SENESCENCE AND EXTENS'EéOfl 3N INLAND LAKES Oi? MISééIGAN Thesis; far the {Baggage of M. S. MICHIGAN STATE UNWERSIW EDWARD ALLISON KERKBY 1957 W! M] Illfil’WflWflfllfllWflWifll 3129 00705 2180 ABSTRACT SENESCENCE AND EXTINCTION IN INLAND LAKES OF MICHIGAN by Edward Allison Kirkby Senescence and extinction were studied in inland lakes with basins in glacial drift in the Lower Peninsula of Michigan. Several hundred lakes were given a cursory examination while 23 others were studied in detail, using a sounding rod to determine sediment thickness and depth to the original bottom. All the lake basins had been modified by sediments since they orig— inated, after the retreat of the fourth stage of the Pleistocene. The dom- inant sediments are peat and marl. A correlation exists between the SIOpe of the original bottom in a lakeward direction and the dominant type of sediment. Original bottoms usually dip at 13 degrees or less in lakes where peat dominates, but 14 degrees or more where marl is the dominant sediment. Calcium carbonate may be carried into any lake basin intersecting the groundwater table but is deposited as marl only where acids do not exist in quantities capable of neutralizing calcium carbonate. The most favorable places for marl deposition would be in lakes with steep original bottoms that limit the growth and migration of attached aquatic vegetation. Shallow and deep lakes are defined on the basis of the original bot- tom leping in a lakeward direction and the dominant sediment. Deep lakes have an original bottom dipping 14 degrees or more and (or) marl is the dominant sediment. Shallow lakes have an original bottom dipping 13 degrees or less and (or) peat is the dominant sediment. Deep lakes are less prone to senescence and extinction than shallow lakes. Edward Allison Kirkby The size and shape of the lakes , size and relief of the drainage area have little bearing on the relative resistance of the lake to senescence and extinction. No correlation exists between the number of extinct lakes and the elevation, surface formations, soils, physiographic prov— ince, and relative age of the region they occur in. No visible evidence of accelerated aquatic vegetation growth due to human effluent, agricul- tural fertilizers and manures were found. Sediment coring may reveal a relationship between sediment types , deposition patterns, and climatic pulsations. Coring was attempted but efforts were unsucces sful . SENESCENCE AND EXTINCTION IN INLAND LAKES OF MICHIGAN By Edward Allison Kirkby A THESIS Submitted to Michigan State University in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Resource Development 1967 ACKNOWLEDGMENTS This writer wishes to thank Dr. Clifford R. Humphrys, Department of Resource Development, Michigan State University, who suggested the problem and under whose guidance this work was completed. Thanks are also extended to Messrs. Robert Kelley, John Rulison, and John Gray, Michigan Department of Conservation, for effort put forth in editing the manuscript. My wife, Barbara, deserves special thanks for not only being a con— stant field companion, but also for recording data and typing the draft manuscript. Edward Allison Kirkby ii TABLE OF CONTENTS Page ACKNOWLEDGMENTS ........................ ii LIST OF FIGURES .......................... v LIST OF MAPS ............................ vi LIST OF PLATES ........................... viii CHAPTER I. INTRODUCTION ..................... 1 Lakes and Lake Activities .............. 1 Statement of Problem and Intentions of Study . . . . 1 Previous Investigations ............... 3 Sources of Information ............... 4 Location of Lakes .................. 4 Procedure . ..................... 4 II. ORIGIN OF INLAND LAKES . ............... 8 III. SENESCENCE AND EXTINCTION IN LAKES ........ 19 Role of Clastic Sediments .............. 19 Role of Marl ..................... 21 Role of Peat ..................... 23 Role of Men ..................... 25 Role of Climate ................... 29 IV. LAKES STUDIED ..................... 31 Barry County .................... 31 Cloverdale Lake ................ 31 Long Lake ................... 34 Head Lake ................... 36 Guernsey Lake ................. 38 Daggett Lake .................. 38 Long Lake ................... 41 Little Payne Lake ................ 41 Carr Lake .................... 44 Osceola County ................... 44 Alexander Lake ................. 47 Big Lake .................... 47 Myrtle Lake .................. 50 Hicks Lake ................... 50 iii CHAPTER Page Park Lake .................... 53 Austin Lake ................... 53 Hewitt Lake .................. 56 Clare County .................... 56 Pike Lake .................... 56 \Nexford County ................... 60 Unnamed Lake ................. 6O Meady Lake .................. 63 Missaukee County ................. 63 Lake Missaukee ................ 63 Goose Lake ................... 67 Long Lake ................... 68 Whitlock Lake ................. 7O Kalkaska County .................. 70 Blue Lake .................... 73 Guernsey Lake ................. 73 V. SUMMARY ........................ 76 VI. CONCLUSIONS AND RECOMMENDATIONS ........ 81 Conclusions ..................... 81 Recommendations for Additional Studies ...... 83 VII. CONTROL OF AQUATIC VEGETATION ........... 85 REFERENCES CITED ......................... 87 APPENDIX .............................. 90 iv LIST OF FIGURES Figure Page 1. Halt of Retreating Ice Front ............... 2 2. Location of Counties Where Lakes Were Studied in Detail .................... 5 3. Sounding Rod Operation ................. 7 4. Slopes of the Original Bottom .............. 78 LIST OF MAPS Map Page 1. Barry County ....................... 32 2. Cloverdale Lake ..................... 33 3. Long Lake ........................ 35 4. Head Lake ........................ 37 5. Guernsey Lake ...................... 39 6. Daggett Lake ....................... 40 7. Long Lake ........................ 42 8. Little Payne Lake .................... 43 9. Carr Lake ........................ 45 10. Osceola County ..................... 46 11. Alexander Lake ..................... 48 12. Big Lake ......................... 49 13. Myrtle Lake ....................... 51 14. Hicks Lake ........................ 52 15. Park Lake ........................ 54 16. Austin Lake ....................... 55 17. Hewitt Lake ....................... 57 18. Clare County ....................... 58 19. Pike Lake ........................ 59 20. Wexford County ..................... 61 21. Unnamed Lake ...................... 62 22. Meady Lake ....................... 64 23. Missaukee County .................... 65 24. Lake Missaukee ..................... 66 25. Goose Lake ....................... 68 26. Long Lake ........................ 69 vi "I a p ’) L. 28. 29. 30. Whitlock Lake . Kalka ska County . Blue Lake Guernsey Lake . vii Page 71 72 74 75 Plate CDVCWCDQOON 10. ll. 12. l3. 14. 15. LIST OF PLATES Page Bedrock Basins ...................... 9 Bedrock Valley ...................... 10 Lakes in Preglacial Bedrock Valley ........... 11 Glacial Drift Valley Lake ................ 12 Lakes in Glacial Drift Valley .............. l3 Pit Lake ......................... 15 Perched Lake ....................... 16 Origin of Two Lake Basins ................ 17 Lake in Cutover Forest .................. 18 Types of Extinction ................... 20 Effects of Shore Erosion ................. 22 Marl and Peat ...................... 24 Effects of Tiling ..................... 27 Deforestation and Reforestation ............. 28 Effects of Drought .................... 30 viii CHAPTER I INTRODUCTION Lakes and Lake Activities Michigan is a water wonderland and a land of lakes, including over 29, 000 natural inland lakes (Humphrys, 1963). Each county has one or more lakes and the number may be increasing with the addition of artifi- cial or man-made lakes. The shores of lakes in the southern part of the Lower Peninsula have been in various stages of develOpment since the advent of the horseless carriage. Now freeways have reduced driving times, as salaries have in— creased and the work week decreases , causing many people to seek out lakes in the northern part of the Lower Peninsula, and Upper Peninsula. Most lakes are used for one or more forms of recreation. Many are used for swimming, waterskiing, fishing, hunting and viewing. Some are used throughout the year, including winter months when ice skating, sleding, ice fishing, snowmobiling, ice boating and sports car racing may be carried on. Unfortunately, not all lakes can support a variety of activities. Many lakes have evolved into swamps and peat bogs where recreation may be limited to bass fishing and duck hunting, at most. Other lakes are ex— tinct, but may be utilized by wild animals, or exploited by peat and marl operators . Statement of the Problem and Intentions of the Study Lakes are grand but most are temporary features on the landscape, geologically speaking. The origin of most lakes in the Great Lakes area may be traced to the oscillatory retreat of glaciers that melted away over 10, 000 years ago. (Figure l.) The basins of most lakes show indications ") i. 1067 am. of memo” Department or Coneervoflon Geological Survey Oivmon Sale" eoate nap L \ MORAINIC SYSTEMS OF MICHIGAN ‘x'l‘v , 4v; 40 ’ [0 00° C . W ‘ I ~ ecnu r_ \ 0 IO N .0 00 ‘0 OOLI. ‘ : ’ \f’ C '_ (I (Dates after Hough, 1958; Wayne, 1965; and Zumberge, 1956) Figure 1. Halt of Retreating Ice Front of senescence or extinction in the form of swampy, peat—filled margins, or shallow areas controlled by aquatic vegetation. This phenomenon has been observed at glacial drift lakes in Indiana (Blatchley, 1901) and Minnesota (Zumberge, 1952) and is probably characteristic of most lakes with origins dating back to the retreat of glaciers during the Pleistocene. Since senescence and extinction are common to most lakes it was felt that a geologic study might produce new evidence useful in deter- mining the causes of senescence and extinction. The intention of this study is to determine how lakes become senescence and extinct; the ex— tent of sediments filling in selected lakes, and why lakes , and parts of lakes become senescent and extinct. This study should be of interest to riparians , lake associations, dredging companies , lake builders and develOpers , geologists , biologists , limnologists, peat and marl producers. Previous Investigations Previous investigations of lake senescence and extinction in Michigan consist of briefly explaining the origin, development, and extinction of lakes, or making cursory inspections of marl and peat deposits and noting their quality and commercial possibilities. These studies did not equate the original bottom lepe with the predominant type of sediment, and re— late senescence and extinction possibilities of the lake. Origin of lakes, former lake levels and extinction is explained in "Inland Lakes of Michigan, " Michigan Geological Survey Publication 30 (Scott, 1921). Inland lakes being extinct or senescent are described in reports about marl (Hale, 1903), peat (Burns, 1904; Davis, 1907), and surface geology (Lane, 1908, p. 126). Inland lake level declines are mentioned for the Lower Peninsula (Rominger, 1876), Muskegon County (McLouth, 1902, p. 105), and part of Oakland County (Stanley, 1936, pp. 52-53). Sources of Information Depth and area of the lakes were obtained from the Fish Division, Michigan Department of Conservation, Lansing. When hydrographs were unavailable, air photos and county soil studies were used as a base for delineating the shape and computing the size of lakes. Drainage area size, maximum feet of relief, prominences and landmarks were determined from air photos and U. S. Geological Survey tOpographic quadrangle sheets, and extent and type of peat deposits adjacent to lakes from county soil studies. Glacial drift thickness information is from oil and gas explor- atory logs published by the Geological Survey Division, Michigan De— partment of Conservation, Lansing. Published and unpublished literature prepared by the Geological Sur— vey Division, Michigan Department of Conservation, was searched for lake references. Cloverdale, Long, and Guernsey lakes were visited during a statewide marl survey (Hale, 1903). Location of Lakes Twenty-three inland lakes in Barry, Clare, Eaton, Kalkaska, Mis- saukee, Osceola, and Wexford counties were studied in detail (Figure 2). In addition, several hundred lakes in the Lower Peninsula were visited and given cursory examinations. Procedure An attempt was made to select lakes underlain by 200 or more feet of glacial drift, without inlets or outlets , having public access, limited shore and upland develOpment, in isolated locations. As might be ex— pected, an accessible lake meeting this criteria was hard to find. The field work was begun in 1963 and completed in 1966. The primary mission at each lake was to determine depths to the present and original bottoms using a sounding rod constructed of one—half inch steel pipe. Pipe lengths to 35 feet were experimented with, but the most satisfactory was 21 feet. The sounding rod was marked at five-foot If s) i . wow! u Mfm l ‘L— WWSW DC ! un- ' 1" l ! W'ol'ésidoi' tab" in}: 10" ' ? ! .., -1... _ s}?! -516!" ' pm I L . .4359 T17“ a nomfl'nmuc I i I l _J .