ML20030A461

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App 3 to Preliminary Hazards Summary Rept for Big Rock Point, Geology & Hydrology of Proposed Reactor Site at Big Rock Point Near Charlevoix,Mi. Prepared for Util
ML20030A461
Person / Time
Site: Big Rock Point File:Consumers Energy icon.png
Issue date: 01/18/1960
From: Zumberge J
CONSUMERS ENERGY CO. (FORMERLY CONSUMERS POWER CO.), MICHIGAN, UNIV. OF, ANN ARBOR, MI
To:
References
NUDOCS 8101090563
Download: ML20030A461 (37)
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{{#Wiki_filter:4 ( GE0IOGY AND HYDROIDGY OF THE PROPOSED REACTOR SITE AT BIG ROCK POINT, NEAR CHARLEVOIX, MICHIGAN James H. Zumberge Geologist Ann Arbor, Michigan 'IOP0 GRAPHIC SETTING Terrain The proposed site lies in the NE Quarter of Section 7, in Township 34 N, Range 7 W, Charlevoix County, Michigan, near the shore of Lake Michigan. The lake shore consists of scattered limestone outcrops alternating with short stretches of beach containing granular materials ranging in size from sand to coarse boulders and limestone rubble. The land rises from a mean lake elevation to 580 feet A.T. to about 700 A.T. a mile or so inland. Topographically, the region within a five-mile radius of the site location can be divided into two categories. The first is more or less parallel to the lake shore and is a zone of low relief which was once submerged beneath the waters of ancestral Lake Michigan. Locally, swampy conditions prevail between low ridges of stabilized beach deposits. The second zone is the upland surface which rises from an elevation of about 700 A.T. to over 900 feet A.T. five miles south-east of the site. The upland surface is a constructional terrain con-sisting of till plain containing NW-SE oriented drumlins which rise 40 i to 60 feet above the general till plain surface. TlO 09 05Yo3

-2 Drainage Surface drainage flows either northward directly into Lake Michigan or southward into Lake Charlevoix and thence into Lake Michigan via Round Lake and Pine River at the town of Charlevoix. The divide between these two watersheds extends in a northwesterly direc-tion from a point just south of Susan Lake in Section 29, thence north-ward into Section 20, northwesterly into the SE corner of Section 18, and finally northward into Lake Michigan. The surface drainage area in which the proposed site is located is bounded on the south and west by the divide just described, on the north by Lake Michigan, and on the east by Susan Creek which originates in Susan Lake and flows northward into Lake Michigan which it enters at a point about one mile esst of Big Rock Point. The total area of this watershed 16 between 3 and 4 square miles. 't o

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~. K, o GEOLOGICAL MAP OF MICHIGAN D o my g/ p..%,f 0 sed 9 zl,j g ,g;y ~ ,% Locon. m e man n. n,,,,n on g 1957 Revision of Pub. 39 [ f /c ..s,. THE CENTENNIAL GEOLOGICAL MAP [ OF MICHIGAN ~ ......;.........t.._,_.... e ....,( o y i t ej,,- g. ~......... _... , et g I we kV PENNSYLVANIAN ,}* 7 ,,k,",,, og no MISSISSIPPI AN D Mb Bo yport m Mm M.c h;go n l Mnm Napo eon.Moeshoti \\ T Mc Cold-oter , " * * ' s e s 's eo. w e s s. u.. g Mbb Bereo Bedfoed N. )t O Me Elis* orth Antrim t MISSISSIPPI AN.DEVONf A N p, M-Do Antrim Q DEVONI A N "***"N Dt Trowerse [M s Drc Rof ers Lity ,r Dd DC Cee f Dde Detroit River Dbb Bois B!anc k O. ,.l.: o,g. ..sl,,, p ,eo: Q .l DEVONI AN-SILURI AN E .D, D.sm Moci.inoc brecc;o p ._('y {* h h ..__._.t_. SILURI AN P g {. sb; Boss isiond j C ,,,,s,,%(, h, .,, 4 ;,, y S s,. St. Ignace [ 3 Sp Point Aun Cbenes I lo [ 5e Engodine \\ s ,_,j, l h' w k r" r' Sm Monistique k Sbb Burnt Bluff g. 3,37 Q a j Sme Moyvil e p

