Water resources of the Marquette Iron Range area, Marquette County, Michigan

Grannemann, N.G. · 1979 · Report

<p>Dependable water supplies are vital to the mining industry in the Marquette Iron Range in Michigan. Development of processes that concentrate and…

Public-domain full text preserved in the Mountain Man Mining Library. Original source: pubs.usgs.gov.

kor Geological Survey . — 1337 Reports-Open file seriEj s UNITED STATES DEPARTMENT OF THE INTERIOR GEOLOGICAL SURVEY WATER RESOURCES OF THE MARQUETTE IRON RANGE AREA, MARQUEITE COUNTY, MICHIGAN U.S. GEOLOGICAL SURVEY Open-File Report 79-1339 Prepared in cooperation with the Michigan Department of Natural Resources . .$ GiT .1°03 INC,/Il;i1:5 lq `y\ FEB 1 91980 7"rj / a R A

CN) III11111#1,1111p111111111111,1 11,e,77 -I /// UNITED STATES , DEPARTMENT OF THE INTERIOR , GEOLOGICAL SURVEY WATER RESOURCES OF THE MARQUETTE IRON RANGE AREA, MARQUETTE COUNTY, MICHIGAN By N. G. Grannemann Open-File Report 79-1339 Prepared in cooperation with the Michigan.Department of Natural Resources Lansing, Michigan

UNITED STATES DEPARTMENT OF THE INTERIOR CECIL D. ANDRUS, Secretary GEOLOGICAL SURVEY H. William Menard, Director For additional information write to: Office of the District Chief Water Resources Division U.S. Geological Survey 6520 Mercantile Way, Suite 5 Lansing, Michigan 48910

CONTENTS Page Definition of terms Conversion factors Local well numbering system Abstract Introduction Purpose Related studies Description of the area Topography Climate Surface water Variations in streamflow Streamflow characteristics Flow duration Low-flow frequency High-flow frequency Lakes and reservoirs Quality of water Major dissolved substances Carp River basin and tributaries to Chocolay River basin Middle Branch Escanaba River basin East Branch Escanaba River basin Michigamme River basin Trace metals Nutrients Dissolved oxygen Temperature Lakes Geology and ground water Bedrock Water-hearing characteristics Unconsolidated deposits Water-hearing characteristics Four principal ground-water resource areas Sands Plain area West Branch Creek area Morgan Creek area Carp Creek area Quality of ground water Bedrock Glacial deposits Summary Selected references Tables

ILLUSTRATIONS Page Figure 1. Marquette Iron Range study area 2. Annual precipitation at Ishpeming 3. Surface-water use in the Marquette Iron Range area 4. Locations of streamflow and water-quality sites . 5. Average monthly precipitation and average monthly runoff at selected gaging stations 6. Variation in discharge of the Middle Branch Escanaba River at Humboldt during dry, average and wet years 7. Average annual runoff at selected gaging stations

8. Flow-duration curves for Middle Branch Escanaba River near Ishpeming, East Branch Escanaba River at Gwinn, and Peshekee River near Champion 9. Low-flow frequency curves for Goose Lake Outlet near Sands Station and Middle Branch Escanaba River near Ishpeming 10. Low-flow characteristics for surface-water sites . . 17 11. Monthly maximum and minimum lake stages for four lakes in the Marquette Iron Range area 12. Relation of specific conductance to dissolvedsolids concentration in surface water 13. Relation of specific conductance to discharge for Middle Branch Escanaba River at Humboldt, Black River near Republic, West Branch Creek near National Mine, and Bear Creek near Princeton 14. Total nitrite plus nitrate concentrations of water from Middle Branch Escanaba River near Princeton, 1969-78 15. Maximum daily water temperatures for the period of record at Middle Branch Escanaba and Peshekee Rivers and Schweitzer Creek 16. Water-quality sampling sites in Teal Lake at Negaunee 17. Temperature and dissolved-oxygen profiles at site 1 in Teal Lake at Negaunee 18. Bedrock formations in the Marquette Iron Range area 19. Glacial deposits in the Marquette Iron Range area 20. Glacial deposits in the Sands Plain area 21. Cross section A-A' of the Sands Plain area 22. Cross section B-B' of the Sands Plain area 23. Cross section C-C' of the Sands Plain area 24. Cross section D-D' of the Sands Plain area 25. Potentiometric surface in glacial deposits of the Sands Plain area 26. Altitude of lowest monthly water levels in Goose Lake test well

ILLUSTRATIONS--Continued Page Figure 27. Glacial deposits in the West Branch Creek area . . . 48 28. Cross sections A-A' and B-B' of glacial deposits in the West Branch Creek area 29. Potentiometric surface in glacial deposits in the West Branch Creek area 30. Glacial deposits in the Morgan Creek area 31. Cross section A-A' of glacial deposits in the Morgan Creek area Sl 32. Glacial deposits in the Carp Creek area 33. Relation of specific conductance to dissolvedsolids concentration of water from glacial deposits 34. Specific conductance of water from glacial deposits in the Marquette Iron Range area . . . . 57

TABLES Page Table 1. Streamflow records in the Marquette Iron Range area 2. Flow duration data 3. Low-flow characteristics 4. Peak flows at gaging stations 5. Surface-water quality records in the Marquette Iron Range area 6. Summary of surface-water quality data available for the Marquette Iron Range area 7. Trace metals in surface water 8. Dissolved-phosphate concentrations in surface water 9. Dissolved oxygen in surface water 10. Duration and range of surface-water temperature . 11. Chemical characteristics of water from Lake Sally near Ishpeming and Perch Lake near Republic 12. Chemical characteristics and physical properties of water from site 1, Teal Lake at Negaunee 3S 13. Trace metals in water from site 1, Teal Lake at Negaunee 14. Nutrient analyses of water from Teal Lake at Negaunee 15. Phytoplankton analyses of water from Teal Lake at Negaunee 16. Log of test well 47N 28W 01DB near Morris Mine 17. Chemical characteristics of water from bedrock 18. Chemical characteristics of water from glacial deposits 19. Iron, manganese, silica, and nitrate in water from glacial deposits 20. Trace metals in water from wells in the Marquette Iron Range area

DEFINITION OF TERMS ifer. A formation, group of formations, or part of a formation that contains sufficient saturated permeable material to yield significant quantities of water to wells and springs. Also called a ground-water reservoir. Base flow. Sustained or fair-weather runoff; in most streams it is composed largely of ground-water runoff. Bedrock. In this report, designates consolidated rocks of Precambrian age. Concentration. The weight of dissolved solids or sediment per unit volume of water; expressed in milligrams per liter (ng/L) or micrograms per liter (ug/L). Contour. An imaginary line connecting points of equal altitude, whether they are points on the land surface, on the bedrock surface, or on a potentiometric surface. Cubic feet per second (ft3/s). A unit expressing rate of discharge. One cubic foot per second is equal to the discharge of a stream through a rectangular cross section 1 foot wide and 1 foot deep at an average velocity of 1 foot per second. Divide. A line of separation between drainage systems. A basin divide or a topographic divide delineates the land from which a stream gathers its water; a ground-water divide is a line on a potentiometric surface on each side of which the poten­ ti.ometric surface slopes downward away from the line. Flow-duration curve. A cumulative frequency curve that shows the percentage of time that specified discharges are equaled or exceeded. Gaging station. A particular site on a stream, canal, lake or reservoir where systematic observations of gage height or dis­ charge are obtained on a continuing basis. Ground water. Water in the ground that is in the saturated zone from which wells, springs, and ground-water runoff are supplied. Ground-water runoff. That part of runoff that has passed into the ground, has became ground water, and has been discharged into a stream channel as spring or seepage water. Hardness. A physical-chemical characteristic of water attributable to alkaline earths, principally calcium and magnesium; ex­ pressed as equivalent calcium carbonate (CaCO3).

Hydrograph. A graph showing the variation of stage, flow, velocity, or discharge with respect to time. Low-flow frequency curve. A graph showing the magnitude and frequency of minimum flows for a period of given length. Partial-record stations. A site where periodic discharge measurements are made without continuous observations of stage. Permeability. A measure of the relative ease with which a porous medium can transmit a liquid under a potential gradient. Potentiometric surface. In aquifers, the levels to which water will rise in tightly cased wells. Where the aquifer is confined, more than one potentiometric surface is required to describe the distribution of head. The water table is a particular potentiometric surface. Regulation. Artificial manipulation of the flow of a stream. Runoff. That part of precipitation that appears in streams; the water draining from an area. When expressed in inches, it is the depth to which an area would be covered if all the water draining from it in a given period were uniformly distributed on its surface. Specific capacity. The rate of discharge of water from a well divided by the drawdown of water level within the well, generally expressed as gallons per minute per foot of drawdown. Specific conductance. A measure of the ability of water to conduct an electric current, expressed in micromhos (pmhos) per centimeter at 25°C. Because the specific conductance is related to amount and type of dissolved material, it can be used for approximating the dissolved-solids concentration of water. For most natural waters the ratio of dissolved-solids concentration (in milligrams per liter) to specific conductance (in micromhos) is in the range 0.5 to 0.8. Storage coefficient (dimensionless). The volume of water an aquifer releases or takes into storage per unit surface area of the aquifer per unit change in head. Subcrop. In this report, a bedrock formation or rock unit that occurs directly under the glacial deposits and that would be exposed if all glacial deposits were removed. Synclinorium. A broad regional fold in rocks in which the strata dip inward from both sides toward the axis. Transmissivity. The rate at which water of the prevailing kinematic viscosity is transmitted through a unit width of the aquifer under a unit hydraulic gradient, generally expressed as gallons per day per foot.

Water year. The 12-month period, beginning October 1 and ending Sep­ tember 30. The water year is designated by the calendar year in which it ends.

CONVERSION FACTORS The inch-pound units used in this report can he converted to the metric system of units as follows: Multiply inch-pound unit By To obtain metric unit cubic feet per second (ft3/s) cubic meters per second (m3/s) cubic feet per second per cubic meters per second per square mile {(ft3/s)/mi2} square kilometer {(m3/s)/km2} degrees Fahrenheit (°F) 1) (1) degrees Celsius (°C) foot (ft) meter (m) inch (in) centimeter (cm) mile (mi) kilometer (km) square mile (mil) square kilometer (km2) 1Temperature °C (temperature °F -32)/1.8. LOCAL WELL NUMBERING SYSTEM The local well number indicates the location of wells within the rec­ tangular subdivision of land with reference to the Michigan meridian and base line. The first two segments of the well number designate township and range, the third segment of the number designates the section and the letters A through D designate successively smaller subdivisions of the section as shown below. Thus, a well designated as 45N 25W 16CCCB would be located to the nearest 2.5 acres acid would be within the shaded area in section 16. A D I mile -1

WATER RESOURCES OF THE MARQUETTE IRON RANGE AREA, MARQUETTE COUNTY, MICHIGAN By N. G. Grannemann ABSTRACT Dependable water supplies are vital to the mining industry in the Marquette Iron Range. Development of processes that concentrate and pelletize low-grade iron ore has permitted mining to expand during the oast two decades. Water demand has increased both for iron ore concen­ tration processes and for the area's general development. Five main streams drain the area. Their total average annual discharge is about 700 cubic feet per second, of which, about 150 cubic feet per second is inflow from outside of this study's limits. The Middle Branch and East Branch Escanaba River flow through the central part of the study area and drain about 60 percent of it. The combined natural flow of these two streams equals or exceeds 100 cubic feet per second 90 percent of the time. Median annual 7-day low-flows are about 0.25 cubic feet per second per square mile in most of the area. Seven stream impoundments and 243 natural lakes provide surface water storage. Surface water is generally of a calcium-magnesium bicarbonate type and dissolved-solids concentrations are generally less than 150 milligrams per liter. Small streams that drain glacial outwash deposits have higher dissolved-solids concentrations than larger streams. Large ground-water supplies may be developed from glacial outwash aquifers along the northern, southern, and eastern boundaries of the study area. Thin, unconsolidated deposits of low permeability occur in the center of the area. Metamorphosed bedrock produces moderate amounts of water only in fracture zones. Sandstones in the eastern part of the area yield water at some locations, but these deposits are seldom utilized because other ground-water sources are more readily available. Ground water in the Marquette Iron Range is generally of suitable quality for most uses. Iron concentrations, however, are frequently high.

INTRODUCTION Iron ore, which has been produced from the Marquette Iron Range since the mid-1800's, has been instrumental in our national development. In 1977, 17 percent of the nation's iron ore was mined in the area (Peterson and Middlewood, 1978). At present, all of this ore is mined from low-grade taconite deposits containing about 35 percent iron, a concentration too low for efficient smelting. Large amounts of water are required for crushing, separating, and pelletizing the taconite to increase its iron content to about 65 percent. Population in the area has grown to keep pace with economic expansion. Between 1960 and 1976 the population of Marquette County increased from 56,154 to 72,097 (U.S. Department of Commerce, 1979 and Marquette County Planning Commission, 1975). Iron mining, community development, and tourism have imposed great demands for water on the area which has only scant supplies of water of good quality currently available. Glacial aquifers are the source of water for eight of the area's snail communities and many domestic users, but stream impoundments and lakes are the source of the largest volume of water used. Purpose The purpose of this study is to assemble, in one report, data collected in the Marquette Iron Range area and to modify, if necessary, any conclusions drawn in Water-Supply Paper 1842 by Wiitala, Newport and Skinner (1967). In that Water Supply Paper, data obtained through 1965, were tabulated and interpreted. Repetition of material in that report has been avoided unless it was considered pertinent to re-evaluations required by new data. A more complete treatment of some aspects of the geology and hydrology of the area can be found in Water-Supply Paper 1842 as well as in the studies cited below. Related Studies Water control in underground mining operations was the primary purpose of a ground-water study of the Marquette iron-mining district by Stuart, Brown, and Rhodehamel (1954). Because the underground mines have been closed this problem no longer exists. In addition, to the report by Wiitala, Newport, and Skinner (1967), parts of the area's water-supply potential have been assessed by Stoimenoff (1972), who established regional draft-storage relationships; and by Supina (1974), who studied the hydrogeology of the outwash deposits northeast of Negaunee. C. J. Doonan and J. R. Van Alstine (unpublished data, 1979) have studied the ground­ water resources of Marquette County, and include a surficial geology map in their report. F. R. Twenter (unpublished data, 1979) is evaluating the geologic and hydrologic data of Marquette County for environmental planning.

