CONTACTóSolid where accurately located; dashed where gradational or approximately located; 

dotted where concealed 

FLUVIAL TERRACE SCARPóCut by channel erosion; symbol drawn at base of scarp, hachures 

on upslope side

FLOOD PLAIN MORPHOLOGIC FEATURESóLines show local scarps of very low relief that 

bound old channels, point bar deposits, or areas of level to rolling topography on St. Joseph and 

Paw Paw River flood plains

CREST OF EOLIAN DUNEóLine symbol drawn on crest of dune ridge 

EOLIAN SEDIMENT TRANSPORT DIRECTIONóDetermined from dune forms

SHORELINE BLUFFóCut by wave and slope erosion; line symbol drawn at base of scarp; 

hachures on upslope side

MELTWATER SEDIMENT TRANSPORT DIRECTIONóFlow direction of glacial meltwater 

stream or lake current, determined from crossbedding or ripple crosslaminations; observation at tip 

of arrow

FLOW DIRECTION OF GLACIAL STREAMóGeneralized flow direction of glacial meltwater 

stream inferred from slope of depositional surface of deposits

CONTOURS ON DEPOSITIONAL SURFACE OF GLACIOFLUVIAL DEPOSITSóContours 

show elevations of reconstructed surface of glaciofluvial deposits; contours drawn on downstream 

maximum extents of present topographic contours, extrapolated in areas of collapse deformation 

or erosion; contour interval 10 feet

DELTA FORESET SLOPE DIRECTIONóSediment transport direction of delta foreset strata, 

measured from dip direction of foreset strata; observation at tip of arrow

GLACIAL LAKE SPILLWAY CHANNELóChannel cut in meltwater deposits; letter symbol 

identifies glacial lake; flow direction of water shown by arrow; number is estimated altitude of 

channel floor, in feet

GRAIN SIZE OF SURFACE MELTWATER DEPOSITS AND LAKE BOTTOM 

DEPOSITSóPattern shows generalized grain size of surface deposit

Coarse gravel, chiefly cobble to boulder gravel, some beds of sand and flow till

Sand and gravel, chiefly pebble to cobble gravel and beds of sand

Sand, fine to coarse, few beds of granular pebbly sand and silt-clay

Very fine sand, silt, and clay, variable proportions

CREST OF MORAINE RIDGEóLine symbol drawn on crest of ridge

RETREATAL POSITION OF STAGNANT ICE MARGINóDetermined from ice-contact slope 

at head of associated meltwater deposit; identified by unit symbol

RETREATAL POSITION OF STAGNANT ICE MARGINóApproximately located in areas of 

eroded, collapsed, or concealed head of associated meltwater deposit; identified by unit symbol

Qc

Qccj

Qed

Qsm

Qal

af

Qaf

Qst

Qmb

Qcl

Qccp

Qikp

Qoko

DESCRIPTION OF MAP UNITS

 Map units include unconsolidated and locally cemented Quaternary surficial materials, >1 m 

(3.2 ft) thick. Sediment types and gravel-clast rock types, described below, are listed in 

decreasing order of abundance; color designations, in parentheses (Munsell, Inc., 2000), are based 

on naturally moist samples. A veneer of eolian silt, mixed with small amounts of fine sand, clay, 

and scattered gravel particles, ranging in thickness from a few centimeters to 3 m (10 ft) covers 

upland hills and plains; this veneer is not mapped. A discontinuous veneer of eolian fine sand, < 1 

to 3 m (<3.2 to 10 ft) thick, is present locally, but is not mapped. Sandy colluvium, <1 m (3.2 ft) 

thick, covers most erosional slopes and is not mapped. Soil descriptions are modified from Larson 

(1980). Subdivision of Quaternary time is based on Richmond and Fullerton (1986).

HOLOCENE

ARTIFICIAL FILL (late Holocene)—Earth and manmade materials that have been artificially 

emplaced, including gravel, sand, silt, clay, compacted select earth materials, garbage, trash, and 

bulky waste. Thickness 1.8-15 m (6-50 ft). Fill is not shown where it is < 2.0 m (6 ft) thick in 

urban areas, and beneath most highway and railroad beds 

LAKE MICHIGAN BEACH AND NEARSHORE DEPOSITS (late Holocene)—Very pale brown 

(10YR 7-8/4) to light gray (10YR 7/2) fine to very coarse sand with minor gravel, moderately 

sorted; local cobble gravel with fine to coarse sand matrix; deposited on modern beaches, and in 

offshore bars and shallow offshore areas; 1-6 m thick; thins and becomes patchy offshore

ACTIVE EOLIAN DUNE SAND (late Holocene)—Very pale brown (10YR 7-8/4) to light gray 

(10YR 7/2) fine to medium sand, massive or in planar or concave crossbeds in planar-tabular sets; 

in active coastal dunes

LAKE MICHIGAN LAKE-BOTTOM DEPOSITS (late Holocene)—Light gray to gray (10YR 

7/2) to gray (10YR 6/1) silt and muddy sand (unit Qml), nonplastic or loose, containing variable 

trace amounts of organic materials; gray fine to very sand (unit Qms), loose; deposited in shallow 

offshore areas; thickens and becomes finer offshore

ALLUVIUM (early to late Holocene)—Grayish brown (10YR 5/2) to pale brown (10YR 6/3) 

sand, gravel, silt, minor clay, and some organic material, deposited by modern streams; in flood 

plains of major rivers alluvium consists of poorly sorted gravel and sand at the base, overlain by 

laminated and thinly bedded sand, silt, and clay; thickness 1.8-9.1 m (6-30 ft); in lower St. Joseph 

River flood plain, unit is >24 m (>80 ft) thick; along smaller streams alluvium is composed of 

poorly sorted sand and gravel derived from adjacent glacial, meltwater, and colluvial materials; 

thickness generally <4 m (13 ft)

ALLUVIAL FAN DEPOSITS (early to middle Holocene)—Very pale brown (10 YR 7-8/4) sand, 

gravel, silt, minor clay, and some organic material, deposited at the mouths of modern streams on 

flood-plain alluvium

HOLOCENE AND LATE WISCONSIN

STREAM TERRACE DEPOSITS (late Wisconsin to middle Holocene)—Very pale brown (10 YR 