-- J." 11 ~ [—6th 396-!" g ' W ' — ) I L If”? I JJ “W I _ __ _|__. _ __ _ meat??— sir—i . _ ‘— ' ~6¢Wraw swans: ‘ . I 1 ml 1 ___)_____J__-f—o)u- 1— 51 um l Figure 2. Location of Counties Where lakes Were Studied in Detail I3" intervals. A steel tape was used to obtain a measurement to the nearest foot. The sounding rod was Operated from a small rowboat while a second person recorded data and stabilized the craft (Figure 3). If the lake bottom was not visible, the sounding rod was moved to and fro as it was lowered vertically. It was difficult to move the sounding rod when the present bottom was reached. The original bottom of the lake basin is the probable bottom formed as the ice melted. The original bottom is composed of Clastic sediments usually overlain by marl, peat or both. It is the place where the sounding rod will not descend further. Often, the original bottom was not reached so efforts were abandoned at that station to locate it. Depths to the present and original bottoms enabled the writer to com— pute bottom lepes, and thickness of sediments. Cross sections were drawn from the measurements. Sediment—type marl, peat, or a combination was determined from samples adhering to the sounding rod. Peat less than one foot thick did not adhere. Submergent aquatic vegetation, muskgrass and pondweed were brought to the surface. Station locations were determined by estimating distances from shore features on U. S. Geological Survey topographic quadrangles. When checked from shore, stations were within 35 to 50 feet of locations on hydrographs used as a base. Greater station location accuracy was pos— sible within 250 feet of the shore. The drainage area was checked for relic shorelines, outlets and in— lets at the 23 lakes studied in detail. Soil composition, shore develOp— ment, and recent lake level changes were also noted. Various types of homemade coring devices of various lengths were built and tested. It was hOped that a continuous core of sediments could be recovered and studied at each of the 23 lakes, thereby shedding new light on sediment deposition. However, the coring phase of this project was unsuccessful and abandoned. '7 I Sounding rod in raised position Sounding rod at original bottom Figure 3. Sounding Rod Operation CHAPTER II ORIGIN OF INLAND LAKES Most of Michigan's inland lake basins are located in glacial drift. Glacial drift is soil materials transported and deposited by glaciers that retreated from the Midwest over 10,000 years ago (Figure 1). However, lake basins existed in Michigan long before the Pleistocene or " Ice Age. " Probably, preglacial lake basins occurred in the bedrock surface as they do today in parts of the western half of the Upper Peninsula and Isle Royale. Such basins originated from folding, faulting, or differential erosion of the rock (Plate 1). Examples are Lake Gogebic and Lake of the Clouds. Lakes may originate in preglacial bedrock valleys that are later dammed by glacial drift (Plate 2). Origin of these lakes may be traced to the time of glacial advances when temperatures declined and precip- itation collected to form ice in the valleys. Ice would preserve the shape of the valleys and become part of the regional ice mass as glaciers ad— vanced over the area. During glacial retreat, ice in the valleys being thicker and probably insulated by glacial drift, would melt at a slower rate than the glacier. A lake basin or basins resembling a valley devel— oped as the ice in the valley melted (Ferris, 1954, p. 31). Examples are several narrow "chains of lakes" in T6—7S, R3-4W, Hillsdale County, an area of thin glacial drift (Plate 3). Lakes similar in appearance and origin to preglacial valley lakes may develop in glacial drift (Plate 4). The difference occurs because the val- leys are located in glacial drift laid down during an earlier glacial advance. An example is the chain of lakes made up of Wilkinson, Cloverdale, and Long lakes, TZN, R9W, Barry County, an area of thick glacial drift (Plate 5). Differential Erosion Plate 1. Bedrock Basins 10 Valley Ice \ Glacier Ice Collects in the Valley as the Glacier Advances Ice in the Valley Becomes Part of the Regional Ice Mass A v v Glacial Drift is Deposited as the Glacier Retreats v Bedrock Valley Lake Plate 2. Bedrock Valley Plate 3. Lakes in Preglacial Bedrock Valley 12 Valley \\ Glacier Ice Ice collects in the valley as the glacier advances Ice in the valley becomes part of the regional ice mass Plate 4. Glacial Drift Valley Lake a o 7 ' ' .., I, . v . ; fl &' ‘ W -‘ " ‘ e . ' l. 0 ‘ ' \ ' t' . - ' t. J " I V *. \J ' ' ‘_ tr In - .‘ {.9}: hr - ..., « ~ - ' ‘ '." _ _ ‘ . e . ' f r \a. l.‘..»..) ' . 4 I i " \k I. \ w o I . : \t’u‘ (v ee ue ?*- ' ' '\ )4 gig?” in ..~,,‘i'r. Vfi if} e “I" .5 ‘ ;’ £3 .1 Plate 5. Lakes in Glacial Drift Valley 14 The majority of inland lakes in Michigan are pit and pot hole lakes whose origin is in blocks of ice separating from the margin of a retreating glacier (Plate 6). The ice block may be buried by glacial drift, gradually melting and leaving a pit. Size and shape of the pit is a reflection of the size and shape of the ice block and the depth is directly proportional to the thickness of the ice block minus the thickness of glacial drift de- posited on it. The pit becomes a lake if it intersects the groundwater table or is intersected by a stream. Examples are Houghton and Higgins lakes, and most smaller inland lakes in Michigan. A perched lake basin is located above the groundwater table (Plate 7). These may start on sandy soils when runoff washes clay particles from surrounding slopes into the bottom and edges of a basin. Clay particles form an impervious seal preventing water from leaving the basin as rapidly as it enters, causing the lake level to rise as more water enters. The perched lake development process may be observed on a small scale on sand dunes during and directly after a heavy rain. Wave action may form sand bars and spits that can gradually close the mouth of a bay, forming a separate lake. Bays and rivers with little current may be dammed by migrating sand dunes to form lakes (Plate 8). Lakes may develop in areas cleared of dense coniferous forests (Sigler, 1927). During the reign of the forests much precipitation would be intercepted by tree limbs or quickly infiltrate the soil before it could runoff. The groundwater table could also be low if it was intersected by tree roots because of the vast amounts of water used by the trees. How- ever, if the timber was cut, precipitation would no longer be intercepted nor would living tree roots lower the groundwater table, so low places, especially basins, could fill with water becoming small lakes (Plate 9). Retreating Glacier Ice Ice Block Calves Off the Retreating Glacier Ice Block is Buried by Glacial Drift .. l I I ...........-w A Ice Block Melts Forming Lake Basin Plate 6. Pit Lake 16 —————_—— \~*/”—/ Groundwater Table Perched Ba sin Sediments Collect in the Basin Raising the Water Level Plate 7. Perched Lake l7 Embayment Lake Basin Bar Forming Across the Mouth of the Embayment Bar Separates the Lake and Embayment Plate 8. Origin of Two Lake Basins 18 Groundwater Table Conifer Forest Growing in a Depression Forest is Cutover Lake Develops in the Depression Plate 9. Lake in Cutover Forest CHAPTER III SENESCENCE AND EXTINCTION IN LAKES Senescence and extinction may affect an entire lake or only a part of it. Senescence is characterized by shallow water covering sediments and roots of flourishing aquatic vegetation where wave action is non- existent or slight. When these characteristics are present, the lake may be nearing extinction. Extinction occurs when the lake basin, or parts of it, no longer con- tains water permanently (Plate 10). Extinction may be temporary, a loss of water without permanent damage to the lake basin, or permanent, when the lake basin's water-holding capacity has been replaced by sediments (Chrow, 1964, pp. 23-41). These stages in lake develOpment are aided by Clastic sediments , marl, peat deposition, and climatic conditions. Man's use of the lake and surrounding upland may accelerate senescence and extinction. Role of Clastic Sediments Clastic sediment deposition probably occurs as soon as an ice-filled depression is exposed by a retreating glacier. The retreating glacier may cover the ice-filled depression with drift composed of sediments ranging from boulders to clay, and deposited in the depression as the ice melts. Thickness of glacial drift regulates the melting time of ice in depressions and the original depth of the lake basin. Clastic sediments may be deposited in lakes by effluent streams and runoff from bare slopes, excavations , ditches , and roads in the drainage area. Wave action may result in shore erosion with the sediments de- posited beneath wave base and in embayments. Shore erosion enlarges the surface area of the lake, but the eroded sediments decrease the depth 19 n'fl Lake Basin ~—— _ -— _ _ '_ _ —n- § ,..—— —‘ __ _ ,/’ Groundwater Table Temporary Extinction Sediments Permanent Extinction Plate 10, Types of Extinction 21 and volume (Plate 11). Wind—blown sand may fill lakes located on sandy soils. Depressions not containing ice may be filled by Clastic sediments deposited by glacier melt-waters eliminating the possibility of a lake originating there. Clastic sediment deposition may be studied when the lake bottom is exposed. However, where these sediments are overlain by marl and peat and it is impossible to examine them without coring because the basins of most glacial drift lakes are composed of Clastic sediments. Role of Marl Marl is a calcium carbonate sediment varying from chalk white to dark gray, usually unconsolidated, and dissolving with effervescence in a mild acid. It is carried by ground water into lakes where it may be pre- cipitated by chemical (Hale, 1903; Lane, 1908), animal (Hale, 1903), or vegetable (Davis, 1903; Pollack, 1918) means. Calcium carbonate occurs in glacial drift as limestone and dolomite fragments moved from bedrock of the same kind by the glaciers. Exposed carbonate fragments may be eroded from glacial drift and deposited in lakes by runoff. However, the greatest amount of carbonate was deposited within glacial drift where it could not be eroded by runoff, but is leached by ground water. The carbonate fragments may be located within the sur- face drainage area, or the groundwater drainage area. Marl may play a major role in the senescence and extinction stages of a lake's develOpment. Its deposition begins in shallow water and gradually moves lakeward, often more rapidly than encroaching vegetation (Bergquist, 1928, p. 280). Shallow water becomes even shallower as marl is deposited thereby reducing wave action and providing a desirable habitat for aquatic vegetation. The marl depositional pattern may result in an abrupt, steep lepe from shallow to deep water (Hooper, 1956, p. 115), the familiar "drop off. " Shore erosion increases the volume. Plate 11. surface area but decreases the depth and Effects of Shore Erosion ‘. 