4 i - l ' GEOLOGIC SFfTING Bedrock Geology 4 Bedrock Topography. The site lies in a belt of lime-a stone of lower Paleozoic age. The rocks exposed along the lake snore are part of-the Traverse Group of Devonian age. Near the shore the bedrock surface is either at the ground or covered by thin unconsolidated glacial and lacustrine deposits. Farther inland, the bedrock surface is buried beneath the till plain. At the city of Charlevoix, the log of the city well reveals 230 feet of Pleistocene sand and gravel over the Traverse limestone. This situation is con: mon place along the entire eastern shore of Inke Michigan and indicates that the streams entering the lake were deeply entrenched into bedrock during a time when the lake level was several hundred feet, lover, about 5,000 years ago. Thus, the maximum relief. of the bedrock topography is much greater than one vould expect from i an examination of outcrops along the shore er: Lake Michigan, J Bedrock Litholocy. Borings'at the site were made by the Raymond Concrete Pile Company to a depth of 40 feet. Two borings 400 feet apart and 500 feet from shore penetrated a grey to black fossiliferous ' limestone with thin shale partin e. Core recovery ranged from a lov of c 24% in the 3 to 9 foot levels of Boring No. " to a high of 100%. Generally, the core recovery was greater than 60% and many sec' ions i of two-foot lengths shoved 100% recovery. Poor core recovery seems to be related to veathered sections of the limestone sections with closely (. T I

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spaced shale partings, or a highly jointed rock, rather than S j ~ ~ cavernous, conditions. Some of.the cores are reported as having low porosity. The limestone bedding planes are nearly horizontal and [ . the regional dip is to the southeast,toward the center of the Michigan r Basin. - The ' log of the Charlevoix water well shows no salt or anhydrite beds down to a depth of 482 feet. Ing of City Well, Charlevoix, Michigan Incation: Section 26, T 34 N, R 6 W. Elevation': 600 feet above sea level, t Drilled before 1901 Thickness Depth (fect) (feet) ~ Pleistocens: Sand 6 6 Gravel 9 15 Fine. sand. 155 170 Gravel 6 176 i Sand, quichsand at 214 feet 54 230 Devonian: - Traverse: 1 Limestone,. fine Brained earthy 10 240 10 250 Limestone, gray Limestone, carthy or chalky, brownish, porous, much oxidized shaly, with a strong shale odor, being in fact in ~1arge part shale 10 260 ' Limestone, dark' gray arcillaceous and comovhat shaly 10 Y(0 Shale, finely stratified. Compact in texture 10 230 Limestone, fossiliferous whitish, con-taining Atrypa reticularis and other foss'_ls 10 290 Limestone, white crystalline, containing considerable crystalline calcite. It carried fragments of Acervularin davidsoni. Some' portions of the samples are compact and argillaccous 10 300 .( e 1 e n .-n w -m- -,--,-w- ,e,--m,1 , ~ -~, ..-----v-+----p. s

6 1 Thickness Depth (feet) (feet) Limestone, white chalky, non-argillaceous, fossiliferous 15 315 Limestone, brownish, earthy and argillaceous with a strong.chale. odor, Bryosa and other fossils have been observed 7 322 l. Shale, gray calcareor.s, of very uniform texture, partially oxidized 8 330 Shale, gray compact calcareoi.c rock, but of massive character 5 335 Fragments of Acervularia davidsoni with the calices' free frou matrix, and evidently embedded in shale. I!o shale, however, is . retained.. 10 345 Shale, gray calcareous, mixed with pure white limestone, the latter containing Favosites and Acervularia 5 350 Limestone,. gray arcillaceous, and some white limestone, with fragments of Spirifer and Acervularia 5 355 Limestone, gray, Acervularia davidsoni is abundant.. Favosites and Atrypa reticularis also occur 5 360 Limestone, gray, compact, and semi-argillaceous crinoid stems; much shale is mixed with the linestone 7 367 Fragments of Acervularia davidsoni and

Favosites 3

370 Limestone, compact, gray, argillaceous 5 375 Rock, fine grained, - compact, argillaceous 12 337 - Limestone and black shale 3 390 Limestone, gray-argillaceous with whiter limestone containing Acervularia 10 400 Shale, chalhy; crumbles and soils fingere, cream colored 2 402' l Shale, bluish gray, slightly calcareous 8 440 Limestone, compact, broun to gray, veathering earthy 5 415 Shale, cream colored calcareous, identical i with rock at 400 feet 5 420-1 Limestone, compact, brown 10 430 Shale, cream colored earthy, calcareous 13 W3 Limestone, brown banded, mingles with black and gray shale containing Atrypa reticularis, etc. 4 M7 Bell formation: Shale, bluish 35 482 l ( i Y ,,..,,w=