7-8/4) to yellow (10 YR 7/6) sand, pebble gravel, minor silt; deposited by streams graded to fluvial 

base levels higher than modern levels or by streams with higher discharge regimes

BEACH DEPOSITS (late Wisconsin to middle Holocene)—Brown to very pale brown (10YR5/3-

7/4) fine to very coarse sand with minor gravel, locally cobble gravel with fine to coarse sand 

matrix in beaches, spits, and bars related to glacial and postglacial lake stages in the Michigan 

basin; unit includes deposits of the Glenwood stage of glacial Lake Chicago (unit Qbcg); Calumet 

stage of glacial Lake Chicago (unit Qbcc); Lake Nipissing stage (unit Qbn)

EOLIAN DUNE SAND DEPOSITS (late Wisconsin to middle Holocene)—Very pale brown (10 

YR 7-8/4) to yellow (10 YR 7/6) fine to medium sand, massive or in planar or concave crossbeds 

in planar-tabular sets; in inland dunes and in dunes related to glacial and postglacial lake stages in 

the Lake Michigan basin; unit includes deposits related to Glenwood and Calumet stages of glacial 

Lake Chicago; Tolston stage, Lake Algoma stage, Lake Nipissing stage

EOLIAN SAND SHEET DEPOSITS (late Wisconsin to middle Holocene)—Very pale brown (10 

YR 7-8/4) to yellow (10 YR 7/6) fine to medium sand, massive, commonly 2-3 m thick

SWAMP AND MARSH DEPOSITS (late Wisconsin to late Holocene)—Black to dark reddish 

brown (5 YR 2.5/1 to 3/3) to gray (10 YR 5-6/1) peat and muck interbedded with and overlying 

laminated silt, clay, and minor sand and gravel; peat is decomposed, fibrous or granular, woody or 

herbaceous; muck is organic, clayey or sandy silt; thickness, including basal silt and clay, 

generally less than 5.5 m (l8 ft) thick

COLLUVIUM DEPOSITS (late Wisconsin to middle Holocene)—Very pale brown (10 YR 7-8/4) 

to yellow (10 YR 7/6) silty sand or sandy silt deposits, consisting of a poorly sorted matrix of sand 

and silt containing 5-20 percent (by volume) pebbles; commonly massive to indistinctly layered; 

locally stratified

LATE WISCONSIN

Glacial Meltwater Deposits

Grayish brown to brown (10 YR 5/2-3) to dark yellowish brown (10 YR 4/4) sand and gravel, and 

light brownish gray (10 YR 6/2) to very pale brown to light yellowish brown (10 YR 7-6/4) 

gravelly sand, fine sand, and silty sand (fig. 1), stratified, poorly to moderately sorted, generally 

calcareous, and light brownish gray (10 YR 6/2) silt and gray (5 Y 5/1) clay, stratified, moderately 

sorted. Gravel composition is polymict, composed of granitic gneiss, sandstone, quartzite, 

conglomerate, carbonate, shale; gravel clasts are subrounded to well rounded, generally 

nonweathered, some coarse gravel clasts are striated. Sand composition is highly variable from 

lithic coarse sand to sublithic fine sand; grains generally are nonweathered. The stratified deposits 

were deposited by glacial meltwater, and are divided into two groups of map units based on their 

sedimentary facies. Deposits of glacial-stream units contain three sedimentary facies, consisting 

of coarse to fine gravel, and sand. Deposits of glacial-lake units contain ice-channel, deltaic, and 

lake-bottom deposits. Ice Channel deposits contain coarse gravel, commonly interbedded flowtill 

deposits, and interbedded sand and gravel in the subsurface. Deltaic deposits consist of sand and 

gravel facies in delta topset sediments, sand and gravel to fine sand delta foreset facies, and fine 

sand to silty sand delta bottomset facies in the subsurface. Sand and gravel glaciolacustrine fan 

facies locally underlies some deltaic deposits. Fine sand and silt-clay lake-bottom facies underlies 

distal delta deposits and lake-bottom plains.

 Stratified meltwater deposits are subdivided into map units on the basis of the distribution, 

stratigraphic relationships, and altitudes of sedimentary facies in different depositional basins that 

were present at the melting margin of the ice sheet. Map units show the extent of sediments in 

each glacial-stream deposit or sediments deposited in or graded to each glacial lake. Each map 

unit contains one or more ice-marginal or near-ice-marginal meltwater deposits, known as 

morphosequences (Koteff and Pessl, 1981). Each morphosequence typically consists of a 

progression of landforms and sedimentary facies, grading from ice-contact landforms underlain by 

coarse-grained facies at the head of the deposit to depositional, noncollapsed landforms underlain 

by finer grained facies in distal parts of the deposit. The heads of ice-marginal deposits are coarse 

grained, locally containing boulders and lenses of poorly sorted flowtill sediments, and they 

characteristically have a zone of collapsed and deformed bedding along ice-contact slopes. 

Glaciofluvial deposits at the surface of each morphosequence are graded to a specific base level, 

which was controlled by the altitudes of various glacial lakes that covered parts of Berrien County.

 Soils associated with upland glacial meltwater deposits generally are alfisols developed either 

entirely in overlying eolian sandy silt deposits, or in sandy silt that overlies sand and gravel 

deposits in the soil C horizon. On slopes and meltwater terrace deposits the alfisols are in sandy 

silt overlying sand and gravel. The alfisols have well developed argillic B horizons, 0.2->1.5 m 

(25->60 in) thick, overlying C horizons in lightly oxidized, calcareous sand and gravel sediments. 

Soils associated with lake bottom-deposits are mollisols commonly developed in eolian silty sand 

deposits that overlie fine sand, silt and clay deposits in the soil C horizon. Mollisols have gleyed 

argillic B horizons, 0.2-0.6 m (10-26 in) thick, overlying nonoxidized sand, silt, or clay sediments.