Many studies of the geology of the Marquette Iron Range have been made because of the importance of iron ore in the area. Among the more recent studies are those by James (1958), Gair and Thaden (1968), Puffett (1974), and Gair (1975). These studies describe the stratigraphy and bedrock geology of parts of the iron range. Boyum (1975) prepared a general geologic map of the area and Leverett (1929) mapped the glacial geology. Martin (1957) compiled an updated version of Leverett's glacial map and Black (1969) has also mapped glacial deposits in the area. Description of the area The Marquette Iron Range study area consists of 610 mil entirely within Marquette County in the north-central part of Michigan's Upper Peninsula (fig. 1). The western boundary of the area coincides with the county boundary and the eastern boundary is a north-south line 2 mi east of Harvey. The northern boundary generally coincides with the drainage divides of the Carp and Middle Branch Escanaba River basins. The southern boundary generally follows the drainage divide of the Middle Branch Escanaba River basin. Excluding the city of Marquette, about 40,000 people live in the area (U.S. Department of Commerce, 1979). Of this number, about 30,000 live in the Ishpeming, Negaunee, Gwinn, and Republic areas. The population of Marquette is 23,606; however, not all of the city is included in the study area. Topography Topographically, the area is highly dissected and rugged along the northeastern boundary, mountainous in the Negaunee-Ishpeming area, and hilly and rolling in much of the remaining area. Relatively flat plains occur east of Goose Lake Outlet, west of Carp Creek, and surround West Branch Creek. Altitudes range from 602 ft at Lake Superior to 1873 ft at Summit Mountain 3 mi south of Negaunee. Climate The climate of the Marquette Iron Range area is modified by Lake Superior. The most noticeable lake effect is the increased cloudiness and greater snowfall during the fall and early winter and the moderating winter temperatures near Marquette. Mean monthly temperatures at Ishpeming range from 14.7°F in January to 65.7°F in July. The lowest recorded temperature is -30°F; the highest is 99°F. Precipitation is greatest during the spring and summer. June has an average precipitation of 3.87 inches and is the wettest month; whereas, February has 1.16 inches and is the driest (Michigan Department of Agriculture, Michigan Weather Service, 1971). Average annual precipitation at Ishpeming is 31.38 inches (fig. 2). Precipitation from April to

LAKE SUPER/OR Michigan Marquette County Doshoso Creek arquette LAKE leer Mehl& me ke SUPERIOR / 444ile Cilocoloy e r , Boston i'l.54— River 7" Lake

Cerft R/ror ,, , e, Diorite D4. 4` , Beacon §, North .4, Teal 1

46'30' , ,,, 46'30' Lake pf1/10413Ini .knta 1 hoe' c., Humboldt Clarksburg Green d Wee ereemweeel eCese 1"."" , Mr Ks lawn Lake Rrnertsir Lake Goose Lori, National e itiiOb A ueANS: 111ialln: /4, k' 'RITMO, 0' iii „ , Republ 414., Park N II SvitY, ER C, ,, 46'20' 46.20' Stomp Lake 4 NILES wino Figure 1.--Marquette Iron Range study area.

September, most of which is rainfall, averages 20.3 inches. Precipitation from November to early March is usually snow; average annual snowfall is 104 inches. In general , snowfall is greatest on the northwest part of the area. Figure 2.--Annual precipitation at Ishpeming. SURFACE WATER The Marquette Iron Range area is drained by five major rivers. The Carp River and tributaries to the Chocolay River flow eastward or northeastward. They drain about 20 percent of the area into Lake Sup­ erior. The Middle Branch and East Branch Escanaba River drain about 60 percent of the area and flow southeastward, joining near Gwinn to form the Escanaba River, which flows southward to Lake Michigan. The Michigamme River drains about 20 percent of the study area and flows southward into Lake Michigan. Seven impoundments, 243 natural lakes, as well as swamps, ponds, and stream channels store water. Surface water is used for domestic supplies by the major cities in the area, for iron ore processing and for hydroelectric generation. Figure 3 is a flow chart showing surface-water uses and streamf low regulation in the study area. Since 1955, 222 years of gaging station record (16 sites) and 181 years of partial record (20 sites) have been collected in the area (fig. 4, table 1).1/ 1/U.S. Geological Survey stations arc assigned 8-digit downstream order numbers on a national basis as shown in table 1. For convenience in the text and on illustrations in this report, only those digits necessary to identify a station have been used.

Lake Michigarnrne Lake Lory Black River Michigamme Eosin Michigamme Reservoir To Lake Michigan via Menominee River Green Creek Greenwood Reservoir Lake Sally System Schweit zer Reservoir Goose Lake cE aO Schweitzer Creek Cataract Basin East Branch Escanaba River To Lake Michigan via Escanaba River Carp Intake Basin EXPLANATION Lakes Reservoirs Cities Tailings and reuse basins plants Hydroelectric 0 generating Overflow — — — — —"— Figure 3.--Surface-water use in the Marquette Iron Range area (data provided by Cleveland-Cliffs Iron Company).

622, ""1"". LAKE SUPERIOR e

442.N7 46'30' 46'30 6t4 .83 ,e583.6 66'.h 578.50 578.7 578.140 .0578.13 0581.7 '&582 583 8° 4,623 p581.2 q80.2 46'20' 46'20' woo. #24 4 MILES EXPLANATION Partial-record station and station number Gaging station and station number Water-quality site and station number Figure 4.--Locations of streamflow and water-quality sites.

Table 1.--Streamflow records in the Marquette Iron Range area Station Drainage Period of record no. Station name area Water year ending September 30 1955 19)O 1k5 1970 J975 Carp Creek at Ishpeming J/ : 04044 300 Gold Mine Creek near Ishpeming Carp River near Negaunee :XXXXXXXXXXXXXXXXX2/ Morgan Creek near Marquette , ,

Big Creek near Harvey

Cedar Creek near Harvey : Cherry Creek near Harvey , XXXXX Middle Branch Escanaba River near Champion : : Middle Branch Escanaba River at Humboldt XXXXXXXXXXXXXXXXXXX Middle Branch Escanaba River near Greenwood : : Black River near Republic *XXXXXX : Black River near Greenwood Black River near Humboldt

Middle Branch Escanaba River near Ishpeming 128.0 XXXXXXXXXXXXXXXXXXXXXX West Branch Creek near National Mine Middle Branch Escanaba River near Suomi Bear Creek near Princeton Middle Branch Escanaba River near Princeton 210.0 :xxxxxxxxxxxxxxxx Green Creek near Princeton : Ely Creek near National Mine

Schweitzer Creek near Palmer XXXXXXXXXXXXXXXXXX Warner Creek near Palmer XXXXXXXX***XXXXXX Goose Lake Outlet near Negaunee

Goose Lake Outlet near Cascade Junction

Goose Lake Outlet near Sands Station XXXXXXXXXXX East Branch Escanaba River near Sands Station 96.6

East Branch Escanaba River at Gwinn XXXXXXXXXXXXXXXXXXXXXXX Dishno Creek near Champion

Peshekee River near Michigamme Peshekee River near Champion XXXXXXXXX)(XXXXXX , Spurr River at Michigamme

Michigamme River near Michigamme XXXXXXXXX Spruce Creek near Republic

Michigamme River at Republic XXXXXXXXXXXXXX Trout Falls Creek near Republic

Michigamme River near Witch Lake WCXXXXXXXW / Partial record of discharge. X, Continuous record of discharge.

Variations in Streamflow Natural streamflow is generally lowest in late summer and winter (fig. 5). It increases slightly after the first frosts, when evaporation decreases and vegetation dies. During spring, melting snow and rains usually result in the highest flow of the year. During sInmer, evapo­ transpiration reduces runoff. Yearly variations in streamflow also occur. Figure 6 shows discharge during dry, average, and wet years for the Middle Branch Escanaba River at Humboldt. Areal runoff variations are usually more noticeable during winter and during dry years when most streamflow is derived from ground-water inflow. Average annual runoff ranges from 11.3 to 22 inches southeast to northwest (fig. 7). Estimated annual runoff from the study area is 16 inches (about 700 ft3/s), of which about 3.5 inches (150 ft3/s) is inflow from outside of the area in the Michigamme River basin. EXPLANATION III Precipitation at Ishpeming 1,7721 Monthly runoff at Middle Branch ri-La Escanaba River at Humboldt Monthly runoff at Middle Branch Escanaba River near Ishpeming Monthly runoff at East Branch I] L-1 Escanaba River at Gwinn PRECV P I TAT ION AND RUNOFF, IN INCHES JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC Figure 5.--Average monthly precipitation and average monthly runoff at selected gaging stations.

INCUBIC FEET PER SECOND WET Annual mean flow is 83.0 ft3/s I iti AVERAGE Annual mean flow is 66.9 ft3/s a Annual mean flow is 34.5 ft3/s ONDJFMAMJJ AS WATER YEAR Figure 6.--Variation in discharge of the Middle Branch Escanaba River at Humboldt during dry, average, and wet years.

88'00

ls : ., Repubh Park Hil , ' , C' 46'20' ae4 Milwaukee Lake 0..T ., frikALMASMS ­ Boer/ , a ?? 88'00' 4 Mil f Deer Lake Boegon Lake Diorite CC. .., y North Teal Lake .,CcIshaarning mr,... Greenwood) '( Clarksburg ) West um.n , c /WerVar ''' Ibvir , , , i, N Lake San', Gown. k:; C reams ,". atiartalMine , , 58: SU MM IT :74 4 1 MOUNTAIN ,_4:, fi

-'' 584 .004. s"Igrat="( if 1, *33 --" Cat µ( 00" EXPLANATION Stotion number Meon annual runoff (in ) Yeors of record Marquette LAKE SUPERIOR L.,- Corp Rise*, Harvey 46'30' -) ,

0 sand. station ( Coloroct Oakein SAWYER ;Bc'tc A Slump Lake 46'20' Figure 7.--Average annual runoff at selected gaging stations (average annual precipitation at Ishpeming is about 31 inches).

Strearnflow Characteristics A stream's potential as a water supply, or for recreation, wastedilution, and other uses can be evaluated by determining flow-duration and discharge frequency characteristics. Flow Duration Flow-duration curves indicate the percentage of time that specified discharges are equaled or exceeded. For example, the discharge of Middle Branch Escanaba River near Ishpeming was equal to or greater than 30 ft3/s 90 percent of the time (fig. 8). Conversely, 10 percent of the time discharge has been less than 30 ft3/s. As indicated in figure 8, the shape of the duration curve can vary from stream to stream (or from place to place on a stream). Comparing duration curves illustrates dif­ ferences in basin hydrology. For the Peshekee River, the steep slope of the duration curve through the full range of high to low flow indicates poorly sustained streamflow--high peak discharges and low drought flows (fig. 8). Streams draining relatively impermeable areas typically have these characteristics. The relatively flat slope of the East Branch Escanaba River (fig. 8) indicates more uniform streamflow--low peak dis­ charges and high drought flows. Streams draining relatively permeable areas have these characteristics.

Middle Branch Escanaba River (1955-72) East Branch Escanaba River (1955-77) Peshekee River

(1960-77)

.

N

/ e Example A mean dally flow of 30f t 3/s may be expected

to be equaled or exceeded 90 percent of the time.

10 20 30 40 50 60 70 80 90 95 98 99 995 999 PERCENTAGE OF TIME EQUALED OR EXCEEDED Figure 8.--Flow-duration curves for Middle Branch Escanaba River near Ishpeming, East Branch Escanaba River at Gwinn, and Peshekee River near Champion.

Streamflow duration data for most gaging and partial record stations in the Marquette Iron Range area are in table 2. This table lists discharges for five points on the duration curve, average discharge, and a variability index. Average discharge represent; the maximum supply that can be developed from a stream. The variability index, computed by dividing the discharge at the 25 percent duration point by the discharge at the 90 percent duration point, describes the slope of the duration curve. Small variability indices, such as those for Gold Mine, Carp, Cherry, Bear, and West Branch Creeks, indicate flat sloping duration curves and well sustained base flows. Large variability indices, such as those for Black and Peshekee Rivers, and Dishno Creek, indicate relatively steep sloping duration curves and poorly sustained base flows. Low-Flow Frequency Annual minimum average discharges for various periods of consecutive days are used to define frequency curves which relate discharge to recur­ rence interval. Families of low-flow frequency curves (fig. 9) define the magnitude and frequency of the annual minimum average discharge for 7-, 30-, and 120-days for Goose Lake Outlet and Middle Branch Escanaba River. Interpretation of a low-flow frequency curve is shown on figure 9 where the 7-day 10-year low-flow of the Middle Branch Escanaba River is 16 ft3/s. Low-flow frequency characteristics for gaging and partialrecord stations are given in table 3 for four recurrence intervals. The low-flow characteristics of streams in the Marquette Iron Range area are largely determined by the location and composition of glacial deposits. Base flows, in cubic feet per second per square mile, are higher in a drainage basin containing outwash than in a basin containing predominatly till. The median (2-year recurrence interval) 7-day annual low flow is a good index of the low-flow characteristics of a stream. In the study area, median 7-day annual low flows average about 0.25 (ft3/s) except in the Chocolay, Peshekee, upper Black, and upper Carp River basins. Low flows with recurrence intervals of 10 years are required when planning the development of waste disposal systems. The 7-day annual minimum discharges for 10-year recurrence intervals at gaged sites are shown in figure 10.

