‘-o 1' -» '--—-'a......n-. ‘i _ 1m:mnnmummnmt m a 055 9692 This is to certify that the thesis entitled The alvars of the Maxton Plains, Drummond Island, Michigan: Present Community Composition and Vegetation Changes. presented by Patrick Stephen Herendeen has been accepted towards fulfillment of the requirements for MS degree in Botany Major professor {/flflé A“. in- / , 12 June 1985 I)ate 0.7639 MS U is an Affirmative Action/Equal Opportunity Institution LIBRARY Michigan State Unlverslty PLACE IN RETURN BOX to remove We checkout from your record. TO AVOID FINES return on or before due due. DATE DUE DATE DUE DATE DUE MSU Is An Affirmative Action/Equal Opportmlty Institution THE ALVARS OF THE MAXTON PLAINS, DRUMMOND ISLAND, MICHIGAN: PRESENT COMMUNITY COMPOSITION AND VEGETATION CHANGES BY Patrick Stephen Herendeen A THESIS submitted to Michigan State University in partial fulfilment of the requirements for the degree of MASTER OF SCIENCE Department of Botany and Plant Pathology 1985 ABSTRACT THE ALVARS OF THE MAXTON PLAINS, DRUMMOND ISLAND, MICHIGAN: PRESENT COMMUNITY COMPOSITION AND VEGETATION CHANGES BY Patrick Stephen Herendeen The alvar vegetation of the Maxton Plains, Drummond Island, Michigan is examined. Alvars are defined as areas of horizontal limestone or dolomite with shallow soil, supporting an open vegetation dominated by herbaceous plants. On the Maxton Plains these communities are largely . dominated by members of the Poaceae and Cyperaceae. The alvars of the Maxton Plains are compared with the alvars in Ontario, Canada and Oland, Sweden. Similarities in the physical setting and vegetation between these regions are discussed. Through plot sampling in eleven alvar sites, composition of the Maxton Plains alvars and its variability is studied. Similarity of sites is calculated using Horn's index. Aspects of the history of the alvar vegetation are examined through use of aerial photographs and deposits of opal phytoliths in the soils. Differences between the aerial photographs taken in 1939 and 1977 indicate some areas of change in position of the alvar-forest boundary. 0931 phytolith deposits provide evidence that is interpreted to suggest an oscillation of the forest-alvar boundary. ACKNOWLEDGEMENTS Through the course of this study I have become indebted to many people for their assistance with various aspects of this work. I should first acknowledge the assistance of my major professor, Dr. S. N. Stephenson. I would also like to thank my committee members, Dr. A. T. Cross, Dr. J. H. Beaman and Dr. D. Beaver for their suggestions on an earlier version of this thesis. Dr. Cross generously provided all the materials and work space required for the opal phytolith and palynological preparations. For this and many rewarding conversations I. am grateful. Mr. K. C. Kelley was an indispensable resource in the early stages of sample preparation. I owe a word of thanks to Dr. R. E. Taggart for his help with several BASIC programs, including his program for constructing ternary diagrams. Also for programming help I thank Mr. Richard Carroll. Thanks are also extended to Dr. J. Wee for advice concerning microscopy and photography techniques. Dr. G. safir kindly provided me with the use of his printer for the final copy of this text. I would like to acknowledge Ms. Kathryn Egan for her help in keeping me current on recent opal phytolith papers in the archaeological literature. I would like to extend thanks to Dave Mahan and The Nature Conservancy for providing financial support during the 1984 field season. Thanks also to Mr. Kim Chapman of the Michigan Natural Features Inventory for valuable conversations and insights. I am grateful to Dr. R. P. Futyma for lending me a copy of his Dissertation. His work provided a valuable resource in understanding the vegetation history in Upper Michigan. Finally) I would like to acknowledge the Johnson family of Drummond Island for many hours of interesting conversation and for help in a number of difficult situations. Their knowledge of the Maxton Plains and of the history of Drummond Island has been invaluable. iii TABLE OF CONTENTS List Of Tables 0 O O O O O O O O O O O O O O O O O O O O O O O O O O O O O I O O O O O O O O O O 0 .vi List Of Figures 0 O O O I O O O O O O O O I O O O O O O O O O O O O O O O O O O O O O O O O O O OViii IntrOduction. O O C O C O O O O O O O O I O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O 1 Geological setting Geology of Drummond Island.............................3 Late Quaternary history of lake levels.................5 Summary of the Post Glacial Vegetation History and Climate of the Great Lakes region. Introduction..........................................l3 General vegetation history............................l4 Migration routes......................................17 Prairie peninsula.....................................l9, Climatic changes......................................22 Alvars and Alvar