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This is to certify that the
thesis entitled
THE VEGETATION AND HYDROLOGY
OF A LAKESIDE WETLAND

presented by

George Wiliiam Knoecklein

has been accepted towards fulfillment
of the requirements for

MS degree in Eishemea &
Wildlife

claimant/2,6 1

Major professor

 

Date June 10, 1981

 

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charge from circulation records

 

09mI9'om00

 

THE VEGETATION AND HYDROLOGY

OF A LAKESIDE WETLAND

BY

George William Knoecklein

A THESIS

Submitted to
Michigan State University
in partial fulfillment of the requirements
for the degree of

MASTER OF SCIENCE

Department of Fisheries and Wildlife

1981

ABSTRACT

THE VEGETATION AND HYDROLOGY
OF A LAKESIDE WETLAND

BY

George William Knoecklein

The vegetation of a lakeside wetland was mapped accord-
ing to Cowardin at al. (1979). Elevations of the growing
surfaces were measured. The tendency for inundation within
types was obtained from the 20-year average lake-surface el-
evation. Lythrum salicaria L. (purple loosestrife) escaped
inundation on high hummocks at the shore. Larix Zaricina
(DuRoi.)K.Koch. (tamarack), Sphagnum sp., BetuZa pumila L.
(bog birch), and Cornus stolonifera Michx. (red oiser dog-
wood) occupied relatively dry sites. Wet sites were occupied
by a deciduous forest (Fraxinus americana L. white ash, dom-
inant), and a band of Viburnum Zentago L. (nannyberry) and
IZex verticillata (L.)Gray. (winterberry) that surrounded it.
Carer spp. (sedges) dominance was confined to intermediate
hydric sites. The distribution of Typha angustifolia L.
(cattail) was unrelated to the annual water cycle. It dom-
inated portions of the Lake Lansing wetland where the annual

rate of water renewal was highest.

to my wife and parents

ii

ACKNOWLEDGMENTS

I would like to express my sincere thanks to Professor
Clarence D. McNabb for providing essential support, inspira-
tion, and guidance in both the compeltion of this work and
in my own personal development.

Thanks is extended to Doctors Howard E. Johnson and
S. N. Stephenson for serving on my graduate committee.
Special acknowledgment is due Dr. Stephenson for verifying
the identification of the plants collected in the wetland.

My fellow graduate students, Ted R. Batterson, Robert
P. Glandon, and Frederick C. Payne deserve thanks, especial-
ly Maureen Wilson who spent many hours helping me collect
data in the wetland.

Special thanks are due my friends, Frederick Kisbany,
Paul Roettger, and John R. Craig (Limnological Research Lab-
oratory Director), who gave much of their time to this work.

Mehdi Siami is sincerely thanked for providing me with
his eternal optimism.

My deepest appreciation goes to my wife, Pamela, for
without her this work would not have been accomplished.

This study was supported by funds provided by the U.S.
Environmental Protection Agency, Clean Lakes Program, under

Cooperative Agreement No. CR 805046-01.

iii

LIST OF TABLES .
LIST OF FIGURES
INTRODUCTION . .
METHODS . . . .
RESULTS . . . .
DISCUSSION . . .

LITERATURE CITED

TABLE

OF CONTENTS

iv

Page

. l3

LIST OF TABLES

Table Page

1. Vegetation of the Lake Lansing wetland system
classified according to criteria of Cowardin
8t CZZ. (1979) o o o o o o o o o o o o o c o o o o 24

LIST OF FIGURES

Figure

1.

The Lake Lansing watershed, showing basin, wet-
lands (pattern), study site (inset), and tran-
sect used to probe the lake for sediment depth
(AB) 0 o o o o o o o o o o o o o o o o o o o o 0

Aerial view of the western portion of the Lake
Lansing wetland . . . . . . . . . . . . . . . .

Continued, aerial view of the eastern portion
of the Lake Lansing wetland . . . . . . . . . .