Table 2.--Flow duration data' (values represent natural streaniflow conditions except as shown in footnotes) Station no. Station name Drainage area (mi2) Average Discharge (Upper number in ft /s; Lower number in (ft3/s)/mi2) Discharge equaled or ewceeded (Upper number in ft /s; Lower number in (ft3/ 8)1 mg) Percentage of days Variability index Q 25/ Q90 Carp Creek at Ishpeming Cold Mine Creek near Ishpeming Carp River near Negaunee 1/ Morgan Creek near Marquette Big Creek near Harvey Cedar Creek near Harvey Cherry Creek near Harvey Middle Branch Escanaba River near Champion Middle Branch Escanaba River at Humboldt 2/ Middle Branch Escanaba River near Greenwood 3/ Black River near Humboldt Black River near Republic 4/ Black River near Greenwood Middle Branch Escanaba River near Ishpeming 5/ West Branch Creek near National Mine Middle Branch Escanaba River near Suomi Bear Creek near Princeton Middle Branch Escanaba River near Princeton 6/ Green Creek near Princeton Ely Creek near National Mine Schweitzer Creek near Palmer 7/ Warner Creek near Palmer 8/ See footnote., at end of table

Table 2.--Flow duration data (values represent natural streamflow conditions except as shown in footnotes) - continued Average Discharge equaled or exceeded Variability Station no. Station name Drainage area (mi2) Discharge (Upper number in ft3/s; Lower number in (ft3/s)/mi2) (Upper number in ft3/s; Lower number in (ft3/s)/mi2) Percentage of days index Q25k, Goose Lake Outlet near Negaunee Goose Lake Outlet near Cascade Junction Goose Lake Outlet near Sands Station 9/ East Branch Escanaba River near Sands Station East Branch Escanaba River at Gwinn 10/ Dishno Creek near Champion Peshekee River near Michigamme Peshekee River near Champion Spurr River at Michigamme Michigamme River near Michigamme Spruce Creek near Republic Michigamme River at Republic 11/ Trout Falls Creek near Republic Michigamme River near Witch Lake 12/ 1/ Flow regulated by dam at Deer Lake storage reservoir 5 mi above station. City of Ishpeming diverted some water into the basin. 2/ From July 1960 to June 1972, some diversion 100 ft above station by industry for iron ore processing. 3/ Flow now regulated by dam at Greenwood Reservoir, partial record data correlated with station 04057800. 4/ Discharge includes some water diverted from above 04057800. 5/ Analyzed for the period 1955-72 before Greenwood Reservoir was completed. 6/ Occasional regulation by dam at powerplant 100 yards above station. Some water diverted and returned below this station. Flow characteristics established by correlation with station 04058000 for the period 1961-72. 7/ Since 1962 flow has been completely regulated by Schweitzer Reservoir 1 mile above the station. Water is diverted by the city of Ishpeming and for iron ore processing. Since 1972 some water has been diverted into the basin via Green Creek. 8/ Since 1972 flow has been effected by waste effluent and mine pumpage. Analyzed for the period 1962-68 and correlated with 04057800. 9/ Some mine water pumped into basin at headwaters. Since 1976 development of the Gribben Lake basin has effectively reduced the drainage area. 10/ Flow effected by Schweitzer Reservoir, diversion by the city of Ishpeming, and diversion for iron ore processing. Since 1972 some water has been diverted into the basin via Green Creek. 11/ Some regulation by abandoned powerplant 0.4 mi above the station. Since 1963 some water has been diverted for iron ore processing and returned 5 mi downstream. 12/ Occasional regulation by dam 14 mi above the station. Some water diverted for iron ore processing.

TTT Goose Lake Outlet C.) (f)

1.2 1.314 1.5 5 6 7 8 9 10 E5 TI Middle Branch Escanaba River E5 mo 10 - Example - The annual minimum 7-day mean discharge will be less than 16 ft 3/s at intervals averaging 10 years. I 1 1 I 1 1 1.2 1.3 14 1.5 5 6 7 8 9 10 RECURRENCE INTERVAL, IN YEARS Figure 9.--Low-flow frequency curves for Goose Lake Outlet near Sands Station and Middle Branch Escanaba River near Ishpeming.

A 2.6 2 8A liarquotta LAKE SUPER/OR 87'30' A 46' 30' 46'30' A A9.I ' Grwrowood .ferrorr A A5.8 A ?: n,„ A0.8 0 5A,' AL AL A2.6 A 5.0 A18 Al? 33A 46'20' 46'20' A40 23A 4 MILES EXPLANATION All 7-day annual minimum discharge, 10 year recurrence interval (ft 3/s) A Partial record station A Gaging station Figure 10.--Low-flow characteristics for surface-water sites. High-Flow Frequency In the past, peak streamflow has not caused serious flooding problems in the Marquette Iron Range area. Most floods occur in the spring as a result of rapid snownelt, heavy continuous rain, and intense local storms. The time of occurrence of floods cannot be predicted; however, their frequency can be estimated if sufficient peak-flow data are available for the stream (usually 10 years). Peak-flow data for stations in the study area with 10 years or more of record are summarized in table 4. This table shows, for example, that at intervals averaging 10 years in length, the Peshekee River near Champion has a flood peak exceeding 3,240 ft3/s and an annual maximum 7-day mean discharge exceeding 2,510 ft3/s.

Table 4.--Peak flows at gaging stations Mean annual 10 year 25 year Highest flood peak flood neak flood peak recorded (upper (upper (upper flood peak Annual maximum 7-day mean discharge number in number in number in (utpilrinum- (upper number in ft3/s; lower ft3/s; ft3/s; ft3/s; ,e r number in (ft3/s)/mi2) lower lower lower ft3/s; number in number in number in lower numStation Station (ft3/s)/mi2) (ft3/s)/mi2) (ft3/s)/mi2) ber in no. name Recurrence interval (ft3/s)/mi2) 2 year 5 year 10 year 25 year Middle Branch Escanaba River at Humboldt 1/ Black River near Republic 2/ Middle Branch Escanaba River near Ishpeming 3/ Middle Branch Escanaba River near Princeton 4/ Warner Creek near Palmer 5/ Goose Lake Outlet near Sands Station 6/ East Branch Escanaba River at Gwinn 7/ Peshekee River near Champion Michigamme River near Michigamme Michigamme River at Republic 8/ Michigamme River near Witch Lake 9/ 1/ From July 1960 to June 1972, some water was diverted 100 ft above this station by industry for iron ore processing. 2/ Discharge includes some water diverted from above 04057800. 3/ Analyzed for the period 1955-72 before Greenwood Reservoir was completed. 4/ Dam for hydroelectric generation located 100 yards above this station. Some water diverted and returned below this station. Peak flows were established for the period 1962-72 before completion of Greenwood Reservoir. 5/ Since 1972 flow has been effected by waste effluent and mine pumpage. Analyzed for the period 1961-68. 6/ Some mine water pumped into the basin at headwaters. Since 1976 development of the Gribben Lake basin has effectively reduced the drainage area. 7/ Flow effected by Schweitzer Reservoir, diversion by the city of Ishpeming, and diversion for iron ore processing. Since 1972 some water has been diverted into the basin via Green Creek. 8/ Abandoned hydroelectric powerplant 0.4 mi above this station. Since 1963 some water has been diverted for iron ore processing and returned S mi downstream. 9/ Abandoned hydroelectric powerplant 14 mi above this station. Some water diverted for iron ore processing.

Lakes and Reservoirs Lakes and reservoirs are valuable resources in the Marquette Iron Range area. Lakes are a source of water for two cities; six reservoirs store water either for use in hydroelectric generation or to supply water for iron ore concentration and pelletizing. Lakes are also the focus of recreation for many people. Most lakes are in the western and southeastern parts of the study area. Lake Michigamme, the area's largest lake (6.7 mil), is near the western border of Marquette County (fig. 1). A plot of the lake's monthly maximum and minimum levels during 1968-76 (fig. 11) indicates that stage increases rapidly during spring. This is primarily due to the relatively high runoff of the Peshekee River, one of the inlets to the lake. Lake Sally and five nearby lakes are the principal source of water for Ishpeming. The backup source of water is Lake Angeline, a natural lake deepened by former underground mining. Because the terrain surrounding Lake Sally is composed primarily of bedrock and thin, discontinuous till, most of the water in the lakes is derived from precipitation and overland runoff (Grannemann, 1978). Lake Sally's water level is regulated by a dam at the lake's outlet. About 3.0 ft3/s of water is withdrawn for the Ishpeming supply. Teal Lake, the source of water for Negaunee, has a snall inlet on its north shore and an intermittently flowing outlet on its northeast side. Glacial outwash partly surrounds the lake and contributes some water to it. A plot of monthly maximum and minimum levels indicates that lake stage fluctuated about 3 ft during 1968-76 (fig. 11). From July 1959 to November 1969 water was pumped from Mather B Mine into Teal Lake at about 2 ft3/s. Declining lake levels after an 11-month drought in 1976-77 prompted resumption of pumping in July 1977. Stage fluctuations for Deer and Goose Lakes are considerably dif­ ferent (fig. 11). Deer Lake, an impoundment of the Carp River 0.5 mi northwest of Negaunee, is regulated for hydroelectric generation. This regulation has caused annual stage variations of as much as 20 ft. During the same period, the stage of nearby Goose Lake varied 3 ft. However, water discharged from Mather B Mine to a small tributary to the lake may reduce the natural variations. Lake level data are also available for Little, Boston, and Witch Lakes in the study area (Miller and Thompson, 1970). The levels of several lakes located near Gwinn are probably controlled by ground water in the surrounding glacial deposits.

Lake Michsgamme near Champion

w 1370

cA MEANSEA IN :AN -J 4 \p, z 1968 1969 1970 1971 1972 1973 1974 1975 1976 1974 1975 1976 WATER YEAR WATER YEAR Deer Loke near Ishpeming Goose Lake near Negaunee

LLJ j cn 1226 Cf) Z 1384 0 z 1224 Yd a

APPROXIMATE ALTI TUDE FEETABOVE 1970 I 9 7 I 1969 1970 1971 1972 1973 1974 WATER YEAR WATER YEAR Figure 11.--Monthly maximum and minimum lake stages for four lakes in the Marquette Iron Range area (dashed where no continuous record collected).

Quality of Water The chemical and physical characteristics of surface waters in a drainage basin are determined primarily by the types of rocks and soils, by topography, vegetation and climatic conditions, and by man's activities. Water quality data from 41 sites (fig. 4) were available to evaluate the chemical and physical characteristics of water in the Marquette Iron Range area. Table 5 shows the type, number of analyses, and period of record of sampling; table 6 summarizes the chemical analyses. Water-quality criteria provide a basis for judging the suitability of water for a given use and serve as a guide in water management. For example, the degree of mineralization of water used for recreation is often not critical but the esthetic appearance is important. For industrial uses, however, concentrations of dissolved and suspended substances may be quite significant. Hard water is generally undesirable for domestic use, yet hardness may be a desirable characteristic of water used for fish propogation. This, the criteria that apply to one use may not apply to another. Major Dissolved Substances The principal cause of seasonal variations in surface-water quality, under natural conditions, is rain or snowmelt. Dissolved-solids con­ centrations generally are highest during periods when little or no new water is being added to the streams and lakes and lowest when rain and snowmelt are highest. Specific conductance of water indicates the amount of material in solution and can be used to estimate the dissolved-solids concentration. Based on observed data, multiplying the specific conductance by 0.6 and adding 19 approximately equals the dissolved-solids concentration of surface water in the study area (fig. 12). For this report, much more data for specific conductance was available than for dissolved solids concentration and comparisons of surface-water quality are usually made using specific conductance. As discharge increases, the specific conductance of water in most unregulated streams decreases (fig. 13). Surface water in the study area has an average dissolved-solids con­ centration less than 150 mg/L--specific conductance less than 220 mhos except in Warner Creek Tributary, Green Creek, and Goose Lake Inlet (table 6). Most surface water is of a calcium-magnesium bicarbonate type; that is, calcium and magnesium constitute more than SO percent of the cations and bicarbonate constitutes more than 50 percent of the anions. The range in percentage of major dissolved substances is as follows: calcium 45 to 71 percent, magnesium 15 to 27 percent, sodium plus potassium 6 to 22 percent, and chloride 8 to 53 percent.

Table S.—Surface-water quality records in the Marquette Iron Range area Station no. 1/ 2/ X Station name Carp Creek at Ishpeming Carp Creek near Ishpeming Gold Mine Creek near Ishpeming Carp River near Negaunee Big Creek near Harvey Cedar Creek near Harvey Cherry Creek near Harvey Middle Branch Escanaba River at Humboldt Greenwood Afterbay near Greenwood Greenwood Diversion near Greenwood Greenwood Release near Greenwood Middle Branch Escanaba River near Greenwood Black River near Humboldt Lake Lory Outlet near Humboldt McKinnon Lake Outlet near Humboldt Lake Lory Outlet near Republic Black River near Republic Black River near Greenwood Middle Branch Escanaba River near Ishpeming West Branch Creek near National Mine Middle Branch Escanaba River near Suomi Bear Creek near Princeton Middle Branch Escanaba River near Princeton Green Creek near Palmer Green Creek near Princeton Ely Creek near National Mine Schweitzer Creek near Palmer Warner Creek Tributary near Palmer Warner Creek near Palmer Goose Lake Inlet near Palmer Goose Lake Inlet near Negaunee Goose Lake Outlet near Cascade Junction Goose Lake Outlet near Sands Station East Branch Escanaba River at Gwinn Peshekee River near Michigamme Peshekee River near Champion Spurr River at Michigamme Michigamme River near Michigamme Michigamme River at Republic Trout Falls Creek near Republic Michigamme River near Witch Lake Occasional chemical or biological quality sample analysed. - Daily maximum and minimum or once daily temperature measurement. Number Period of Record of Water year Samples ending September 30 1960 lin.S 1970 1975 : — : XXWXY XatiCXX

' H S 4: xxx,cxxxxxxxx ,

, ' ' ' , , :

Calculated dissolved-solids concentration= specific conductance X 0.6 +19 SPECIFIC CONDUCTANCE, IN MICROMHOS AT 25 DEGREES CELSIUS Figure 12.--Relation of specific conductance to dissolved-solids concentration in surface water.

U) U) ct cr Black River 5 (1) z (.7) -—1 z -65

- w 150 W z

z w in 125 cr z a E ioo (8) lx I— 30

cc) --Average Discharge It 50 100 150 200 250 300 350 400 450 500 20 40 60 80 K)0 120 140 160 180 200 DISCHARGE, IN CUBIC FEET PER SECOND DISCHARGE, IN CUBIC FEET PER SECOND West Branch Creek cr z

Wu ztn 100 W O w Z Lc) —Average Discharge It 0 0 10 20 30 40 50 60 70 80 90 100 DISCHARGE, IN CUBIC FEET PER SECOND U) z (7) w 120 (-) zw 100 „J W Z (2) Lc) a a U) 10 20 30 40 50 60 70 80 90 100 DISCHARGE, IN CUBIC FEET PER SECOND Figure 13.--Relation of specific conductance to discharge for Middle Branch Escanaba River at Humboldt, Black River near Republic, West Branch Creek near National Mine, and Bear Creek near Princeton.