Glacial-Stream Deposits—Interbedded sand and gravel, moderately to poorly sorted, horizontally 

stratified. Deposits grade downstream from 1) coarse gravel facies in ice-proximal heads of units, 

to 2) sand and gravel facies, to 3) pebbly coarse sand facies in distal parts of some units. The 

coarse gravel facies consists of massive cobble gravel beds that have a poorly sorted sand matrix; 

beds of small boulders are common. Coarse gravel beds generally are less than 1 m (3.2 ft) thick; 

beds composed of finer grained sediment are rare. The sand and gravel facies is most prevalent; it 

consists of pebble and cobble gravel beds interbedded with beds of medium-to-coarse sand. 

Cobble gravel beds are massive or planar bedded, poorly to moderately sorted, and have local 

imbrication of clasts; pebble or cobble gravel beds also contain planar/tabular and trough 

crossbeds. Gravel beds are 0.2-1.2 m (0.7-5 ft) thick. Sand beds are chiefly coarse sand with 

pebbles and granules, poorly sorted, in trough and planar/tabular crossbeds. Medium- and finesand ripple cross-laminated beds are minor constituents. The pebbly coarse sand facies consists 

chiefly of coarse sand with pebbles in trough and planar/tabular cross-beds, and in planar beds. 

Thin beds of pebble gravel are minor constituents. 

 Map units containing only glacial-stream deposits in Berrien County originated as valley-train 

outwash deposits, which are preserved in valleys as eroded terrace deposits that extend to icemarginal heads of outwash east of the County. The valley-train terrace deposits have smooth 

downstream surface profiles, and the deposits overlie older glacial-lake deposits.

PAW PAW MELTWATER TERRACE DEPOSITS (late Wisconsin)—Grayish brown to dark 

yellowish brown, very pale brown to light yellowish brown pebble gravel and sand grading 

downstream to coarse sand; surface altitudes of terrace slope from 201 m to 190 m (660 ft to 625 

ft); relict braid channels engrave the surface; 3.7-12.1 m (12-40 ft) thick; graded to the Calumet 

stage of glacial Lake Chicago

ST. JOSEPH MELTWATER TERRACE DEPOSITS (late Wisconsin)—Grayish brown to dark 

yellowish brown, very pale brown to light yellowish brown pebble-cobble gravel and sand grading 

downstream to coarse sand; surface altitudes of terrace slope from 204 m to 190 m (670 ft to 625 

ft); relict braid channels locally engrave the surface; 3.7-12.1 m (12-40 ft) thick; graded to the 

Calumet stage of glacial Lake Chicago

ST. JOSEPH-KANKAKEE MELTWATER TERRACE DEPOSITS (late Wisconsin)—Grayish 

brown to dark yellowish brown, very pale brown to light yellowish brown pebble-cobble gravel 

and sand grading downstream to coarse sand; surface altitudes of terrace segments slope from 730 

ft to 720 ft; locally collapsed; 3.7-9.1 m (12-30 ft) thick; graded to outwash alluvial surfaces in the 

Kankakee River valley 

Glacial-Lake Deposits—Sand, sand and gravel, and silty sand in deltaic, ice-channel, and 

glaciolacustrine fan deposits, and fine sand, silt, and clay in lake-bottom deposits. Deltaic deposits 

have glacial-stream topset beds, 0.6-18.3 m (2-60 ft) thick, composed of coarse gravel, sand and 

gravel (overprint patterns), and pebbly sand facies, which overlie deltaic foreset and bottomset 

facies. Foreset facies include: 1) sand and gravel foreset facies, consisting of gravel, pebbly sand, 

and coarse sand, poorly to moderately sorted, in 2-10 m (6.5-33 ft) thick sets of thin foreset beds 

which dip 25-35o; 2) sandy foreset facies, consisting of fine to medium sand, moderately sorted, in 

interbedded parallel-laminated and ripple cross-laminated sets of beds that are 2-5.2 m (6.5-16 ft) 

thick and that dip less than 25o; draped laminations of silt and clay are common in lower beds. 

Delta bottomset facies are: 1) sand and gravel bottomset facies, consisting of coarse pebbly sand in 

planar/tabular crossbeds and parallel-bedded fine sand, silt and clay, in sets of beds that dip less 

than 5o; 2) sandy bottomset facies, consisting of fine sand, silt, and minor clay, in ripple crosslaminated and parallel-laminated beds that dip less than 5o. Total thickness of deltaic sediments is 

6-45.2 m (20-150 ft). Ice-marginal deltas in Berrien County contain sand and gravel and sandy 

foresets, including beds of silty flowtill, and thick sandy bottomset facies. Glaciolacustrine fans 

contain sand and gravel and sandy foreset and bottomset facies, and minor till, flowtill, and finegrained lake-bottom sediments; fans underlie some deltaic deposits. Lake-bottom deposits 

(overprint pattern) contain two facies: 1) sandy facies, consisting of fine sand to silt in parallel 

laminated and minor ripple cross-laminated sets of beds; 2) silt-clay facies, consisting of silt-tovery fine sand, and clay in parallel laminations, microlaminations, and minor ripple crosslaminations; deposits with laminations of variable thickness have clay laminae <2 mm thick; varve 

deposits of this facies consist of couplets of microlaminated silt-to-very fine sand, and massive or 

graded clay; couplets are 0.4-10 cm (0.1-4.0 in) thick; vertical sequences of varves show little 

variation in couplet thickness.