Vertical profile of the early post-glacial lake
basin along line AB of Figure l . . . . . . . .

Bathymetry of the early post-glacial lake basin
under the wetland. Existing boundaries of the
lake's surface are shown by the dashed line . .

Contour map of the wetland surface. Hummocks
dominated the topography lakeward of the stip-
pled zone; they did not exist shoreward of that
zone 0 O O O O O O O O O O O O I O O O O O O I O

Vegetation types dominating the Lake Lansing wet-
land after Cowardin et aZ., (1979) with addition-
al refinements; the zone of Sphagnum occurrence,
sedge dominance in the Persistent Emergent Wet-
land type, and nannyberry/winterberry dominance
in the Broad-leaved Deciduous Scrub-Shrub Wet-
land type are shown . . . . . . . . . . . . . .

Range of elevation of growing surface for each
vegetation type displayed against the annual
fluctuation in lake level averaged over a 20
year period . . . . . . . . . . . . . . . . .

vi

Page

ll

l4

16

19

21

26

INTRODUCTION

Wetlands in the temperate zone have vegetation patterns
that have developed since Pleistocene glaciation. Vegetation
patterns continue to change over time. For example, wetlands
on the shores of lakes tend to expand as sedimends build up
in the adjacent shallows and the leading edge of vegetation
encroaches on the basin. Lakeside wetlands that have been
developing for long periods of time tend to have a slope to
the hydrosoil leading from the edge of the lake to the older
and higher landward portions. Changes in the elevation of
the water in such wetlands will coincide with changes in the
elevation of the surface of the lake. The interaction be-
tween the slope of the soil and changes in the elevation of
water produce a set of environmental conditions that could
influence the distribution of plants.

The distribution of wetland plants has been shown to be
influenced by the depth of standing water (Reed, 1902;
Pearsall, 1919; Graham and Henry, 1933; Sharp, 1951; Kadlec,
1962; Harris and Marshall, 1963; Dix and Smeins, 1967;Walker
and Coupland, 1968; Millar, 1973; Van der Valk and Davis,
1976; Teskey and Hinckley, 1977). Fluctuations of water
level within and between seasons (Lewis et aZ., 1928;
[McDonald, 1955; Rutter, 1955), and the length of the annual

l

2
period of inundation (Sharp, 1951; Harris and Marshall, 1963;
Millar, 1973; Teskey and Hinckley, 1977) have been implicated
as well. Edaphic factors such as redox potential, soil chem-
istry and organic content (Misra, 1938; Pearsall, 1938),
water chemistry (Walker and Coupland, 1968; Dix and Smeins,
1967; Walker and Wehrhahn, 1970), and competition (Rutter,
1955) have also been examined as determiners of the distrib-
ution of plants in wetlands. However, a consensus emerges
from the literature that the water dominates the set of en-
vironmental factors controlling distribution (Rutter, 1955;
Dix and Smeins, 1967; Walker and Coupland, 1968).

The purpose of this investigation was to examine the re-
lationship between the distribution of wetland vegetation and
changes in the elevation of water in lakeside wetland over
the course of a year. Maps of the depth of sediments accu-
mulated in the lake basin beneath the wetland, and of the
distribution of plants on these sediments, were developed so
that changes in these features of the wetland over time could

be documented.

METHODS

The site of this work was Lake Lansing, Ingham County,
Michigan. The lake and its watershed are,shown in Figure 1.
The Lake Lansing basin lies on the LaGrange Moraine of the
glacial front known as the Saginaw Lobe (Martin 1955).