Vegetation. Alvar as a geomorphological and ecological term.......28 Description of the physical features of the alvars of the Maxton Plains....................................29 Soils of the Maxton Plains alvars. Methods...........................................31 Results...........................................32 Summary of the climatic data for Drummond Island......32 Comparison of the Maxton Plains alvar setting with alvars of other regions..............................38 Maxton Plains alvar vegetation. Introduction......................................42 Floristic composition of the alvars...............46 The uniquenatureof the vegetation of the Maxton Plains alvars.............................51 Comparison of the alvar vegetation of the Maxton Plains with the alvars of other regions..............54 Naturalness of alvar vegetation.......................58 Vegetation analysis. Introduction..........................................61 Methods...............................................62 Results and discussion Vegetation composition and variability between sites............................................67 Similarity of sites ..............................72 Relationships between biogeographic groups........79 Relationship between species composition and size of sites.........................................86 summarYOOOOOOOOOOOCOOOOO0....OOOOOOOOOOOOOOOOOO0......0.0.92 iv History of the alvar vegetation of the Maxton Plains Introduction..........................................94 Vegetation history as studied through aerial photographs Methods...........................................95 Results and discussion ...........................96 Utility of opal phytoliths in paleoecological studies: a literature review Introduction.....................................102 Nature of opal phytoliths and phytolith deposits.102 Occurrence of opal phytoliths in plants..........lO7 Differentiation of opal phytoliths in the Poaceae.........................................108 Paleoecological uses of opal phytolith deposits..114 Summary .........................................122 Opal phytolith evidence of vegetation history of the Maxton Plains Methods..........................................124 Results and discussion...........................134 Summary..................................................167 Suggestions for further work that is needed to make opal phytolith deposits of greater utility paleo- ecologically............................................169 Literature Cited.0.0...O.0.00.00.00.00.0.0.0.000000000000170O Appendix A Maps of the Maxton Plains....................l78 Appendix B A checklist of the taxa found on the Maxton Plains alvars...........................................l83 Appendix C Alphabetical listing of the species encountered on the alvars of the Maxton Plains......................187 Appendix D Results of the vegetation sampling...........l90 Appendix E Species lists for sites studied in 1984......203 Appendix F Notes on the sites surveyed in 1984..........205 Appendix G Calculated similarity values.................206 LIST OF TABLES 1. Summary of the soil data for the eleven sites where vegetation has been sampled. 2.Soil data from site #29-2 showing variability of measured soil parameters. 3. Summary of the climatic data for De Tour vil lage from 1964 to 1983. 4. Summary of the climatic data for the critical period of June through September. 5. Comparison of climatic data for De Tour village and Oland, Sweden. 6. Percent cover of species in 11 sites as calculated from vegetation sampling in 1983. 7. Number of species and percent cover of species by biogeographic group. 8. Relationships between biogeographic groups of species as represented by number of species in each group occurring in a site. 9. Relationships between biogeographic groups of species, and with area of the alvar site, as represented by correlations using percent cover of species. 10. Number of opal phytoliths observed in soil samples from both the alvar sites dominated by Sporobolus and Schizachyrium and the alvar sites lacking dominance by these species, and the transects indicated. 11. Differences in composition of opal phytolith. deposits in soils from alvar sites dominated by Sgorobolus and Schizachyrium (Sh/SS) and alvars lacking the dominance of these species (Others). 12. Results of vegetation sampling for site 28/29-1. 13. Results of vegetation sampling for site 28/33-1. 14. Results of vegetation sampling for site 29—2. vi 33 34 36 37 41' 68 80 82 85 145 147 190 191 192 15. 16.‘ 17. 18. 19. 20. 21. 22. 23. 24. Results Results Results Results Results Results Results Results Species Sorensen index of community similarity calculated of of of of of of of of vegetation vegetation vegetation vegetation vegetation vegetation vegetation vegetation sampling sampling sampling sampling sampling for for for for for site site site site site 33-2. 33-4. 34-1. 34-2. 