LAKE-BOTTOM DEPOSITS, GLACIAL LAKE CHICAGO, GLENWOOD STAGE (late 

Wisconsin)—Pale brown fine sand at the surface locally, moderately sorted, laminated, and gray 

silt and clay, laminated; surface of lake-bottom plain 189 m (620 ft) altitude; 1-9.1 m (3-30 ft) 

thick; deposited in shallow water, nearshore lake environments

DEPOSITS OF GLACIAL LAKE BARODA (late Wisconsin)—Lake-bottom deposits consisting 

of fine sand, silt, and clay; littoral deposits composed of pebble gravel and sand, and ice-marginal 

glaciodeltaic deposits consisting of sand and gravel topset beds overlying gravel and sandy foreset 

beds; reportedly totaling as much as 21.3 m (70 ft) thick. The dam for this large ice-marginal lake 

was older deltaic deposits of glacial Lake Dowagiac and other deposits of the Valparaiso morainic 

system in northern Indiana. The lake extended northward and westward as the ice margin 

retreated. Units include deposits related to lowering stages of the lake, which were controlled by 

lake spillway channels cut in older deposits in Indiana and Illinois at altitudes descending from 

about 225 m to 201 m (720 ft to 660 ft). Lake Baroda lowered to the Glenwood stage of glacial 

Lake Chicago following retreat of the ice margin from northern Indiana. Deposits of glacial Lake 

Baroda are correlated with the Lake Border morainic system (Leverett, 1908, Leverett and Taylor, 

1915, Lineback and others, 1983, Farrand, 1985).

LAKE-BOTTOM DEPOSITS, GLACIAL LAKE BARODA (late Wisconsin)—Pale brown fine 

sand at the surface locally, moderately sorted, laminated, and gray silt and clay, laminated; surface 

of lake bottom plains 207 m to 201 m (680 ft to 660 ft) altitude; 1-9.1 m (3-30 ft) thick; deposited 

in shallow water, nearshore lake environments 

LITTORAL DEPOSITS, GLACIAL LAKE BARODA (late Wisconsin)—Pale brown fine to very 

coarse sand, pebble gravel, and minor silt and clay; coarse-grained deposits are moderately sorted, 

planar bedded and cross-bedded; fine-grained deposits are laminated; surface of beach berms 216 

m to 201 m (710 ft to 660 ft) altitude; 1-6 m (3-20 ft) thick; deposited in beaches, locally below 

shoreline cliffs, and in offshore bars and deltas in shoreline lake environments 

LA BOYER ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Sand and gravel grading 

to pebble gravel and coarse sand, overlying sand, silt, and clay in subsurface; deposits include 

glaciotectonic thrust faults and recumbent folds in transverse ridge that is as high as 232 m (760 ft) 

at head of deposit; surface altitudes of glaciofluvial plain slope from 222 m to 213 m (730 ft to 

700 ft)

DEPOSITS OF GLACIAL LAKE DOWAGIAC (late Wisconsin)—Ice-marginal and near-icemarginal glaciodeltaic deposits consisting of sand and gravel topset beds overlying dipping gravel 

and sandy foreset beds and thick sandy and silty bottomset and lake-bottom beds. The dam for 

this large ice-marginal lake was older deposits of the inner Kalamazoo moraine on the southeast 

side of the basin, including Portage Prairie deposits (unit Qikp). The lake expanded northward and 

westward as the ice margin retreated; the open water of the lake extended through successively 

collapsed deposits to the lake spillway, which was a channel cut in deposits (unit Qikp) at about 

225 m (740 ft) altitude. Lake Dowagiac lowered to the high level of glacial Lake Baroda 

following retreat of the ice margin from the western limit of the lake. Units include surface sandy 

lake-bottom deposits of glacial Lake Dowagiac of Leverett (1908). Deposits of glacial Lake 

Dowagiac are correlated with the Valparaiso morainic system (Leverett, 1908, Leverett and 

Taylor, 1915, Lineback and others, 1983, Farrand, 1985).

BAINBRIDGE ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include nine small ice-marginal deltas; surface altitudes of glaciofluvial plains 

slope from 244 m to 224 m (800 ft to 735 ft); deltaic deposits overlie silty lake-bottom deposits 

(unit Qdl). The local depositional basin extended along the ice margin from Pipestone Creek area 

to 2 km southwest of Coloma

BIASTOCK ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include two large ice-marginal deltas; surface altitudes of glaciofluvial plains 

slope from 244 m to 232 m (800 ft to 760 ft); deltaic deposits overlie sandy lake-bottom deposits 

in the subsurface, and grade down delta frontal slopes to lake-bottom plains (unit Qdl). The local 

depositional basin extended along the ice margin from Pipestone Creek area to Bainbridge Center

SHANGHAI ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include one large and one small ice-marginal delta; surface altitudes of 

glaciofluvial plains slope from 232 m to 224 m (760 ft to 735 ft); deltaic deposits overlie sandy 

lake-bottom deposits in the subsurface. The local depositional basin extended along the ice 

margin from 2 km north of Berrien Springs to west of Shanghai Corners

ORONOKO ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include four large ice-marginal deltas; surface altitudes of glaciofluvial plains 

slope from 238 m or 232 m to 224 m (780 or 760 ft to 735 ft); deltaic deposits overlie sandy lakebottom deposits in the subsurface. The local depositional basin extended along the ice margin 

from 3 km southwest of Berrien Springs to 1 km north of Hess Lake

PIPESTONE ICE-CHANNEL AND ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)— 

Multiple deposits undifferentiated but include deposits of five ice channels or ice-marginal deltas; 

surface altitudes of glaciofluvial plains slope from 232 m to 225 m (760 ft to 740 ft). The local 

depositional basins developed in large melted holes along the edge of the the ice margin in Sodus 

and Pipestone Townships; collapsed margins of deposits are overlain by more distal deposits of 

unit Qds 

BERRIEN ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—One large ice-marginal 

delta; surface altitudes of glaciofluvial plain slope from 247 m to 235 m (810 to 770 ft); deltaic 

deposits overlie sand, silt, and clay lake-bottom deposits in the subsurface. The local depositional 

basin extended from Little Indian Lake to Berrien Springs. 