Most of the adjacent land has a sand—gravel-clay soil depo-
sited during the retreat of Pleistocene glaciers (Army Corps
of Engineers, 1970). The lake has a surface area of 181.6
ha, a volume of 4124 x 103 m3, mean depth of 2.3 m, and a
maximum depth of 10 m. Shallows are extensive in the lake
basin; 79% of the lake is 3 m or less in depth. An outlet
drains the lake; it typically discharges only in the spring.
Six intermittent streams, draining wetlands in the eastern
portion of the watershed, empty into the lake. Six storm
drains discharge into the lake along its western boundary.
Seepage has been found to be a major factor in the annual
water budget of the lake (Batterson and McNabb, unpublished).
Estimates of net seepage for intervals of the year have shown
a large seepage input to the lake typically occurs in the
spring. There is a net seepage loss from the lake in summer,
fall, and winter. These movements of water are thought to
occur primarily through the wetlands around the lake

(Batterson, 1980). The retention time (volume of the lake/

Figure 1. The Lake Lansing watershed, showing basin, wet-
lands (pattern), study site (inset), and tran-

sect used to probe the lake for sediment depth
(AB).

‘~"~‘ -"

Control «’— ,

Structure

   
    
  

Lake Lansing

6
volume of annual stream discharge) has been calculated to be

19.5 years (ibid.). The location of the lakeside wetland
used in this study is shown in Figure 1.

The position of the early post-glacial clay seal of the
Lake Lansing basin was determined by probing downward in the
substrate beneath the wetland and the adjacent lake. Three-
meter attachable sections of 1.9 cm diameter glavanized pipe
were used for this. The end of the pipe was open and a plug
of clay brought to the surface was used as verification that
the probe had been in the bottom. Measurements of the sed-
iments were made through the ice at 20 m intervals along line
AB of Figure l in the winter of 1979-1980. Six transects
running lakeward from the roadway surrounding the wetland
were established at measured distances from the runoff chan-
nel of the wetland. Two of these transects were located to
the east of the runoff channel; four were to the west. Sed-
iment depths were determined along these at intervals of 5 to
20 m. The position of depth contours in the space between
these transects was estimated from random measurements made
between the transects. A bathymetric map of the early post-
glacial lake basin beneath the hydrosoil was made from these
data.

A contour map of the soil-surface of the wetland was
made from measurements of elevation along the transect lines
used to determine the depths of sediments. The position of
contours between these transects was estimated from random

measurements made between the six transects. These data were

6
volume of annual stream discharge) has been calculated to be

19.5 years (ibid.). The location of the lakeside wetland
used in this study is shown in Figure l.

The position of the early post-glacial clay seal of the
Lake Lansing basin was determined by probing downward in the
substrate beneath the wetland and the adjacent lake. Three-
meter attachable sections of 1.9 cm diameter glavanized pipe
were used for this. The end of the pipe was Open and a plug
of clay brought to the surface was used as verification that
the probe had been in the bottom. Measurements of the sed-
iments were made through the ice at 20 m intervals along line
AB of Figure 1 in the winter of 1979-1980. Six transects
running lakeward from the roadway surrounding the wetland
were established at measured distances from the runoff chan-
nel of the wetland. Two of these transects were located to
the east of the runoff channel; four were to the west. Sed-
iment depths were determined along these at intervals of 5 to
20 m. The position of depth contours in the space between
these transects was estimated from random measurements made
between the transects. A bathymetric map of the early post-
glacial lake basin beneath the hydrosoil was made from these
data.

A contour map of the soil-surface of the wetland was
made from measurements of elevation along the transect lines
used to determine the depths of sediments. The position of
contours between these transects was estimated from random

measurements made between the six transects. These data were

7
collected in the interval March 1980 to September 1980. The

reference point for all measurements was the 259.60 m eleva-
tion datum on the concrete outfall structure of the lake. On
days when soil elevation was. measured in the wetland, ele-
vation of the lake's surface was first measured at the dam.
Elevation of the soil-surface was then determined by measur-
ing its position in relation to the elevation of the lake and
groundwater in the wetland. These data were collected on
mornings following periods of calm air in order to avoid
seiche effects. In the lakeward portion of the wetland, hum-
mocks formed the surface from which dominant plants grew.
Here, the elevation of the top of the hummocks was used to
construct the contour map of the surface of the wetland.