7 I Surricial Deposits Gle.cial Drift. The cite area lies within the boundaries of the Late Uicconcin drift deposits of Pleistocene age. A narrow belt parallel to the chore of Lahe Michigan contains thin lacustrino deposits and beach sandc and gravels associated with former higher stagec of Lake Michigan which prevailed at various timec cince the lact retreat of the Lahe Michi an glacial lobe. Thece deposits range b from fine cands to coarce gravel and weathered limestone bedrock. The upper curface it the product of the last ice advance which deposited a stony till of variable thicknecc over the entire area. In the site area the till is very thin or wholly lacking due to the many episodes of 11ke hictory. The ancectral lakec removed much of the till by wave crocion, and in places, replaced it with beach deposits or lacustrine sediments. Soils. Generally, the soils in the immediate site area have weakly developed Podzol profiles, are very well drained, and extreucly poor from the agricultural pdint of view. The uajor soil in the area is the Eastport Series which in col:monly developed on low cand ridges and dry cand benches, but can also occur on bedrock flats, stony vet clays, and chingle and cobbly beaches. The upland soils, developed on the drumlin-till surface, belong to the Emmet-Rocelayn Accociation. The coil textures are mostly sandy loamn of meditu:1 fertility. Their vell drained character reflects the generally high permeability of the morninic materials on which they are developed. (

8 f. GROUED UATER 4 The general geologic setting, topography, and climatic conditions of the region pavide a basis for a gancral evaluation of the grotnd water conditions. The water table at the site area was at 579 feet in 1/ay, 1959, as shown by the notes accompanying Boring No. 1 of the Raymond Concrete Pile Company report dated Ihy 8,1959 This shows that water table rather than artesian conditions prevail. It can be assumed that the water table rises gradually from Lake Michigan back tr. the drainage divide described under surface drainage in this report. It cannot be stated definitely that this surface drainage divide is coincident with the ground water divide because even though the surface drainage on either side is graded to either Inke Michigan or Iake Charlevoix, both of which have the same I mean surface elevation, the slope of the land on the Iake Charlevoix I ] side of the divide is much steeper than on the Iake I!ichigan side. Steeper water table gradients, therefore, may result in a water table i divide that is closer to the Iake Michigan base level than the surface drainage divide vould indicate. Nevertheless, the 1 4 er table divide j is,most likely not much different than the surface drainage divide I between the two lakes. I The eastern margin of the watershed is Susan Creek which i forms a very definite boundary insofar as both surface and subsurface water novement is concerned. The preliminary copy of the U.S.G.S. f to7ographic rap directly cast of the Charlevoi:: Quadrangle shows Sucan ( 4 +, -+- --,-,-,7 ,,m-,.., -.,,.,, -e

~. 9 i t 1 Creek to be a permanent st" cam. Even though a Good portion of the f base flow undoubtedly comes from Susan Lake, Susan Creek itself is undoubtedly effluent in character and draws on ground water storage to sustain its base flow,.however small, during periods of drought. Ground Uater Movement. Ground water that originates i as infiltration from rainfall which falls on land west cf Susan Creek, south of Iake Michigan, and north or east of the divide between. ~ Lakes Michigan and Charlevoix, vill eventually reach Iake Michigan, i either directly by normal ground water movement toward the lake or by ground water flov into Susan Creek and thence to Iake Michigan as surface run-off. In terms of vagrant ground water released at the proposed site itself, such water would flow to the lake very quickly except in times of a rapid rise in lake level during a seiche, in which case some delay would result becauce of a reduced hydraulic gradient between the site and the lake. Ircally, where the water table causes svampy conditions because of its proximity to the surface svales between old beach ridges, the uover. ant toward the lake vould be retarded. 4 j t i