RANGE LINE ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—One large icemarginal delta; surface altitudes of glaciofluvial plain slope from 238 m or 232 m to 224 m (795 ft 

to 750 ft); flowtill deposits exposed in northwestern part of ice-contact head; deltaic deposits 

overlie sand, silt, and clay lake-bottom deposits, and probable collapsed coarse ice-channel 

deposits in the subsurface. The local depositional basin extended from 3 km east of Buchanan to 1 

km south of Pennellwood

LAKE-BOTTOM DEPOSITS, GLACIAL LAKE DOWAGIAC (late Wisconsin)—Pale brown 

fine sand at the surface locally, moderately sorted, laminated, and gray silt and clay, laminated; 

surface of lake bottom plains 219 m to 210 m (720 ft to 690 ft) altitude; 1->15.2 m (3->50 ft) 

thick; deposited in deep to shallow ice-marginal lake environments 

ICE-MARGINAL DELTAIC DEPOSITS, GLACIAL LAKE DOWAGIAC, 

UNDIFFERENTIATED (late Wisconsin)—Multiple deposits undifferentiated but include deposits 

of at least eight small ice-marginal deltas and two large near-ice-marginal deltas; surface altitudes 

of glaciofluvial plains slope from 250 m to 229 m (820 ft to 750 ft). Deltaic deposits are highly 

collapsed, and overlie sandy lake-bottom deposits in the subsurface. Two local depositional 

basins developed along the edge of the the ice margin: one basin extended from southwest to 

northeast of Galien, the other expanded from Clarks Lake northward 6 km. A third depositional 

basin formed as ice melted away from the ice-contact heads of units Qikp and Qoko; two large 

near-ice-marginal deltas prograded into this arm of Lake Dowagiac, which spilled over the 

regional drainage divide along the Indiana Toll Highway at altitude of about 226 m (742 ft)

FAIRLAND ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include at least two large ice-marginal deltas; surface altitudes of glaciofluvial 

plains slope from 244 m to 229 m (800 ft to 750 ft); deltaic deposits overlie sand, silt, and clay 

lake-bottom deposits in the subsurface. The local depositional basin extended from Niles to the 

the ice margin from Little Indian Lake to 1 km north of Smith Lake

CARMODY ICE MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include at least two large ice-marginal deltas and ice-channel deposits; surface 

altitudes of glaciofluvial plains slope from 247 m to 232 m (810 ft to 760 ft); deltaic deposits 

overlie sandy lake-bottom deposits in the subsurface. The dam for this local ice-marginal lake was 

older deposits of the inner Kalamazoo moraine on the southeast side of the basin. The local 

depositional basin developed within a large melted reentrant in the ice margin that extended from 

2 km south of Coloma to Bainbridge Center and eastward to the lake dam in Cass County. This 

local lake lowered to the level of Lake Dowagiac following ice margin recession from western 

Cass County.

EAU CLAIRE ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include at least one large and three small ice-marginal deltas and ice-channel 

deposits; surface altitudes of glaciofluvial plains slope from 244 m or 238 m to 232 m (800 ft or 

780 ft to 760 ft); deltaic deposits overlie sandy lake-bottom deposits in the subsurface. The dam 

for this local ice-marginal lake was older deltaic deposits of units Qdb, Qf, and Qikk on the 

southeast side of the basin. The local depositional basin developed along the ice margin from 

Berrien Springs and Eau Claire to 3 km east of Naomi. This local lake lowered to the level of 

Lake Dowagiac following ice margin recession from the ice-contact head of the deposit

DEPOSITS OF GLACIAL LAKE MADRON (late Wisconsin)—Ice-marginal glaciodeltaic 

deposits consisting of sand and gravel topset beds overlying dipping gravel and sandy foreset beds 

and thick sandy and silty bottomset and lake-bottom beds. The dam for this ice-marginal lake was 

older deltaic deposits of units Qikp and other deposits in northern Indiana and Cass County. The 

spillways for this lake was a channel cut in Qikp deposits 2.5 km southeast of Buchanan, and 

channels cut in older deposits in norther Indiana. The lake expanded northward and westward as 

the ice margin retreated; the open water of the lake extended through successively collapsed 

deposits to the lake spillways. Lake Madron lowered to the level of glacial Lake Dowagiac 

following retreat of the ice margin from the western limit of the lake. Deposits of glacial Lake 

Madron are correlated with the Valparaiso morainic system (Leverett, 1908, Leverett and Taylor, 

1915, Lineback and others, 1983, Farrand, 1985).

ICE-MARGINAL DELTAIC DEPOSITS, GLACIAL LAKE MADRON,UNDIFFERENTIATED 

(late Wisconsin)—Multiple deposits undifferentiated but include at least seven small ice-marginal 

deltas; surface altitudes of glaciofluvial plains slope from 244 m to 241 m (800 ft to 790 ft) in the 

northern basin, and from 238 m to 232 m (780 ft to 760 ft) in the southern basin; deltaic deposits 

overlie sandy lake-bottom deposits in the subsurface. Two local depositional basins developed 

along the edge of the the ice margin: one basin extended from southern Three Oaks Township to 

Pine lake, the other expanded from Clear Lake to Boyle Lake

RED BUD ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include three small ice-marginal deltas; surface altitudes of glaciofluvial 

plains slope from 244 m to 241 m (800 ft to 790 ft); deltaic deposits overlie sand, silt, and clay 

lake-bottom deposits in the subsurface. The local depositional basin extended along the ice 

margin from Weaver Lake to 1 km north of Madron Lake

LAKE-BOTTOM DEPOSITS, GLACIAL LAKE MADRON (late Wisconsin)—Pale brown fine 

sand at the surface locally, moderately sorted, laminated, and gray silt and clay, laminated; surface 

of lake bottom plains 219 m to 210 m (720 ft to 690 ft) altitude; 1->15.2 m (3->50 ft) thick; 

deposited in deep to shallow ice-marginal lake environments 

KEELER ICE CHANNEL AND ICE MARGINAL DELTAIC DEPOSITS (late Wisconsin)— 

Multiple deposits undifferentiated but include three small ice-marginal deltas and ice-channel 

deposits; surface altitudes of glaciofluvial plains slope from 271 m or 265 m to 256 m (890 ft or 

870 ft to 840 ft); includes ice-channel deposits as high as 259-256 m (850-840 ft) altitude inferred 

to be ongrade to delta glaciofluvial plains that slope to 241 m (790 ft) in Keeler Township in Cass 

County; deltaic deposits overlie sandy lake-bottom deposits in the subsurface. The dam for this 

local ice-marginal lake was older deltaic deposits of the inner Kalamazoo morainic system in Cass 

County. The local depositional basin extended from 2 km northwest of Brush Lake to melt 

channels in the ice margin north and northwest of Pipestone Lake. Keeler deposits are correlated 

with the inner Kalamazoo morainic system (Leverett and Taylor, 1915, Lineback and others, 1983, 

Farrand, 1985).