A record of the surface elevation of Lake Lansing for
the interval 1960 to 1980 was obtained from the U.S.
Geological Survey. Their measurements were made from late
March through November, the ice-free period for the lake.
Measurements at 5-day intervals over the 20-year period were
averaged. From the result, predictions could be made of the
most probable elevation of water in the wetland for intervals
of the growing season. Knowing elevations of the soil in the
wetland, inferences could be made concerning the timing of
inundation, and the degree of inundation in various parts of
the wetland.

The vegetation of the Lake Lansing wetland was mapped
using the classification scheme given by Cowardin et a1.

(1979). The boundaries of vegetation types were located in

8

relation to the six transects in the wetland and to portions
of line AB (Figure 1) that ran through the wetland. The pat-
tern of distribution of the vegetation was transposed to a
scaled map made from the 1970 U.S. Geological Survey's top-
ographic map of the East Lansing, Michigan quadrangle. Low
level aerial photographs of the wetland (Figure 2) were ex-
amined to confirm the general position of vegetation types
and the shapes of their boundaries. Once boundaries were
established, measurements of elevation were made to obtain
the range in elevation occupied by each type. The sampling
procedure was biased toward points of maximum and minimum
elevation. A comparison of the ranges in elevation occupied
by types could indicate preference of types for wet or drier
portions of the system.

A list of the common species in the wetland was gener-
ated from collections made over the course of two years;
species were grouped according to vegetation types of
Cowardin et a2. (1979). Plant nomenclature follows Gleason

and Cronquist (1963).

Figure 2. Aerial view of the western portion of the Lake
Lansing wetland.

10

 

11

Figure 2 continued. Aerial view of the eastern portion of
the Lake Lansing wetland.

12

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RESULTS

The Lake Lansing wetland is a dynamic system that has
been developing since recession of the Pleistocene glaciers.
Evidence for this exists in the sediments accumulated be—
neath the wetland and in the adjacent lake. Figure 3 shows
a vertical profile of the early post-glacial basin along line
AB of Figure 1. The accumulation of sediments along line AB
has resulted in a displacement of the lake toward the east.
Organic material dominates the appearance of sediments be-
neath the wetland; the data of Siami (1981) suggests the or-
ganic matter content is in the range of 30 to 65% of the dry
weight. The low relief topography of the land surrounding
the wetland, the small size of the drainage basin adjacent to
the south portion of the lake, and the absence of appreciable
stream flow through the wetland, argue for the position that
eroded soil materials have not contributed appreciably to the
buildup of the sediments. They have originated primarily
from the growth and partial decomposition of the vegetation
of the wetland itself. Figure 4 shows the bathymetry of the
portion of the early post-glacial lake basin over which the
wetland has grown. The parent sediment of the lake basin
lies 2 m to 11 m below the surface of the wetland.

A contour map of the surface of the wetland is given in

13

14

Figure 3. Vertical profile of the early post-glacial lake
basin along line AB of Figure l.

HL- 1

_ 1).].

 
      

Horizontal scale

Existing Lake

Sediments

.....

Post Glacial

 

SHELEW NI Hldafl

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16

Figure 4. Bathymetry of the early post-glacial lake basin
under the wetland. Existing boundaries of the
lake's surface are shown by dashed line.

l7

 

18

Figure 5. Lakeward of elevation <259.70 m, hummocks dominate
the soil topography. They are not found shoreward of the de-
markation line shown in Figure 5. The height of hummocks in-
creases going lakeward from the demarkation line. This is
shown in Figure 5 where elevations within the zone of hum—
mocks are for hummock tOps. The soil was loose underfoot in
the hummock zone; the root-mat of the vegetation was the sole
source of support in the wetland near the lake. Shoreward of
the demarkation zone, the soil was firm. Comparison of Fig-
ure 5 with the bathymetric map of Figure 4, shows that ap-
proximately 3 m of firm soil occurredin the southeast corner
of the wetland; as many as 5 m of firm soil existed in the
southwest portion.