Carp River basin and tributaries to Chocolay River basin.--Water quality data have been collected at four sites on the Carp River and its tributaries (fig. 4). The site on Carp River (station 444) is down­ stream from the points where Ishpeming and Negaunee discharge treated effluent. Dissolved-solids concentrations of water from Carp River near Negaunee ranged from 50 mg/L during spring runoff to 160 mg/L at low flow. Carp and Gold Mine Creeks near Ishpeming have higher dissolvedsolids concentrations than Carp River near Negaunee. Ground water, the principal component of base flow to these tributaries, is mostly responsible for the higher mineralization because it has a higher dissolved-solids concentration. Quality of water in Big, Cedar, and Cherry Creeks near Harvey does not vary greatly. Specific conductance of water from Big and Cedar Creeks averaged about 150 umhos and that from Cherry Creek averaged about 180 umhos. Middle Branch Escanaba River basin.--Water quality data have been collected at 15 sites within the Middle Branch Escanaba River basin. Average specific conductance at eight of these sites was less than 100 pmhos. Some small streams contain water of highly variable quality. For example, the lowest specific conductance, 27 pmhos,was measured in the upper reach of Black River; the highest, 550 umhos, was at Green Creek near Palmer. Green Creek, whose specific conductance near Palmer averaged 304 pmhos, has the highest dissolved-solids concentrations in the Middle Branch Escanaba River basin. Hardness averaged 91 mg/L and ranged from 9 to 150 mg/L. Lake Lory Outlet, a tributary to Black River, has an average specific conductance of 184 and a maximum of 285 umhos. Water from Lake Lory Outlet, however, does not have a major effect on quality of water in the Black River, and, at the confluence with the Middle Branch Escanaba River, the chemical characteristics of the two streams do not differ appreciably. West Branch and. Bear Creeks are in similar hydrologic settings, but the average specific conductance of water from Bear Creek is 2.3 times greater than that of water from West Branch Creek. The difference is probably caused by the directions of ground-water flow and difference in soil types, which affect the chemical characteristics of base flow to the streams.

Quality of water of the Middle Branch Escanaba River near Princeton has been more variable than at most other locations. Although the average dissolved-solids concentration is about the same as at other stations on the Middle Branch Escanaba River, the maximum specific conductance (340 mhos) and the maximum magnesium concentration (16 mg/L) are higher than at most other sites. The minimum specific conductance and magnesium concentration was 39 'mhos and 1 mg/L respectively. The sampling site is about 100 yards below an impoundment used for hydro­ electric generation, which may account for some of the variability in these constituents. Water from McKinnon Lake Outlet near Humboldt, Lake Lory Outlet near Republic, Middle Branch Escanaba River near Soumi, and Green Creek near Palmer has the highest total manganese concentrations. Dissolved iron concentrations ranged between 30 and 2,700 'g/L. Although iron was not measured each time manganese was measured, their common occurrence and chemical similarity suggests that iron concentrations were also high at times when manganese concentrations were high. East Branch Escanaba River basin.--Water-quality data have been collected at nine locations in the East Branch Escanaba River basin. Water from Ely Creek near National Mine, Schweitzer Creek near Palmer, and East Branch Escanaba River at Gwinn all have similar chemical characteristics. The specific conductance from these streams averaged about 150 'mhos. Water from Goose Lake Inlet near Negaunee had the highest dissolved-solids concentrations in the basin--427 mg/L or specific conductance of 632 mhos. Calcium and sulfate concentrations were also high at this site, probably due to underground mine pumpage from rock units that contain gypsum (Wiitala, Newport, and Skinner, 1967). Currently these mines are inactive, and water is no longer pumped from the gypsiferous rock units. Water from Goose Lake Outlet near Sands Station has a higher average dissolved-solids concentration than water from sites farther downstream in the basin. Ground-water inflow in the lower reaches of Goose Lake Outlet may account for the higher mineralization. Water from Warner Creek Tributary near Palmer had an average spec­ ific conductance of 253 umhos and ranged from 125 to 430 'mhos. At East Branch Escanaba River at Gwinn, downstream from Warner Creek Tributary, specific conductance is less. The highest concentration of manganese (1,500 pg/L) was found in water from Warner Creek Tributary near Palmer; the highest concentration of iron (4,200 pg/L) was found in water from the East Branch Escanaba River at Gwinn.

Michigamme River basin.--Water-quality data have been collected at seven sites on the Michigamme, Peshekee, and Spurr Rivers in the Michigamme River basin. Near Michigamme, the specific conductance of the Peshekee River averaged 39 mhos and ranged from 26 to 70 mhos. Spurr River at Michigamme and Trout Falls Creek near Republic had similar chemical characteristics. Specific conductance of these streams averaged 86 mhos. Between Michigamme and Witch Lake, the average specific conductance of the Michigamme River increased from 50 to 98 mhos. Most other dissolved constituents nearly doubled in concentration also. At low flow, specific conductance increased as much as five times between these two sites. At high flow, however, there is little dif­ ference in chemical characteristics. Iron and manganese concentrations are generally lower in the Michigamme River basin than in other basins in the Marquette Iron Range area. Trace Metals Trace metal concentrations were analyzed for 14 sites on streams in the Marquette Iron Range area (table 7). Because none of these streams are sources of drinking water, no comparison was made between the analyzed values and drinking-water standards. Instead, the analyzed values for trace metals were compared to recommended water-quality standards for aquatic life (U.S. Environmental Protection Agency, 1977). Copper and mercury may occasionally exceed the recommended maximum con­ centrations for some aquatic organisms. Mercury is commonly associated both with copper minerals and sedimentary iron deposits (Fleischer, 1970). Copper mineralization occurs in the Kona Dolomite in the Marquette Iron Range area (Reed, 1966). High concentrations of copper and mercury are not unusual in streams draining such areas. Other trace metals were not found in amounts exceeding maximum concentrations recommended by EPA. Nutrients Nitrogen and phosphorus are essential nutrients for algal and aquatic plant growth. Concentrations of these nutrients vary throughout the year and from stream to stream, being lowest during the growing season when nutrients are utilized by plants. The lowest nitrogen concentrations usually occur in late summer and early fall (fig. 14). Concentrations usually increase in winter as plants die and decay, releasing nitrogen and phosphorus. Average dissolved phosphate concen­ trations of water from streams in the study area ranged from 0.10 to 0.28 mg/L (table 8).

Table 7.--Trace metals in surface water (analyses by U.S. Geological Survey; results in micrograms per liter except as indicated) DisHexaDissolved valent Total DisDisDisDisDissolved cadchrochrosolved solved Total solved solved charge arsenic mium mium mium copper lead mercury nickel zinc Date (ft3/s) (As) (Cd) (Cr6) (Cr) (Cu) (Pb) (Hg) (Ni) (Zn) 04044200 - CARP CREEK AT ISHPEMING E10 CS 04044400 - CARP RIVER NEAR NEGAUNEE 04044563 - BIG CREEK NEAR HARVEY E22 E25 <.5 04044583 - CHERRY CREEK NEAR HARVEY E19 04057800 - MIDDLE BRANCH ESCANABA RIVER AT HUMBOLDT 04057900 - BLACK RIVER NEAR REPUBLIC 04058100 - MIDDLE BRANCH ESCANABA RIVER NEAR PRINCETON 04-2S-62 100, 04058120 - GREEN CREEK NEAR PALMER E10 04058200 - SCHWEITZER CREEK NEAR PALMER 04058350 - GOOSE LAKE INLET NEAR NEGAUNEE

E40 E 4 04058400 - GOOSE LAKE OUTLET NEAR SANDS STATION 04058500 - EAST BRANCH ESCANABA RIVER AT GWINN 04062200 - PESHEKEE RIVER NEAR CHAMPION 04062400 - MICHIGAMME RIVER NEAR WITCH LAKE

, K X-, X x x

)?( IX( f44 ' x JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC Figure 14.--Total nitrite plus nitrate concentrations of water from Middle Branch Escanaba River near Princeton, 1969-78.

Table 8.--Dissolved-phosphate concentrations in surface water (analyses by Cleveland-Cliffs Iron Company during 1969-73; results in milligrams per liter) Mean Minimum Maximum Number Station concentration concentration concentration of no. Station name (PO4) (PO4) (PO4) samples 04058100 Middle Branch Es0.16 canaba River near Princeton 04058120 Green Creek near Palmer 04058250 Warner Creek Trib- utary at Palmer 04058500 East Branch Escanaba River at Gwinn 04062230 Michigamme River near Michigamme 04062400 Michigamme River near Witch Lake Dissolved Oxygen Waters containing 5 mg/L or more of dissolved oxygen are usually suitable for supporting a well balanced aquatic fauna. The range of dissolved oxygen concentrations at 15 sites was 4.8 to 12.4 mg/L (table 9) . Most streams in the area generally have concentrations greater than 5 mg/L. Temperature The variations in maximum daily water temperatures at four loca­ tions in the Marquette Iron Range area arc shown in figure 15. Data collected at two sites on the Middle Branch Escanaba River show that generally winter temperatures are lower and summer temperatures are higher above Greenwood Reservoir than they are below it (fig. 4). During some short periods in early summer, however, reservoir operations increase water temperatures downstream. The range and duration of water temperature at stations with continuous temperature records are summarized in table 10. Lakes Chemical analyses of water from Lake Sally near Ishpeming, Perch Lake near Republic, and Teal Lake at Negaunee indicate that water in these lakes is of a calcium bicarbonate type that ranges from soft to moderately hard (tables 11 and 12). The dissolved solids concentration of water from Lake Sally and Perch Lake is about half that of water from Teal Lake.

Table 9.--Dissolved oxygen in surface water (analyses by U.S. Geological Survey) ConcentraPercent tion of saturation dissolved of dissolved oxygen oxygen Station Date Station name (mg/L) no. Carp Creek at Ishpeming Carp Creek at Ishpeming Carp Creek at Ishpeming Carp River near Negaunee Carp River near Negaunee Big Creek near Harvey Big Creek near Harvey 04044 563 Big Creek near Harvey Cherry Creek near Harvey Cherry Creek near Harvey Middle Branch Escanaba River at Humboldt Middle Branch Escanaba River at HUmboldt Black River near Republic Black River near Republic Middle Branch Escanaba River near Princeton Middle Branch Escanaba River near Princeton Middle Branch Escanaba River near Princeton Middle Branch Escanaba River near Princeton Middle Branch Escanaba River near Princeton Green Creek near Palmer Green Creek near Palmer Schweitzer Creek near Palmer Schweitzer Creek near Palmer Goose Lake Inlet near Negaunee Goose Lake Inlet near Negaunee Goose Lake Outlet near Sands Station Goose Lake Outlet near Sands Station East Branch Escanaba River at Gwinn East Branch Escanaba River at Gwinn East Branch Escanaba River at Gwi.nn East Branch Escanaba River at Gwinn East Branch Escanaba River at Gwinn East Branch Escanaba River at Gwi.nn East Branch Escanaba River at Gwinn East Branch Escanaba River at Gwinn East Branch Escanaba River at Gwinn Peshekee River near Champion Peshekee River near Champion Michigamme River near Michigamme Michigamme River near Michigamme Michigamme River near Michigamme Michigamme River near Witch Lake Michigamme River near Witch Lake

Middle Branch Escanaba River Middle Branch Escanaba River at Humboldt neor Greenwood a U)

(7) j cr u)

w -J 8 2 z OCT NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT WATER YEAR WATER YEAR Schweitzer Creek near Palmer Peshekee River near Champion a: a. 0 W er w W w

-J .rz

7)(

OCT NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC JAN FEB MAR APR MAY JUNE JULY AUG SEPT WATER YEAR WATER YEAR IN Figure 15.--Maximum daily water temperatures for the period of record at Middle Branch Escanaba and Peshekee Rivers and Schweitzer Creek.

Table 10.--Duration and range of surface-water temperature (measurements by U.S. Geological Survey) Daily maximum water temperature (°C) (equal to or greater than Maximum Minimum Period value shown) tempertemperStation of Percentage of days ature ature no. Station name record 10 25 50 70 75 90 Middle Branch Es- 1973-77 21' 17 7.3 0.5 0.4 0.2 canaba River at Humboldt Greenwood Afterbay 1974-77 17 15 7.0 2.4 2.2 1.5 near Greenwood Greenwood Diver1974-77 18 15 6.7 2.8 2.5 2.0 sion near Greenwood Greenwood Release 1974-77 19 16 7.7 2.5 2.4 1.6 near Greenwood Middle Branch Es- 1974-77 20 17 7.1 1.6 1.2 .5 canaha River near Greenwood Black River near 20 16 5.5 .3 .3 .1 Republic Middle Branch Es- 1962-75 20 16 5.9 .4 .3 .1 canaha River near Ishpeming Schweitzer Creek 17 14 6.6 1.9 1.2 .2 near Palmer Peshekce River 22 17 5.1 .3 .3 near Republic Table 11.--Chemical characteristics of water from Lake Sally near Ishpeming and Perch Lake near Republic (analyses by Michigan Department of Public Health; results in milligrams per liter except as indicated) Specific conductance Dissolved solids pH Hardness 1.ocation Date (wmhos) (sum of constituents) (units) (Ca, Mg) Lake Sally Lake Sally Lake Sally Lake Sally SC) Lake Sally Lake Sally 61) Lake Sally Perch Lake Dissolved Dissolved Dissolved Dissolved Dissolved Dissolved calcium magnesiion sodium potassium bicarbonate carbonate Location Date (Ca) (Mg) (K) (1CO3) (CO3) Lake Sally 04-27-55 Lake Sally 07-16-59 Lake Sally 03-10-66 Lake Sally 08-12-71 lake Sally 11-30-73 Lake Sally 08-28-74 S Lake Sally 09-16-75 1) Perch lake 08-14-58 Dissolved Dissolved Dissolved Total Total Total Location Date sulfate (SO4) chloride (CI) fluoride (F) silica (Si0a) iron (Fe) (ug/L) manganese (Mh) (ug/L) Lake Sally Lake Sally Lake Sally Lake Sally Lake Sally Lake Sally Lake Sally Perch Lake S

Temperature and dissolved-oxygen profiles at site 1 in Teal Lake (fig. 16) are shown in figure 17 for nine dates during the 1976 water year. In winter, under ice cover, water temperatures range from 0°C near the surface to bottom in spring and fall. Dissolved oxygen concentration is generally near saturation at all depths in spring and fall, but in winter and summer it decreases rapidly as depth increases. Trace metal analyses of water from site 1 in Teal Lake are shown in table 13. None of the maximum concentrations exceed drinking-water standards (National Academy of Science and National Academy of Engine­ ering, 1974). Water from site 1 was also analyzed for 23 pesticides and other organic compounds on six different dates. All values for tested compounds were less than detection limits. 46°31'15 46°30'25 87°39'00" 87°37'30" Base from U.S. Geological Survey 1:62,500 quadrangle SCALE I mile Figure 16.--Water-quality sampling sites in Teal Lake at Negaunee.

