation found on kettle ponds 4. The Eastern Hemlocks that you see around you are one of the several varieties of evergreen that grow around Hogback Pond. This slow- growing, long-lived tree grows well in the shade. They have numerous short needles spreading directly from the branches in one flat layer. -
Des Moines Lobe Retreated North- What It Means to Be Minnesotan
Route Map Geology of the Carleton College Esri, HERE, DeLorme, MapmyIndia, © OpenStreetMap contributors, and the GIS ¯ user community 1 Cannon River Cowling Arboretum 2 Glacial Landscapes 3 Glacial Erratics 4 Local Bedrock A Guided Tour 5 Kettle Hole Marsh College BoundaryH - Back IA Parking Glacial Erratic Cannon River Tour Route Other Trails 0250 500 1 000 Feet, 5 HWY 3 4 LOWER ARBORETUM 3 2 H IA 1 Arb Office HWY 19 UPPER Tunnel IA ARBORETUM under Hwy 19 Lower Lyman Recreation IA Center HALL AVE HALL West IA Gym Library Published 5/2016 Product of the Carleton College Cowling Arboretum. For more information visit our website: apps.carleton.edu/campus/arb or contact us at (507)-222-4543 Introduction Hello and welcome to Carleton College’s Cowling Arboretum. This 1 800 acre natural area, owned and managed by Carleton, has long been one of the most beloved parts of Carleton for students, faculty and community members alike. Although the Arb is best known for its prairie ecosystem, an amazing history full of thundering riv- ers, massive glaciers, and the journeys of massive boulders lies just below the surface. This geologic history of the Arb is a fascinating story and one that you can experience for yourself by following this 2 self-guided tour. I hope it’s a beautiful day for a walk hope and that you enjoy learning about the geology of the Arb as much as I did. The route for this tour is about three miles long and will take you 1-2 hours to complete, depending on your walking speed. -
Pleistocene Geology of Eastern South Dakota
Pleistocene Geology of Eastern South Dakota GEOLOGICAL SURVEY PROFESSIONAL PAPER 262 Pleistocene Geology of Eastern South Dakota By RICHARD FOSTER FLINT GEOLOGICAL SURVEY PROFESSIONAL PAPER 262 Prepared as part of the program of the Department of the Interior *Jfor the development-L of*J the Missouri River basin UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1955 UNITED STATES DEPARTMENT OF THE INTERIOR Douglas McKay, Secretary GEOLOGICAL SURVEY W. E. Wrather, Director For sale by the Superintendent of Documents, U. S. Government Printing Office Washington 25, D. C. - Price $3 (paper cover) CONTENTS Page Page Abstract_ _ _____-_-_________________--_--____---__ 1 Pre- Wisconsin nonglacial deposits, ______________ 41 Scope and purpose of study._________________________ 2 Stratigraphic sequence in Nebraska and Iowa_ 42 Field work and acknowledgments._______-_____-_----_ 3 Stream deposits. _____________________ 42 Earlier studies____________________________________ 4 Loess sheets _ _ ______________________ 43 Geography.________________________________________ 5 Weathering profiles. __________________ 44 Topography and drainage______________________ 5 Stream deposits in South Dakota ___________ 45 Minnesota River-Red River lowland. _________ 5 Sand and gravel- _____________________ 45 Coteau des Prairies.________________________ 6 Distribution and thickness. ________ 45 Surface expression._____________________ 6 Physical character. _______________ 45 General geology._______________________ 7 Description by localities ___________ 46 Subdivisions. ________-___--_-_-_-______ 9 Conditions of deposition ___________ 50 James River lowland.__________-__-___-_--__ 9 Age and correlation_______________ 51 General features._________-____--_-__-__ 9 Clayey silt. __________________________ 52 Lake Dakota plain____________________ 10 Loveland loess in South Dakota. ___________ 52 James River highlands...-------.-.---.- 11 Weathering profiles and buried soils. ________ 53 Coteau du Missouri..___________--_-_-__-___ 12 Synthesis of pre- Wisconsin stratigraphy. -
Chapter One the Vision of A
Oak Ridges Trail Association 1992 - 2017 The Vision of a Moraine-wide Hiking Trail Chapter One CHAPTER ONE The Oak Ridges Moraine is defined by a sub-surface geologic formation. It is evident as a 170 km long ridge, a watershed divide between Lake Ontario to the south and Lake Simcoe, Lake Scugog and Rice Lake to the north. Prior to most THE VISION OF A MORAINE-WIDE HIKING TRAIL being harvested, Red Oak trees flourished along the ridge – hence its name. Appended to this chapter is an account of the Moraine’s formation, nature and Where and What is the Oak Ridges Moraine? history written by two Founding Members of the Oak Ridges Trail Association. 1 Unlike the Niagara Escarpment, the Oak Ridges Moraine is not immediately observed when travelling through the region. During the 1990s when the Oak The Seeds of the Vision Ridges Moraine became a news item most people in the Greater Toronto Area had no idea where it was. Even local residents and visitors who enjoyed its From the 1960s as the population and industrialization of Ontario, particularly particularly beautiful landscape characterized by steep rolling hills and substantial around the Golden Horseshoe from Oshawa to Hamilton grew rapidly, there was forests had little knowledge of its boundaries or its significance as a watershed. an increasing awareness of the stress this placed on the environment, particularly on the congested Toronto Waterfront and the western shore of Lake Ontario. The vision of a public footpath that would span the entire Niagara Escarpment - the Bruce Trail - came about in 1959 out of a meeting between Ray Lowes and Robert Bateman of the Federation of Ontario Naturalists. -