Vegetation types dominating various portions of the
Lake Lansing wetland are shown in Figure 6. Confining the
description of the vegetation to the categories of Cowardin
et a2. (1979) resulted in a loss of detail in regard to dom-
inant forms. In particular, the broad-leaved deciduous type
was dominated by Vibernum Zentago L. (nannyberry) and flex
verticiZZata (L.) Gray (winterberry) on the south and east of
the forested wetland, while Betula pumila L. (bog birch) and
Cornus stolonifera Michx. (red osier dogwood) dominated the
remaining portion of the type. The persistent emergent wet-
land could similarly be separated into areas of Typha
angustifolia L. (cattail) and Carer spp.(sedge) dominance.
Lythrum salicaria L. (purple loosestrife) and C.stoZonifera

dominated the few species that were found in a 3 m band at

19

Figure 5. Contour map of the wetland surface. Hummocks
dominated the topography lakeward of the stip-

pled zone; they did not exist shoreward of that
zone.

 

 

Figure 6.

21

Vegetation types dominating the Lake Lansing wet-
land after Cowardin at aZ., (1979) with addition-
al refinements; the zone of Sphagnum occurrence,
sedge dominance in the Persistent Emergent Wet-
land type, and nannyberry/winterberry dominance
in the Broad-leaved Deciduous Scrub-Shrub Wet-
land type are shown.

22

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23
the shoreline of the wetland. Sphagnum sp., while not dom-
inating the cover, grew in a bed beneath the needle-leaved
deciduous type and extended south eastward beyond the bound—
ary of that type. These refinements of the vegetation pat-
tern are shown in Figure 6. Species found within the vege-
tation types are shown in Table l.

The water level of Lake Lansing fluctuates on an annual
cycle that tends to be constant from year to year. The an-
nual cycle is characterized by high water early in the grow-
ing season; maximum elevations tend to occur in late April
and early May. Elevation of the lake's surface declines
through the growing season to a low in September. The water
level typically rises slowly in the fall. The hydrosoil of
the wetland is frozen in winter, and covered with snow in
most years. Runoff from the watershed usually begins in late
February (Glandon et aZ., 1981). The surface of the lake
thaws near mid-March, and the hydrosoil of the wetland,
shortly thereafter.

The average annual surface elevation cycle for Lake
Lansing is shown in Figure 7. A comparison of elevation of
the lake with elevation in the wetland (Figure 5) yields in-
formation on the tendencies for inundation to occur in parts
of the wetland. In the southwest sector for example, an el-
evation gradient exists; near the roadside, water does not
ordinarily reach the surface of the soil. In the lowest por-
tion of the wetland, (the zone of demarkation for hummocks),

the soil tends to be flooded from April to mid-July. Going

24

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Figure 7. Range of elevation of growing surface for each
vegetation type displayed against the annual
fluctuation in lake level averaged over a 20
year period.

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lakeward from the demarkation zone, the growing surface for
plants becomes progressively drier due to increasing hummock
height. At the lake shore, hummocks stand 10 cm of more
above the 20-year average maximum lake elevation. The water
table drops in the wetland as the lake's elevation declines
during the growing season. In September, the water table is
typically 15 cm to 35 cm below the surface of the wetland.
The distribution of dominant vegetation types in relation to

the annual cycle of lake elevation is shown in Figure 7.

DISCUSSION

The net productivity of the vegetation of the Lake
Lansing wetland provides material annually for the buildup
of the soil of the wetland and filling the adjacent lake
basin. The data of Siami (1981) show that the Lake Lansing
wetland has been advancing into the lake at a rate of 0.2 -
0.4 m yr"1 over the past 23 years. L. salicaria forms a
tight, narrow (<3 m) fringe of vegetation at the edge of the
wetland. The plant is adapted for pioneering the advance
into the lake basin. Aerenchyma in the base of the stem and
in the upper root system, provides buoyancy on the soft, un-
consolidated, organic sediments at the fringe of the lake.
The plants are anchored by a root system that is perennial,
and that becomes extensive over time. Tight clusters of
stems arise each year from the root stocks; stem density at
Lake Lansing was found to be as high as 2000 shoots m"2 of
which 20% was new growth. At the fringe of the lake, biomass
production by L. salicaria can be supported by mineral nutri-
ents taken form the lake. Roots have access to lake water
circulated by wave action at the fringe, particularily
during the high water of April and May. ’