34-3. sampling for site 34-5. sampling for site 36-6. sampling for site 36/31-1. lists for sites surveyed in 1984. for sites examined in 1984. 25. Horn's index of community similarity calculated for sites examined in 1983. 193 194 195 197 198 199 200 201 203 206 207 LIST OF FIGURES 1. Approximate shorelines (present elevation) for the Nipissing (ca. 650 ft.) and Algoma (ca.625 ft.) Great Lakes stages. 2. Time of emergence of a given elevation from the waters of Lake Huron. Data represent radio-carbon dated shoreline features from Manitoulin Island. The shoreline of Lake Huron is calculated to have been at the 620 ft. level (present elevation) approximately 3560 years ago. Data is from Lewis (1970). 3. Similarity of communities sampled. This calculation of similarity is based on the Shannon diversity index and Horn's index of community overlap (Brower and Zar 1977). 4. Similarity of communities as calculated using Sorensen's coefficient of similarity. This value is calculated using species presence as recorded in species lists and thus does not account for differences in importance of species. See text for discussion of group designations. 5. Relationship between area of alvar and number of species recorded. 6. Map of the Maxton Plains representing changes in vegetation boundaries that have taken place between 1939 and 1977. 7. Opal phytolith morphology classes as defined by Twiss et al. (1969). 8. Ternary diagram representing the relationship between categories A, B and C. This figure demonstrates the procedures involved in plotting either percentage data or count data. 9» Opal phytoliths isolated from reference materials. Danthonia spicata (1-7), Schizachyrium scoparium (8- 11). 11L Opal phytoliths isolated from reference materials. Spgrobolus heterolepis (12-16), Bromus kalmii (17-18). \dii 10 73 76 91 98 112 132 135 137 11, Opal phytoliths isolated from reference materials. Poa pratense (19-23), Agropyron trachycaulum (24-26), Festuca ovina (27-31). 12. Ternary diagrams representing the relationships between pooid, panicoid and chloridoid opal phytoliths. 13. Ternary diagrams representing the relationships between panicoid and chloridoid phytoliths and diatom remains. 14. Ternary diagrams representing the relationships between pooid, chloridoid and long cell phytoliths. 15. Ternary diagrams representing the relationships between silica cell and long cell phytoliths and diatom remains. 16. Map of Michigan. 17. Main map of the Maxton Plains of Drummond Island. 18. Map of Maxton Plains with site numbers. 139 156 158 162 164 178 179 181- INTRODUCTION This study of the alvars of the Maxton Plains of Drummond Island was initiated for several reasons. Very little has been published concerning this area and it is hoped that this study will contribute some information in this regard. The physical setting of the region and the vegetation are quite unusual. The alvars are areas of horizontally bedded dolomite with very shallow'soil and they- support a vegetation dominated by grasses, sedges and other herbaceous taxa. The occurrence of a grassland community in northern Michigan is unexpected. The composition of these grasslands is unusual in that they are composed of a large number of both midcontinental and northern disjunct species. There are nine vascular plant species occurring on the alvars that are listed as either "threatened" or of "special concern" in Michigan. These grasslands are also unique in that they are the only areas in Michigan that are dominated by three state listed taxa, namely: Sporobolus heterolepis, Eleocharis compressa and Carex scirpoidea. The objectives of this study are as follows: 1) To evaluate the composition of the alvar vegetation, as well as its variability between sites. 2) To evaluate similarities between sites. 1 3) To investigate relationships between biogeographic groups of species. 4) To investigate relationships of species composition to size of alvar site. 5) To study aspects of the history of the alvar vegetation. The vegetation analysis is based.on plot sampling in eleven sites and species lists for 18 other alvar sites. Study of the vegetation history is based on use of aerial photographs from 1939 and 1977, as well as on analysis of opal phytolith deposits in the soils of the alvars and adjacent transitional areas. With few exceptions nomenclature for plant specieS' follows Voss (1972) for the Gymnosperms and Monocots and Gleason and Cronquist (1963) for the Dicots. Voucher specimens are deposited in the Michigan State University Herbarium (MSC). This report will start with a summary of the geological setting of the study area and a summary of the postglacial vegetation history and climate of the Great Lakes region. Comparisons of the Maxton Plains alvars will then be wade with the alvars of both Ontario and Oland, Sweden. These comparisons will make clear the unusual nature of alvar regions. The vegetation analysis will follow and the report will then conclude with the investigation of vegetation