Table 12.--Chemical characteristics and physical properties of water from site 1, Teal Lake at Negaunee (analyses by U.S. Geological Survey, sample depth was 3 ft., results in milligrams per liter except as indicated) Transparency Specific conductance Dissolved solids Dissolved solids (secchi disk) (umhos) (residue at 1800C) (sum of constituents) (in) Average Minimum Maximum Number of samples Dissolved solids p11 Hardness Noncarbonate (tons per acre ft) (units) (Ca, Mg) hardness Average Minimum Maximum Number of samples Dissolved Dissolved Dissolved Sodium Dissolved Calcium magnesium sodium Percent adsorption potassium (Ca) (Mg) (Na) sodium ratio (K) Average Minimum Maximum Number of samples Alkalinity Carbon Dissolved Dissolved Dissolved Bicarbonate Carbonate dioxide sulfate chloride fluoride (HCO3) (C0j) (CaCU3) (CO2) (SO4) (C1) (F) Average Minimum Maximun Number of samples Dissolved silica iron iron manganese manganese (Si02) (Fe) (Fe) (Mn) (Mn) (ug/L) (ug/L) (ug/L) (ug/L) Dissolved Total Dissolved Total Average 18 Minimum Kaximum SOO Number of samples Table 13.--Trace metals in water from site 1, Teal Lake at Negaunee (analyses by U.S. Geological Survey; results in micrograms per liter) Total Total arsenic barium cadmium chromium cobalt Date Total Total Total (As) (Ba) (Cd) (Cr) (Co) <10 <10 Total Total Total Total Total copper lead mercury nickel zinc Date (Cu) (Pb) (It) (Ni) (Zn)

TEMPERATURE, IN DEGREES CENTIGRADE 10 20 0 10 20 0 10 20 0 10 20 0 10 20 0 10 20 0 10 20 0 10 20 U15 F25 DISSOLVED OXYGEN, PERCENT SATURATION 50 100 0 50 100 0 50 100 0 50 100 0 50 100 0 50 100 0 50 100 0 50 100 0 50 100 1 f — —

I—

r w 10

w 15 I— w 20

/ I 1 ' '..

Oct. 23,1975 Dec. 30,1975 Feb. 6,1976 Mar. 9, 1976 Apr. 23, 1976 May 21, 1976 June 25, 1976 July 26, 1976 Sept. 23, 1976 Figure 17.--Temperature and dissolved-oxygen profiles at site 1 in Teal Lake at Negaunee.

The growth of algae is usually limited by the amount of nitrogen and phosphorus available. Total nitrogen concentrations at site 1 in Teal Lake averaged 0.34 mg/L and ranged from 0.12 to 0.51 mg/L (table 14). Most of the nitrogen is organic. Total phosphorus concentrations averaged 0.03 mg/L and ranged from 0.01 to 0.16 mg/L. Algal growth potential is generally highest in late winter and early spring when nutrients are abundant. It is lowest in late summer and early fall when nutrients are incorporated in algae and other plants. The highest con­ centrations of algae occurred in late summer and early fall when bluegreen algae are the dominant type (table 15). During this period, the diversity of algal species is low. The maximum diversity of species occurs during spring and early simmer. GEOLOGY AND GROUND WATER Bedrock of the Marquette Iron Range area is composed of igneous, metamorphic, and sedimentary rocks, of Archean and Proterozoic age (Pnecambrian). Although seldom used as a source of water, bedrock plays an important role in the area's water resources. Except for occasional outcrops, it is overlain by unconsolidated glacial deposits and alluvium of varying thickness. The availability of ground water at a given location depends on the geology and topography. Bedrock Bedrock in the area is composed of metasedimentary rocks, including the Negaunee Iron-formation, of early Proterozoic age, and gneiss and schist of Archean age (fig. 18). In a narrow strip along the eastern part of the area, sandstones of late Proterozoic age subcrop. The Negaunee Iron-formation is the current source of iron ore that is mined in the area (fig. 18). The formation, primarily composed of chert and iron minerals, is more easily eroded than most of the sur­ rounding metamorphic rock because of its mineral composition and fracturing. Water-bearing Characteristics Sandstone is a potential source of water in most of its subcrop area. However, water generally is more readily available from the overlying glacial deposits, and bedrock aquifers are seldom tapped. Water in igneous and metamorphic rocks is stored and transmitted in secondary pores caused by fracturing. Because these openings constitute a very small part of the total volume of the rocks, the water-bearing capacity is low. Yield depends on the number of fractures intercepted by the well. Water produced from bedrock is often highly mineralized.

Table 14.--Nutrient analyses of water from Teal Lake at Negaunee (analyses by U.S. Geological Survey; sample depth was 3 ft.; results in milligrams per liter, except as indicated) Total Total Total Total Total Hydro- Total ni- ammo or- kjelTotal lyz- or- Total Algal trate nia ganic dahl Total Total Total ortho- able ganic or- Chlo- Chlo- growth Total Total plus nini- ninini- phos- phos- phos- phos- ganic roro- potenni- ni- ni- tro- tro- tro- tro- tro- phor- phor- phor- phor- car- phyll phyll tial trate trite trite gen gen gen gen gen ous ous ous ous bon (A) (B) bottle Date (N) (N) (N) (N) (N) (N) (N) (NO3) (P) (P) (P) (P) (C) (ug/L) (ug/L) test SITE 1 05-15-75 0.07 0.00 0.07 SITE 2 09-25-7 5 S.0 Table 15.--Phytoplankton analyses of water from Teal Lake at Negaunee (analyses by U.S. Geological Survey) AUmber of List of Percentage of genera genera total cell constituting having count by 5 percent or 15 percent genera having Total Iskav)er of more of or more 15 percent or Date of cell gel 'ra the total of the total more of the sample count id,ntified cell count cell count total cell count SITE 1 Melosira Fragilaria 1,300 Botryococcus Sphacrocystis Dinobryon Agmenellum Anacystis 1,120 Mclosira An 09-25-75 11,080 Anacystis Anabacna Schrooderia Dinobryon Anacystis Trachelomonas 1,200 Fragilaria Anacystis Mclosira Dinobryon 06-25-70 10,000 Anacystis 07-20-70 15,000 Anabacna 1,060 Nitzschia Anacystis SS SITE 2 2,700 Sphaerocystis Cyclotclla Mclosira 1,400 Botryococcus Melosira Anacystis Anabacna 4,430 Anacystis

MARQUETTE SYNCLINORIUM Dior; 46' 30' 46'30' °Clarksburg REPUBLIC Tilden TROUGH `Z:Z22:25 Mine Republic Mine 46'20' Prints EXPLANATION w H Sandstone Metamorphosed sediments and basic intrusives; includes Negaunee Iron formation z Metamorphosed granite rocks Schist, metagabbro, and serpentinite Figure 18.--Bedrock formations in the Marquette Iron Range area (adapted from Boyum, 1975 and Hamblin, 1958) PROTEROZOIC

Differential weathering and erosion of metamorphic bedrock has produced depressions that are now filled with glacial sediments and constitute the area's ground-water reservoirs. Bedrock erosion and glacial deposition have been controlling factors in the location of stream channels and lakes. Unconsolidated Deposits A thin mantle of till (ground moraine) overlies bedrock in about half of the Marquette Iron Range area. Till, in the form of end moraines, and outwash deposits cover most of the remaining area except for about 10 mil of lake deposits in the northeastern part (fig. 19). The outwash is composed primarily of sand or sand and gravel. Although end moraines generally have large amounts of clay, some of the end moraines in this area are composed of relatively large amounts of sand and gravel with silt and some clay. Glacial lake deposits consist of stratified layers of sand, silt, and clay. Alluvium is deposited in the flood plains of modern river valleys. It is generally composed of large amounts of sand and gravel. Water-bearing Characteristics Glacial deposits are the primary aquifers in the study area. Sand and gravel in these deposits have high porosity and permeability and are capable of storing and transmitting greater amounts of water than con­ solidated rock. Clay and silt in the deposits have high porosity but low permeability and yield little or no water to wells. Outwash is the area's best aquifer and, where more than 150 ft thick, yields large quantities of water. Major areas of thick, permeable outwash deposits and thus the four principal ground-water areas are near West Branch, Morgan, and Carp Creeks and at Sands Plain. Based on specific yield, saturated thickness, and areal extent of the deposits, an estimate of the amount of water in these aquifers is 21 x 109 ft3 (for comparison, the amount of useable storage in Greenwood and Schweitzer Reservoirs is 1.2 x 109 ft3, or one-seventeenth of that stored in glacial aquifers). Till is generally an unsorted material that does not yield water readily. However, in same places, where it contains thick beds of sand and gravel, domestic supplies may be obtained. Lake deposits will yield enough water for domestic supplies if they contain sufficient amounts of sand. Alluvium is generally a good aquifer. Withdrawal of water from alluvium may induce recharge from its associated stream.

Morgan Creek Carp Creek area area Mar,""" LAKE SUPERIOR 87'30 46'30' 46'30 Sands — Plain area ( 46'20' / 46'20' 88'00' West Branch Creek area 4 1411.15 EXPLANATION Outwash End moraines Lake deposits Figure 19.--Glacial deposits in the Marquette Iron Range area.

Four Principal Ground-Water Resource Areas In the Marquette Iron Range area, dependable water supplies have been obtained for many years from areas that contain thick sandy glacial outwash deposits. The hydrogeology of the four principal areas are described in detail in the following sections. Sands Plain Area The Sands Plain area lies between East Branch Escanaba River and Lake Superior (fig. 20). Glacial deposits as much as 400 ft thick occur as outwash, end moraines, and lake deposits. These unconsolidated materials are bordered on the north and west by bedrock or thin till over bedrock. The outwash occurs in two relatively flat parallel plains trending northwest-southeast. They are composed primarily of sand or sand and gravel at the surface with layers of silty sand or sand and clay at depth (figs. 21-24). The end moraines are more heterogeneous in composition, but contain some sand and gravel layers in addition to the more typical clay, silt, and sand, and gravel mixture. Topographically, the moraines form steep gradients that slope toward Lake Superior. The underlying bedrock surface is irregular and slopes eastward to Lake Superior. Surface topography, driller's logs, and seismic data indicate a preglacial stream channel in the area from Cherry Creek west­ ward to Palmer. A valley in this position during glaciation would have been selectively deepened and widened by glacial erosion and then filled by glacial deposits. Few wells are completed in bedrock because the overlying glacial deposits are thick and yield sufficient quantities of water for most purposes. Many wells penetrate at least 200 ft of unconsolidated material without reaching bedrock. The movement and occurrence of ground water and surface water in the Sands Plain area are closely related. Streams flowing from the area have the highest base flows and lowest flood peaks of any streams in the Marquette Iron Range area (tables 2-4). Precipitation readily infiltrates the predominantly sandy outwash, percolates to the ground­ water reservoir, and then flows downgradient toward Lake Superior. High base flows are particularly characteristic of streams draining the base of the outwash plains. Of these streams, Cherry Creek has the highest average discharge per square mile, 4.2 (ft3/s)/mi2. If all rainfall from average precipitation on the Cherry Creek basin went to runoff, the resulting streamflow would be 2.3 (ft3/s)/mi2. Therefore, a minimum of 2 (ft3/s)/mi2 is contributed to the stream by ground-water flow from outside the drainage basin boundaries.

Lake Supenor EXPLANATION Wells Outwosh End moroines Lake deposits Bedrock outcrops 87°20' A th' Location of cross sections shown on figures 21-24 SC ALE 3 Miles Figure 20.--Glacial deposits in the Sands Plain area.

FEET EXPLANATION Cloy Clay, silt, and fine sand Land Surface o o -0­ Cloy, silt, sand, and grovel Silt and sand Sand Sand and grovel Potentiometric Sur face

101, 4 Bedrock 46N 26W 12 DD-Well location MILES Figure 21.--Cross section A-A' (fig. 20) of the Sands Plain area. FEET 47N26W27 BCCCD B' EXPLANATION N fsi 47N25W 21CC a z z Cloy — — Cloy, silt, and fine sand ti

Silt and sand 1000Sand 25W23BA Sand and gravel 900Land ft Surface Bedrock 47N 26W 26 DB - Well location r Potentiometric Surface ib MILES Figure 22.--Cross section B-B' (fig. 20) of the Sands Plain area.

46N 25W 14ABA 45N 24W 5 CC 24W FEET EXPLANATION 1300Land 120°- Surface Clay Cloy, silt, and fine sand 1100­ C v 7 Cloy, silt, sand, and gravel 1000­ Potentiometric Surfoce Silt and sand 900­ Sand Sand and grovel k:$1 Bedrock 47N 25W 35 DBC- Well location 2 3 4 5 6 7 8 9 10 II 12 13 14 15 16 17 18 MILES Figure 23.--Cross section C-C' (fig. 20) of the Sands Plain area. 47N 25W B CADCD O

Land EXPLANATION FEET - Cloy, silt, and fine sand Surface z z

Cloy, silt, sand, and grovel °6% Sand Sand and grovel Silt and sand wiz Potentiometric Surface 47N 25W 20 CC-Well location MILES Figure 24.--Cross section ?f-l)' (Fig. 20) of the Sands Plain area.

A map of the potentiometric surface, figure 25, indicates that the general direction of ground-water flow is northeastward. Ground-water recharge from Goose Lake Outlet flows toward Silver, Cherry, and Cedar Creeks. Base-flow investigations in 1963-64 indicate that, at low-flow, between 2 and 4 ft3/s are lost from Goose Lake Outlet in the first 3 miles below Goose Lake. Pelesier Lake has no apparent outlet and may contribute water to the outwash plain ground-water reservoir. The bedrock outcrop paralleling Goose Lake Outlet and East Branch Escanaba River forms a ground-water divide that does not coincide with the surface divide (fig. 25). Lake Swertor R26W1 R25W R25W Study area EXPLANATION

Well location — 800— Contour line showing altitude of potentiometric surface. Contour interval is 100 ft. Datum is mean sea level. Approximate ground-water divide. SCALE 3W1. Figure 25.--Potentiometric surface in glacial deposits of the Sands Plain area.