23 The presence of marl is usually indicated by a white to gray coating on semi—emergent vegetation, stones, and other objects. Marl is also indicated by the plant Potentilla _s_p. (Bergquist, 1928, p. 282) while Chara _s_p. , muskgrass, and Potamogeton sp. , pondweed, grow in areas where marl is accumulating. Marl pebbles may occur where there is an abundance of phosphates (Eyster, 1958) or indicate the purity of marl (Pollack, 1918, p. 251). Role of Peat Peat is the partially decomposed remains of water-saturated stems , leaves , and seeds. It varies in color from light yellow when young, to dark brown when older and more decomposed (Soper, 1922). Peat is ap— proximately 10 percent solid matter and 90 percent water, with a specific gravity of 0. l to l. 06, and weighing seven to 65 pounds per cubic foot (Seper, 1922, p. 13). Specific gravity and weight of peat are dependent on moisture content, type of peat, decomposition and sediments deposited with it. Muck is the darkest and most thoroughly decayed peat (Transeau, 1906, p. 35). Peat may be traced to vegetation being introduced to lakes in their youth by wind and birds (Schlicting, 1958). The first aquatic plants to adapt to a new environment are pioneers who improve the lake bottom hab- itat so less tolerant vegetation can root. Succession that follows is shallow-water vegetation gradually moving lakeward as soon as depth, light, water temperature, aeration, physical and chemical composition of the substratum, are favorable for their survival. The accumulation of plant debris accelerates the filling-in process of the lake basin and con- solidates the false bottom (Dansereau, 1952, p. 510). Vegetation may also be aided in its lakeward trek as a result of outlets being eroded, lowering the lake level. Plant succession reduces evapotranspiration losses by shielding the water from solar radiation, dropping its temperature and evaporation rate (Chrow, 1964, pp. 6—23). 2 4 Marl Plate 12. Marl and Peat 25 Aquatic vegetation types may adapt to one environment more readily than another with the most prolific growth of attached vegetation occurring on sedimentary peat, organic mud or clayey inorganic mud (Veatch, 1933, p. 411). Pontederia _s_p. , and Sagittaria 3‘12- , arrowhead, may grow with Nymphaea sp. , water lily, or nearer shore but are most prolific in shallow alkaline water over clayey inorganic mud and peaty sand (Veatch, 1933, p. 413). Vegetation can change an alkaline marl lake, or parts of it, into an acidic peat environment. This change will occur when decomposing veg- etation nearly covers parts or all of a lake basin (Veatch, 1933, p. 411). When this condition is reached, acid—tolerant plants such as leatherleaf may develOp and gradually crowd out the original alkaline vegetation. Deep, Open water may remain alkaline until completely surrounded by acid bog vegetation (Veatch, 1933, p. 411). The acidic or alkaline reac- tion arises from decomposing vegetation in the lake and not directly from either living or dead marginal vegetation (Welch, 1936, p. 739). A lake may be completely ringed by aquatic vegetation or a bOg margin. The bog margin prevents upland sediments from entering and decreases the surface area of the lake and the effectiveness of wave action. Extinction is rapid once a bog margin and false bottom develop (Jewell, 1929, p. 473). Natural regression of the lake basin toward drier conditions occurs when the transpiration rate of vegetation becomes greater than the water- retaining capacity of the peat mass (Dansereau, 1952, p. 494). Organic matter may accumulate at the rate of two feet annually (Coburn, 1933, p. 58) but a long—range estimate of 0.72 to 2. 16 inches per century (Soper, 1922, p. 13) seems more likely. Mats of aquatic vegetation have been reported to grow lakeward one foot every three years (Olson, 1944, p. 41). Role of Men Man's activities can also decrease the size of lakes. These include 26 dredging outlets , improving drainage facilities , upland develOpments, water pumpage, allowing effluent to enter, deforestation and reforestation. Historically, land covered by lakesthas been considered more valu— able than the lakes. Often the outlet was dredged with intentions of com— pletely draining the lake. This activity was successful in many instances but equally as unsuccessful in others resulting in a shallower lake fit neither for plowing or fishing. Such a lake could easily be commanded by aquatic vegetation. Better drainage was reported as a cause of lower lake levels in the Huron River valley over 60 years ago (Weld, 1904, p. 48). Tiling of fields in the drainage area (Plate 13) of a lake may have an adverse ef- fect on the lake level (Veatch, 1940, p. 103). Good drainage increases runoff causing less water to reach the groundwater table, thus lowering it. A lower groundwater table means less available water to replenish evapotranspiration losses from the lake. Runoff is also increased by extensively developing the drainage area. Roofs , roads and ditches speed water to the lake where it may be dis- charged through an outlet. Pumping water from the lake or drainage area in quantities the ground— water reservoir is unable to immediately replenish may cause the lake level to decline and vegetation to invade. Excessive pumping lowers the groundwater table and lake level. Effluent entering a lake will charge it with nitrates and phosphates that make for prolific algal booms. Residues deposited reduce the volume of the basin. Riparians may contribute 15—20 grams of nitrogen per person per day to the lake through use of private sewage disposal systems placed adjacent to the lake so they can drain through ground water into the lake (Nichols, 1965, p. 1322). Effluent entering Crooked Lake in Barry County from a nearby dairy products processing plant adversely affected the qual- ity of water, causing a prolific growth of aquatic vegetation. The same was true of "treated sewage” entering Jordan Lake at Lake Odessa. Groundwater Table Before tile Tile Tile installed recently Lower lake level and groundwater table Plate 13. Effects of Tiling 28 Deforestation (Plate 14, Figure 1) may accelerate senescence (Jewell, 1929 , p. 471). Without humus or forests to protect upland lepes, water may easily erode them, depositing clastic sediments into the lake. With no forest cover, rain may pack the soil, increasing runoff. Reforestation (Plate 14, Figure 2) may have a long-range effect on water yield (Eschner, 1965). A dense growth of conifers may intercept a good share of available precipitation. Roots can also lower the ground- water table. Ero ion A _,_2'4il’ A“ , ‘ n" l‘ , .g‘.’;-y ’ .— .—— a '- Cla stic Sediments ,._;3..x;2,-.. .. , Groundwater Table Figure l . Deforestation Tra ns piration Interception of Precipitation " f in” / Groundwater Table Figure 2 . Reforestation Plate 14. Deforestation and Reforestation 29 Role of Climate Climatic conditions have varied in the past as they do today. Cli- matic variations may be indicated by archeological records , fossil animals and plants, spores and pollen. Pollen indicates higher temperatures than today, lasting from about 5000 to about 2000 B. C. followed by a general cooling trend that reached a minimum about 500 B. C. , followed by another temperature rise. The last major warming trend before the present time, occurred about 1000 to 1300 A. D. About 1600 A. D. the climate changed again toward cooler conditions and a "Little Ice Age" that lasted from about 1650 to about 1850 A. D. In the northern hemisphere, during the past century, there have been cyclic fluctuations, warmer to colder trends , each lasting about a decade. The trend has been toward warmer temperatures than re- corded in decades prior to 1900. Since 1920, there has been a mean an- nual rise in temperature of about 3. 5° F. , and the rise in winter temper- atures has been about twice as much as summer temperatures (Dorf, 1960). Presently, the northern hemisphere may be entering a 90-year cycle of cooler temperatures (Maynard M. Miller, 1967, oral communication). The earth may be heading toward another glacial stage, perhaps 10,000 to 15,000 years hence (Dorf, 1960, p. 362). Aquatic vegetation may be aided by local hydrologic changes, shown by shorelines and lake level evidence at higher elevations than the present lake level. Shorelines and evidence of lower lake levels would be con— cealed by sediments. Warmer climate conditions caused the glaciers to retreat, accompanied by less precipitation and lower lake levels. Cooler weather triggered minor glacial advances characterized by greater precip- itation and probably higher lake levels. Lower lake levels enabled vegeta— tion to migrate lakeward and left shallow water areas shallower or exposed to the atmosphere. When lake levels rose again or returned to their former higher levels , much of the aquatic vegetation died when it was unable to adapt to greater depths. Vegetational remains accumulated resulting in 30 the area of accumulation being shallower than prior to low water condi- tions (Plate 15). Aquatic vegetation may root easily in soil that lies under newly formed water area (Indiana Water Resources Division, 1949, p. 7). Climatic related fluctuations in lake levels continue to occur, with higher levels after abundant precipitation, and lower levels in times of drought. Drought ends and lake level rises. Vegetation must readjust. Peat deposits remain. Plate 15. Effects of Drought CHAPTER IV LAKES STUDIED Barry County Eight lakes were studied in Barry County (Map l). Glacial drift was at least 200 feet thick in the vicinity of the lakes. Barry County was subject to a drought resulting in a 28. 88 inch pre- cipitation deficiency from 1960 through 1964 (Michigan Water Resources Commission, 1965, p. 6) and a 20. 75 inch precipitation deficiency from January 1962 to June 1964 (Michigan Water Resources Commission, 1964). Drought conditions prevailed through August 1965. Lower lake and stream levels resulted from drought conditions. Many lake levels were the lowest in recent history according to area residents. Other lake levels were normal. Cloverdale Lake Cloverdale Lake (Map 2) is in sections 20 and 29, T2N,R9W, but has been intermittent in the latter section for about 40 years (Deeter, 1928). The surface area in January 1959 was 58 acres (Michigan Department of Conservation) or about 125 acres if the intermittent area was included. The surface area was 12 acres with a maximum depth of about 30 feet in August 1964. Cloverdale Lake was served by an inlet from Wilkinson Lake, and an outlet flowed into Long Lake. A water-powered mill was Operated between Cloverdale and Long Lakes in earlier times (Lake, 1873) using 15 (Hale, 1903, p. 117), or 16 (Hale, 1903, p. 110) feet or more difference in lake levels. An elevation difference of 12 feet between Cloverdale and Long Lakes is noted on a U. S. Geological Survey topographic quadrangle (Hastings 15" sheet, 1951) of the area. The inlet and outlet have not 31 32 T 9' 4 N T 3 {3 N 7 5 . 4 T 5 0 2 '3 § N T 1 . N R10W R9W R8W R7W 2. Cloverdale Lake 6. Daggett Lake 3. Long Lake 7. Long Lake 4. Head Lake 8. Little Payne Lake 5. Guernsey Lake 9. Carr Lake Map 1. Barry County 33 Map 2 C /overdalc Lake N Jeala, T8 N, R9W A ’45 Aerca -"~-~ 3OF1'.’ 