10 i PG!P TEST ANALYSIS There is little doubt that any ground water that originates as infiltration from rainfall which falls on land vest of Susan Creek, south of Lake Michigan, and north or east of the divide between Lakes Michigan and Charlevoix, vill eventually reach Lake Michigan, either directly by normal ground water movement toward the lake or by ground water flow into Susan Creek and thence to Lake Michigan as surface runoff. In terms of vagrant ground water released at the pro-posed site itself, such water would flov to the lake very quickly ex-cept in times of a rapid rise in lake level during a seiche, in which case some delay would result because of a reduced hydraulic gradient between the site and the lake. Locally, where the water table causes svampy conditions because of its proximity to the surface svales 1 between old beach ridres, the movement toward the lake would be retarded. On December 9, 10, 1959, pump tests were run to deter-mine the coefficients of Transmissibility (T) and Storage (S). The tests were run on Borings #5, 6, and 7 On December 19, 1959, a slug j test was run on Boring #3 This test was designed to measure the infiltration capacity of the clay on the site area. Aquifer Selection. The initial evaluation of the sub-surface geology indicated that a thick sequence of Traverse limestone is overlain by about 50 feet of compact clay till. The upper 10 feet ( of limestone is badly fractured, indicating higher velocities of i e- ,v

11 ground vater conpared to the surrounding geologic materials. It vas, therefore, decided to drill three borings (see sketch map of boring locations) using f5 as the pump vell and f6 and 57 as observation wells. These borings were ccupleted to depths of 59' 11", 64' 3", and 59' 9", respectively, and penetrated up to 13' of fractured lime-stone. These borings essentially penetrate the fractured zone which averages about 10 feet in thickness. Water levels in the wells in-dicated artesian conditions as would be expected. Boring f5 showed a sand zone from 23' 5" to 29' 5" whichproducedaflowof033 gallon / minute. The static level of the sand was 1 33 feet above the ground surface or at an elevation of 591 98. This zone vill be discussed on Page 14. A slug test was run on Boring #3 at a depth of 8.5 - 20 feet. The vell was entirely in clay, and the test si m the capac-ity of the capping clay to transmit water. Pump Test. Upon completion of the wells, static water levels were taken, and a chort test run to determine the approximate well capacity for an eight-hour pump test which would utilize the maximum amount of dravdown allovable. On December 9, test #1 was commenced, pumping at a rate of 5 2 gpm. Astandard5/8inchBadgerwatermeterwasusedwith a stop watch to regulate the discharge. An electrical contact water level recorder was used on Boring 85 and tape readings were taken on Borings #6 and 7 Readings were taken according to a prearranged sched- -ule with each observer using a synchronized watch. Between 60 and 90 l

12 N LAKE MICHIGAN ( LOW WATER LINE, ELEV. 578 5 l AUG. 12, 1955' BANK SEEPAGE, APPROX. ELEV. 581 DEC. 1Q, 1959 p I)3 )3 ) C= ,Os s,,N 3 -g- .,J ~ s ', # \\\\ 3'J n JJyys m 18 s ~ OO====== ,,0

======- /y e BORING # 7 BORING g 3 g / FLEV. 590.8 t/ ELEV. 590.4 It itb % \\\\ II 30 ft i' BORING # 5 Is ' ' ' ~~ - -',f , BORING # 6 f li ELEV. 590 7 e ELEV. 589 9 LOCATION MAP OF WELLS USED DURING FUMP TESTS on DECEMBER 9, 10, 1959 Scale in Feet Q 1097.55.025 0 5.0 100 I 7

13 .t minutes, the water level in Boring (5 dropped 10 feet indicating a rapid change. in transmissib lity. The suction head produced was too large for the pu=p and,.therefore, test #1 was suspended. On December 10, after allowing the static level to recover, test (2 was begun with a discharge of 4.0 cpm. The pressure cone was not reduced sufficiently du: ing this test to allow dewatering of the aquiter which essentially occarred during the first test. After [ 8 hours of draudown, 5-1/2 hours of recovery were measured. Results. The draudoun vs time and recovery vs time r relationships allow the determination of the coefficient of transmis-sibility, T, defined as the flow of water in gallons / day (under a hydraulic gradient of one) through a rock cross section with a width of one foot and a depth equal to the thickness of the water bearing formation. Also, it permits the deternination of, S, the coefficient of storage which is defined as the volume of water released from storage per unit surface area of aquife,r per unit change in the component of head normal to that surface. Under artesian conditions in a vertical column one foot by one foot, the storage coefficient equals the volume of water in cubic feet released from an aquifer when the piezometric surface declines one foot. Calculation for the Big Rock Point Plant was made by use of the Theis, Jacob and Theim methods *. These methods are well known and standard in well hydraulics. For the slug test, a standard slug formula of T = 114*6 V (1/tm) was used where: V equala volume of .the slug in gallons, tm equals time since slug injection in minutes, and s equals the residual head above the static. i

  • See Appendix B for draudown and recovery data fram all wells.