The growth habit of L. salicaria leads to the formation

of woody and fibrous hummocks. In the Lake Lansing wetland,

29

30

the elevation of the tops of these hummocks at the edge of
the lake, was higher than the elevation of hummocks that ex-
tended 50-75 m shoreward from the fringe. Plants behind the
fringe, with the possible exception of Carex spp., did not
appear to be hummock builders. From the observations at
Lake Lansing, the question arises as to whether non-hummock
builders behind the fringe could become dominant on estab-
lished hummocks of L. salicaria, thus confining L.saZicaria
over time to a narrow fringe that moves lakeward on newly
accumulated sediments. A repeat of this baseline study in
the future could provide information to answer that question.

Figure 7 combines the elevation range of the growing
surface for each vegetation type and the 20-year annual cycle
of elevation of water in the lake and wetland. The figure
can be used to identify three divisons of hydric sites in the
system. The first and driest of the three was on hummocks
in the lakeward portion of the wetland. The vegetation map
shows that those hummocks higher than the 20-year maximum
water elevation (259.80 m) were occupied by Sphagnum sp.,
the needle-leaved deciduous scrub-shrub type (Larix Zaricina
(DuRoi) K. Koch. dominant), and the broad-leaved deciduous
scrub-shrub type (B. pumiZa and C. stolonifera dominant).
Sphagnum grew on the tops and sides of hummocks, but was not
found on the sides below the mean maximum water elevation of
259.80 m. Wetzel (1975) and others have described the om-
brotrophic tendency of Sphagnum; its water and nutrient re-

quirements are met primarily by atmospheric input, rather

31
then by groundwater and soil. The data in Figure 7 show that
the base of the stems of L. Zaricina (tamarack), B. pumiZa,
and C. stolonifera were also not normally inundated. Regard-
ing L. Zaricina, this is expected from its well know dis-
tribution in bogs (Lewis at aZ., 1928). The literature lacks
documentation of the water regime reqirements for B. pumiZa
and C. stolonifera. The consistency of the observation re-
ported here, namely that the base of these plants tends to
escape annual inundation, must await documentation from fu-
ture studies.

The forested wetland type (Framinus americana L. domi-
nant), and V. Zentago-I.verticiZZata subtype of the broad-
leaved deciduous scrub-shrub type, occupied the wettest por-
tion of the Lake Lansing system. Hummocks were not present
in the zones of dominance of these plants. The forest was
largely confined to soil elevation of 259.67 - 259.84 m. On
the average, it was inundated 35 days to 85 days each year.
The period of annual inundation for V. Zentago and I.
verticiZZata, surrounding the forest on the south and north-
east, tended to be the same as for the forest. While small
specimens of many of the trees species of the forest were
found on lakeware hummocks, representatives of the shrubs
were not. Ther was a lake of firm substratum to support the
weight of mature trees in the hummock zone; however, there
was no evidence in the field, such as wind-blown saplings,
that laCk of a compacted substratum was limiting the lake-

ward spread of the forest.‘ The literature is lacking in

32

sufficient information on the ecological requirements of the
forest species and the shrubs (V. Zentago and.I.verticiZZata)
to explain their confinement within wet-site boundaries of
the Lake Lansing system.