'Nax. DcP‘H-w // I ~‘\ Jcole IinSBOOFt "" — —5hor¢/ine -/?5'? —_Jher¢ [inc —I964 SPLJA ‘J 7h?” \ \p A\p W‘ ”0“, ---- ‘ P-Peaf’ , V rt Scale [in-40!": C ? I . D II “D e < P ‘65 < P I»! Joundiny Rod Re cord faflon h weed 34 functioned since 1956. In August 1964 the lake level was four to six feet below the 1920 level according to local residents. The drainage area is about 400 acres. It is composed of unsorted sand, gravel, boulders and clay. Dark brown, pulpy peat deposits sur— round the lake. The east shore is the site of seven cottages and a county park. A boat livery is operated on the south shore. Access to the water was through a dredged channel. The original bottom slopes lakeward at three degrees. Dark brown, pulpy peat is deposited over the original bottom. The peat may also be yellow—brown to light brown where dead aquatic vegetation has decom- posed at the water's edge. Pondweed was the only noticeable attached aquatic vegetation growing. It grew prolifically up to depths of 11 feet. Dead pondweed built an abrupt SIOpe of about 35 to 40 degrees along the eastern shore at the waters edge. The vegetation was deposited by wind and wave action, being held against the shore by the addition of more dead pondweed. Long Lake The Long Lake (Map 3) level has remained unchanged for the past 40 years (1964) according to local residents. An outlet flows most of the year but an inlet from Cloverdale Lake has not functioned since 1956. The drainage area is about 1 , 150 acres with maximum relief of about 115 feet. The drainage area is composed of unsorted sand, gravel, boulders, and clay. Parts of the drainage area are used for pasturing cattle. Nu- merous cottages are present but additional space is available for devel- opment. A resort and boat livery are located on the east shore. The original bottom slopes lakeward at 14 to 18 degrees. Chalky gray marl is deposited over it. Calcium carbonate in solution gives the lake an emerald blue cast. The present bottom slopes lakeward at less than one degree in the "shallows , " water less than four feet deep in the north and central parts, 35 Map .3 Long Lake Jag/.5: I630 (21,72 MR 9 W 289 A a re: N 43 Ft ~Max. Q¢P+h c Scale [in-960Ff: Sounding and Record \ I , III [‘17 4, J41 254871016517 ll (I ll ll 9 I It VVV P "/ AH-Arrowhoade \ BR-Bulrueh CT-Caffai/e WL‘Wafor Lilia \ .3 \\ :53. \Z P- Poof W- Wa+¢r NqMar'l VCrt Jcalc Iin. = 30 Ff: to about 35 degrees elsewhere. The latter measurement was common, sometimes less than 20 feet from shore, giving an appearance of a "drOp- off. " A dark brown, fine-textured peat layer, less than six inches thick is deposited over marl in the shallows at the north end of the lake. Pondweed, muskgrass , water lily, arrowhead, and bulrush were the attached aquatic vegetation growing in 1964. Pondweed grew at a depth of 17 feet. However, pondweed and muskgrass seldom grew at depths over 10 feet. Water lily and arrowhead grew at depths to five feet, but most prolifically in the shallows. Bulrush grew sparse in depths to three feet. Cattail grew on peat deposits adjacent to the shore and lakeward but seldom at depths greater than a few inches. Head Lake The drainage area of Head Lake (Map 4) is 403 acres with maximum relief about 100 feet. The drainage area is composed of unsorted clay, gravel and boulders , with a maximum relief of about 100 feet. Parts of the drainage area are used for pasture. About 10 cottages and mobile homes are distributed along the shore leaving most of the lake frontage available for develOpment. Access may be gained from a county road passing within 10 feet of the west shore. The lake level has not fluctuated over two feet during the past 25 years (1965) according to local residents. The lake level was about six inches below normal in August 1965. The original bottom slopes lakeward at two to four degrees. Dark brown, pulpy peat is deposited over the original bottom. Peat is yellow- brown in areas where it recently decomposed. Brown leavy peat occurred in places near the east shore where oak leaves have accumulated. Pondweed , water lily, arrowhead, and bulrush were the attached aquatic vegetation growing in 1965. Pondweed grew at depths to six feet. Water lily grew at depths to two feet. Arrowhead grew sparsely at depths to one foot. Bulrush grew at depths to one and one—half feet. 37 Map 4 He 0 d La He Sec. 8 (’9, TZN, 92 W_ ?7Acr¢5 6Ff‘l‘7ax. Depth Scale lin= 450Ft l6 \ - / \ (I \\ \WL" \ \ \/ fl, ’ \g l A H- Arrowhe ad \§ l I \\ IWL \ t I I BR-Dulrueh \7 )5 ” ’5 WL-w + Lu ~ \\ O .7 7 \9 A! ’___‘_,—v-’"\ \ -‘x I J \\ // I” \ (’~“'“ I (k WI. \\-3 I \\ \vs I“ ' \\ " / \\ ’,/ WI. I z a f 5: .5 :7 Q 1,“, A ;_ #7 w p W-Wa+er M II xz 13 I4 I! /6 l7 {s B' p-p.a+ A e 4 4 t ‘ W t ‘ V‘Pfi Scale [in-ZOFf. \_______, p Joundlng Rod Record filter/on ,2 3455 ~75 9101/ Ills/IIIM’N'IO Dggfh 4.9425312422235655! Oriya/00pm 5 /7 so l6 :5 :I 19:: 7 4 I: I: 6 [6 N 231410 figWCCd -V VVWVM—JgrtVWK/ww 38 Marl was not recovered at any station but it was observed in a spoil pile left from dredging in the southeast part of the lake. Guernsey Lake Guernsey Lake (Map 5) consists of two basins, " Big Guernsey” (the western basin) and "Little Guernsey. ' A dredged channel connects the two basins and replaces a natural, vegetation clogged channel. Water flows east through the channel. An outlet flows most of the year. The drainage area is about 825 acres with maximum relief of about 100 feet. The drainage area is composed of unsorted sandy gravel, boulders , and clay. Cattle are pastured on part of the drainage area. About 25 cottages and a trailer park have been built leaving additional space for development. A boat livery on Big Guernsey provides access. The original bottom slopes lakeward at 19 to 58 degrees with a mean of 37. 5 degrees for six measurements. Chalky to organic gray marl is deposited on the original bottom. The organic gray color is characteristic in areas of abundant aquatic vegetation. A marl shelf has developed along the east and south sides of Big Guernsey. The lakeward edge of the shelf dips at 35 to 40 degrees. A wide marl beach occurs along the northern side of Big Guernsey. Pondweed, water lily, arrowhead, and bulrush were the attached aquatic vegetation growing in 1964. Pondweed grew at depths of three feet. Cattail flourished on peat deposits bordering the lake at depths of a few inches . Daggett Lake Daggett Lake (Map 6) is in public ownership with a campground and bathing beach on the east shore. The drainage area is 385 acres with maximum relief of about 120 feet. The drainage area is composed of un- sorted gravelly sand, boulders, clay, and sorted sand. The lake level declined about three feet from summer 1962 to summer 1965, with a four-inch decline occurring during the latter summer. The \& Hop 5 Guernsey Lake HI. I ."/l 60C./7‘/91 TZN,R7W ZIBAcrea F13 A ZBF‘I‘. Max. Depf‘h ,, \ I, 7;“ I A5colc nn =600Ft: (\‘ _. r , g‘ifif/ A3/ I - I a w ‘ 00 t wz.\ 58D \ \ ~\ \\ \ o—‘\\ \\ \ (,‘ (‘\ ‘—’~\ \ \\ (/ W2\_‘ (\ \\WL\:\\) r”\ \(‘___ \ ’ .‘x\ \ \V \‘r’ C7 8c 09 p' E ' ”E \ ’ 8c\> \ 1 I \ WL V V V v "V/\ 3‘ __ r \\ S n \\ WL,/) _ (\(JL 1) ”5:3 ”Mt-4 \ '1 \ ’ "‘ ~-’* ‘~ I \ \ {CT ‘ . - I \\ l \‘ P l 'n / I Prcéent’ Jhcrel: e \ 65 HIT z, I O (I, \ Peal Deposlts ' W w ~ ’ P [‘7 r1 / " // L / 3' 3 I \ 24 a: I / /“ I \\ M // 1‘53) [7 , I 1 / P /’;' \ / I ;~/ /, BR-Bulrush Vcrf: Jcalc linzaop’t / I/é::”’ (T, CT‘Caffail W- Wo+cr / I ,4? WL‘Wafer z_;/y M-Marl I - l (\{j' / HP Pea+ . 1‘ I I ‘ ’\\\:fl‘:\\g;.3 Z’I \ \\ _) to r \' 221 I \\ W P P\ \ {LI-J2" I P WW “'5’“ (7:5 ‘- \ I «E76527 '~’ PI \ l ‘ - \ I W7...‘ d’ \_‘/’ Jounding Rod Record 4561 [273437 /6/8 I! I, I4! 9 IOII RUM/5167 I I u] IJ4II5'I0/lolzl III/1 7 8010/] VVVVV/ V’ 55’ . A ‘ VLL___ / .‘_.... \\ / IZ (é NOPG ////\' [ \W DaggeH Lake cr/fiy \(j, 6cc.l,TZMRIOW // a; I cr ‘3 /4 Acres - (I / j ' \ l5Ft-Max. Dcp+h 3 Jcalc Iin.=/50F+. AH-Ar‘rowhead / CT‘CG++OII WL- Wa+¢r L'I 1‘ I y I \ 1 \ 4 \\ Z \ : A‘ i \ I, '3‘ l | : I { // WL )9 IO / 5 I 7: - i -_ § I: _ I? f I, l 'WL’ B l ‘ I l I 4‘ l \‘ \J I \ p \\ \-” \‘ ' // // /// J6 /I / I ‘/—~\~/ /// ‘ // 51 p I l { \ ‘ .- \~‘\ W“ ch‘cr- \hp” \\\ p“P¢a+ w1\\ / Vcrf. 5ca/o lin=30ffi \\ f6 5‘ A' D 9 /_o ” 5 £2 43 44 5’ w / P 7‘ 317an l2345678 IOU/(I’ll gaff}? //59//69I 4/0/05/ Dayna/003M .3 5 N Is u I; I! 8 9 u /'7 /o a 8‘ Pondwcad v v v lv,v V ., l, , 41 surface area and maximum depth decreased from 15 acres and 18 feet to 14 acres and 15 feet. The original bottom lepes lakeward at 7 to 11 degrees. Dark brown to yellow—brown, pulpy peat is deposited over the original bottom. Pondweed, water lily, and arrowhead were the attached aquatic veg— etation growing in 1965. Pondweed grew at depths to nine feet. Water lily grew at a depth of two feet. Arrowhead grew at a depth of one foot. Cattail, marsh grass and sedges were common on peat deposits bordering the lake. Long Lake Long Lake (Map 7) is in public ownership and development is limited to a state park day camp on the eastern shore where part of the lake basin is dredged to make a swimming area. The drainage area is 207 acres with maximum relief, about 60 feet. The drainage area is composed of unsorted sand, boulders and clay, and deep sorted sand. The lake level rose three inches from early August to late September 1965. The outlet of Long Lake is dammed. The original bottom 510pes lakeward 3 to 16 degrees. Marl was de- posited over the original bottom and peat deposited over the marl. The marl is chalky to organic gray containing seed cases. The organic gray cast is darkest where the overlying peat is three or more feet thick. The peat is dark brown and pulpy, reaching a maximum thickness to six feet. Pondweed, water lily, and bulrush were the attached aquatic vegeta— tion growing in 1965. Pondweed grew at various places; water lily grew along the north shore. Bulrush was most prolific, covering large areas. Little Payne Lake The drainage area of Little Payne Lake (Map 8) is 25 acres with max- imum relief of about 10 feet and composed of deep sorted sands. The up- land is undeveloped. Access is over a county road within a few feet of the ea st shore . 42 Map 7 L on 9 l. a he scazoztzuzznm mow I45. 7 Acres 4 F ‘t -Nax. Depfh .5:an BR“ Bulruch / WL- Wahr Lilia: I_I V W- We fer P-Poa+ N-Marl Vcr'l: Jca le lin.‘ JOF‘f. Sounding Rod Record 31‘0in" I 2 J 4 Jr 1 II 14 M [/2344 z/////// .3666 43374534 I: III 2721’” I! V vv 43 Sounding Pod vPecar-d Pia/96 tiff/e Payne Lake 3¢c./9,T3N,n/OW IO Acres Z7Ft-Nax. Depfh Jae/o [in =ZOOFt C C' a a’ w w K E5 N L\\ W-v Warfar- 1‘7" Marl Var-k Jen/c Ii... :ZOF-fi Jfafion [2345678 Depfh 517/III3/4 Origina/Dggfh 6 :1 2f :7 la z! [6 la Pond weed 44 The original bottom slopes lakeward at 39 to 73 degrees. Chalky gray marl is deposited over the original bottom. Calcium carbonate in solution gives the water an emerald blue cast. Attached aquatic vegeta- tion is limited to a few minor areas occupied by water lily and bulrush. A narrow thin peat deposit surrounds the shoreline of the lake. Carr Lake The drainage area of Carr Lake (Map 9) is 102 acres with maximum relief of 25 feet. The drainage area is composed of unsorted clay, gravel, and boulders. A woody peat underlain by dark brown, pulpy peat is adja— cent to all but the west shore. The peat deposits have limited develop— ment of the lake to one cottage and a mobile home. A boat livery on the west shore provides access. The original bottom slopes lakeward at 28 to 73 degrees with Chalky gray marl deposited over it. A marl shelf on the west side dips lakeward at 33 degrees. Calcium carbonate in solution gives the lake an emerald blue cast. Pondweed, muskgrass , water lily, and bulrush were the attached aquatic vegetation growing in 1965. Pondweed and muskgrass grew at depths to eight feet, water lily to four feet. Bulrush grew sparse to dense between the water lily and shore. Cattail grew on the moist peat deposits out to depths of a few inches. Osceola County Seven lakes were studied in Osceola County (Map 10). Glacial drift thickness was 500 feet or more in the vicinity. Osceola County, and surrounding counties, experienced drought condi— tions that resulted in a 6. 99-inch precipitation deficiency from 1960-1964 (Michigan Water Resources Commission, p. 6, 1965) and a 5. 31-inch pre— cipitation deficiency from January 1963 to June 1964 (Michigan Water Re- sources Commission, 1964). Drought conditions ended early in 1965. 45 Map 9 Carr La he \ T4N. ne—vw N 29.5A6res 44 Ff: -P7ax. Depth Scale [in =JOOFf' A 18A: 8345' C5 C’D ' W W H w M \ \ W— Wafer- N‘Nar/ Vcrf'. dear I. /in. = JOFf‘. B}?