A

14 i-The pump test formulae are based on the assumptions that (1) the aquifer is uniform in thickness, (2) that the aquifer is both homogeneous and isotropic, and (3) of infinite areal extent. These l' conditions are never realized in nature and ::pecially so in bedrock aquifers. However, the-test formulae represent the best approach that is economically feasible. Therefore, departures of the results can be attributed directly to departures of the rock. Table 1 showc the values of T and S for both tests, and the three different methods. Even with so many departures from the ideal conditions, there is good conformity between the average values of the three methods. i JACOB THEIS THED4 Well No. T S T S T TEST #1 1.8xlof 6 dd 337 7 dd 818 7 8x10-TEST 82 5 rec 528 834 7 1 637 6 dd 464 109 4.2x10-6 491 3 86x10-5 rec 352 s 7 dd 754 rec 880 1 75x10-5 668 2.11x10-5 AVERAGE 590 1.19x10-5 590 2 99x10-5 527 i TABLE #1 Transmissibilit;y (T) and Storage (S) 4 w e-__m-4-. m.

15 'i As transmissibility-(T) is in gpd/ft of aquifer and permeability is in gpd/ft, the average vah e 'of T is divided by the thickness of the fractured zone to arrive at the permeability. The average permeability is then seen to be somewhere between 52 7 2 gal./ day /ft and 59. gal./ day /ft, The slug test yielded a transmissibility of 4.0 gal./ day /ft. Since the amount of open' hole was 11 5 feet, the per-2 meability of the clay is 0 35 gal./ day /ft, i Conclusions on ground water flow under existing conditions: (1) The static water levels in the three wells in the test area show that the fractured rock zone is under artesian condi-tions. The elevatica of the static levels indicates that there is a 1 -- I pressure drop towards Lake Michican. The elevations also indicate [ that there is leakage from the clay into the fractured limestone. y } Taking the average value of (T) equ'l to 590 gcl./ day /ft, and the i approximate thickness of the-fractured zone as 10 feet, the flow 4 velocity under existing hydraulic gradients equals 0.05 ft/ day. This ] value is very low compared to most sand and gravel aquifers. (2) The drawdown and recovery vs time relationships indicate i direct connection between the fractured bedrock and Lake ) Michigan. Using the recovery data from Boring #7, and the drawdown data from #6, positive boundary conditions, i.e., recharge to the aquifer system, were established as being approximately 820 and 850 feet from the pumping well. Lake Michigan is 500 feet away at its -{ clenest point. Recharge would not be expected to show appreciably 1 -e----i-t-- -,r.4-,- ,-,-s em-*- y e. ,--en=r-a w --- r +w- --a-'* --ve'--v -t

16 until the pressure cone had intersected a sizeable section of the lake. (3) The overlying clay till has an exceptionally low transmissibility,andgivesflowvelocitiesofabout0.002ft/ day. This rate is largely dependent on the hydraulic gradient which fluc-tuates. However, even if the velocity were doubled it would still be low. (4) The artesian sand in Boring #5 is believed to represent a beach sand, deposited during the interval elapsed durin6 the deposition of the underlying and overlying till. The overlying tillshowsanaveragepenetrationofabout57 blows /12incheswhile theunderlyingtillhasanaveragepenetrationof109 blows /12:nches. Well drillers in the area report that artesian sand pockets are hit within 50 feet of the present lake level. The static of the sand indicates that the source area is probably 1000 feet south of the test aree. Examination by the writer df the area immediately south showed surface expressions of old beaches with back shore swamps. One of these back shore swamp areas is pictured by the writer as being connected to the subsurface sand by a sand smear similar to tl. se now present on the surface. Buried beach deposits may be ex-pected in the area, where they will be of limited areal extent, with small yields such that they could only be suitable for small scale The hi h static indicates that these sand bodies domestic purposes. S are under high pressure and will not permit water to enter them, but to the contrary leak water to the surrounding area. In this respect, 4 the sand acts as a boundary to the passage of water. n. s w,