CUSHING ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Two small ice-marginal 

deltas; surface altitudes of glaciofluvial plains slope from 271 m or 265 m to 256 m (890 ft or 870 

ft to 840 ft). The dam for this local ice-marginal lake probably was stagnant glacial ice; the local 

depositional basin probably was a small melt hole near the edge of the ice margin. Cushing 

deposits are correlated with the inner Kalamazoo morainic system (Leverett and Taylor, 1915, 

Lineback and others, 1983, Farrand, 1985).

PORTAGE PRAIRIE ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—One large and 

two small ice-marginal deltas; surface altitudes of glaciofluvial plains slope from 262 m to 241 m 

(860 ft to 790 ft); deltaic deposits overlie sand, silt, and clay lake-bottom deposits in the 

subsurface. The dam for this local ice-marginal lake was older deltaic deposits of the inner 

Kalamazoo morainic system in northern Indiana. The local depositional basin extended from Cass 

County, Michigan, and northern St. Joseph County, Indiana, to Buchanan. This local lake drained 

following ice margin recession from the Kalamazoo morainic system and headward erosion of 

meltwater streams in the Kankakee River valley in northern Indiana. Portage Prairie deposits are 

correlated with the inner Kalamazoo morainic system (Leverett and Taylor, 1915, Lineback and 

others, 1983, Farrand, 1985).

OAK FOREST ICE-MARGINAL DELTAIC DEPOSITS (late Wisconsin)—Multiple deposits 

undifferentiated but include small ice-marginal deltas; maximum surface altitude of glaciofluvial 

deposits 283 m (930 ft); highly collapsed. The dam for this local ice-marginal lake probably was 

stagnant glacial ice; the local depositional basin probably was a large melt hole near the edge of 

the ice margin. Oak Forest deposits are correlated with the outer Kalamazoo morainic system 

(Leverett and Taylor, 1915, Lineback and others, 1983, Farrand, 1985).

Till and Moraine Ridge Deposits

Gray clayey silt sediment, consisting of a very poorly sorted matrix of silt, clay, and sand (fig. 1) 

containing commonly 1-10 percent (by volume) pebbles and few small cobbles, and very few 

scattered boulders; generally nonstratified, homogeneous, compact. Gravel clasts are subangular 

to subrounded; some have been glacially faceted and striated; most gravel clasts and sand grains 

are nonweathered; many gravel clasts have thin silt caps that adhere to their upper surfaces. 

Gravel composed of local shale bedrock constitutes 40-60 percent of clasts. Fine to coarse sand 

fraction contains conspicuous black, platy shale fragments. Till forms a compact, nonlayered 

sediment having subhorizontal fissility and subvertical joints, few thin lenses of sorted silt and fine 

sand, and gravel clasts with long-axis fabrics generally oriented in the direction of glacier flow. 

This till facies is subglacial till of lodgement or meltout origin. 

 The compact till is present in a smooth till-sheet deposit in wide lowland areas and in moraine 

ridges in the western part of Berrien County; thickness is 2->24 m (6->80 ft). Till generally 

overlies bedrock, known from offshore subcrops on the bottom of Lake Michigan, and is inferred 

to underlie stratified meltwater deposits in the eastern part of the County. Locally the gray silty till 

overlies or is interbedded with stratified sediments at the ice-contact heads of some meltwater 

deposits.

 Soils associated with till deposits generally are alfisols developed in silty sand that overlies 

compact till deposits in the soil C horizon, or in the compact till. The alfisols have well developed 

argillic B horizons 0.2-0.6 m (9-27 in) thick overlying C horizons in lightly oxidized, calcareous 

till deposits. 

CLAYEY SILT TILL DEPOSITS OF THE LAKE BORDER MORAINE (late Wisconsin)— 

Gray (5YR 5/1) to grayish brown (10YR 5/2) compact clayey silt till at the surface overlying 

stratified sand and silt, and minor gravel and clay. Till consists of clayey silt matrix with little 

sand, containing 5-10 percent pebbles and few small cobbles. Gravel clasts include shale, 

sandstone, limestone, dolomite, granite, gneiss, quartzite, and tillite. Gray till, 6 m (20 ft) thick, 

overlies glaciolacustrine fan deposits exposed in lake bluffs north of Benton Harbor; gray till > 26 

m (85 ft) thick underlies moraine ridges in the southwestern part of the County. Moraine ridges 

are 6-13 m (20-40 ft) high, with symmetric cross sections and curved but locally irregular crest 

traces; ridge crests commonly attain 207 m (680 ft) altitude, rising to 213 m (700 ft) in the 

northern part of the county; moraine ridges include the Covert Ridge of the Lake Border moraine 

of Leverett (1908). Offshore, the till is overlain by a gray medium to coarse sand and gravel, 

which is interpreted to be a surficial lag deposit derived from eroded till; the till is also overlain by 

thin, patchy, very fine to fine sand lake-bottom deposits and near shore sand deposits. Till was 

deposited subglacially, generally subaqueously in glacial Lake Baroda; deposits are correlated 

with the Saugatuck till of Larson and Monaghan (1982).

CLAYEY SILT TILL DEPOSITS OF THE VALPARAISO MORAINE (late Wisconsin)—Gray 

(5YR 5/1) to grayish brown (10YR 5/2) compact clayey silt till, consisting of clayey silt matrix 

with little sand, containing 5-15 percent pebbles and small cobbles. Gravel clasts include shale, 

sandstone, limestone, dolomite, granite, gneiss, quartzite, and tillite. Gray till, >14 m (45 ft) thick, 

is interbedded within stratified sediments of unit Qdo. Gray till, > 2 m (6 ft) thick, underlies 

sandy sediments of unit Qdr. Till was deposited subglacially, generally subaqueously in glacial 

Lake Dowagiac; deposits are correlated with the Saugatuck till of Larson and Monaghan (1982).

