Map of Indiana Showing Physiographic Divisions John C

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Map Of Indiana Showing Physiographic Divisions John C. Steinmetz, Indiana State Geologist By Henry H. Gray Miscellaneous Map 69 Bloomington, Indiana: 2001 M I C H I G A N ER ST. JOSEPH EXPLANATION LAKE MICHIGAN RD O X DRAINAGEWAYS B E LEX L E P P lk M STEUBEN N h O A M C LAGRANGE G O a I X CH C r E MI ST JOSEPH L LAKE L L t P A A M IN LAPORTE IN R RA A ELKHART iver O NORTHERN MORAINE AND O R S C M Y O A DEKALB LAKE REGION O MARSHALL M W L AIS E A R NOBLE LPA PORTER G N VA A I r STARKE N A e I R iv LAKE H A O R Ri YS T R M ve A U D e r W O KOSCIUSKO h ke E YM N p ka NAG PL UR se MAUMEE LAKE PLAIN REGION an RAI D UB Jo R. K D A e E N e KE A . m A t au NK S KA M ES N WHITLEY MAUMEE PULASKI FULTON AI LAKE JASPER OR ALLEN M S PLAIN CENTRAL TILL PLAIN REGION t W . SA M NEWTON AR a W ry WABASH 's HUNTINGTON R MIAMI Salamonie iv SOUTHERN HILLS AND IROQUOIS WHITE Lake WELLS er Mississinewa Sa Wabash ADAMS la CASS Lake m LOWLANDS REGION o TILL ni M e i River ss BENTON i s BLUFFTON s i CARROLL n e R PLAIN HOWARD w iv GRANT a er TILL JAY BLACKFORD Southern limit of Wisconsin WARREN Ri TIPPECANOE PLAIN ver glacial deposits CLINTON TIPTON TIPTON DELAWARE HAMILTON MADISON FOUNTAIN River RANDOLPH TILL BOONE NEW CASTLE Southern limit of older CENTRAL MONTGOMERY O H I glacial deposits TILL PLAINS WABASH PLAIN AND DRAINAGEWAYS WAYNE VALLEY r k ve ee White i HENRY r HANCOCK R PARKE C MARION HENDRICKS VERMILLION ue Bl PUTNAM n coo FAYETTE UNION Rac RUSH I L L I N O S L I L M r Brookville A e R iv Lake T R SHELBY I N SV JOHNSON W IL MORGAN LE h H i I L tew Cataract LS ater ite CLAY Lake Wh DECATUR FRANKLIN VIGO OWEN R BARTHOLOMEW iv MONROE T e r N N S U E O C A BROWN TE R M SULLIVAN M O A DEARBORN P L S River W A T P P R N T A R Monroe A D S B U I C k N B RIPLEY N Lake P A r S K G A o U E S L C L F V A H R JENNINGS U P I T L N G U A GREENE L C D T E A R E C N N OHIO A R JACKSON S O W O T U B L r S F e L M v R O LAWRENCE B i O O A O R W t R W SWITZERLAND s E a N E W L D K L D h A A i te N JEFFERSON N DAVIESS M D D k r I o T C KNOX F SCOTT H E L MARTIN U L Wabash P E L S WASHINGTON A C A River N R D P te Eas M hi t EN T Patoka CLARK W ORANGE Lake P ka L to A a P T CHARLESTOWN River DUBOIS E FLOYD PIKE A HILLS GIBSON CRAWFORD U BOONVILLE 0 10 20 30 MILES HILLS POSEY HARRISON WARRICK PERRY SPENCER 0 10 20 30 KILOMETERS VANDERBURGH OH R I IVE O R Modified from Gray, H. H., 2000, Physiographic Divisions of Indiana, Indiana Geological Survey K E N T U C K Y Special Report 61, Plate 1. Indiana Geological Survey | An Institute of the Office of the Vice Provost for Research 611 N. Walnut Grove Ave., Bloomington, IN 47405-2208 | 812.855.7636 | [email protected] | igs.indiana.edu.