Currently, ground water is not withdrawn in amounts sufficient to modify flow patterns except possibly in the vicinity of K. I. Sawyer Air Force Rase. Climatic and seasonal variations in water levels in a well near Goose Lake Outlet are shown in figure 26. The average trans­ missivity and storage coefficient of the aquifer, 130,000 gpd per ft and 0.16 respectively, was determined from a pumping test at this well (Wiitala, Newport, and Skinner, 1967). Near Sands Station, where aquifer thickness is less, transmissivity is estimated to be 24,000 gpd per ft. At K. I. Sawyer Air Force Base the glacial deposits have a transmissivity of 70,000 gpd per ft and a storage coefficient of 0.004. These values indicate that the aquifer is locally confined. Large scale groundwater withdrawals from the Sands Plain area would eventually reduce flow in Goose Lake Outlet and Silver, Cherry, and Cedar Creeks as well as the Chocolay River. w 1207 a 206 w co a 1203 Iw 1202 z D A / 1 L 1 1 11111111111111_111111111111111111 1967 1 1968 I 1969 1970 1 1971 I 1972 I 1973 1 1974 j 1975 1 1976 1 1977 Figure 26.--Altitude of lowest monthly water levels in Goose Lake test well (47N26W36BBDB).

West Branch Creek Area Glacial outwash surrounds West Branch Creek along the southern border of the Marquette Iron Range area. It covers about 25 mil and is bordered by end moraines and bedrock outcrops (fig. 27). The outwash is composed primarily of silt and fine sand as well as sand and gravel (fig. 28). In general, logs of wells drilled in this area indicate that the outwash near West Branch Creek has finer grain size than at Sands Plain. 87° 50' 87°45' Study area EXPLANATION Wells Outwash End moraines R29W R28W R28W R27W Bedrock outcrops oA 4 Location of cross sections shown on figure 28 SCALE 3 Miles Figure 27.--Glacial deposits in the West Branch Creek area. The outwash between West Branch Creek and Green Hills is probably the thickest and has the coarsest grain size of any other in the area. Deposits as thick as 100 ft also occur north of the Middle Branch Es­ canaba River in what is believed by the author to be a buried valley.

A 46N 28W 30DC8 FEET Nf 7 DO rr.r ,„ n z '0 z 7W Land io

Surfoce 46N 2 a S. o

Potentiornetric

It TT Surface MILES EXPLANATION B Ni Cloy, silt, and fine sond g Clay, silt, sond, and gravel FEET U m m U m —

1500N

N W A Wn

Land ♦ Sand 1400Surfoce Vo O pL 0,0, 'fo.

Sond and gravel 1300Potentiometric c4r4 Surfoce Bedrock k 0. I 46N 28W 27 DAD-Well location MILES Figure 28.--Cross sections A-A' and B-B' (fig. 27) of glacial deposits in the West Branch Creek area.

A map of the potentiometric surface (fig. 29) indicates that ground water is generally flowing toward West Branch Creek, Middle Branch Escanaba River, and Black River. On the northwestern side of West Branch Creek, the ground-water gradient is steeper than on the southeastern side. The aquifer's transmissivity, based on flow-net and specific capacity tests, is estimated to be 10,000 to 30,000 gpd per ft (Wiitala, Newport, and Skinner, 1967). Study area EXPLANATION

Well location —1400— Contour line showing altitude of potentiometric R29W R28W R28W R27W surface. Contour interval is 20 ft. Datum is mean sea level. SCALE 3 Mile. Figure 29.--Potentiometric surface in glacial deposits in the West Branch Creek area. Morgan Creek Area The principal water-bearing sediments in the Morgan Creek area are outwash deposits (fig. 30) that fill two closed bedrock depressions. The well sustained base flow of Morgan Creek indicates the effect of the ground-water reservoir on streamflow (tables 2 and 3). The outwash is predominantly fine to medium sand with gravel and occasional clay layers (fig. 31). Depth to ground water in the buried valleys is generally less than 20 ft (Supina, 1974). Based on specific capacity data, the aquifer transmissivity is 5000-7000 gpd per ft.

Study woe EXPLANATION Wells Outwash Thin glacial deposits , A A Location of cross section shown on figure 31 SCALE 3 Miles Figure 30.--Glacial deposits in the Morgan Creek area. EXPLANATION A FEET Cloy Cloy, silt, and fine sond Land (1 -0 Clay, silt, sand, and gravel N Surface Silt and sand Sand Potentiometric

Surface Sand and gravel 414t Bedrock 48N 26W 27 CC - Well location MILES Figure 31.--Cross section A-A' (fig. 30) of glacial deposits in the Morgan Creek area.

Carp Creek Area Three separate outwash deposits occur in the Carp Creek area. Moraines, thin glacial deposits, and bedrock outcrops delineate the three areas near North Lake, Boston Lake, and Second River (fig. 32). 46030' EXPLANATION Outwosh End moraines Thin glociol deposits Bedrock outcrops SC ALE Miles Figure 32.--Glacial deposits in the Carp Creek area (adapted from Stuart, Brown, and Rhodehamel, 1954). Lithologic data from well 47N 28W 01DB indicates that the outwash near North Lake is as much as 216 ft thick and consists of two aquifers separated by a clay layer. The upper aquifer is composed of coarse sand and gravel; the lower consists of fine to coarse sand (table 16). Pumping tests made in conjunction with mine dewatering studies indicate that, near Morris Mine, the outwash may yield as much as 1,600 gal/min and have transmissivi.ties that range from 3,070 to 85,000 gpd per ft (Stuart, Brown, and Rhodehamel, 1954). The range of storage coefficients from 0.00004 to 0.4 indicates that aquifers in the area are both confined and unconfined. Southeast of Boston Lake outwash in a buried valley has a maximum thickness of about 150 ft (Stuart, Brown, and Rhodehamel, 1954). Ground water moves southward from Boston Lake toward Lownoor Lake whose outlet is tributary to the Middle Branch Escanaba River. The maximum thickness of outwash near Second River is about 250 ft in a buried valley. The general direction of ground-water movement is toward the Middle Branch Escanaba River.

Table 16.--Log of test well 47N 28W 01DB near Morris Mine Formation Thickness Depth to of bottom of stratum stratum (ft) (ft) Sand and gravel Sand and gravel Sand, coarse Sand and gravel Gravel, coarse Clay, red Hardpan Sand, medium-fine Sand, coarse Sand, fine Sand, medium-fine Rock cuttings and clay Quality of Ground Water Ground water is frequently more highly mineralized than surface water because it has been in contact with rocks and soils longer. The type of rocks present is important in determining the chemical characteristics of the water. In general, the degree of mineralization of water from glacial deposits is less than that from bedrock.

Bedrock The chemical characteristics of water from bedrock are mostly due to rocks of different composition, the amount and type of fracturing near the source of water, and the direction and rate of ground-water movement. Chemical characteristics vary widely from place to place. For example, dissolved-solids concentrations range from 69 to 5,050 mg/L in the Marquette Iron Range (table 17). The sampling depth and the degree of mineralization are not necessarily related because fracturing or rock type can provide pathways for less mineralized water to in­ filtrate to great depth. Generally, however, water from greater depth is more mineralized than that from shallower depths. Most of the chem­ ical anaylses of water from bedrock contained in this report were obtained from Stuart, Brown, and Rhodehamel (1954), who collected samples from underground mine seepage. Glacial Deposits The chemical characteristics of water from glacial deposits are primarily due to the mineralogy and grain size of the ground-water reservoir and the rate and direction of ground-water movement. In the Marquette Iron Range, water from glacial deposits has less variable chemical characteristics than water from bedrock. For example, the average dissolved-solids concentration of water from glacial deposits was 107 mg/L, and the range was from 26 to 352 mg/L (table 18). Multiplying specific conductance by 0.6 gives the approximate dissolvedsolids concentration (fig. 33). Specific conductance averaged 174 mhos and ranged from 23 to 605 umhos. In general, ground water having the highest specific conductance in the area occurs near Goose Lake (fig. 34). Many domestic supplies in the Marquette Iron Range area use water from glacial deposits. Hardness, which is an important characteristic of water for domestic uses, averaged 81 mg/L. Ten percent of the samples were classified as hard (121-180 mg/L), 60 percent as moderately hard (61-120 mg/L), and 30 percent as soft (0-60 mg/L). The temperature of ground water averaged 8.3 °C and ranged from 5.5 to 11.0°C; pH values averaged 7.6 with a range from 6.2 to 9.7. Water in glacial deposits in the Marquette Iron Range is generally of a calcium bicarbonate type. Average, maximum, and minimum concentrations for the major dissolved constituents are given in table 18. The cation and anion composition of water is as follows: Average Range (percent of cations (percent of or anions) cations or anions) Calcium 40 to 77 Magnesium 10 to 54 Sodium plus potassium 2 to 33 Bicarbonate 14 to 90 Sulfate 0 to 70 Chloride 0 to 75

Table 17.--Chemical characteristics of water from bedrock (analyses by U.S. Geological Survey; results in milligrams per liter except as indicated; Depth: W, well; M, mine) NonLocaSpeccartion Water ific bonDisBiTotal Obser-(townDate tempconate solMagPocarTotal manganvaship of eraducHardhardved CalneSotashonSulChloFluoiron ese Total tion no. and range) sample Depth (ft) ture tance ness ness pH (°C) (umhos) (Ca,Mg) (Ca,Mg) (units) solids cium (Ca) sium (Mg) dium (Na) sium (K) ate fate (H(D3) (SO4) ride (C1) ride (F) (Fe) (wg/L) (RN (ug/L) Silica (Si02) nitrate (NO3) 46N28W01 08-28-63 97W 47N26W05 08-17-59 47N26W06 01-13-60 295051 47N26W06 01-24-52 130951 S 47N26W06 01-24-52 141.351 52.0 180.0 47N26W06 02-01-52* 13101 22.0 100.0 Lf1 47N26W06 01-28-52 47N26W06 01-28-52 47N26W06 01-28-52 420M 47N26W06 10-15-54 47N26W06 01-28-52 47N26W06 01-30-52 239251 47N26W06 01-31-52 265651 35.0 340.0 47N26W19 09-28-61 176W 47N28W01 03-25-52 1683M 155.0 1080.0 :z21 47N28W01 03-25-52 1683M 151.0 963.0 47N28W01 03-25-52 1906M SOO 47N28W01 03-25-52 1705M Mean 34.5 162.0 Minimum Maximum 155.0 1080.0 1:00 Number of samples

cr w F- 400 cr w Co M a cr CD 300

Z 250 Dissolved solids 0.6 X specific conductance cf)— o r--,: 200 o w 150 _J0 Cr) (J) 0 0 100 200 300 400 500 600 700 800 900 1000 SPECIFIC CONDUCTANCE, IN MICROMHOS AT 25 DEGREES CELSIUS Figure 33.--Relation of specific conductance to dissolved-solids concentration of water from glacial deposits.

160,, 140 Marquett LAKE SUPERIOR 8 7 ' 30 ' 193 114 p 22 68 46'30' 46 30' 306 S200 Q,290 *110 440 2.0 238 151 145 .2 300*

'114 195270: .220 85

16.20'

1€3

1999278 46' 20' 4 MILES 178* EXPLANATION Well location, number is specific conductance in micromhos at 25°C Specific conductance, less than 100 micromhos Specific conductance, from 101 to 300 micromhos Specific conductance, from 301 to 650 micromhos Figure 34.--Specific conductance of water from glacial deposits in the Marquette Iron Range area.

Maximum calcium and sulfate concentrations in ground water in the area adjacent to Goose Lake Outlet were 48 and 108 mg/L, respectively. This relatively high mineralization of ground water was probably caused by infiltration of water from Goose Lake Outlet. One source of calcium and sulfate was mine pumpage from rock units containing dispersed gypsum. Although this pumpage was stopped in 1971, insufficient data are available to assess how the ground-water chemistry has changed. During 1976- 77 maximum concentrations of calcium and sulfate were 34 and 6.6 mg/L, respectively, at the Goose Lake test well (47N 26W 36BBEB). However, this well is neither in the same location nor of the same depth as the wells previously sampled (table 18). Analyses of water from wells near K. I. Sawyer Air Force Base in­ dicate that the dissolved-solids concentration of water in this area has increased over the past several years. Pumping may have altered ground-water flow in the area. Iron and manganese are relatively high and are the most objection­ able constituents in water from glacial deposits. In 30 percent of the analyses, iron exceeded the maximum permissable concentration of 3,000 ug/L for drinking water set by the U.S. Environmental Protection Agency (1977). Total iron averaged 2,080 ug/L, and ranged from 9 to 26,000pg/L (table 19). In about 15 percent of the analyses, manganese concentrations exceeded the recommended maximum concentration. The average silica and nitrate concentrations were 11 and 1.7 mg/L, respectively. Water from three wells was analyzed for trace metals, pesticides, phenols, and PCBs. Trace metal analyses indicate that, for most con­ stituents, concentrations were less than maximum recommended limits for drinking water (table 20). Phenols were detected at Goose Lake test well (47N 26W 36BBDB) on June 1 and November 3, 1976; concentrations were 1 and 3 lig/L, respectively. However, no phenols were detected on July 18, 1977. In November 1976, a concentration of 0.1 0g/L PCB was detected at Ely Township well (47N 28W 03CCDC). PCB was not detected when analyses were made in September 1975 and July 1977.