MISSISSIPPIAN

COLDWATER SHALE (Lower to middle Mississippian)

Qml

Qms

Mc

Qdr

Qdb

Qlt

Qivt

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Qec

Qcr

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Qds

Qdb

Qdo

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Qdps 

Figure 1.—Grain-size classification of meltwater stratified deposits and till deposits

Boulders Cobbles Pebbles Granules

Very

coarse

sand

Coarse

sand Mediumsand Finesand

Very

fine

sand Silt Clay

GRAVEL PARTICLES

Coarse gravel deposits

SAND PARTICLES FINE PARTICLES

Sand and gravel deposits

Sand deposits

Fine deposits

(ranges from 100 percent gravel particles to

75 percent gravel particles and 25 percent 

sand particles)

(ranges from 75 percent gravel particles and 

25 percent sand particles to 25 percent gravel 

particles and 75 percent sand particles)

(ranges from 25 percent gravel particles and 75 percent

sand particles through 100 percent sand particles to 50 

percent sand particles and 50 percent fine particles)

(ranges from 50 percent sand particles 

and 50 percent fine particles to 100 percent 

fine particles)

(contains nonsorted matrix, which is a mixture of sand and fine particles in differing proportions, 

and scattered gravel particles)

Till deposits

(nonsorted)

Meltwater 

stratified deposits

(sorted and layered)

Coarse deposits

(greater than

50 percent

sand and (or)

gravel particles)

Particle Diameter

Inches

Millimeters

10

256

2.5

64

.16

4

.08

2

.04

1

.02

.5

.01

.25

.005

.062

.0025

.062

.00015

.004

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EXPLANATION OF MAP SYMBOLS

785'

Qo

Correlation of Map Units

Alluvial Deposits Eolian

Deposits

 Glacial

Deposits

Ice Margin Recession

Slope

Deposits

Holocene

Late

Pleistocene QUATERNARY

Meltwater

 Deposits

 Swamp and

Marsh Deposits

 Beach 

Deposits

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Qst

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Ice Margin Recession and Readvance?

Ice Margin Recession

Inner Kalamazoo

Morainic System

Valparaiso

Morainic System 

Lake Border

Morainic System

Erosion and soil formation

Lake Bottom and

Nearshore Deposits

Qml

Mc

Bedrock

MISSISSIPPIAN

Multiple Glacial Advances

Profound Erosion

Qoko Outer Kalamazoo

Morainic System

Ice Margin Recession

Qikt

Deposits of

glacial Lake

Dowagiac

Deposits of 

glacial Lake

Baroda

Qdl

Qcl

Morainic System

Deposits of 

glacial Lake

Chicago

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Qdf

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Qec

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Qdb

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Qdrb

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Deposits of

glacial Lake

Madron

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Qmlb Qml

Qdl

EXPLANATION OF THE SURFICIAL GEOLOGIC MAP, MAP UNITS, 

AND ACCOMPANYING FIGURES

The surficial geologic map shows the distribution of surficial materials at land surface 

and in the shallow subsurface in Berrien County, southwestern Michigan. These materials overlie 

local carbonate bedrock and shale bedrock, which crops out only on the bottom of Lake Michigan 

west of the county. The geologic map differentiates surficial materials of late Quaternary age on 

the basis of lithologic characteristics, stratigraphic relationships, and age, as shown in the 

correlation diagram and described in the description of map units. Constructional geomorphic 

features composed of thick surficial deposits, such as moraine ridges and eolian sand dunes, are 

distinguished as map units and by map symbols. Ancillary figures provide additional information 

about particle-size classifications and materials classification and thickness (fig. 1), and the 

distribution of moraines and glacial ice lobes of the southern Lake Michigan region (fig. 2).

Surficial materials in Berrien County are mostly nonlithified deposits of glacial, 

meltwater, alluvial, colluvial, eolian, marsh and swamp, and lake estuarine origin. Carbonatemineral cement has lithified the meltwater deposits locally. Surficial materials are known also as 

unconsolidated soils, which include coarse-grained soils, fine-grained soils, or organic finegrained soils as described by engineering classifications. Surficial materials underlie and are the 

parent materials of modem pedogenic soils that have developed in them at the land surface. 

Materials in different map units are distinguished lithologically by grain size, mineralogy, and 

structure. Organic sediments in marsh and swamp, and lake estuarine deposits underlie modern 

wetland areas. Eolian deposits are shown as units where they are >l m thick. Eolian loess, a 

mixture of silt, clay, and fine sand, containing scatterd gravel clasts, overlies most glacial 

meltwater deposits in the upland areas. Loess varies in thickness from <1 m to >3 m locally; it is 

not shown on the map. Lake-bottom deposits underlie moderate to deep offshore areas in Lake 

Michigan. Alluvial deposits underlie modern flood plains and stream terraces, and are 

differentiated on the basis of weathering characteristics, stratigraphic relationships, and 

topographic position. Colluvial deposits are shown where they accumulated on hillslopes above 

erosional lake shoreline scarps. 

Deposits of glacial origin are subdivided on the basis of grain-size and sedimentary 

characteristics, origin, and age. Glacial deposits are related to the late Wisconsinan glacial episode 

of the Michigan ice lobe (Leverett, 1902, Lineback and others, 1983, Hansell and others, 1999). 

Till deposits consist of nonsorted sediments deposited from ice. Moraine ridges are laterally 

continuous bodies of thick glacial and meltwater deposits that cross the county in a northnortheasterly direction (Leverett and Taylor, 1915, Lineback and others, 1983, Farrand, 1985). 

End moraines are distinguished as groups of map units and are of two kinds: 1) moraines 

composed of glacial meltwater deposits, and 2) moraines composed chiefly of till at the surface. 