- Bu/rush CT‘Caffall WL‘ Wa+er Li/y Joundi Rod pocord Jfa flan ll 7 It" I ”II/l —./V v V I IO 33 RDndwccd 46 15 1'7 f4 1'6 . 13 1'2 11 R10W R9W R8W R7W 11. Alexander Lake 15. Park Lake 12. Big Lake 16. Austin Lake 13. Myrtle Lake 17. Hewitt Lake 14. Hicks Lake Map 10. Osceola County zooHr—a ZLDI—‘I—J ZONr—l ZVI—II-a 47 Alexander Lake The drainage area of Alexander Lake (Map 11) is 102 acres with max- imum relief of 70 feet. The drainage area is composed of unsorted gravelly sand, boulders and clay. Parts of the drainage area are used for agricul- ture. A swamp surrounding the lake had limited upland develOpment until recently. In 1965, a channel was dredged through the swampy peat de- posits and cottage lots were plotted on the channel. Access is gained from a county road adjacent to the west shore. The lake level has risen about one foot within the past ten years killing some upland vegetation growing on the peat deposits. The lake level rise is probably due to the county road being built higher at the lake outlets. The culverts conveying water away from the lake may also be higher than the natural outlets. The original bottom lepes lakeward at one to three degrees with dark brown pulpy peat deposited over it. Pondweed, water lily, and arrowhead were the attached aquatic veg— etation growing in 1965. Pondweed grew at depths to 12 feet, water lily to five feet. Arrowhead commonly grew with pondweed at depths less than four feet. Big Lake The drainage area of Big Lake (Map 12) is about 950 acres with max- imum relief of 70 feet. The drainage area is composed of unsorted clay, gravel and boulders. Parts of the drainage area are under cultivation. Numerous cottages have been built on Big Lake, but additional lake front- age is available. Peat deposits have limited development along the south shore. Access may be gained through a county park and at several boat liveries. Big Lake is served by an outlet and intermittent inlet. The lake level was about six inches below normal in August 1964. The original bottom slopes lakeward at 5 to 10 degrees. Chalky to 48 Map M Alexander Lake 50c.ZZ,T/7N,PBW 5.7 Acre: I7F‘f: “Max. Depfh Scale Iin.-/00F't A H—Arrawhead W L‘Waf’er Lily \.-__ W-Wafer P-Pea+ Vert Scale lin. BZOF‘I: Soundin Rod Record 6 Station 91/5 717797 V’s/fww 4 f V d V 49 Hap Id ' Big L a He Jae. 7I'l8,T/7/V,F?7W l 240 Ac rec \ 85 Ft-Max. Dep'I-h \ \AH I BR .. seal. Iin.= 600Ft \ \......._,/ '\9 __’_V_h D~\Z_.§o' ( /{ a my \/ A H-Arrowhoad. .2 BR-Bulrush V ‘ \ C T-Caffail- \\“t\ L\ WL-Wa+er Lily . B 4 l: —B A I 2A! a 3 48! C 5 6C: D 7 D, # w w w NW w m M n n W— Waf'er F—fi w 41,: M~Narl x l/ f: 5 I l' .= % er cac m JOFt Joundi Rod Record 0‘ “‘1 I: 9 l 9 .s' 4 1 e Hal . ed l5 y lo 171: 'B' I? If! , . V w If t”- 50 organic gray marl containing seed cases is deposited over the original bottom. The organic gray marl occurred in areas of abundant aquatic veg- etation. The marl forms a shelf from shore with the lakeward side dipping about 40 to 55 degrees. Deposits adjacent to south shore consist of dark brown, woody to pulpy peat reaching a maximum thickness of about three feet at the lakeshore. Pondweed, water lily, arrowhead, and bulrush were the attached aquatic vegetation growing in 1964. Pondweed grew at depths to 16 feet. Water lily grew at depths to three feet. Arrowhead grew at depths to two feet. Bulrush grew alone and in association with arrowhead, to depths of two feet. The attached aquatic vegetation was limited in its lakeward migration by the abrupt lakeward edge of the marl shelf. Myrtle Lake Myrtle Lake (Map 13) is undeveloped but part of the drainage area is used for pasturing cattle. The drainage area is about 410 acres with maxi— mum relief of about 55 feet. The drainage area is composed of unsorted gravelly sand, boulders and clay, and deep, sorted sand. Access is by a county road near the eastern shore. The recent lake level history is that of a declining lake level for 13 years, until spring 1965. By late August 1964 the surface area had de- clined from 5. 2 to 2. 5 acres. Woody upland vegetation, mainly willows, encroached rapidly before being halted by a lake level rise of about three and one-half feet during the spring and summer 1965. The lake level rise covered the base of willows with three feet of water. Attached aquatic vegetation is nearly nonexistent with pondweed being observed at only one station. Absence of attached aquatic vegetation may reflect the sudden lake level rise or the rich organic brown color of the water that allows light to penetrate only one and one-half to two feet. Hicks Lake Hicks Lake (Map 14) is in a drainage area of about 480 acres with $80. [Sf/6, T’BNJ REL 9Ft-Max. Dep-i‘h e .r. In F a w L ... \oo _ A 2 a .m . P \Aan. _ ’A u... .r. u up v o u. r A I N W 0. P9 2 o n a . C MN 5 J m Vet-1‘: «Seal. ”n. =3 £0Ff: Sl .4... ~“mm...- .—-_. ,.....L.- .90. ._.: Sec. (Sf/6, TIBN. REL 5.2 Ac res 9F‘t-Max. Dep+h Jeale Iin.= 85/:1‘: Myrtle Lake Map I.) Verf: Jeale lin. = 60F?! Sl ’ 'y 1., K. __ If i» / s. _ {A .4 ., \ . .. .037 . in? .1/ .m .. ~ ,.. 4 \x J , _ .. _, ’l.‘ .Lu. I l ., a . . . r . )4.» . t .. . _ .‘ _ . .Hg .5 . .s .. \‘ _ .. a .; rfl.HB«.u...n.~ t]. J .. tr ....Hu.b..n its 5.1 .14.» ..,.u...!\ ,. . . (.5... 1.91.3.6... .r. . ._ _ . _. A 52 Nap 14 f I » . H 37' ;’ '- HIGHS Lahe . jg; \25’, I Jee. 20121, TIQN, R8 w ’ / ,I & IJJAcrea / , ’ ,I’ #6 g5. aoFt-Max. Depfh ‘f,/// /’ A I A 5Col¢ lln.=45'OF‘l'. @/ f/ ’2 I, W€// AH-Arrowhead A / / _ ’ 1’ 3’? BMW”. w-wa+..- WL- Wafer Lily P-quf Vert Scale lin- SOFf. [2' 3 4, “(Anga p \‘tx ‘VT‘\XV l \ \ \ 53 maximum relief of about 90 feet. The drainage area is composed of un- sorted clay, sand, gravel and boulders. Parts of the drainage area are used for pasture. Peat deposits surround all but the eastern shore, the site of numerous cottages. A public access site is on the northeast cor- ner of the lake. The lake level was nine inches below normal in July 1964. The original bottom SIOpes lakeward at one to four degrees. Dark brown, pulpy peat was deposited over the original bottom. Pondweed, water lily, arrowhead, and bulrush were the attached veg— etation growing in 1964. Pondweed grew at depths to 16 feet, water lily to five feet. Arrowhead was growing with water lily at depths of a few inches to about one foot. Bulrush grew at depths to three feet and cat- tails grew over part of the moist peat deposits and out into water a few inches deep. Park Lake Park Lake (Map 15) is in a drainage area of about 70 acres with max- imum relief of about 50 feet. The drainage area is composed of unsorted sandy clay, gravel and boulders, and deep sorted sand and is under cul- tivation. Park Lake is in private ownership but access was permitted by the owner. The original bottom slopes lakeward at 6 to 12 degrees and is covered with dark brown pulpy peat. Pondweed, water lily, and bulrush were the attached aquatic vegeta— tion growing in 1965. Pondweed had nearly covered the present bottom at depths to nine feet, and was observed at all but two stations. Water lily and bulrush grew sparse and intermingled adjacent to all shores at depths of one and one—half feet or less. Austin Lake Austin Lake (Map 16) is in a drainage area of about 540 acres with maximum relief of 70 feet. The drainage area is composed of unsorted sandy gravel, and clay and boulders. Peat deposits surround all but a ,ue'. ,. / ” \\ Pa rlt L alve / BR- Bulrueh \ Sec. marge/v, new II "E WL- Wafer- LUV \ 8.2 Acree / ' 9Ff.‘ ~Max. Depfh // ( Joule lin.‘ 125’”: / / // | / / / / l . I4 I I A ‘1‘ I _ 4 4 _ 9;. _. 3 3L 1 \l 15 \ \\ ‘ \ 1‘ \ \ l6 \ l \ \ \ \ \ \ \ | \ \ \\ \ /’7 \ \ \ \\ \\~_ fl, \\‘\ ‘\\ /"// we a I .3 4 ' ' A - z . A W-Wofe-r ' \ p-P00+ l vue Joule linuZOFx P 55 AH « -~‘\“ ”37’1/ \‘ Hap I6 AW/ AH'Am-owheed Ausf/n [-ch /// ~C H’ '1 53c.llfl4,Tl8N,RlOP // C: 1: f" L, V,,\ acme Acree /;/ w a ” H’ ‘ 37Ft-Max.0ep1 / a ’ A Scale lin.=ZZSF+. // A / 5‘ a' w [I I 00 c D w p . 5 . ---- \‘\ 5' W‘Wafer P- Peal Ver'l: Joe/e ”n. - 30F}. 56 small part of the east shore where most of the ten cottages on this lake are located. The lake level was normal 'in August 1965. The original bottom lepes lakeward at one to seven degrees. Dark brown, pulpy peat is deposited over the original bottom. Pondweed, water lily, and arrowhead were the attached aquatic vegetation growing in 1965. Pondweed grew at depths to 12 feet and water lily at depths to seven feet. Arrowheads grew at depths to one foot in isolated patches. Cattails grew on the peat deposits and lakeward to depths of a few inches. Hewitt Lake Hewitt Lake (Map 17) is in a drainage area of about 79 acres with maximum relief of about 75 feet. The drainage area is composed of un— sorted sandy gravel, clay and boulders, and deep sorted sand. Parts of the drainage area are used for pasture. Farm buildings and a barnyard are about 100 feet from the south shore of the lake where a boat livery is operated. Eleven cottages are along the shore. The original bottom slopes lakeward at 9 to 11 degrees with dark brown, pulpy peat deposited over it. Clastic sediments, mainly sand, were deposited in a small area near the north shore. This is from soil erosion on the adjacent upland. The elastic sediments displaced peat previously deposited at that point. Pond- weed, water lily, and arrowheads were the attached aquatic vegetation present in 1965. Pondweed grew at depths to 11 feet, water lily at depths to five feet and arrowheads to one foot. Clare County Pike Lake was studied in Clare County (Map 18). Glacial drift in its vicinity is over 500 feet thick. Drought conditions in Clare County are the same as in Osceola County, described on page 44. Pike Lake Pike Lake (Map 19) is in a drainage area of about 179 acres with maximum \ ‘9... 4" A _ 5 7 All-Arrowhead WL‘WOf'.‘f Lily C 5 - C las‘lic 6 e diments flap /7 Hewifi‘ Lake a“. 27/55, 72 ON, 9 IO w 20.4Acree JOF’t-Max. DcPf-h lin.=l50Ft 6 Z 95' W p I "If ' D W D p l, . ‘ W- We‘l‘r’ .l‘ P-Pecn‘ 1“ Verl: Jag/e [in 830/: 7 0‘8 I .00? \ / f 5‘- M {l {A I .3 5 l l I l 3 z ‘ " ‘WL 5 l l ’ I ” I 3 76 IO “““i\\ 58 zer—J zmHt-l ZONE! ZVr—II—J R6W RSW R4W R3W 18. Pike Lake Map. 18. Clare County BR- Bulrush \ FIG-Harsh Gmu\\ 4 WI: Wa+cr U," \ Ha I? ’4 Pike La/Te SchZ T/BMR6 W I4 AGI'OJ ”Ft—Max. Depfh JCOIO lin. =IBOF‘t W \ W—Wafcr' p_ P~P¢a+ Vcr'l‘. Scale Iin.'£OFt \\”/\~ _____________ -I’ II a 14 I; 15 I? (6 49 B IOIOI ’71: ’0’ 56- 2410311 ////— 314 V, 60 relief of about 10 feet. The drainage area is composed of deep sorted sand. Pike Lake is in public ownership and the east shore is a popular roadside campground. The lake level declined about two and one—half feet during the ten years prior to spring 1965. Woody upland vegetation rapidly advanced over the former bottom. However, the lake level rose about two feet during the spring and summer, 1965 , covering vegetation that had ad- vanced. The original bottom slopes lakeward at two to four degrees and is under a cover of dark brown, pulpy peat. Pondweed, water lily, and bulrush were the attached aquatic vegeta— tion growing in 1965. Pondweed grew at depths to 10 feet. Water lily grew sparse at depths to two feet. Bulrush grew at depths to three feet. Marsh grass grew abundantly on the western side of the lake and sparsely with water lily at depths to two feet. Wexford County Two lakes were studied in Wexford County (Map 20). Glacial drift in the vicinity of the lakes is over 700 feet thick. Drought conditions in Wexford County are the same as in Osceola County described on page 44. Most lake levels were below normal. Unnamed Lake This lake (Map 21) is in a drainage area of 21 acres with maximum relief of about 30 feet. The drainage area is composed of unsorted gravelly sand, boulders and clay, and was recently cutover for pulpwood. The lake is undeveloped. Access is possible from a trail adjacent to the north shore. The lake level was about four inches below normal in August 1965. The original bottom slopes lakeward at 5 to 13 degrees with dark brown, pulpy peat deposited over it. Pondweed and water lily were the attached aquatic vegetation growing in 1965 with pondweed at depths to 10 feet and water lily to four feet. Marsh grass and cattail grew at the waters edge. 61 2.2 2'1 R12W R11W R10W R9W 21. Unnamed Lake 22. Meady Lake Map 20. Wexford County ZNNr—j zooNr—J ZANH Zo—INF‘J ' 62 C T / -7rfi‘\ Nap Z/ / ,3 \\ Unnamed // w L \\ NE&,5¢c.5, TZZMRQW ’/’/, ________ —-‘~‘ \\ /. 