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Introduction to Geological Process in Illinois Glacial
INTRODUCTION TO GEOLOGICAL PROCESS IN ILLINOIS GLACIAL PROCESSES AND LANDSCAPES GLACIERS A glacier is a flowing mass of ice. This simple definition covers many possibilities. Glaciers are large, but they can range in size from continent covering (like that occupying Antarctica) to barely covering the head of a mountain valley (like those found in the Grand Tetons and Glacier National Park). No glaciers are found in Illinois; however, they had a profound effect shaping our landscape. More on glaciers: http://www.physicalgeography.net/fundamentals/10ad.html Formation and Movement of Glacial Ice When placed under the appropriate conditions of pressure and temperature, ice will flow. In a glacier, this occurs when the ice is at least 20-50 meters (60 to 150 feet) thick. The buildup results from the accumulation of snow over the course of many years and requires that at least some of each winter’s snowfall does not melt over the following summer. The portion of the glacier where there is a net accumulation of ice and snow from year to year is called the zone of accumulation. The normal rate of glacial movement is a few feet per day, although some glaciers can surge at tens of feet per day. The ice moves by flowing and basal slip. Flow occurs through “plastic deformation” in which the solid ice deforms without melting or breaking. Plastic deformation is much like the slow flow of Silly Putty and can only occur when the ice is under pressure from above. The accumulation of meltwater underneath the glacier can act as a lubricant which allows the ice to slide on its base.
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Indiana Glaciers.PM6
How the Ice Age Shaped Indiana Jerry Wilson Published by Wilstar Media, www.wilstar.com Indianapolis, Indiana 1 Previiously published as The Topography of Indiana: Ice Age Legacy, © 1988 by Jerry Wilson. Second Edition Copyright © 2008 by Jerry Wilson ALL RIGHTS RESERVED 2 For Aaron and Shana and In Memory of Donna 3 Introduction During the time that I have been a science teacher I have tried to enlist in my students the desire to understand and the ability to reason. Logical reasoning is the surest way to overcome the unknown. The best aid to reasoning effectively is having the knowledge and an understanding of the things that have previ- ously been determined or discovered by others. Having an understanding of the reasons things are the way they are and how they got that way can help an individual to utilize his or her resources more effectively. I want my students to realize that changes that have taken place on the earth in the past have had an effect on them. Why are some towns in Indiana subject to flooding, whereas others are not? Why are cemeteries built on old beach fronts in Northwest Indiana? Why would it be easier to dig a basement in Valparaiso than in Bloomington? These things are a direct result of the glaciers that advanced southward over Indiana during the last Ice Age. The history of the land upon which we live is fascinating. Why are there large granite boulders nested in some of the fields of northern Indiana since Indiana has no granite bedrock? They are known as glacial erratics, or dropstones, and were formed in Canada or the upper Midwest hundreds of millions of years ago.
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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__________________________________
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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.
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4. Results & Analysis
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Illinois Map 10 2001 George H. Ryan, Governor Department of Natural Resources Brent Manning, Director ILLINOIS STATE GEOLOGICAL SURVEY William W. Shilts, Chief Geologic Road Map of Illinois: N Natural Resources Building East Dubuque Warren 615 East Peabody South Beloit Richmond Antioch 84 CHAIN- 173 Champaign Illinois, 61820-6964 APPLE RIVER Rockton 173 O-LAKES Zion ILLINOIS CANYON LAKE BEACH LE-AQUA-NA Lake Summerset Galena 78 Durand Roscoe 94 Surface Deposits and Landscapes 26 76 132 Harvard Lena 75 2 Fox Lake 251 90 14 47 83 Machesney 173 Waukegan MCHENRY DAM E 20 Stockton 70 Park ROCK CUT & LAKE DEFIANCE W Pecatonica McHenry North Chicago Woodstock David A. Grimley, Barbara J. Stiff, and Michael J. Andrew Loves Park 23 60 73 Belvidere 12 20 Marengo 176 41 Freeport 176 Mundelein Winnebago 20 Lake Forest Surface deposits compiled from Hansel and Johnson (1996), Lineback (1979), and Willman and Frye (1970) 84 59 Rockford Cherry Valley Crystal Lake 14 22 90 Huntley Lake Zurich Highland Park S Forreston MISSISSIPPI Carpentersville PALISADES 72 Byron 68 Genoa 94 Savanna Mount Carroll Lanark Arlington 26 2 Kirkland 62 Hts. 72 Hampshire WISCONSIN glacial outwash Mount Morris Mt. Prospect Evanston lake plain 39 20 Elgin Des 64 LOWDEN Skokie Driftless 47 Schaumburg Plaines Lake Michigan 52 290 WHITE CASTLE 64 41 Area PINE ROCK Oregon Sycamore 31 Milledgeville Polo FOREST 19 Michigan 19 St. Charles 20 LOWDEN-MILLER Rochelle 43 De Kalb 64 88 38 Oak Chicago 38 Elburn 59 355 Park 290 Fulton 2 Ashton 251 88 Wheaton Chicago MORRISON- Dixon Cicero ROCKWOOD 25 294 34 88 23 Morrison Sterling Downers 30 Rock Falls Waterman Hinckley Sugar Grove Naperville Grove 50 41 A 84 78 30 Aurora IOWIOWA 55 12 90 26 Amboy SHABBONA LAKE Oak A.