Table 20.--Trace metals in water from wells in the Marquette Iron Range area (analyses by U.S. Geological Survey; results in micrograms per liter) Total Total Total Total Total berylTotal Total cadchroTotal Total arsenic barium lium bismuth boron mium mium cobalt copper Date (As) (Ba) (Be) (Bi) (B) (Cd) (Cr) (Co) (Cu) GOOSE LAKE TEST WELL (47N26W36BBDB01)

<10

') Ely Township Well (47N28W03Ccdc01) <10

HUMBOLDT OBSERVATION WELL (47N29W02ADDA01) Total Total Total Total molyb- Total Total stron- vanalead denum nickel silver tium dium Date (Pb) (Mo) (Ni) (Ag) (Sr) (V) GOOSE LAKE TEST WELL (47N26W36BBDB01)

Ely Township Well (47N28W03Ccdc01)

HUMBOLDT OBSERVATION WELL (47N29W02ADDA01) Total Total Total Total Total Total Total alumTotal gerTotal seletitanzir­ zinc tin inum gallium manium lithium nium ium conium Date (Zn) (Sn) (Al) (Ga) (Ge) (Li) (Se) (Ti) (Zr) GOOSE LAKE TEST WELL (47N26W36BBDB01)

11-03-76 170

Ely Township Well (47N28W03Ccdc01) 06-01-76 130

07-20-77 710 Humboldt Observation Well (47N29W02Adda01) 07-20-77 160

SUMMARY Iron mining, community development, and tourism have imposed large demands for water in the Marquette Iron Range area. Stream impoundments and lakes are the sources for most water used in the area. Glacial aquifers are the source of water for many domestic users and eight small communities. The five major rivers draining the area have an estimated annual runoff of 16 inches (about 700 ft3/s), of which about 3.5 inches (150 ft/s) is inflow from outside the study area. The Middle Branch and East Branch Escanaba River drain about 60 percent of the area. Their combined discharge equals or exceeds 100 ft3/s 90 percent of the time. Small streams draining glacial outwash have well sustained lowflows. The median annual 7-day low-flows in the Middle Branch and East Branch Escanaba River are about 0.25 (ft3/s)/mi2. In parts of the Carp and Chocolay River basins low-flow is as much as 4.0 (ft3/s)/mi2. In the Michigamme River basin, a median annual 7-day low-flow as little as 0.07 (ft3/s)/mi2 occurs. Surface water in the study area has an average dissolved-solids concentration less than 150 mg/L except in Warner Creek Tributary, Green Creek, and Goose Lake Inlet. Most surface water is of a calcium-magnesium bicarbonate type. Copper and mercury may occasionally exceed maximum concentrations recommended by EPA for some aquatic organisms. Dissolvedoxygen concentrations are greater than 5 mg/L in most streams. Generally, winter water temperatures are lower and summer temperatures are higher in the stream above Greenwood Reservoir than below it. Chemical analyses of water from three of the area's lakes indicates that the water is of a calcium bicarbonate type that ranges from soft to moderately hard. Trace metals were below maximum concentrations re­ commended by EPA for drinking water, and pesticides were below detection limits at Teal Lake at Negaunee. Bedrock in the Marquette Iron Range area is composed of igneous, metamorphic, and sedimentary rocks of Precambrian age. Although seldom used as a source of water, bedrock is important to the area's water resources. Differential weathering and erosion of the bedrock produced depressions that are now filled with glacial deposits that are the principal aquifers in the area. Outwash deposits, composed mostly of sand and gravel, are the best aquifers in the area. In the Sands Plain area, glacial deposits are as thick as 400 ft and have transmissivities as high as 130,000 gpd per ft. Most of the ground water in this area is unconfined, but pumping tests near K. I. Sawyer Air Force Base indicate that it is locally confined. Transmissivities in the West Branch Creek area are estimated to be 10,000 to 30,000 gpd per ft. Other areas of outwash occur near Morgan and Carp Creeks in the northern part of the study area.

Water from bedrock is generally more mineralized with increased depth. The variability of mineralization is indicated by dissolvedsolids concentrations, which ranged from 69 to 5,050 mg/L. In glacial deposits, ground water is less mineralized with dissolved-solids concen­ trations ranging from 26 to 352 mg/L. Most of this water is moderately hard (61-120 mg/L) and of a calcium bicarbonate type. Iron and mang­ anese exist in relatively high concentrations and are the most object­ ionable constituents in water from glacial deposits. Total iron con­ centrations averaged 2,080 pg/L but the maximum concentration was 26,000 pg/L.

SELECTED REFERENCES Black, R. F., 1969, Valderan glaciation in western upper Michigan, Proceedings of twelfth conference of Great Lakes Research, International Association of Great Lakes Research, p. 116-123. Boyum, B. H., 1975, The Marquette mineral district of Michigan: The Cleveland-Cliffs Iron Company, Ishpeming, Michigan, in conjunction with the 21st Annual Institute on Lake Superior Geology, Northern Michigan University, 59 p. Fleischer, Michael, 1970, Summary of the literature on the inorganic chem­ istry of mercury, in U.S. Geological Survey Professional Paper 713: D. 6-16. Gair, J. E., 1975, Bedrock geology and ore deposits of the Palmer quadrangle, Marquette County, Michigan: U.S. Geological Survey Pro­ fessional Paper 769, 159 p. Gair, J. E., and Thaden, R. E., 1968, Geology of the Marquette and Sands quadrangles, Marquette County, Michigan: U.S. Geological Survey Professional Paper 397, 77 p. Grannemann, N. G., 1978, Water supply potential of the Lake Sally system, Marquette County, Michigan: U.S. Geological Survey Open-File Report 78-1046, 14 p. Hamblin, W. K., 1958, Cambrian sandstones of northern Michigan, Michigan Department of Conservation Geological Survey Division, Publication 51, 146 p. James, H. L., 1958, Stratigraphy of Pre-Keweenawan Rocks in parts of northern Michigan: U.S. Geological Survey Professional Paper 314-C, 44 p. Leverett, Frank, 1929, Moraines and shore lines of the Lake Superior basin: U.S. Geological Survey Professional Paper 154-A, 72 p. Marquette County Planning Commission, 1975, Marquette County Compre­ hensive plan: 234 p. Martin, H. M., 1957, Map of the surface formations of the Northern Peninsula of Michigan: Michigan Department of Natural Resources, Geological Survey Division Publication 49.

Michigan Department of Agriculture, Michigan Weather Service, 1971, Climate of Michigan by stations. Miller, J. B., and Thompson T., 1970, Compilation of data for Michigan Lakes: U.S. Geological Survey open-file report, 368 p. National Academy of Science and National Academy of Engineering, 1974, Water quality criteria, 1972: U.S. Government Printing Office, Washington, D. C. Peterson, E. C., and Middlewood, E., 1978, Minerals in the Economy of Michigan: U.S. Bureau of Mines, State Mineral Profile - 7, 14 p. Puffet, W. P., 1974, Geology of the Negaunee quadrangle Marquette County, Michigan: U.S. Geological Survey Professional Paper 788, 51 p. Reed, R., 1966, Copper mineralization in Animikie sediments of the Eastern Marquette Iron Range, Marquette County, Michigan: The Compass, v. 45, p. 47-55. Stoimenoff, L. E., 1972, Regional draft-storage relationships for central and western Upper Peninsula of Michigan, U.S. Geological Survey Open-file report, 13 p. Stuart, W. T., Brown, E. A., and Rhodehamel, E. C., 1954, Ground-water investigations of the Marquette iron-mining district: Michigan De­ partment of Conservation, Geological Survey Division Technical Report 3, 91 p. Supina, R. D., 1974, A geological-geophysical ground-water study for Negaunee Township, Marquette County, Michigan: Michigan Tech­ nical University, Unpublished masters thesis, 56 p. U.S. Department of Commerce, 1979, Current population report, 1976. U.S. Environmental Protection Agency, 1977, Quality criteria for water: U.S. Environmental Protection Agency Report, 256 p. Wiitala, S. E., Newport, T. G., and Skinner, E. L., 1967, Water resources of the Marquette Iron Range area, Michigan: U.S. Geological Survey Water-Supply Paper 1842, 142 p.

Tables

Table 3.--Low-flow characteristics (values represent natural streamflow conditions except as shown in footnotes) Lowest annual average discharge for indicated period of consecutive days and recurrence interval Station no. Station name 2-yr (Upper number in ft3/s; lower number in (ft3/s)/mi2) 7-day 30-day 120-day 5-yr 10-yr 20-yr 2-yr 5-yr 10-yr 2-yr 5-is 10-/y 20-15 Carp Creek at Ishpeming Gold Mine Creek near Ishpeming Morgan Creek near Marquette Cherry Creek near Harvey Middle Branch .o Escanaba River near Champion Middle Branch Escanaba River at Humboldt 1/ Middle Branch Escanaba River near Greenwood 2/ Black River near Humboldt Black River near Republic 3/ Black River near Greenwood Middle Branch Escanaba River near Ishpeming 4/ West Branch Creek 5.0 near National Mine .26 Middle Branch Escanaba River near Suomi Bear Creek near Princeton Middle Branch Escanaba River near Princeton 5/ Green Creek 4,5 near Princeton Ely Creek near National Mine Warner Creek near Palmer 6/ Goose Lake Outlet 7.5 near Negaunee See footnotes at end of table.

Table 3.--Low-flow characteristics (values represent natural streamflow conditions except as shown in footnotes) - continued Lowest annual average discharge for indicated period of consecutive days and recurrence interval Station Station (Upper number in ft3/s; lower number in (ft3/s)/mi2) no. name 7-day 30-day 120-day 2-yr 5-yr 10-yr 20-yr 2-yr 5-yr 10-yr 20-yr 2-yr 5-yr 10-yr 20-yr Goose Lake Outlet near Cascade Junction Goose Lake Outlet near Sands Station 7/ East Branch Escanaba River near Sands Station East Branch Escanaba River at Gwinn 8/ Dishno Creek near Champion Peshekee River near Michigamme Peshekee River near Champion Spurr River at Michigamme 0406223) Michigamme River near Michigamme Spruce Creek near Republic Michigamme River at Republic 9/ trout Falls Creek near Republic Michigamme River near Witch Lake 10/ .26 1/ From July 1960 to June 1972, some diversion 100 ft above station by industry for iron ore processing. 2/ Flow now regulated by dam at Greenwood Reservoir, partial record data correlated with station 04057800. 3/ Discharge includes some water diverted from above 04057800. 4/ Analyzed for the period 1955-72 before Greenwood Reservoir was completed. 5/ Occasional regulation by dam at powerp1.ant 100 yards above station. Some water diverted and returned below this station. Flow characte, ,ctics established by correlation with station 04058000 for the period 1961-72. 6/ Since 1972 flow oas been effected by waste effluent and mine 9umpage. Analyzed tor theweriod 1962-68 and correlated with 04057800. 7/ Some mine water pumped into basin at headwaters. Since 1976 development of the Gribben Lake basin has effectively reduced the drainage area. 8/ Flow effected by Schweitzer Reservoir, diversion by the city of Ishpeming, and diversion for iron ore processing. Since 1972 some water has been diverted into the basin via Green Creek. 9/ Some regulation by abandoned powerplant 0.4 mi above the station. Since 1963 some water has been diverted for iron ore processing and returned 5 mi downstream. 10/ Occasional regulation by dam 14 mi above the station. Some water diverted for iron ore processing.

Table 6.--Summary of surface-water quality data available for the Marquette Iron Range area (analyses by U.S. Geological Survey; results in milligrams per liter except as indicated; if only one value was available, it is reported as mean) DisColor DisDisolDisSpec- (plaDissolDissolved DisDisDissolved Total Dis­ cific tinsolved solved bisolsolsolsolids Nitrite Dis Total solved umved magved pocarved ved ved conresiTotal plus Total solved ManganmanDisduccoHardcalnesotasbonsulchlofluodue Nitrate Nitrate Iron Iron ese ganese charge tance at Nitrogen Nitrogen (Fe) (Fe) (Mn) (Mn) pH bait ness cium sium dium sium ate fate ride ride (ft3/s) (umhos) (units) units) (CaCO3) (Ca) (Mg) (Nh) (K) (HCO3) (904) (C1) (F) 180°C (NO ) (N) (ug/E) (ug/L) (ug/L) (ug/L) Carp Creek at Ishpeming (04044200) Mean Minimum Maximum 30S SO Number of samples Carp Creek near Ishpeming (04044210) Mean Minimum Maximum SO rp River R Number of samples Gold Mine Creek near Ishpeming (04044300) Mean Minimum Maximum Number of samples SS Carp River near Negaunee (04044400) Mean Minimum Maximum Number of samples IS IS IS S90 - Big Creek near Harvey (04044563) Mean Minimum Maximum Number of samples S Chocolay R iver Bas in Cedar Creek near Harvey (04044574) Mean Minimum Aiximum Number of samples Cherry Creek near Harvey (04044583) Mean Minimum Maximum Huber of samples Middle Branch Escanaba River at Humboldt (04057800) Mean Minimum Maximum NUmber of samples 19

Table 6.--Summary of surface-water quality data available for the Marquette Iron Range area (analyses by U.S. Geological Survey; results in milligrams per liter except as indicated; if only one value was available, it is reported as mean) - continued Speccific conDisduccharge tance pH (ft3/s) (pmhos) (units) Color (platinumcoHardbalt ness units) (CaCO3) DisDissolsolved ved magcalnecium sium (Ca) (Mg) Dissolved sodium (Na) Dissolved potassium (K) Disolved bicarbonate (HCO3) DisDissolsolved ved sulchlofate ride (SO4) (C1) Dissolved fluoride (F) Dissolved solids residue at 180°C Total Nitrate Nitrogen (NO ) Total Nitrite plus Nitrate Nitrogen (N) Total Iron (Fe) (pg/L) Dis solved Iron (Fe) (pg/L) Total Manganese (Mn) (pg/L) Dissolved manganese (Mn) (ug/L) Middle Branch Escanaba River near Greenwood (04057820) Mean Minimum Maximum Number of sample, .., 2S a 1( 2, 1" 2:, 1.: .., SO Black River near Humboldt (04057850) Mean Minimum Maximum Number of samples S Lake Lory Outlet near Humboldt (04057855) Mean Minimum Maximum Number of samples S McKinnon Lake Outlet near Humboldt (04057860) Mean Minimum Maximum .h Number of samples S SO ' Lake Lory Outlet near Republic (04057870) i:. ,,, Mean Minimum Maximum Number of samples LS -o Black River near Republic (04057900) Mean Minimum Maximum Number of samples 15 2.S Black River near Greenwood (04057980) Mean Minimum S Maximum Number of samples S Middle Branch Escanaba River near Ishpeming (04058000) Mean Minimum Maximum Nbmber of samples

Table 6.--Summary of surface-water quality data available for the Marquette Iron Range area (analyses by U.S. Geological Survey; results in milligrams per liter except as indicated; if only one value was available, it is reported as mean) - continued DisColor DisDisolDisSpec- (plaDissolDissolved DisDisDissolved Total Discific tinsolved solved bisolsolsclsolids Nitrite Dis Total solved conumved magved pocarved ved ved resiTotal plus Total solved ManganmanDisduccoHardcalnesotasbonsulchlofluodue Nitrate Nitrate Iron Iron ese ganese charge tance pH bait ness cites sium dium sites ate fate ride ride at Nitrogen Nitrogen (Fe) (Fe) (Mn) (Mn) (ft3/s) (umhos) (units) units) (CaCO3) (Ca) (Mg) (Na) (K) (HCO3) (S104) (CI) (F) (NO3) (N) (ug/L) (ug/L) (ug/L) (ug/L) West Branch Creek near National Mine (04058020) Mean ,, 6' :,i.,lim.,ra o.0 Maximum Number of samples S S S S S Middle Branch Escanaba River near Soumi (04058050) Mean Minimum SO Number of samples Riximum Bear Creek near Princeton (04058080) Minimum Mean Maximum a Number of samples Middle Branch Escanaba River near Princeton (04058100) Mean Minimum Maximum Number of samples 116 Green Creek near Palmer (04058120) Mean Minimum Maximum Number of samples SO SO SI Green Creek near Princeton (04058130) Mean Minimum Maximum Number of samples Ely Creek near National Mine (04058170) Mean Minimum Maximum Number of samples Schweitzer Creek near Palmer (04058200) Mean Minimum Maximum Number of samples S2