5 Ac r06 /’/ “\ \ 9Ft—Nax. Dcpfh ’/ ’ \\ Jen/c lin.= 60Ff. I \ \ I, I, ll \\ V x’ ’ \ \ / . \\ /,/ ' c T- Cam” \ \ I] / WL- Wafer Lily \\ \\ / lI . ) f..- "——-‘\ a A l L L 4 :4; Q- A' H W-Wefsr' P 5"?” .. M, ' . ,. .. Vcrt aka!!! find-05’- ! ~ , .s L 4 It... a: 4L 44 w \ 63 Meady Lake Meady Lake (Map 22) is in a drainage area of about 103 acres with maximum relief of about 70 feet. The drainage area is composed of un- sorted sandy gravel, boulders and clay, and deep sorted sand. The lake is surrounded by a narrow margin of peat giving it a bog appearance. The peat is dark brown and pulpy, but is black, woody, and leavy at the sur- face where it is overgrown by leatherleaf. The lake is in public ownership and undeveloped. Access is possible from a trail passing within one-tenth mile of the lake. The original bottom slopes lakeward at 8 to 20 degrees and dark brown pulpy peat was deposited over it. Attached aquatic vegetation was limited to pondweed observed at one station. Missaukee County Four lakes were studied in Missaukee County (Map 23). Glacial drift thickness in the vicinity of lakes studied exceeds 500 feet. The Missaukee County area experienced a precipitation deficiency of 6. 31 inches from January 1962 to June 1964 (Michigan Water Resources Commission, 1964). However, in 1964 accumulated precipitation was 0. 1 inch above normal (Michigan Water Resources Commission, 1965, p. 6). Most lake levels in this county were below normal. Lake Missaukee Lake Missaukee (Map 24) is in sections 1, 2, 3, 10, 11, and 12, T22N, R8W, and sections 6 and 7, T22N, R7W. The drainage area is com- posed of unsorted gravelly sand and sandy clay, and deep sorted sands. The lakeshore is extensively develOped with several hundred cottages, resorts, marinas, a county campground and beach, and Lake City. The lake level has declined since'the mid—1920's when Lake Missaukee was served by outlets flowing from nearby Goose and Crooked Lakes. By the late 1930's, the inlets were no longer flowing, causing local residents to fear the lake level decline was~due to the city removing 640 gallons of ()4 Map £6 Meady Lake Section .34, TZJMR‘? W N 4.5 Acres ----- l3 Ft-Nax. Dcpfh Scale [in-IOOFt A 1 £ ~P f § § 1 5 A, \ W W-Wafer' P-Pcaf P Vcrf: Deal. lin. '50,”. 3' 2 lg // J 1,2 I; I1 I 5 W p Rod Record 9 Soundin 6 7 II // Ill l0 7 4 I ’2! \ ‘— -. - I a I | Jfa Hon 3 M I: II II I I/ [[710 I s. w "" ’.‘ IDa ' '. H. # 6S R8W 24. 25. 26. 27. R7 W R6W Lake Missaukee Goose Lake Long Lake Whitlock Lake Map 23. Missaukee County RSW zNNv—J zwmv—J -z.i>t\>I—3 zI-‘Ni-J ‘ Jinnarfifé I I Map 2.4 ‘7 Lake Nisaauhee Tad N, R7‘8 W ' [880 Acres C ’5 ’6 ZOF't.-Max. Depth ---LZ__46\LK‘\ I Jcalz liar-W013} / ’- 55::35' 6 l I ‘ p ' BR- Bu Irush \ WL- Wafer- Li I, 55‘ Var-t Jcalo Ifn.‘ JOFt W- Warfar- p- Rat‘- 67 water a minute from a shallow nearby well. The well was later discontinued but the lake level continued to decline from a maximum depth of 27 feet in 1941 to 20 feet in 1964. The lake level was three feet lower in August 1964 than in June 1955 , the highest level in recent years. The original bottom slopes lakeward at one to three degrees. Dark brown, pulpy peat is deposited over the original bottom. Pondweed, water lily, and bulrush were the attached aquatic vegeta- tion growing in 1964. Pondweed flourished at depths to 12 feet. Water lily grew sparse at depths to three feet. Bulrush grew at depths to two feet. Goose Lake Goose Lake (Map 25) is in a drainage area of about 180 acres with maximum relief of about 15 feet. The drainage area is composed of deep sorted sand. The lake is undeveloped with the exception of the public— owned northern shore, which includes a campground. The lake level has declined since the 1930's when an outlet flowed into Lake Missaukee. The surface area and maximum depth have declined from 100 acres and 14 feet in 1940 to about 85 acres and 12 feet in 1965, surrounding the lake with peat deposits. The lake level declined over one foot from 1963 to August 1965. The original bottom SIOpes lakeward at two to seven degrees with dark brown, pulpy peat deposited over it. Peat may also be yellow-brown to light brown and contains vegetative parts in areas of prolific water lily growth. Pondweed and water lily were the attached aquatic vegetation growing in 1965. Pondweed grew at depths to 11 feet. The water lily grew prolif- ically to depths of five feet. Marsh grass and cattails grew on surrounding peat deposits . Long Lake Long Lake (Map 26) is in a drainage area of about 304 acres with 68 Map £5 ~~\ . Goose Lake WI. \ Jog-”£8155. T23N,R8w ,..\ l/...--. \ 85 Ac rec “‘\..../’ I5 ' p ’ IZ Ft-Max. 02pm ‘ r 5calc lin.=460Ff.' ’ Z I I x“ 1 a ['76 I Q I éVL I1T___ -____/ Q. a \ a \ UL \ t } .4 P Former g \ toIond : N)\ s f ' '5 ’ \\I« g l : a.“ i | Z ‘ s 1: cr- CaH‘uil \\ : ne- Marshyrasa \ , VL-Vd’crLi/y I"/ x P \ I g I \ , I / z I \ / I I \ " i 7 If}; / ‘l I ’ / .I , l/ ’/ \... I \x‘ /’/ ’ . VL ~—--— /’ Preacrn‘ Jhorc/mo P,’ - ——-—P¢af DCPOJ;*J crime ’a- "’ I p :__./Ij/\‘._________________ I _ I3 I [53 W‘Wa+¢r P-Poa+ Von? Jen/0 lmfiJOF‘t I '39 P ' Nap Z6 N L ong L 0 I1 2 \ . 54:16.17.“ (39', 723/1438 W \ 60.5 Acres WL I7Ft- Max. Dep'I-h Jen I. Iin. '4 4OOF‘I: (— \‘~ \ \‘ Is!) “ I \\ I’ \e I z \n 47 ‘~ 5 9 I.” '. ’0 '\ c' l 3 \ I \\ \ 3 ”Pygggn“ JMII‘“ OR I-I- w-Poa 6 Dope: If; I -‘-" ~\ 7 BR. fluIruh WL‘ UNICI'cr My 1. \\ i I WI. \- .......... W- Wa+¢r P- Pea-I- ‘ Vcrf: Jcalc II'n IJOF'I: I I P I, ‘ I are flan fh I 7 ENNIS/SI 104 I I7I I IIIoIosngIqu II 8 IT VV*V1V.V II . 72 O r 70 maximum relief of about 40 feet. The drainage area is composed of deep sorted sand. The lake is in public ownership and a campground is on the eastern shore. The lake level has declined for several years , about three feet during the past five years (1965). The original bottom SIOpes lakeward at two to five degrees. Yellow— brown to dark brown pulpy peat is deposited over the original bottom. Yellow-brown peat has some dead vegetation still visible in areas of pro— lific water lily growth. Most of the peat is dark brown. Pondweed, water lily, and bulrush were the attached aquatic vegeta- tion growing in 1965. Pondweed grew at depths to 13 feet, water lily to five feet and bulrush grew at depths to two feet. Marsh grass grew on the surrounding peat deposits. Whitlock Lake Whitlock Lake (Map 27) is in a drainage area of about 370 acres with maximum relief of about 135 feet. The drainage area is composed of un— sorted sandy gravel, boulders and clay, and deep sorted sand. Dark brown peat deposits occur on all lakeshores. The lake is in public ownership and undeveloped. Cattails growing at depths of nine inches suggest the lake level rose about six inches recently (July 1965). The original bottom SIOpes lakeward at 2 to 10 degrees and dark to yellow-brown pulpy peat is deposited over it. The yellow—brown peat oc- curs in areas of prolific water lily growth where there is also parts of par- tially decomposed leaves. Pondweed and water lily were the attached aquatic vegetation growing in 1965. Pondweed grew at depths to 10 feet. Water lily grew prolifically to depths of five feet. Kalkaska County Two lakes were studied in Kalkaska County (Map 28). Glacial drift thickness in the vicinity is over 500 feet. Precipitation deficiency was similar to Missaukee County, page 63. Nap Z 7 WhI'I/oc/T L GHQ Sec. 30,TZJN, R8W [.3 Acres II Fir-Max. Depfh /in. = ZSOFI‘: (Jca In) C T" C aH‘aII: WL- Wafor Li/I'c: ‘- ‘—---—- Soundi Rod Record JI’a‘Hon / Z 3 4 5 Io II I: I Depth I Io 5 4 I 5 e // Io De #7 ’ o / I8 ’3 f I V V V V V V V 1’ Q Y Vcrt Scale Iin.=ZOFI'. w— anr P-rEcaI' 72 59 3'0 R8W R7W R6W R5W 29. Blue Lake 30. Guernsey Lake Map 28. Kalka ska County ZOENF—l ZVNI-B zoowi—J szv—J \J (A) Many lake levels in Kalkaska County were the lowest in the memory of local residents . Blue Lake Blue Lake (Map 29) is in a drainage area of about 91 acres with max- imum relief of some 13 feet. The drainage area is composed of deep sorted sand. Blue Lake is the site of six cottages With the northern shore in public ownership. The lake level was six inches below normal in August 1965. The original bottom slopes lakeward at 2 to 17 degrees. Marl and peat were deposited on it and chalky to organic gray marl overlies a small area of the original bottom. The marl is overlain by dark brown, pulpy peat, the dominant sediment over most of the original bottom, and con- tinues to be deposited. Pondweed, water lily, and bulrush were the attached aquatic vegeta- tion growing in 1965. Pondweed grew at depths to five feet, water lily at depths to four feet, and bulrush to depths of two feet. Guernsey Lake Guernsey Lake (Map 30) is in a drainage area of about 73 acres and maximum relief of about 45 feet. The drainage area is composed of un— sorted gravelly sand, boulders, and clay. Guernsey Lake is in public ownership with a campground and improved beach on the northern shore. The lake level has declined about three feet in the past five to eight years (1965) with the surface area declining from 31 to 27 acres. The original bottom slopes lakeward at 10 to 19 degrees. Chalky gray marl was deposited over the original bottom. A marl shelf was built lakeward from the north and east shores. The lakeward edge of the shelf dips 40 to 45 degrees and calcium carbonate in solution gives the water an emerald blue cast. Attached aquatic vegetation was limited to bulrush growing at depths to three feet. I ’5 ————————— \‘\5F? Map a? \ \\ B/ue Lake /’ ’ ‘ \\ 5‘C-QI7'Z7MFP7W (p / H \ Z7Acrcs WL I /'\ 5R~ ELI/rush \ _ \ // I" L) WL- Wo'i‘or LII, \ ’3 Ff Mex. 02pm / i 1' \\ 5cale has/80f?! / L", \Iz \ \ \x \ A ’ \' N 7 i ' I I «L 1 .4 -5! 6 -1. — I, A I I [I I/ I3 / 4 i x I, \ I I \ P . \\--—-”’ ’6 ,/l §~-' 68R Presenf Short/inc B 4 2 I AVA 4 4 w J ‘5 7 4 9’ A P \ *7 P 5C0 IQ IinJZOFI'JiIcr-fi 5’ W- Wafer M'MOr’I P-Pcof Sounding Rod Record 31'0 ron Dc h . / Ma r/ (Foe?) m: Wide? ' // / 4 /0 / .11- 7‘3 \ a 3 ‘\ Guernsey Lake A4 5") Jec./9I‘30,TZ7N,F?8W ’1' N Z7Acr‘cs " 5 5 44 Ft.‘Nax.Dep+h // I7 6 \\ Scale /I'nch=300Ft‘. / b \ linch=ZOFt(V¢rI'icaH I Len / BR-Bulrush I ,I' [I [I \ ’ I 2 3; 4 . 5 6 7 , l I A‘ . #A a e \\ [I W \ I ‘ // M M\ I I —-- l9 ’ ”f F 6M F \ I I4 I" \\ C 331/06 0 H 'D E E \\ W \\ W M \\ N \\ \‘ 409 : \ \\ \\ F / l7! / F’ W I3 / E’ 5 M W‘ Waf‘er I, M'Marl ‘ DIZ II )1 ' \ D I \ ” I . \ I __p,.35¢n+ fihore/me \ / " V fiend/09 .399! 3299 3*01‘50’7 I it .2 »_ Lou}? L ' Q31?“ I 3 I -’ _ a w.-- C”"‘:‘.".'?El 3120*” " (Elf? .27 '5 res; 2; , Eggs-3333.1...Laci __ CHAPTER V S U M MARY Data collected from the 23 lakes studied in detail is summarized in Table 1. It is obvious from Table l and the lake basin profiles that all of the lake basins have been modified by sediments, but size and shape of the lakes, size and relief of the drainage areas have little bearing on the relative resistance of the lake to senescence and extinction. An interesting relationship exists between the lepe of the original bottom and the dominant type of sediment deposited on it, summarized in Figure 4. Original bottoms usually dip at 13 degrees or less in lakes where peat. dominates, but 14 degrees or more where marl is the dominant sediment. Since all of the lake basins in this study intercepted the ground- water table, the following hypothesis is advanced; calcium carbonate may be carried into any lake basin intersecting the groundwater table but is deposited as marl only where acids do not exist in quantities capable of neutralizing calcium carbonate. The most favorable environment for marl deposition would be in lakes with steep original bottoms that limit the growth and migration of attached aquatic vegetation. If the growth of aquatic vegetation is limited, there would. only be limited amounts of de— composing and acid—producing vegetation. Shallow and deep lakes, and parts of lakes, may be defined on the basis of the original bottom angle dipping in a lakeward direcrion and the dominant sediment. Deep lakes have an original bottom dipping 14 de- grees or more and/or marl is the dominant. sediment. Shallow lakes have an original bottom dipping 13 degrees or less and/or peat is the dominant sediment. Deep lakes remain relatively deep and are less prone to senescence 76 77 Table 1. Summary of Lake Data Original Bottom Dominant Drainage Lakes Size Depth Slope Sediment Area Relief Barry County Cloverdale 12 30 3 Peat 400 47 Long 289 48 14 to 18 Marl 1150 115 Head 97 6 2 to 4 Peat 403 100 Guernsey 218 28 19 to 58 Marl 825 100 Daggett 14 15 7 to 11 Peat 385 120 Long 145.7 4 3 to 16 Marl & 207 60 Peat Little Payne 10 27 39 to 73 Marl 25 10 Carr 29. 