changes. GEOLOGICAL SETTING. Geology pf Drummond Island. The bedrock of Drummond Island is composed of dolomite of the Niagaran Series (Middle Silurian). This unit is part of a broadly curving arc of resistant rock which extends from Niagara Falls, north through the Bruce Peninsula, north and west to the islands of Lake Huron, west to the southern part.of the Upper Peninsula of Michigan and then south to the Door Peninsula of Wisconsin. On much of northern Drummond Island the overlying Devonian shales and limestones have been eroded away to expose a flat, shallowly dipping dolomite "pavement" (Dorr and Eschman, 1970). The bedrock surface on the plains is nearly flat to slightly rolling and slopes from northwest to southeast with a gradient of one percent or less. A series of ledges runs roughly east-west across the western part of the Maxton Plains and vary in height from one to two meters. These ledges could be old shoreline features or they could be the result of glacial plucking. Areas just north of a ledge tend to be quite wet and poorly drained due to the damming effect of the ledges while those areas immediatly south of a ledge tend to be much drier. Vegetation zones tend to conform to these physical features quite closely. The dolomite exhibits a jointing pattern which is quite conspicuous over large areas of the Maxton Plains. Joints in the dolomite serve to trap weathered rock and fine grained mineral matter, organic materials and.water which may then promote colonization by plants. These vertical joints provide a source of moisture to the immediately adjacent vegetation, even through the driest periods. An equivalent amount of water is unavailable to plants located only a short distance away. The southern portion (approximatly halffl of Drummond Island is covered by surface deposits of lake sediment origin while the northern portion is reported to have surface deposits originating from glacial end moraines. However, over an extensive portion of the Maxton Plains there is little or no‘glacial till, though there are many glacial erratic boulders scattered throughout.]fl:ha3'not been determined whether till was never deposited in these areas or that it was originally present but was later removed through water erosion during fluctuating postglacial lake levels. As a result of this scanty deposit, all mineral material for soil development must have either come from the products of dolomite weathering or have been transported in by air or water. Much of the silicate clay and fine sand in the scanty soils are likely derived from the dolomite parent material since silica constitutes approximately five percent (by weight) of this rock. Late Quaternary history 9: lake levels. At the peak of the Wisconsinan glaciation, all cu? Michigan was covered by glacial ice. The deglaciation process involved several temporary retreats and readvances of the ice. Final deglaciation.of eastern upper Michigan began after the peak of the Greatlakean ice advance about 11,500y B.P.(years before present). As the ice retreated, Lake Algonquin expanded northward. The first halt in deglaciation of the Upper Peninsula is marked by the Newberry Moraine. A second, longer lasting halt is represented by the Munising Moraine where the ice front remained.for perhaps several centuries, allowing development of the main Lake Algonquin strandlines (Futyma, 1981). At the maximum extent of Lake Algonquin (ca. 10,600y BJL) most of eastern upper Michigan, all of Drummond Island and most of Manitoulin Island were under water. Most of the exposed land of this region consisted of small islands, mostly on the Newberry Moraine and the Niagara escarpment. The outlets of Lake Algonquin are placed at 605 ft at the DesPlaines and St. Clair Rivers (Flint, 1971). Due to differential rebound the strandlines that mark the Algonquin level in northern Michigan are considerably higher. The isobase trend (lines of equal deformation) was determined by Futyma (1981) to be S. 75° E. Though Futyma did not specificly examine Drummond Island, the maximum Algonquin lake surface can be estimated from the isobase trend to have been roughly 919 ft. (280 m) for this area. There was no exposed land on Drummond Island at this time since the highest point on the island is 750 ft. In the Huron basin the main Algonquin stage ended ca. 10,600y B.P. with the opening of successively lower outlets to the east through North Bay. The water level continued to drop to a low water phase (Lake Stanley- Huron basin, Lake Chippewa- Michigan basin), which was reached by ca. 9800y BrP. (Terasmae and Hughes, 1960; Hough, 1963; Wayne and Zumberge, 1965). According to Flint (1971), the outlet for Lake Stanley was the Ottawa River at 165 ft. (present elevation) and the Lake Chippewa outlet was the Mackinac. River at 230 ft. Hough (1963) estimated the original elevation of Lake Stanley to have been 180-200 ft. The Lake Stanley-Chippewa phase ended with elevation of the North