i 17 (5) Existing wells in the area are of two types. The shallow wells which are less than 70 feet deep and the deep wells of generally over 150 feet and up to 350 feet in depth. Just north of Charlevoix Lake and in a band approximately one-half mile wide', stretching IN-SE parallel to the lake, are found many shallow type wells. These wells are located in permeable sands or gravels lying above a tight clay till whose upper surface is thought to be depressed in the immediate area of Lake Charlevoix. Wells of Type //2 are generally found elsewhere in the area. They are in the Traverse limestone, at considerable depth, and under artesian conditions for the most part. Theaa wells yield up to 50 gpm, but are mostly in the 15-20 gpm range. No heavy producing 9 vells are known of within 2 miles of the site area. Lake Levels The Lake Survey Divisiori of the U.S. Corps of Engineers issues monthly bulletins of levels of the Great Lakes. The period of record for Lakes Michigan and Huron is from 1860 to the present. Lake level fluctuations u e of two types, long-range and short-range. The long-range variations are those related to variations in precipitation over the years, whereas the short-range fluctuations are caused by sec3onal variances in regional precipita-tion, or very short changes in lake levels due to seiches. Long-Term Fluctuations. Thn level of Lake Michigan has varied from a low of 577 35 feet A.T. which occurred in February, i 1926, to a high of 583 68 feet A.T. in June of 1886. This amounts to a maximum difference in level of 6 33 feet during the period of record (1860-1959). 1

18 t Short-Term Fluctuations. Seasonal variation in precipitation produces a seasonal variation in levels of the Great Lakes. The average difference in the level of Lake Michigan between July (high water) and February (low water) is about one foot, but dif-ferences of as much as two feet and as little as O feet have been recorded between these two months for any one water year. Both the long-term and short-term seasonal f1.ctua-tions have the same effect on the water table which rises and falls with the level of the lake, at least in the vicinity of the shore. Seiches. Short-term water level fluctuations with periods of a few hours are called seiches. They are produced by some meteorological force such as high winds or rapid changes in atmospheric pressure. In either case, lake levels fluctuate two to three feet in less than a day. Such rapid changes in the lake level have some affect on the near shore ground water because the water table is graded to the water plane of Lake Michfgan. High levels reduce the hydraulic gradient of the water table and result in sluggish movement in the near shore area. Such changes are only temporary, however. Lake Currents The site lies on the south side of Little Traverse Bay, an east-west embayment opening into the northern end of Lake Michigan. Investigations of the currents of Lake Michigan by the Great Lakes Research Institute of the University of Michigan suggest that two directions of currents exist in Little Traverse Bay. They I are both apparently controlled by wind conditions in the area centered e

i 19_ l i around the Straits of Mackinac. When the prevailing westerly or northwesterly winds are blowing, a clockwise current moves in the bay which gives rise to a westward moving longshore current on the southern shore of the bay, as demonstrated in the Synoptic Cruises IV and V on June 28 and 29, respectively, in 1955 However, when the winds come from the north or nextheast quadrant, the current changes to a counterclockwise direction, thereby reversing the longshore movement on the south shore of the bay so that it moves in an easterly direction from the site area toward the head of the bay, as shown in 4 Synoptic Cruises VI and VII on August 9 and lo, respectively, in 1955 The question naturally arises as to which condition prevails most frequently, the eastern or western direction of flow. The answer is based on both meteorological and geological evidence. Wind direction data obtained from the U.S. Coast Guard Lifeboat Station at Charlevoix indicates that the wind is from the northeast quadrant less than 20fa of the time. It follows that the westward moving shore current near the site area is the normal situation. Evidence in support of this conclusion also comes from the presence of a mile-long spit extending into Little Traverse Bay from the north shore at Harbor Springs. This spit curves eastward toward the head of the bay. It is inconceivable that this spit could maintain its orientation with any current other than the clockwise current which prevails when the westerly winds are blowing. Actually, the pattern of currents in the bay may be more complicated than indicated by the synoptic cruises of the Great Lakes ( Research Institute. Also, the proposed site area is some 15 miles

20 2 from Petoskey at the head of the bay, and it has not been proved with certainty that water entering Lake Michigan at Big Rock Point would, in fact, move all the way to Petoskey at the head of the bay. t