5 44 28 to 73 Marl 102 25 Osceola County Alexander 5.7 17 1 to 3 Peat 102 70 Big 240 85 5 to 10 Marl 950 70 Myrtle 5. 2 9 l to 9 Peat 410 55 Hicks 155 33 l to 4 Peat 480 90 Park 8. 2 9 6 to 12 Peat 70 50 Austin 29. 2 37 1 to 7 Peat 540 70 Hewitt 20. 4 30 9 to 11 Peat 79 75 Clare County Pike 14 ll 2 to 4 Peat 179 10 Wexford County Unnamed 1. 5 9 5 to 13 Peat 21 30 Meady 4.5 13 8 to 2.0 Peat 103 70 Missaukee County Missaukee 1880 20 1 to 3 Peat 2600 250 Goose 85 12 2 to 7 Peat 180 15 Long 60. 5 l7 2 to 5 Peat 305 40 Whitlock 13. l 11 2 to 10 Peat 370 135 Kalkaska County Blue 27 13 2 to 17 Peat 91 13 Guernsey 127 44 10 to 19 Marl 73 45 90° The least and greatest angles of the original bottom + Marl dominates - Peat dominates Figure 4. Slopes of the Original Bottom and extinction, because the growth of attached aquatic vegetation is limited by depth and marl. For attached aquatic vegetation to migrate lakeward within the depth and light limitation of the species , sediments must be deposited to reduce the depth. Marl will be the dominant sediment de- posited, but most attached aquatic vegetation cannot grow as well on marl as on clay or peat. The growth of attached aquatic vegetation will also be retarded by wave action. Cooler water, characteristic of deep lakes , will evaporate slower than warm water. Shallow lakes become shallower and are more prone to senescence and extinction because attached aquatic vegetation can root and migrate more readily. Dead vegetation decomposes to form peat which makes the lake even shallower resulting in greater aquatic vegetation migration and control. There is also less wave action in shallow water to hinder the growth of aquatic vegetation and exchange warm surface water, with deeper, cooler water. 79 All lakes contained pondweed, but it grows mcst prolifically in the peat lakes. In Myrtle Lake, Osceola County; Blue Lake, Kalkaska County; and Meady Lake, Wexford County; a near absence of pondweed may be due to ecological imbalances. A topographic sheet and soils map study of over 3,000 extinct lakes, Greenwood peat deposits, in 18 Michigan counties indicates that extinct lakes can occur at any elevation, on and in association \Vl’l‘l moraines, till plain, outwash plain, glacial drainageways and lake plain in almr‘:st any type of soil. Extinct lakes also occur in every geograihic region and physiographic province of Michigan. No correlation exists betv-Iee-n the number of extinct. lakes and relative age of the region they occur in. A soils map study of several thousand lakes in 18 Michigan counties indicates that peat deposits are most common adjacent to west shores where wave action is usually minimum. However, peat deposits are not. restricted to the west shore, but may occur wherever shallow water exists and wave action is minimum. Drought will affect shallow lake levels more severely than deep lake levels. Lake levels are lowered more readily on shallow lakes due to greater evapotranspiration losses not immediately replenished. Lower lake levels also mean vegetation can migrate more rapidly lakeward, due to reduced depths. The shallow lake shoreline will recede more rapidly enabling upland vegetation to encroach. Minor amounts of clastic sediments, mainly clay in solution, gave the water a cloudy appearance in areas of active shore erosion, and runoff from the adjacent upland. Sand had eroded from the upland displacing peat previously deposited, in Hewitt Lake, Osceola (”Ecunty. No evidence of accelerated aquatic vegetation growth due to effluent was found, despite riparian dependence on septic tanks, chemical toilets and outhouses. Agricultural fertilizers and manures had not. visibly af— fected the lakes . 80 Conifers growing in the vicinity of lakes studied in Kalkaska, Mis— saukee, and Wexford counties may have affected lake levels during the recent drought. Several local residents nored that lake levels have de— clined almost continuously since the 1930's. Most of the trees were planted close together in the 1930's. However, recent vegetation on the shores of these lakes is usually a volunteer growth of poplar less than 10 years old. The study could have been improved by recovering a continuous core of sediments from each lake. A core study could have shed light on cyclic deposition due to climatic pulsations. Senescent lakes too shallow and weedy for swimming and waterskiing may be an ideal habitat for bass, ducks, fishermen and hunters. Senescent lakes, too shallow for power boats, may be ideal locations for nature groups and others who would rather hear loons than see lunatics tearing around. Extinct lakes are a source of peat and marl, habitat for wild animals, and a site for peat farming. Peat bogs usually contain an autobiography of climatic and flora information of the region in the form of plant. spores and pollen, as cores may reveal. CHAPTER Vi CONCLUSIONS AND RECOMMENDATLOF‘JS Qflslséieus The original basin of each of 23 lakes Studied in detail had been modified by sediments. Dark brown, pulpy peat is the dominant sediment in lakes with orig- inal bottoms dipping lakeward at 13 degrees or less. Peat lakes are shallow lakes, more fertile, and more prone to senescence and ex.— tinction, than deep marl lakes. Marl is the dominant sediment in lakes with original bottoms dipping lakeward at 14 degrees or more. Marl lakes are deep lakes. All lakes show some degree of senescence and/or extinction. Senes- cence is exhibited in shallow areas controlled by attached aquatic vegetation where wave action is non-existent or slight at the most. Extinction is shown by peat and marl deposits adiacent to the present water area. Extinction may occur in lakes at any elevation, in association with moraines, till plains, outwash plains, glacial drainageways, and lake plain in almost any type of soil. Extinct lakes occur in every geographic region and physiographic province of Michigan. Peat deposits are most common adjacent to west shores where wave anion is usually minimum. Peat deposits may occur wherever shallow water exists and wave action is usually minimum. Practically all inland lakes contain pondweed, growing most prolif— ically over peat deposits between shore and depths of 10 feet. A lack 81 10. ll. 12. 13. 14. 15. 16. 17. 18. 19. 20. 82 of pondweed may indicate an ecological imbalance, or the lake has been treated to rid it of this aquatic nuisance. Attached aquatic vegetation is most prolific in areas of peat deposits covered by shallow water. Marl is a less favorable soil for vegeta- tion growth. The lakeward migration of attached aquatic vegetation is retarded by abrupt slopes at the edge of marl shelves. Wave action, waterskiers, and swimmers retard the growth of attached aquatic vegetation. There is a direct relationship. between the growth of attached aquatic vegetation, the depth of water and available light. There is also a relationship between the present shoreline and upland vegetation en- croachment on the lake. Calcium carbonate is carried into lake basins intersecting the ground- water table in glacial drift but marl will be deposited only if acids do not exist in quantities that may neutralize the calcium carbonate. Calcium carbonate in solution gives the lake an emerald-blue cast. Marl is less indurated and easier to penetrate with a sounding rod in the more northern lakes (Kalkaska County) than in southern lakes (Barry County). Deep lakes and deep parts of a lake can usually be located because of vigorous wave action when the wind is blowing, and a lack of at- tached aquatic vegetation. Lower lake levels are common during periods of prolonged drought. Lake levels usually rise when precipitation returns to normal. Reforestation projects may have a long-range effect on the ground— water table and lake levels, where trees are planted close together . The size and shape of the lake, and the size and relief of the drain— age area has little if any bearing on the resistance of the lake to senescence and extinction. No correlation exists between the number of extinct lakes and the relative age of the region they occur in. 21. 22. 23. 24. 25. 26. 27. 83 Each lake must be considered on its individual merits. Cores of lake sediments would provide information about cyclic dep- osition in response to climatic pulsations. Senescent lakes may be an ideal habitat for wild fowl and bass. Senescent lakes may be of value to hunters, fishermen, and nature groups. Extinct lakes are habitat for wild animals. Extinct lakes may be of value to peat and marl producers, peat farmers, and palynologists. Artificial lakes should be designed to allow a minimum of area between the shoreline and a depth of 10 feet. Recommendations for Additional Studies Devel0p a simple coring device and coring technique that could be used from a small rowboat. Take one core from each of 100 or more lakes from the Indiana-Michigan boundary line to Lake Superior. Study and correlate sediments. pollen and spores. A chemical and physical analysis of lake sediments recovered as cores. Analyses may reflect the geological and limnological history of the lake and drainage basin. The origin of lakes versus their resistance to senescence and extinc— tion. The discussion in Chapter II shows that. lakes may originate in different ways. A study may indicate that lakes of a particular origin are more prone to senescence and extinction than lakes of a different origin. A comprehensive revision of Michigan Geological Survey Publication 30, "Inland Lakes of Michigan" by I. D. SCOtt, 1921. Hydrographs, lake studies, and glacial geology studies have resulted in new in— formation about lakes and the regions they occur in. This information would aid not only in revising Scott's interpretations but also in expanding the number of lakes described. With so much emphasis being placed on the recreational value of wa'er, this cut-of-print publication is again needed. Investigate groundwater quality and lake water quality versus senes- cence and extinction. A connection exists between quality; salts, organic matter, pH, acids, alkalines: and senescence and extinction, but is there a combination of water constituents that predominate in senescent. and extinct .. Study fish, animals. insects, and flora associated With senescent and extinct lakes and areas of lakes. Perhaps a species or its be- havior indicates senescence or exrinction. A comparison between lake development and property evaluation adja- cent to areas exhibiting senescence and extinction. The value of recreational property should be less in areas of senescence and ex— tinction than in Other areas of the lake not displaying these charac— teristics. DevelOp an easy to use checklist for prospective riparians. Develop a method or technique for determining the distance to the original bottom without having to use a sounding rod or take a core. CHAPTER VII CONTROL OF AQUATIC VEGETATION Aquatic vegetation may be controlled by mechanical and chemical methods, and manatees, a weed—eating sea animal. Mechanical weed control includes dredging. a mowing machine arrangement adapted to Operating underwater, and. a set of bed springs. A permit from the Michigan Department of Conservation is needed for each dredging project. Dredging removes the weeds and the soil they grew on but it also leaves spoil piles on shore and an artificial appearance. A mowing machine is manufaCtured and marketed by a Wisconsin firm. The success and use of this machine is unknown. A set of rusty bedsprings attached to a power boat by rcpe was used to restrict aquatic weed growth on part of Hicks Lake, Osceola County. Mechanical methods must be repeated annually but do not kill or endanger animal life as chemical methods may. Chemical methods vary with the type of vegetation and lake charac— teristics. Several chemical companies have develOped aquatic herbicides. Each compound has its own characteristics and application. Due to danger to animals and humans , a permit is required from the Michigan Department of Conservation for applying some chemicals. More information can be found in ”Aquatic Weeds and Their Control in Michigan, available from the Publications Room, Michigan Department. of Conservation, Lansing, Michigan 48926. The manatee loves aquatic vegetation, clearing 100 cubic yards of vegetation—clogged water or 100 pounds if vegetation a day. They have been experimented with in Florida where they would rather eat than repro- duce, and sometimes die from respiratory ailments during cold snaps. For these reasons. they would not be an efficient way of. eliminating aquatic vegetation in Michigan. 