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557 IL6gui 1980-D uide to the geology of the Quincy North area David L Reinertsen Commemorating the 50th Field Trip Season and the Survey's 75th year. Cross section of one of the larger sinkholes exposed along the west siJe of State Route 336 at Stop 2. Printed by authority of the State of Illinois/1980/500 copies 'L L 'NO | STATE GEOLOGICAL l SURVEY | f 3 3051 00006 8142 , A guide to the geology of the Quincy North area In 1930 the Geological Survey was 25 years old and the new Educational Extension Section was conducting its first field trips. Dr. M. M. Leighton, the Survey's third Chief, had created the section and its program "...to cooperate with the science teachers of the state and furnish them information regarding geology, such as will be helpful in their teaching of earth history and the development of life.' Part of the Section's work was to start a series of six annual "earth history field trips." More than 250 teachers and laymen attended the first year's trips near Dun- dee, La Salle-Starved Rock, Charleston- Mattoon-Eff i ngham , Harri sburg-Shawneetown Quincy, and Rock Island. In its 50 years (except for the war years 1942 to 1945), Ed. Extension has conducted more than 290 field trips. In 1979, 367 people from all walks of life attended the Survey's four field trips. 0m, ~x~w* 4 <#P\* -M* mmm-"* s U / • '« '-^L^<*-^ Teachers on the Quincy field trip, October 4, 1930, assemble in a quarry. Figure 1.
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About the Dahlen Esker by Lorraine A. Manz
2 3 y a w h g i H e t a t S D a h le n r ke Es About the Dahlen Esker By Lorraine A. Manz First described in detail by Jack Kume in 1967, the Dahlen esker is the one of the best examples of its kind in North America. Eskers are long, sinuous, steep-sided ridges consisting of sediments (mainly sand and gravel with lesser amounts of silt and glacial till) deposited by meltwater streams flowing through tunnels or ice-walled channels at the base or within a stagnant or retreating glacier. When the ice melted these sediments were preserved more-or-less in place as ridges that mark the course of their parent stream, so like the compaction ridges described on page 17, eskers are topographic reversals. The Dahlen esker is located in northeastern North Dakota between the towns of Dahlen and Fordville. It is clearly visible as a prominent ridge from State Highway 32, which crosses its eastern end about half a mile north of the Grand Forks-Walsh County line. The esker was deposited approximately 12,000 years ago by a stream flowing in an ice-floored tunnel near the base of a stagnating glacier. It is roughly 400 feet wide at its base and Kume (1967) estimated its length at about four miles. The crest of the ridge rises to a maximum height of 80 feet and although it is generally level, numerous gaps give it an irregular appearance. The gaps, which have been widened and deepened by modern stream erosion, were probably formed at the same time as the esker, most likely by sediment collapse as the underlying ice melted.