Bay outlet. Water levels rose for approximately 3,000 - 4,000 years until discharge was resumed through the stable Algonquin outlets at Chicago (Des Plaines River) and Port Huron (St. Clair River), in addition to the outlet at North Bay. This triple outlet phase defines the Nipissing Great Lakes phase in postglacial lake level fluctuations and is now thought to have occurred from ca. 6,100 to 3,900y ILP. with a peak water level of 605 ft. at the outlet, dated at ca. 5,500y B.P. (Lewis, 1968: Smith, 1968: Harrison, 1971). Nipissing strandlines are well developed erosional features in northern Lake Huron. The shoreline at Sault Ste. Marie is represented by a 9 - 15 meter bluff with its base at about 197 m. (645 - 650 ftJ (Cowan, 1978). Lewis (1970) reports Nipissing shoreline features on Manitoulin Island to range from 640 ft. (1951mJ on the south to 655 ft. (200 nu) on the north end of the island. Prominent bluffs south of the Maxton Plains on Drummond Island are within the range of elevations reported above and are likely Nipissing in origin. Figure 1a shows the extent of exposed land on Drummond Island during the stable phase of Lake Nipissing. At this time all of the Maxton Plains was under water. The Nipissing Great.Lakes phase ends with the closing of the North Bay outlet through the Ottawa River and the- gradual lowering of water level by erosion of the Des Plaines River and St. Clair River outlets. The water level dropped for approximately 500 years until it reached a temporarily stable level at 592 ft. (180 mJ by about 3,200y ELP. Water level was maintained during the Algoma phase, 3,200y B.P. to ca. 2,500y B.P. (Lewis, 1970). Elevations of Algoma strandlines near Little Current, Manitoulin Island are suggested to be ca. 625 ft. (190.5m) (Lewis, 1968). Figure 1b illustrates the approximate position of the Algoma shorelines on the Maxton Plains of Drummond Island. Renewed erosion of the Port Huron outlet allowed gradual lowering of water level to reach 580 ft. (176.8 m) (based on present elevation) by ca. 2,000y B.P. (Wayne and Zumberge, 1965). Time of emergence of a land area such as the Maxton Plains from Lake Huron can be estimated from the timing of lake level changes and the rate of rebound. Lewis (1970) Paxton Plains C‘Q‘B‘””’\ {S ‘\ r\ ..... Present elevation M.\ a; \ \ __Nipissing andAlgcma "‘§ 4 81131811128 v- Nipissing W \5 V MaxtcnPlains .—-._‘—P :- /‘-"""‘"\ l K - \ K \ N \ b. s. c~ ‘ - .9 \J 1'45 ‘ \ .0: ° { ‘ «J Algoma \. Figure 1 Approximate shorelines (present elevation) for the Nipissing (ca. 650 ft.) and Algoma (ca. 625 ft.) Great Lakes stages. made the following measurements and calculations for recent uplift on Manitoulin Island. The total amount of post Nipissing emergence above Lake Huron is 18-23 m. (60-75 ft.): 6.7 m. (22 ft.) by lowering of lake level and the remainder, JJu3-16.3 m. (38-53 ftJ, is due to uplift. Lewis calculates the uplift to have been at a constant rate of 2.2:.7 mm/yr. (0.73:.2 ft/lOOyrs.) for the past 5,000 years for Little Current, Manitoulin Island. Lewis has identified and dated old shoreline features and organic deposits on Manitoulin Island and relates their present elevation to elevation at the time of emergence from Lake Huron. The followingis a partial listing of these sites showing present elevation, original elevation and time of emergence: Original Time of Present Elevation Site Elevation Emergence 582.0ft.(177.4m.) 581.0ft.(177.1m.) 1901130yBP 584.0ft.(178.0m.) 582.3ft.(l77.5m.) 510:180yBP 595.1ft.(181.4m.) 587.3ft.(179.0m.) 1500:600yBP 600.0ft.(182.9m.) 587.9ft.(179.2m.) 1660:150yBP 606.6ft.(185.0m.) 590.2ft.(179.9m.) 2180:300yBP 632.2ft.(192.7m.) 602.4ft.(183.6m.) 4740:140yBP Assuming that the rates of rebound on Drummond and Manitoulin Islands have not been significantly different, it is possible to estimate time of emergence of the Maxton Plains area from these data. Figure 2 represents the elevations of these dated shoreline features plotted against time of emergence. From these data it is possible to correlate these variables and predict time of emergence for 10 Figure 2 Time of emergence of land from the waters of Lake Huron. Data represent radio carbon dated shoreline features from Manitoulin Island. The shoreline of Lake Huron is calcu- lated to have been at the 620 ft level (present elevation) approximately 3560 years ago. Data is from Lewis (1970). ll Auceeeum encuen eueea. eocemueee uo alas 33 soon 22” 39.. m8“ 3: 3.. P h E P e D b I III \ \ \ - \ \ chi. \ oh.ls \\\ \ \ \ .m.n .» comm .ao .3 8o .