Meltwater deposits, which are sorted and stratified, are divided into two groups: glacial-lake and 

glacial-stream deposits. These meltwater deposits are further subdivided into map units on the 

basis of their distribution in different depositional basins, and the relationships of sedimentary 

facies within the depositional basins. The correlation diagram shows the relative ages of 

numerous moraines and meltwater lake and stream deposits that accumulated at the glacier margin 

in local depositional basins during retreat of the Michigan ice lobe. In deposits of glacial lakes, 

map overprint patterns show the distribution of fine-grained lake-bottom sediments and sand and 

gravel deposits of delta topset beds. Map unit descriptions provide details about glacial-lake dams 

and spillways, and drainage of the lakes. 

This map is preliminary and has not been reviewed for conformity with U.S. 

Geological Survey editorial standards or with the North American Stratigraphic 

Code. Any use of trade, product, or firm names in this publication is for descriptive 

purposes only and does not imply endorsement by the U.S. Government.

This map was produced on request, directly from digital files, on an electronic 

plotter.

Qml Qms

Figure 2. Relationships of late Wisconsin glacial lobes, sublobes, and 

advances within lobes and sublobes. Numbers indicate relative ages of 

surface tills in respective sublobes (oldest to youngest) in this region. 

Hachues indicate limits of ice-margin readvances; arrows indicate 

generalized ice-flow directions within lobes and sublobes (Lineback and 

others, 1983).

Berrien

County

Qorb

30

20

20

10

10

30

102 192 024

102 199 024

102 205 024

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Qmrb

Qdr

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Qec

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Qoko

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Qoko

DEPARTMENT OF THE INTERIOR

UNITED STATES GEOLOGICAL SURVEY

PREPARED IN COOPERATION WITH THE OPEN–FILE REPORT 01-156

MICHIGAN GEOLOGICAL SURVEY DIVISION

AND THE

CENTRAL GREAT LAKES GEOLOGIC MAPPING COALITION

Qikp

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Qcl

Qbl

Qbl

Qbl

Qbl

Qbl

af

Qbl

Qdl

Qbb

Qvt

Qbbb

Qvt

Qvt

Qvt

Qvt

Qvt

Qvt

Qlt

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Qvt

Qlt

Qlt

Qlt

Qlt

Qlt

Qvt

Qvt

Qlt

Qlt

Qlt

Qlt

Qlt

Qlt

Qlt

Qlt

Qlt

Qlt

Qlt

Qvt

Qvt Qccp

Qccp

Qccp

Qal

Qccp

Qccp

Qccp

Qbbb

Qvt

Qccj

Qccj

Qccj

Qccj

Qccj

Qccj

Qst

Qst

Qal

Qal

Qdl

Qdl

Qvt

Qvt

Qmu

Qmu

Qmu

Qmu

Qmu

Qdu

Qdo

Qdo

Qdl

Qsd Qdl

Qdbi

Qdbi

Qdbi

Qds

Qds

Qds

Qds

Qikk

Qikk

Qec

Qec

Qikk

Qikk

Qec

Qec

Qec

Qikc

Qdps

Qdps

Qdps

Qdps

Qdps

Qdb

Qdb

Qdb

Qdb

Qdb

Qdb

Qcr

Qc

Qdl

Qdl

Qdl

Qal

Qed

Qed

Qsd

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Qsd

Qsd

Qcr

Qcr

Qcr

Qbb

Qikk

Qikk

Qal

Qst

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Qdb Qdl

Base map from U.S.. Geological Survey

digital line graph files of hypsography and hydrography

from Benton Harbor and South Bend 1:100,000 scale

topographic map series

SURFICIAL GEOLOGIC MAP OF BERRIEN COUNTY, MICHIGAN

By

U.S. Geological Survey

Edited and integrated by

Byron D. Stone

2001

1 0 1 2 3 4 5 6 7 8 9 10 KILOMETERS

SCALE 1:100 000

1 0 1 2 3 4 5 6 7 8 MILES

Geology mapped 1997-2001 

Digital cartographic compilation by 

S.C. Schindler, 1998, V.S. Williams and

B.D. Stone, 2000, B.D. Stone, 2001

Map compiled from field data registered to

1:24,000-scale topographic maps

Geologic units and features on this map are 

registered to 1:100,000-scale base-map features

Qdbi

APPROXIMATE MEAN

DECLINATION, 1998 MAGNETIC NORTH TRUE NORTH

4  ̊

785'

Qo

735'

Qd

Qmrb

Qmrb

Qmrb

Qmb

Qmb

Qmb

Qmb

Qmb

Qmb

Qbn

Qes

Qes

Qes

Qbn

Qbl

Qsm

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Qsm

Qjk

Qjk

Qst

Qjk

Qmlb

CONTRIBUTING GEOLOGISTS

 

Byron D. Stone

Wayne L. Newell

Scott C. Lundstrom

Van S. Williams

Kevin A. Kincare1

Dennis W. O'Leary

Emily M. Taylor

William C. Burton 

Thomas R. Armstrong 

J. Stephen Schindler 

Gregory J. Walsh

Robert P. Koeppen

Randall C. Orndorff

C. Scott Southworth

Benjamin A. Morgan

Paul E. Carrara

Ralph R. Shroba

Peter W. Barnes

 

1

Michigan Geological Survey

SUPPORT FOR FIELD STUDIES AND 

DIGITAL COMPILATION 

Robert B. Fraser

Elizabeth Campbell2

Donald G. Queen

Mike Herder

James M. McNeal

James E. Quick

 

2

Virginia Geological Survey

Qvt

Qvt

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Qms

Limit of lake survey

Lake Michigan

Lake Michigan

Qlt

Qlt

Qlt

Qml

Qml

Qml

Qms

Qmb

Qmb

Qmb

Qms

Qms

Mc

Mc

Mc

Qaf

Qaf

Qaf

Qaf

Qaf

Topographic and bathymetric contour interval 5 m

86 ̊ 15'

86 ̊ 15'

42 ̊ 42 ̊

86 ̊ 30'

86 ̊ 30'

86 ̊ 45'

86 ̊ 45'