85 86 Man-made lakes may be constructed so there is a minimum Oppor- tunity for attached aquatic vegetation to live. The shores could be de— signed so the bottom SIOpes steeply lakeward to depths greater than 10 feet. Periodically the water should be drained, so aquatic vegetation and peat deposits may be scraped away. Another solution is an asphalt or cement strip surrounding the lake from shore to a depth of 10 to 12 feet. Periodically, this strip should be scrubbed, to eliminate aquatic veteta— tion that may find a means of growing. REFERENCES CITED Bergquist, S. G. , 1928, Some aspects of marl deposition in Oceana County: Mich. Acad. Sci. Papers (1927), v. 8, p. 279—84. Blatchley, W. S. , 1901, Ind. Geol. Survey Ann. Rept. (1900). 782. p. Burns, G. P. , 1904, Formation of peat. in Dead Lake tabs}: Mich. Acad. Sci. 6th Rept. (1904), p. 76-77. Chrow, Ven Te (editor), 1964, Handbook of applied hydrology: McGraw- Hill Book Co. 1418 p. Coburn, H. , D. Dean and G. M. Grant, 1933, An ecological study of Bryant’s bog, Cheboygan County, Michigan Mich. Acad. Sci. Papers (1932), v. 17, p. 57-65. Dansereau, P. , and F. Segadas—Vianna, 1952, Ecological study of the peat bogs of eastern North America; 1, structure and evolution of vegetation: Canadian Iour. Botany, v. 30, p. 490—520. Davis, C. A. , 1903, A contribution to the natural history of marl“ Mich. Geol. Survey, v. 8, pt. 3, p. 65—97.. Davis, C. A. , 1907, Feat; essays on its origin, uses, and distribution in Michigan. Mich... Geol. Survey Ann. Rept. ("1906), p. 94—395. Deeter, E. Bu and F. W. Trull. 1928, Soil survey of Barry County, Mich- igant’ U. S. Dept. of Agr. , Ser. 1924. no. 10. 20 p. Dorf, E. , 1960, Climatic changes of the past and present: Am. Scientist, v. 48, p. 341-64. Eschner, and Satter‘lund, 1965 (abs. l Am. Geophys. Union Trans. , V. 45, no. 1, p. 72-73, Mar. Eyster, H. C. , 1958, Bioassay of water from a concretion- forming marl lake: Limnology and Oceanography, v. 3, no. 4, p. 455-58. Ferris, I. G. , and others, 1954, Ground-water resources of southeastern Oakland County, Michigan: Mich. Gecl, Survey Prog. Rept. 16. 158 p. Hale, D. I. , 1903, Marl (boglime) and its application to the manufacture of Portland cement: Mich. Geol. Survey, v. 8, pt. 3.. 399 Dc HOOper, F. F. , 1956, Some chemical and morphometric characteristics of southern Michigan lakes: Mich. Acad. Sci. Papers (1955}, v. 41, p. 109—30. 87 88 Hough, I. L., 1958, Geology of the Great Lakes; Univ. 111. Press, Urbana. 313 p. Humphrys, C. R., and I. Colby, 1963, Summary of acreage analysis charts from lake inventory bulletins 1 to 83-." Mich. State Univ. Re- source Devel. Dept. Water Bull. 15. 3 p. Indiana Water Resources Division, 1949, Outdoor Ind., v. 16, no. 12, p 6-9, Dec. Jewell, M. E. , and H. W. Brown, 1929, Studies of northern Michigan bog lakes. Ecology, v. 10. no. 4, p. 427-75, Oct. Lake, D. 1., 1873, Atlas of Barry Co., Michigan from actual survey by and under the direction of D. I. Lake, C.E.‘ C. O. Titus, Phila- delphia. Lane, A. C. , 1908, Summary of the surface geology of Michigan: Mich. Geol. Survey Ann. Rept. (1907}, p. 89-152. McLouth, C. D. , 1902, Some general remarks on the tOpography, soils, water sources, and flora of Muskegon County" Mich. Geol. Survey Ann. Rept. (1901), p. 104-107. Michigan Land Economic Survey, 1927 , Soil and lay of the land map of Kalkaska County: Mich. Dept. of Conserv. Land Economic Survey. Michigan Water Resources Commission, 1964, Total precipitation and departure from normal: July. Michigan Water Resources Commission, 1965, Quarterly Bulletin, v. 47. 6 p. Nichols, M. S. , 1965, Nitrates in the environment Am. Water Works Assoc. Iour. , v. 57, no. 10, p. 1319-27, Oct. Olson, I. E. O., 1944, Ecological studies of Pierport, Bear Lake and ngewater bogs in Michigan: Mich. Acad. Sci. Papers (1943), V. 29, p. 31-50. Pollack, I. B. , 1918, Blue—green algae as agents in deposition of marl in Michigan lakes: Mich. Acad. Sci. 20th Rept. , p. 247-60. Rominger, C., 1876, Lower Peninsula, 18734876. Mich. Geol. Survey, v. 3. 161 p. Schlicting, H. C. , 1958, The role of water fowl in the dispersal of algae: Ph.D. dissertation, Dept. of Botany and Plant Pathology. Mich. State Univ. . East Lansing. Scott, I. D. , 1921, Inland lakes of Michigan; Mich. Geol. Survey Pub. 30. 383 p. Sigler, D. , and M. L. \Nollett, 1927, An ecological study of Hogback . bog, Cheboygan County, Michigan: Acad. Sci. Paper (1926), v. 6, p. 295-302. SOper, E. K. , and C. C. Osbon, 1922, The occurrence and uses of peat in the United States: U..S.G.S, Bill. 728. 205 p. Stanley, G. M. , 1936, GeolOgy of the Cranbrook area. Cranbrook Inst. of Sci. Bull. 6. 56 p. Transeau, E. N. , 1906, The bogs and bog flora of the Huron River; 4, the ecological characteristics of the bog flora and their causes: Bot. Gaz. , v. 41, no. 1, p. 17-42, Jan. Turabian, K. L. , 1965, A manual for writers of term papers, theses, and dissertations: Univ. of Chicago Press. 110 p. Veatch, I. O. , 1933, Some relationships between water plants and water soils in Michigan: Mich. Acad. Sci. Papers (1932), v. 17, p. 409-13.. Veatch, I. O. , 1940, Soil profiles in relation to the recession and extinc— tion of Michigan lakes: Soil 801., v. 50, p. 103—14. Wayne, W. I. , and]. H. Zumberge, 1965, Pleistocene geology of Indiana and Michigan: The Quaternary of the United States, p. 63-83. Welch, P. S. , 1936, Limnological investigation of a strongly basic bog surrounded by an extensive acid forming bog mat: Mich. Acad. Sci. Papers (1935), v. 21, p. 727-51. Weld, L. H. , 1904, Botanical survey of the Huron River valley; 2, a peat bog and morainal lake: Bot. Gaz. , v. 37, no. 1, p. 39-52, Jan. Wonser, C. H. , and M. M. Galloway, 1942, Land type map, Missaukee County: Mich. State Coll. Agr. Exp. Sta. Zumberge, I. H. , 1952, The lakes of Minnesota: their origin and classi- fication: Minn. Geol. Survey Bull. 35. 99 p. Zumberge, I. H. , and I. E. Potzger, 1956, Late Wisconsin chronology of the Lake Michigan basin correlated with pollen studies: Geol. Soc. Am. Bull. , v. 67, p. 271-88. APPENDIX A POINTS TO CONSIDER WHEN BUYING LAKE PROPERTY Any depression holding water is a potential site of lakefront property in Michigan. Many good sites remain on natural lakes but abandoned gravel pits are being cleaned up, and small streams are being dammed to provide additional "lake frontage.‘ While investigating senescence and extinction,- I talked to many riparians, sportsmen, realtors , and lake- lot promoters .7 The writer's interpretation of riparians views , pitfalls , and advice is summarized as follows: 1. Never buy property sight unseen, even on the advice of a friend or relative. If you are unable to visit the site forget about it until you can make personal inspections. 2. Visit the site at different times of the year. Are the neighbors noisy? Is the lake infested with aquatic vegetation? Is the trip to this lake too long, especially in the winter? Most of all, does the lake and area offer the comforts and conveniences you are looking for or already take for granted? 3. Ask the realtor or salesman about building restrictions on the lake and in the township, taxes, maintenance of the road leading to the property you are. interested in, recreation rights and restrictions , visitor and pet restrictions . sewage facilities , rubbish and garbage collection, and health facilities or doctors in nearby towns. Also ask the sales- man or promoter about ownership of the. lots; do they own the lots or merely have an option on them? Are the lakefront lots zoned against future subdividing, industrial development, and certain types of com- mercial establishments , such as an amusement facility? Is there a lake association actively engaged inimproving the lake? 90 91 4. After visiting the lake and talking to a realtor or salesman, gather all the information you can about the lake and area from official sources. See the township assessor for valuation and tax information, the local conservation officer for fishing, hunting, public access, and lake-level stability information. A hydrograph, showing depths and bottom condi- tions may be available from the Publications Room, Department of Conservation, Lansing, Michigan 48926. The county road commission can tell you about road maintenance. A technician in the U. S. Soil Conservation Service office, usually located at the county seat, can show you the location of peat deposits and other soils that are unfavor- able building sites. Also visit a nearby town and look around. While in town inquire about rubbish and garbage pickup at the lake. With this information, the property can be considered more objectively and you can also determine the reliability of the salesman or realtor. 5. If you are still interested in the property, go back for a serious second look. Try to talk with people who have been there for some time and also try to go out on the lake without the salesman or realtor. Is there aquatic vegetation or has it been sprayed to give the lake a more showy weedless appearance? If you are not satisfied, look at other lakes, comparing values, likes and dislikes. There is a great deal of unad- vertised lake prOperty available so you can disregard comments about this prOperty being "the last of the good lake frontage available in the county. " 6. If the lake level is maintained by a dam inquire about maintenance and liability of the dam. Usually each riparian is responsible. 7. Man-made lakes vary in quality. Some are nothing more than dammed brooks that formerly trickled through a swamp. The swamp is still there except it is now covered by a few feet of water. Stumps and brush may be seen in lakes of poorer quality, giving them a mill pond appearance. Remember, the size and cost of the dam does not guarantee that nature will fill it. Some lake levels must be maintained by water 92 pumped from deep wells with the riparians sharing the water bill. In Michigan there is no law to prevent the construction of a second dam upstream, thus lowering the lake level of an earlier built man-made lake located downstream. Most riparians are glad they own a cottage. To the satisfied, a cot- tage is a relaxed retreat from the fast pace and pressures of daily living, where they can be together as a family. The 400-miles or more round trip that many cover during a weekend is worth it just to get away from the desk and neighbors. The commonest complaints heard from riparians were in regard to the substantial investment and upkeep of a cottage versus limited use, espe- cially after the children have grown up and left home. Waterskiers and large high-powered boats rate a close second on the complaint list, espe- cially from older peOple interested in fishing and rest. "111111 11111111111111 I