\ \ \ \ \ «on can . cam one «No . Dam Present elevetion (ft. above see level) 12 a given elevation. The 620 ft. level on Manitoulin Island. is predicted to have first been exposed ca. 3558 years ago. It is evident from this information that the main part of the Maxton Plains (590-615 ft.) has been above water and available for plant growth for less than 3,500 years. It should be noted, however, that this time represents the time of final emergence from the water and that there have been areas of continually exposed and chronically disturbed land available, fluctuating shorelines and isolated high points, for colonization by plants since the decline of Lake Algonquin water levels. SUMMARY OF THE POSTGLACIAL VEGETATION HISTORY AND CLIMATE OF THE GREAT LAKES REGION. Introduction. The sequence of postglacial vegetation and climatic changes in the Great Lakes region are reviewed briefly here so that the characteristics of the present vegetation of the Maxton Plains can be understood and compared with the vegetation of the surrounding region and put into a historical context. The pertinent literature is too' voluminous to review thoroughly but several comprehensive reviews are available (Ogden, 1969; Davis,l983 and Webb gt 31., 1983). There have been few palynological studies reported from the northwest end of the Lake Huron basin. Recently palynological studies in‘eastern Upper Michigan (Futyma, 1982) and on Manitoulin Island (Warner, 1980) have been reported. Most of the studies which concern regional vegetation history and climate change have been conducted on sites in Minnesota, Wisconsin, northern Illinois and Indiana and southern Michigan. It would be helpful to have more palynological evidence from along the shores of the Great Lakes so that migrations associated with these shorelines could be better assessed. Unfortunately studies from these areas are also limited in number. An outline of the timing and nature of the major vegetation changes and migration 13 l4 routes is given in the following paragraphs and then evidence for prairie expansion and for Holocene climatic changes is considered in more detail. General vegetation history. The late-glacial vegetation record in the Great Lakes region provides evidence of a short-lived, narrow belt of tundra, whereas in southern.New England there is evidence for a much longer interval of tundra vegetation, lasting perhaps until 12,000 y. BJL (Davis, 1967). Terasmae (1967) notes that there is no evidence of a long-lasting tundra environment anywhere north of the Great Lakes in late-' glacial time. He also shows that as northern Lake Superior was being deglaciated about 10,000 y. B.P., arctic species could have invaded the northern Great Lakes region by several routes, all restricted to lakeshore and riverside habitats. These are: 1) west of Lake Superior, 2) at Sault Ste. Marie through the Upper Peninsula of Michiganq and 3) through southern Ontario by way of the Bruce Peninsula and around Georgian Bay. Arctic species had migrated into the northern Great Lakes region by 9,000 y. BCP. Tundra vegetation was very rapidly invaded byelements of the early boreal forest assemblage, being replaced in all but the most sheltered areas along the lakes (Terasmae 1967). One such protected area still supporting species with tundra affinities was described from the Old Woman Bay of Lake Superior by Soper and Maycock (1963). 15 Warner (1980) concludes that the first vegetation to colonize the bedrock highlands of Manitoulin Island approximately 10,500 y. B.P. was probably an open, prairie- like, spruce parkland, dominated by grasses and sedges. He considers that this vegetation probably resembled the vegetation that covers Great Coche Island todayn a region that is quite similar to the Maxton Plains. The exact nature and extent of the early boreal forest is still in question because of several unusual characteristics of the pollen record. Terasmae (1968) believes that the late-glacial boreal forest was probably more open because of the greater percentage of nonarboreal. pollen in these assemblages. Cushing (1965) notes that the pollen of spruce-dominated, boreal forest areas are unusually rich in pollen of heleophilous herbaceous taxa such as Artemisia and Ambrosia and in other species from differing biogeographic affinities. This assemblage has been interpreted in various ways including: reworked sediments; long distance transport of pollen of deciduous forest types into’an open vegetation near the northern treeline: mixed coniferous hardwood forest with nearby grassland; and a mixture of vegetation types including swamp, coniferous forest, oak savanna and prairie. Cushing (1965) points out that with the diversity of microhabitats that were possible on this new landscape, such a diversity of species assemblages could be possible. Davis (1967) notes that the vegetation of the same period (ca. 12,000-10,500 y. BJA) in New England may have resembled a park-tundra or spruce-oak l6 woodland and that by 10,500 y. B.P. an open spruce woodland had developed. Late-glacial time in the Great Lakes region and New England wascnuaof continual vegetational disequilibrium resulting from climatic change, soil development and species migrations (Delcourt and Delcourt, 1983). The Delcourts note that during this time the ecotone between boreal forest and deciduous forest widened into a broad belt (latitudinal) which extended from the western Great Lakes to New England. Climatic change in eastern North America has been addressed by many, most recently by Bryson (1983), Bartlein gt 21° (1984) and Dean gt a__l_. (1984). Davis (1983) has presented . rates and directions of Holocene migrations of boreal and deciduous forest taxa onto the deglaciated landscape of eastern North America. By 11,000-10,000 y. BAP. the boreal forest of the Great Lakes region started to deteriorate, presumably due to climatic change but perhaps also as a result of differences in migration rates between various species (Wright, 1964, 1968a). In the area north of Lake Huron and east of Lake Superior the early boreal forest was replaced by the Great Lakes-St. Lawrence forest (=Northern Mixed Hardwood Forest) which has occupied that region ever since (Terasmae 1968). Throughout the middlewest, openings in the boreal forest created by fire and windthrow were gradually'being filled by combinations of birch, alder, pine, oak and elm, depending onlocality (Wright, 1968b).' This transitional forest was 17 soon replaced (within 1,000 years) by the developing prairies in eastern and northern Minnesota (Wright, 1968a). The work of Webb 25:21: (1983) supports this timing of the development of prairie vegetation in this region. Other views as to the sequence and timing of vegetation changes coincident with the time of decline of the early boreal forest must also be recognized. Geis and Boggess (1968) and Gleason (1922) postulated that prairie vegetation replaced boreal forest with no intervening deciduous hardwood stage. Transeau (1933) considered that the boreal forest was replaced with deciduous taxa and that prairie expansion occurred subsequent to this. Benninghoff (1964)_ proposed that prairie vegetation existed much earlier in late-glacial time as openings in the boreal forest and that it functioned as a barrier to the migration of certain temperate forest taxa. The composition, floristic richness and duration of a mixed hardwood forest in the Great Lakes region was probably largely dependent on location. Wright (1968a) shows that in Illinois, boreal forest gave way to deciduous forest, whereas in Kansas and Nebraskaprairie succeeded boreal forest almost immediately. Prairie did not reach Illinois until 8,000 y B.P. Migration routes. Various migration routes have been suggested in discussions of vegetation development. Davis (1983) uses 18 pollen records for boreal and deciduous forest taxa of eastern North America to examine rates and directions of movement. Her work points out the individualistic nature of species movements and the fact that vegetation did not change with one formation replacing another, but rather with individual species becoming established and others declining. The western, southern and eastern migration routes into northern Ontario (Teresmae, 1967) have already been outlined. Terasmae also notes that the migration routes for arctic species were likely restricted to lakeshores and riverbank habitats. The levels, lateral extent and outlets. of the glacial lakes changed rapidly and this could have been quite important in the dispersal of arctic and other water dispersed species. Terasmae (1968) notes that species could migrate northward on the Bruce Peninsula and then to Manitoulin Island without crossing any water barriers. When drainage from Lake Huron to the Georgian Bay shifted to the channel between Manitoulin Is. and the Bruce Peninsula, all those species that had reached Manitoulin Is. could migrate on to Cockburn Is. and Drummond Is. Similarly, migrations of taxa of other biogeographic affinities from other directions along the shorelines must have been possible. Some forest taxa are suggested to have migrated in association with the Great Lakes. Curtis (1959) and Wright (1964) infer that pine and other taxa reached Minnesota and Wisconsin by way of the northern end of Lake Michigan. Benninghoff (1963) suggests that Fagus and Tsuga reached 19 Michigan from the east along the north shore of Lake Erie. Curtis (1959) notes that during the time when Lake Michigan had dwindled to the low Lake Chippewa stage (ca. 10,000- 9,000 y B.P.) there was ample opportunity, with the reduced water barrier, for direct westward migration of forest taxa from lower Michigan, and, I wish to add, for direct eastward migration of prairie taxa. The Prairie Peninsula. The Prairie Peninsula is a continuous wedge-shaped area of grassland vegetation which extends eastward from the. eastern edge of the prairie in Iowa to northern Indiana and then as isolated localities in northern and southwestern Ohio and southern Michigan. The Prairie Peninsula was originally described by Transeau (1935) in a paper outlining characteristics of the formation and the surrounding vegetation. There has been much debate as to the timing and causes of the origin of this extension of the prairie. Much of the debate is no doubt due to the fact