21 REFERENCES 1. Abrams Aerial Survey Corporation, Aerial Photos of the site area flown November 1957, (scale 1:6000). 2. Department of Conservation, Michigan Geological Survey: a. An Index of Michigan Geology, by Helen Martin and Muriel Straight, 1956. Page 226 gives location of bedrock out-crops on the south shore of Little Traverse Bay. b. Map of surface formations of Michigan, by Helen Martin, 1957 Centennial Geological Map of Michigan (revised,1957), c. by Helen Martin. 3 Great Lakes Research Institute, Currents and Water Masses of Lake buchigan, by John C. Ayers, et. al., 1958. Figures 13 (p. 30), 24 (p. 53), 38 (p. 79), and 51 (p. 104). 4. Melhorn, W.N., Valders Glaciation of the Southern Peninsu]a of Michigan,195h, unpublished Ph. D. thesis, Univ. of Itchigan, Dept. of Geology. 5 Michigan Geological Society Annual Guidebook, The Traverse Group of the Northern Part of the Southern Peninsula of Michigan, 1949, by William Kelley. Map No. 4 shows aerial map of the Traverse formation for Charlevoix and Emmet Counties, Michigan. 6. Raymond Concrete Pile Company, Gov Division, Test Boring Report, Borings No. 1 and No. 2 at Big Rock Point, Michigan, May 8, 1959 7 Spurr, S.H. and Zumberge, J.H., Inte Pleistocene Features of Cheboygan and Emmet Counties, Michigan, 1956, Amer. Jour. Sci., vol. 254, p. 96-109 8. U.S. Army Corps of Engineers, Lake Survey Division, Monthly Bulletin of Lake levels for August 1959 9 U.S. Dept. of Agriculture: a. Photo Index Mosaic of Charlevoix County, Michigan, 1938, (sheet 1 of 3). b. Photo Index Mosaic of Emmet County, Michigan,1938, (sheet 2 of 2). Both of these include the area surrounding Little Traverse Bay. i 10. U.S. Geological Survey, Topographie Branch, Charlevoix and Charlevoix Lake 15-minute Quadrangle topographic maps. ( 1 l

22 11.

Wilson, J.T., Zudberge, J.H., and Marshall, E.W., A Study of Ice on an Inland Lake,1954, Snow Ice and Permafrost Research Establishment, U.S. Corps of Engineers, Report 5 12.

Veatch, J.O., Soils and Lands of Michigan,1953, Michigan State College Press, 13

Zumberge, J.H., Effects of Ice on Shore Development, 1954, Proceedings of the 4th Conference on Coastal Engineers,
p. 201-205 14.
Zumberge, J.H., Guidebook for the Friends of the Pleistocene Midwest Section, 1956.

c

L' APPENDIX A WELL

  • LOGS OF BORIHGS USED DURING PUMP TEST Boring ES, Elevation 590 7 i

O' - l' Sandy loam and organic matter. l' - 7'5" clayey brown sand and broken limestone. 7'5" - 23'5" Hard sandy and gravelly brown ciny, few limestone fragments. 23'5" - 29'5" compact medium brown sand, some gravel. 29'5" - 48'i Hard sandy brown clay, some gravel, few boulders I and limestone fragments. 48'i - 49'7" compact. clayey brown sand, gravel and broken limestone. 49'7" - 59'11" Limestone, poor recovery. I Boring f6, Elevation 589 9 O' - 2'10" Broken limestone, some claycy sand. i-l- 2'10" - 14'i Sandy medium to medium hard brown clay, some gravel. 14'i 41'5" Hard sandy and gravelly brown clay, few limestone fragments. 41'5" - 46'i Sandy medium brown clay, little gravel. 46'1 - 55'3" Hard sandy and gravelly brown clay, some broken limestone. 55'3" - 64'3" Limestone, good to poor recovery. Boring #7, Elevation 590.4 O' - 3'8" Loose brown sand, some limestone. 3 '8" - 7'0" ' compact clayey brown sand, and broken limestone. 1 7'0" - 16'10" Hard sandy brown clay, some gravel and broken limestone. 16'10" - 22'10" Boulders and hard brown clay. 22'10" - 46'11" Hard sandy and gravelly brown clay, some limestone fragments. 46'11" - 59'9" Limestone, recovery fair. Boring #3, Elevation 590.8 ] (No log) (-

  • These logs are from Raymond Concrete Pile Company preliminary reports.

6 APPENDIX B l 1 ( j ~

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