In relation to the annual water cycle, sedges occupied
a intermediate hydric site in the Lake Lansing wetland.
Dominance of this plant type occurred on or near the 259.80rn
contour. In this position, individuals would normally es-
cape inundation, or be flooded for a short period in the
spring. Sedges did not dominate intermediate sites through-
out the wetland. Portions of stands of the broad-leaved de-
ciduous scrub-shrub type (B. pumiZa and C. stolonifera dom-
inant) and the persistent emergent type (T. angustifolia
dominant) shared the intermediate water regime. Individuals
of species of broad-leaved deciduous shrubs and cattails that
grew on the banks of the drainage channel flowing into the
wetland, were more robust and at least 1 m taller then those
in the interior of the system at 50 m from the stream. This
pattern suggests that interior hummocks regions of the wet-
land were nutrient poor. In addition, beds of Carer spp. in
wetlands are thought to occupy sites that are nutrient poor
(Prince, personal communication). The literature offers no
insights regarding the interaction of water and nutrient re-
gimes on control of sedge dominance in freshwater wetlands.
The location of stands of Carer in the interior of the Lake
Lansing wetland, may be a response, at least in part, to nu-

trient conditions too poor to support the cattails and shrubs.

33
From the observations made in this study, experimentation re-
garding these factors appears—to be in order.

T. angustifolia dominated the emergent wetland type
shown on the map of the Lake Lansing system except for the
area of sedge dominance and the L. salicaria fringe at the
shore of the lake. The cattail was abundant on all three of
the hydric sites. Its distribution appeared to be related
to drainage patterns rather than to aspects of the annual
cycle of water elevation. Stands of T. angustifolia in the
northwest and southeast sectors surrounded intermittent
drains. The plant dominated along the roadway forming the
southern boundary of the study site. Runoff from the road
entered the wetland in that area. Additionally, the roadbed
served as a dam during periods of high runoff; overland flow
was constricted to a culvert diScharging to the stream chan-
nel through the wetland. Seepage likely took place through
the roadbed at times when a head of water occurred behind it.
These observations suggest that T. angustifolia could toler-
ate the variable range of water elevations existing in the
wetland, and dominated in areas of relatively high water re-
newal rates. Prince (personal communication) suggested that
stands of this plant tend to develop in portions of local
wetland systems where availability of mineral nutrients is
relatively high.

From this discussion, and Figure 7, it is apparent that
the distribution of certain vegetation types in the Lake

Lansing wetland could be correlated with the cycle of annual

34

inundation of the system. L. salicaria escaped inundation
on high hummocks at the shore of the lake. Vegetation types
dominated by L. Zaricina, Sphagnum sp., and scrub-shrub dom-
inants B. pumiZa and C. stolonifera, occupied relatively dry
sites on hummocks away from areas of intermittent drain flow,
road runoff, and seepage. Wet sites were occupied by a de-
ciduous forest (F. americana dominant), and a band of V.
Zentago and I. verticiZZata that surrounded it on three
sides. Stands of drier-site scrub-shrub dominants tended to
extend into intermediate sites. The distribution of Carex
spp. dominance was confined to intermediate sites in the in-
terior of the wetland system. In this position, the rate of
mineral nutrient supply to Carer was hypothesized to be low.
The distribution of T. angustifolia was unrelated to the an-
nual cycle of inundation; the plant dominated across the
hydric gradient in the system. It is suggested that T.
angustifolia dominated portions of the Lake Lansing wetland
where the annual rate of mineral nutrient input was highest.

Ecologial controls on the distribution of dominant veg-
etation in freshwater wetlands are poorly known. The litera-
ture provides few insights as to the degree of generality of
the observations made in this study. Comparable studies

from other sites are needed.

LITERATURE CITED

LITERATURE CITED

Batterson, T.R. 1980. Arsenic in Lake Lansing, Michigan.
Ph.D. thesis, Michigan State University. 79 pp,

Cowardin, L.M., V. Carter, F.C. Golet, and E.T. LaRoe. 1979.
Classification of wetland and deepwater habitats of
the United States. U.S. Government Printing Office
Washington, D.C. 103 pp.