Inventory of Glaciers, Glacial Lakes and the Identification of Potential
Asia‐Pacific Network for Global Change Research Inventory of Glaciers, Glacial Lakes and the Identification of Potential Glacial Lake Outburst Floods (GLOFs) Affected by Global Warming in the Mountains of India, Pakistan and China/Tibet Autonomous Region Final report for APN project 2004-03-CMY-Campbell J. Gabriel Campbell (Ph.D.), Director General International Centre for Integrated Mountain Development G. P. O. Box 3226, Kathmandu, Nepal, [email protected] The following collaborators worked on this project: Prof. Xin Li (Ph. D.), Cold and Arid Regions Environmental and Engineering Research Institute, (CAREERI), Chinese Academy of Sciences (CAS), Lanzhou, P. R. China, [email protected] Mr. Gong Tongliang, Bureau of Hydrology Tibet Autonomous Region, Lhasa, P. R. China, [email protected] Dr. Tej Partap. CSK Himachal Pradesh Agricultural University, Palampur, Himachal Pradesh, India, [email protected] Prof. Dr. B. R. Arora, Wadia Institute of Himalayan Geology (WIHG), Department of Science & Technology, Government of India, Dehra Dun, Uttaranchal, India, [email protected] Dr. Badaruddin Soomro, Pakistan Agricultural Research Council (PARC), Islamabad, Pakistan, [email protected] Inventory of Glaciers and Glacial Lakes and the Identification of Potential Glacial Lake Outburst Floods (GLOFs) Affected by Global Warming in the Mountains of India, Pakistan and China/Tibet Autonomous Region 2004-03-CMY-Campbell Final Report submitted to APN J. Gabriel Campbell (Ph.D.) Director General, International Centre for Integrated Mountain -
Glaciation in East Africa
GLACIATION IN EAST AFRICA Glaciation: it refers to the overall effect of glaciers on the landscape resulting into both erosional and depositional features Glacier is a thick/large mass of ice of limited width, moving from the area of accumulation (snow field) following pre-existing valleys due to gravity. Or Glacier is an accumulated/compacted mass of ice/snow moving in a restricted channel/valley from a highland to a low land. Glaciers have different names for example mountain glaciers and valley glaciers/alpine glacier. Glaciers move continuously from higher ground to lower ground under the influence of gravity and are enclosed within the valley walls. The action of glacier includes glacier erosion, transportation and deposition. These processes will lead to the formation of glacier scenery. Glaciers in East Africa are only found in high mountainous areas of Kenya, Kilimanjaro and Rwenzori. This is mainly because those mountains (Kenya, Kilimanjaro and Rwenzori) are high above the snow line (4500m). In East Africa glacial activities are limited to a few places, this is due to a number of factors that limit the formation of snow and this include: The latitudinal position of East Africa across or astride the equator hence, the temperatures are generally hot and therefore not conducive for the existence of glacier anywhere and anyhow in East Africa. In East Africa the snowline is very high about 4800m, which only the three highest mountains can reach which explains them having the glacial activities. Snowline is that line where there is permanent snow and ice. It can be at ground level at poles. -
Pine Hill Esker Trail
mature forest, crosses a meadow and goes back 1.04 miles: Trail turn-around, at the location of into forested terrain. Unique for this trail are its wetland and a permanent stream. eskers and kettle ponds and the views of a 1.19 miles: Optional (but recommended) side wetland pond where Rocky Brook flows into the loop on the left side, shortly after remnants of the Stillwater River. The trail is located on DCR circular track. watershed protection land, so dogs are not 1.23 miles: Trail loops gently to the right. Deep allowed. down to the left is a small pond (a kettle pond). Length and Difficulty 1.32 miles: Side trail rejoins the return trail. 1.55 miles: Trail junction of Sections A, B and C. For clarity, the trail is divided into three sections: The trail description continues with Sect. C A, B and C, with one-way lengths of 0.65 mi., 0.45 outbound. mi. and 0.45 mi., respectively. The full hike, as 1.58 miles: Wet area most of the times of the described below, includes all three sections. The year. side loop on Sect. B is included on the return. The 1.78 miles: View to wetland pond where the A+B+C trail length is 3.1 mi., while the two shorter Stillwater River meets Rocky Brook. The distant versions, A+B or A+C, are both 2.2 mi. in length. structure is part of the Sterling water system. The elevation varies between 428 ft and 540 ft, 2.00 miles: Trail turn around point at the edge of with several short steep hills.