Table 6.--Summary of surface-water quality data available for the Marquette Iron Range area (analyses by U.S. Geological Survey; results in milligrams per liter except as indicated; if only one value was available, it is reported as mean) - continued Color Spec- (placific tinconumDisduccocharge tance pH bait (ft3/s) (umhos) (units) units) DisDissolsolved ved magHardcalneness cium sium (CaCO3) (Ca) (Mg) Dissolved sodiem (Nu) Dissolved potassium (K) Disolved DisDisbisolsolcarved ved bonsulchloate fate ride (HCO3) (SO4) (C1) Dissolved fluoride (F) Dissolved solids residue at 180°C Total Nitrate Nitrogen (NO ) Total Nitrite plus Nitrate Nitrogen (N) Total Iron (Fe) (ug/L) Dis solved Iron (Fe) (ug/L) Total Manganese (Mn) (ug/L) Dissolved manganese (Mn) (ug/L) Warner Creek Tributary near Palmer (04058250) Mean Minimum Maximum Number of samples 72 1,r 2.S

Warner Creek near Palmer (04058300) Mean Minimum Maximum Number of samples Goose Lake Inlet near Palmer (04058337) Mean Minimum Maximum Number of samples 11S z Goose Lake Inlet near Negaunee (04058350) .0 Mean Minimum Maximum Number of samples a Goose Lake Outlet near Cascade Junction (04058370) Mean Minimum Maximum Number of samples Goose Lake Outlet near Sands Station (04058400) Mean Minimum Maximum Number of samples 11 East Branch Escanaba River at Gwinn (04058500) Mean Minimum Maximum Number of samples 114 S4 76 Peshekee River near Michigamme (04062100) Mean Minimum Maximum Number of samples

Table 6.--Summary of surface-water quality data available for the Marquette Iron Range area (analyses by U.S. Geological Survey; results in milligrams per liter except as indicated; if only one value was available, it is reported as mean) - continued Speccific conDisduccharge tance pH (ft3/s) (umhos) (units) -Color (platinumcoHardbait ness units) (CaCO3) DisDissolsolved ved magcalnecium sium (Ca) (Mg) Dissolved sodium (Na) Dissolved sium (K) Dis­ olved bicarbonate (11003) DisDissolsolved ved sulchlofate ride (904) (C1) Dissolved fluoride (F) Dissolved solids residue at Total Nitrate Nitrogen (NO ) Total Nitrite plus Nitrate Nitrogen (N) Total Iron (Fe) (ug/L) Dis solved Iron (Fe) (ug/L) Total Manganese (Mn) (ug/L) Dissolved manganese (Mn) (ugiL) Peshekee River near Champion (04062200) Mean Minimum Maximum Number of samples SO SO Spurr River at Michigamme (04062220) Mean Minimum Maximum Number of samples Michigamme River near Michigamme (04062230) Mean Minimum Maximum Number of samples 113 u Michigamme River at Republic (04062300) Mean Minimum Maximum Number of samples Trout Falls Creek near Republic (04062320) Mean Minimum Maximum Number of samples Michigamme River near Witch Lake (04062400) Mean Minimum Maximum Number of samples 124 38.0 14.0 SO IS SO SO

Table lc.--Chemical characteristics of water from glacial deposits (analyses by U.S. Geological Survey except for those indicated by asterisk which were analyzed by Michigan Department of Public Health; results in milligrams per liter except as indicated) Spec­ ific NonObservation numLocation (township and Date of Depth of well Water temperature conductance carHard- bonate ness hardpH Dissolved Calcium Magnesium Po­ tasSodium sium Bicarbonate Sulfate Chloride Fluoride ber range) sample (ft) (°C) (omhos) (Ca,Mg) ness (units) solids (Ca) (14g) (Na) (K) (11003) (SO4) (Cl) (F) 45N24W05C 4SN24W20DBB 10-19-70 3 4SN2SW0IBCA 06-24-65 45N25W02888 07-09-73 45N25WI1BC 09-06-63 45N25W23AC 09-10-63 45N25W2SABB 10-19-70 SO 45N25W28AB1 11-10-70 9 45N25W28AB2 11-18-70 45N26W03DA 08-28-63 45N26W15 17.0 14.0 45N26W15A 34.0 15.0 45N28W11ADA 10-16-70 45N28W1111C 10-16-70 180 26.0 11.0 46N24W05C 46N25W09B 46N25W11C 07-26-63 189 46N25W160 46N2SW36-6 11-19-74 106 46N2SW36-6 10-22-74 106 46N25W36-6 01-08-74 106 46N25W36-1 07-19-6S 135 46N25W36-3 07-26-66 110 10.0 5.0 ' 46N25W36-4 07-17-69 120 10.0 46N25W36-5 07-19-65 102 46N25W36-2 07-19-65 4.S 46N25W36-2 03-16-60 46N25W36-7 07-09-70 110 46N25W36-7 07-17-69 106 46N2SW3681 07-29-68 136 10.0 20.0 16.0 46N25W3681 07-10-67 136 46N25W36111 07-26-66 136 10.0 46N25W3681 07-19-65 136 46N25W3681 03-16-60 136 46N25W36113 07-26-66 106 46N25W3683 07-19-65 106 46N25W3683 03-16-60 106 46N25W3686 07-29-68 106 23.0 13.0 46N25W3686 07-10-67 106 46N25W36B8 07-10-67 106 105.0 22.0 46N25W36B8 07-26-66 106 10.0 46N25W3688 07-19-65 106 46N25W36D4 07-09-73 141 46N25W36D4 07-10-72 141 46N25W361)4 06-21-71 141 46N25W361)4 07-09-70 141 46N25W36D4 07-17-69 141 46N25W3604 07-29-68 141 46N2SW36D4 07-10-67 141 SO 46N25W361)4 07-26-66 141 10.0 46N25W361)4 07-19-65 141 46N25W36U5 07-09-73 144 46N25W3605 07-10-72 144 13,0 46N26W36D5 06-21-71 144

Table 18.--Chemical characteristics of water from glacial deposits (analyses by U.S. Geological Survey except for those in dicated by asterisk which were analyzed by Michigan Department of Public Health; results in milligrams per liter except as indicated) continued Spec­ ific NonObservation WM - ber Location Depth Nat, concar- (township Date of temp,- ductHard- bonate and of well atur, ance ness hardpH range) sample (ft) (PC) (umbos) (Ca,MR) ncss (units) Dissolved solids Cal­ cium (Ca) Megnesium (Mg) Po­ tasSodium slum (Na) (K) Bicar­ bonate (41:03) Sulfate (SO4) Chlo­ ride (Cl) Fluoride (F) 46N25W36D5 07-09-70 144 lo 46N25W36D5 07-17-69 144 46N25W36D5 08-19-68 144 46N25W36D5 07-10-67 144 8.S 46N25W36D6 07-26-66 46N25W36D6 07-19-65 46N26W12D 46N26W31C 46N27W17D 46N27W19D 07-08-64 111 46N27W31C 46N28W01B 46N28W08A 46N28W12C 46N28W15D 46N28W27D 46N28W32 46N29W18DB* 04-07-66 SO 46N29W18DB* 02-08-73 29.0 13.0 46N29W19-1 04-07-66 26.0 11.0 ,2 46N29W19-1 02-08-73 26.0 12.0 46N29W19-4 02-08-73 31.0 13.0 46N29W22A 46N29W36 47N24W28C 07-08-64 112 47N25W12C 07-08-64 102 7.S 47N2SW1SC 09-06-63 245 47N25W19C 07-09-64 137 48.0 14.0 47N2SW19CC 09-27-67 47N25W20C 07-25-63 103 47N25W21C 07-16-64 160 47N25W22A 08-28-63 140 41.0 11,0 47N25W27C 47N25W328 07-24-63 122 47N26W24A 47N26W24A 47N26W25A1 07-24-63 43.0 13.0 47N26W25C SO 47N26W25D 07-09-64 122 40.0 11.0 47N26W26D 47N26W368 0S-28-64 6,5 1(19 47N26W368BD 07-18-77 47N26W36B80 11-03-76 47N26W3611BD 06-01-76 IS)) 47N26W36C1 05-28-64 47N26W36C2 07-09-64 125 47N27W08118 06-14-71 44.0 16.0 47N27W09 11-30-73 105 1SS 44.0 11.0 47N28W03C 47N28W03CCD 07-20-77 (1 47N28W03CC0 11-04-76 7.S 47N28W03CCD 06-01-76 IRS 47N28W03CCD 09-23-7S 47N28W08B

Table 18.--Chemical characteristics of water from glacial deposits (analyses by U.S. Geological Survey except for those indicated by asterisk which were analyzed by Michigan Department of Public Health; results in milligrams per liter except as indicated) - continued Spec­ ific NonObserLocation Depth Water concarDisMegPovation (township Date of temperductHard- bonate solCalnetasBicarSulChloFluonum - and of well ature ance ness hardpH ved cium sium Sodium sium bonate fate ride ride ber range) sample (ft) (°C) (umhos) (Ca,Mg) ness (units) solids (Ca) (Mg) (Na) (K) (11003) (SOS ) (CO (F) 47N28W12CA 11-12-70 -- 47N28W15A 47N28W28C 47N28W35C 47N29W02A :0 47N29W02D0A 07-20-77 47N29W02111 09-27-67 47N29W03D 80:0 47N29W31D 02-23-66 110 47N29W34C 47N29W34C 47N29W36D 48N26W23ACA 10-16-70 48N26W25C 48N26W35C 48N28W308 48N29W19C 07-08-64 127 48N29W26

48N29W26 Mean R2 Minimum Maximus 105.0 22.0 Number of samples

Table 19.--iron, manganese, silica, and nitrate in water from glacial deposits (analyses by U.S. Geological Survey except for those indi­ cated by asterisk which were analyzed by Cleveland-Cliffs Iron Com­ pany; results in micrograms per liter except as indicated) DisDisTotal solved Total Total ObserDate Total solved mangan- man- silica nitrate vation of iron iron ese ganese (Si02) (NO3) number Location sample (Fe) (Fe) (mg/L) (mg/L) 45N24W2ODBB 45N2SWO1BCA 45N25W02BBB 45N25W11BC 09-06-63 1600 45N25W23AC 45N25W25ABB 45N25W28AB1 45N25W28AB2 45N26WO3DA 45N26W15 4 5N28W11ABC 45N28W11ADA 46N25N36-6 46N25N36-6 46N25N36-6 46N25N36-1 46N25N36-3 46N25N36-4 ff)0 46N25N36­5 46N25N36B1 07-29-68 4200 46N25N36B1 07-10-67 1500 46N25N36B1 07-26-66 1000 46N25N36B1 46N25N36B1 46N25W09B 07-24-63 3000 46N25W11C 46N25W16D 46N25W36-2 07-19-65 1900 46N25W36-2 46N25W36-7 46N25W36-7 46N25W36BB 07-10-67 2300 46N25W36BB 46N25W36BB 46N25W36B3 07-26-66 1100 46N25W36B3 46N25W36B3 46N25W36B6 46N25W36B6 46N25W36D4 46N25W36D4 46N25W36D4 46N25W36D4 46N25W36D4 4 6N2 5W36D4 46N25W36D4 46N25W36D4 07-26-66 1300 46N25W36D4 46N25W36D5 46N25W36D5

Table 19.--Iron, manganese, silica, and nitrate in water from glacial deposits (analyses by U.S. Geological Survey except for those indi­ cated by asterisk which were analyzed by Cleveland-Cliffs Iron Com­ pany; results in micrograms per liter except as indicated) - continued DisDisTotal solved Total Total ObserDate Total solved manganmansilica nitrate vation of iron iron ese ganese (Si02) (NO3) number Location sample (Fe) (Fe) (Nh) (Nh) (mg/L) (mg/L) 46N25W36D5 46N25W36D5 46N25W36D5 46N25W36D5 46N25W36D5 46N25W361)6 46N25W36D6 46N25W31C 46N27W17D 46N27W31C 46N28W01B 46N28W08A 46N28W12C 46N28W32 46N29W18DB 46N29W18DB 46N29W19-1 46N29W19-1 46N29W19-4 46N29W22A 46N29W36 47N25W15C 47N25W19CC 09-27-67 1000 47N25W20F 07-25-63 8100 47N25W21C 47N25W22A 47N25W328 47N26N36BB1)B* 07-19-76 2800 47N26N3688DB* 08-11-76 2900 47N26N36BBDB* 09-13-76 3000 47N26W24A 47N26W24A 47N26W25A1 47N26W36B 47N26W36BBDB 07-18-77 3100 47N26W36BBDB 11-03-76 5800 47N26W36BBDB 06-01-76 3800 47N26W36BBDB* 12-28-77 2800 47N26W36BBDB* 11-29-77 3400 47N26W36BBDB* 10-27-77 3400 47N26W36BBDB* 08-02-77 3400 47N26W36BBDB* 07-18-77 4600 47N26W36BBDB* 06-17-77 3200 47N26W36BBDB* 12-16-76 3100 47N26W36BBDB* 02-04-76 2200 47N26W36BRDB* 04-23-76 2600 47N26W36BBDB* 06-01-76 2900 47N26W36BBDB* 06-18-75 3300 47N27W08BB 47N27W09

Table 19.--Iron, manganese, silica, and nitrate in water from glacial deposits (analyses by U.S. Geological Survey except for those indi­ cated by asterisk which were analyzed by Cleveland-Cliffs Iron Com­ pany; results in micrograms per liter except as indicated) - continued DisDisTotal solved Total Total ObserDate Total solved manganmansilica nitrate vation number Location of sample iron (Fe) iron (Fe) ese (Mh) ganese (Mn) (Si02) (mg/L) (NO3) (mg/L) 47N28W03C 10-17-62 5600 47N28W03CCDC 07-20-77 26000 47N28W03CCDC 11-04-76 4600 47N28W03CCDC 06-01-76 8100 47N28W03CCDC 09-23-75 6300 47N28W12CA 47N28W28C 47N29W02A 47N29W02DDA 07-20-77 7200 47N29W02DA 09-27-67 4700 47N29W03D 47N29W31D 02-23-66 2600 47N29W34C 47N29W34C 47N29W36D 48N26W23ACA 48N26W25C 48N28W30B 48N29W26 48N29W26 Mean Minimum Maximum Number of samples SO U S. GOVERNMENT PRINTING OFFICE: 1980 653-052/109