Dix, R.L. and F.E. Smeins. 1967. The prairie, meadow, and
marsh vegetation of Nelson County North Dakota. Can.
J. Bot. 45: 21-58.

Glandon, R.P., F.C. Payne, C.D. McNabb, and T.R. Batterson
1981. A comparison of rain-related phosphorus and ni-
trogen loading from urban, wetland, and agricultural
sources. Water Research 15: 881-887.

Gleason, H.A. and A. Cronquist. 1963. Manual of vascular
plants of northeastern United States and adjacent
Canada. VanNostrand. New York. 810 pp.

Graham, H.W. and L.K. Henry. 1933. Plant succession at the
borders of a kettle-hole lake. Bulletin of the Torrey
Club 60: 301-315.

Harris, S.W. and W.H. Marshall. 1963. Ecology of water-
level manipulations on a northern marsh. Ecology
44(2): 331-343.

Kadlec, J.A. 1962. The effects of a drawdown on a water fowl
impoundment. Ecology 43: 267-281.

Lewis, F.J., E.S. Dowding, and E.H. Moss. 1928. The vege-
tation of Alberta. Part II. The swamp, moor, and bog
forest vegetation of Central Alberta. J. Ecol.

16: 19-70.

Martin, H.M. 1955. Map of the surface formation of the
southern Peninsula of Michigan. Publication No. 49.
Michigan Department of Conservation, Lansing, Michigan.

McDonald, M.N. 1955. Cause and effect of a die-off of
emergent vegetation. J. Wildf. Man. 19: 24-35.

35

36

Millar, J.B. 1973. Vegetation changes in shallow marsh wet-
lands under improving moisture regime. Can. J. Bot.
51: 1443-1457.

Misra, R.D. 1938. Edaphic factors in the distripution of
aquatic plants in English Lakes. J. Ecol.26: 411-451.

Pearsall, W.H. 1919. The aquatic and marsh vegetation of
Esthwaite Water. Part V. The marsh and fen vegetation
of Esthwaite Water. J. Ecol. 6: 53-74

Pearsall, W.H. 1938. The soil complex in relation to plant
communities. Part III. Moorlands and bogs. J. Ecol.
26: 298-315.

Reed, H.S. 1902. A survey of the Huron River Vallengart I.
The ecology of a glacial lake. Bot. Gazette 32:
125-1390

Rutter, A.J. 1955. The composition of a wetheath vegetation
in relation to the water table. J. Ecol. 43: 507-543.

Sharp, W.M. 1951. Environmental requirements of a fresh-
water marsh and the ecology of some aquatic plants.
Pro. Northeast Game Conf. Feb. 23, 1951. mimeo 6 pp.

Siami, M. 1981. Arsenic profiles in sediments and sedimen-
tation processes along the slope of a lake basin.
Ph.D. thesis, Michigan State University.58 pp.

Teskey, R.D. and T.M. Hinckley. 1977. The impact of water
level changes on woody riparian and wetland communities.
Vol. I. Plant and soil responses to flooding. Vol. III.
Central forest region. U.S. Government Printing
Office, Washington, D.C. 30 PP. 36 pp.

U.S. Army Corps of Engineers. 1970. Reconnaissance Report
Eutrophication Problem Lake Lansing, Michigan. U.S.
Army Corps of Engineers, Washington, D.C. 25 pp.

Van der Valk, A.G. and C.B. Davis. 1976. Changes in the com-
position structure and production of plant communities
along a perturbed wetland coenocline. Vegetatio 32(2):
87-96.

Walker, B.H. and R.T. Coupland. 1968. An analysis of vege-
tation-environment relationships in Saskatchewan
Slought. Can. J. Bot. 46: 506-522.

Walker, B.H. and C.F. Wehrhahn. 1970. Relationships between
derived vegetation gradients and measured environmental
variables in Saskatchewan wetlands. Ecology 52: 85-95.

37

Wetzel, R.G. 1975. Limnology. W.B. Saunders Co. Phila-
delphia. 743 pp.