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Interior Plains and Arctic Canada Plaines Mterieures Et Region
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Proceedings of the Indiana Academy of Science
The Erie Lobe Margin in East-Central Indiana During the Wisconsin Glaciation 1 William J. Wayne, Indiana Geological Survey Abstract The ice sheet that deposited the Trafalgar Formation during the Tazewell Subage became inactive east of White River after building the Knightstown Moraine and disappeared by downwasting. Patches of low- relief ice-disintegration hummocks cover much of the Tipton Till Plain in east-central Indiana south of the Union City Moraine, where kames, eskers, and ice-walled disintegration channels are the dominant geo- morphic features of the landscape. The low Union City Moraine marks the margin in east-central Indiana of the Lagro Formation, a till sheet de- posited by the Erie Lobe during the Cary Subage of the Wisconsin (glacial) Age. The moraine disappears as a recognizable topographic feature across Delaware County because in that region the Erie Lobe ice rode over the thin sheet of stagnant ice that still remained from the earlier advance that deposited the Trafalgar Formation. Introduction The topographic features produced by melting ice in east-central Indiana—particularly in and around Muncie—have intrigued geologists for nearly a century. Phinney described them in two reports published in the 1880's, in which he recognized the esker system at Muncie and described but did not name the moraines of that area (12, 13). He regarded the eskers and troughs to have been formed by feeder channels for the flood of "Collett's Glacial River" farther south. Leverett, who devoted nearly his lifetime to study of the glacial deposits of the central United States, mapped and named a narrow ridge across Randolph County, the Union Moraine (9, pp.
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Geology Colloquium Glacial Deposits
Geology Colloquium Thursday, April 12th, Dr. Mark Abbot, Univ. of Pitt The Holocene Environmental History of the Central Andes from Lakes and Glaciers 4:00 pm in Room 310 White Hall. Refreshments will be available at 3:45 PM. Everybody is welcome! Glacial Deposits • Lodgement Till • Ablation Till • Flow Till Form a Committee and see what you get… Till Genesis: Till Work Group 1977-82 Report (Dreimanis) Till Subglacial Till Supraglacial Till Sub- Melt- aqueous & Out & Subaerial Sublim Mass- ation Movement Till Till (Flow Till) Melt-Out Till Melt-Out Lodgement Till Deformation Till Mass-Movement Till Mass-Movement Key: Subaquatic Till Melt-Out Ortho- Till Allo-Till 1 Till - a Type of Glacial Sediment Basal till from the last major glaciation ~ 18,000 years ago; Loch Torridon, Scotland. M. J. Hambrey photo. http://www.swisseduc.ch/glaciers/glossary/till-en.html Glacier-Till Contact, Iceland Photo by Tom Lowell 2 Striated Boulder, Hargraves Glacier, B.C. Photo by Tom Lowell Striated Boulder, Solheimajokull, Iceland. Photo by Tom Lowell Largest Erratic in Maine MAINE DEPARTMENT OF CONSERVATION PHOTO http://www.state.m e.us/doc/nrimc/pu bedinf/photogal/su rfical/surfphot.htm 3 DEPOSITIONAL LANDFORMS COMPOSED OF TILL: • Moraines = Ice-Marginal Positions Image from Judson L. Ahern http://dynamic.ou.edu/notes/glaciers/moraines.jpg Alpine Moraines Moraine = Landform on Margins of Glacier Lateral Moraine Medial Moraine End Moraine Medial Moraines 4 Photo by Tom Lowell Moraine System, Sierra Nevada, California Massive Lateral & End Moraines New Zealand Photo by Tom Lowell 5 End Moraines Terminal Moraine Recessional Moraines Athabaska Glacier, Alberta Moraine from “Continental” Glaciers: Iceland Photo by Tom Lowell http://www.state .me.us/doc/nrim 700c/pubedinf/facts m ht/bedrock/meg eol.htm Basin Ponds Moraine <60 m Mt.
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Landtype Associations (Ltas) of the Southeast Glacial Plains 222Kc05 222Kc04 Scale: 1:1,200,000 Wisconsin Transverse Mercator NAD83(91) Map SEGP3 - Ams 222Kc06
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