that the patterns of vegetation changes have been different in different geographic areas. Transeau (1935) postulated that a climatic change resulting in a greater frequency of prolonged droughts caused an expansion of prairie into the deciduous forest and that fires and exposure have since favored the persistence of the prairie vegetation. Similarly, Wright (1968a) states that, in Minnesota, the 20 Prairie Peninsula dates from mid-postglacial time and was due to recurrent summer droughts eliminating mesic deciduous trees, while in Kansas and Nebraska, prairie succeeded the boreal forest immediately. Geis and Boggess (1968) and King (1981) show that in Illinois the Prairie Peninsula was established by 8,000 y B.P. and that it followed the late- glacial boreal forest, prior to the invasion of deciduous hardwood taxa. Several students have suggested that the expansion of the prairie, and associated climatic changes, were asynchronous throughout the midwest and eastern United States, both north to south and west to east. Wright (1968a) notes that the period of drier and/or warmer climatic conditions (Xerothermic or Hypsithermal) appears to have occurred earlier in central Minnesota than it did in New England. Recently a detailed chronology of these events in the midwest was assembled by Webb et al. (1983). They show several interesting features of the asynchronous movement of the prairie-forest ecotone. They show that by 9,000 y B.P. prairie forb pollen types had increased and the 10% contour (of prairie pollen in relation to total counted) had moved eastward from western Minnesota and Iowa to southwestern Wisconsin and northern Illinois. Between 8,000-7,000 y B.P. there was an eastward increase in prairie-forb pollen in northcentral Minnesota and southern and western Wisconsin but a decrease in northern Illinois. By 6,000 y B.P. there was continued retreat of prairie in 21 Illinois and also in northern Minnesota, yet prairie remained at its eastern extreme in southeastern Minnesota and southwestern Wisconsin. From 6,000-3,000y BAP. prairie- forb pollen in northern and western Minnesota decreased as prairie retreated to the west. At this same time there was an eastward advance of prairie in central Illinois, indicated by an increase of prairie-forb pollen in Iowa, Illinois and northern Indiana, Jones and Beavers (1964a) estimate that a period of 5133 years of prairie Vegetation was required to accumulate the quantity of opal phytolith material present in the soils of central Illinois. Prairie vegetation established early in this period would have the. time necessary to produce this volume of opal. This renewed expansion of prairie vegetation along the Prairie Peninsula may be an important event with regard to species migrations. Relatively early in this period (6,000— 3,000 y B.P.) the levels of Lakes Huron and Michigan had crested at the high Nipissing stage and then gradually through time had dropped to their present positions. Any prairie species that were able to disperse along lakeshores and water courses would have found newly exposed and uncolonized substrate available to them. The distribution of many prairie species today along lakeshores and water courses is an indication of this dispersal pattern. It was also during this time period that the Maxton Plains began to emerge from Lake Huron. After 3,000 y BmP. the prairie border moved westward in the south but was stable in the north (Webb 33 El: 1983). This westward movement was the result of a slow but persistent invasion of the prairies by deciduous forest taxa (Geis and Boggess 1968). It is easier to understand the basis of the disagreements as to the details of the prairie- forest vegetation changes when it is clear that the events were asynchronous from region to region. Climatic changes. Climatic changes are often invoked to explain changes in vegetation. That this is not always so has been recognized by many authors and clearly demonstrated most. recently by Davis (1983) in her illustration of differential rates and directions of migrations of boreal and deciduous forest taxa. The eastward expansion of the prairie is generally accepted to have been the result of climatic changes. The exact nature of these changes has not been ‘agreed upon, with periods of warmer and/or drier conditions being proposed. The term "Hypsithermal" for this interval is now the most widely accepted in North American literature, with xerothermic, altithermal, megathermal and others rejected for various reasons (Deevey and Flint, 1957). Much of the confusion as to terminology and interpretation comes from the fact that: 1) it is difficult to separate the effects of temperature and precipitation 2) many of the early ideas of climatic changes in northeastern United States came from the European literature where a "climatic optimum" of warm and moist conditions during the 23 Atlantic was to have been followed by the Sub-Boreal with a thermal maximum of 2-3°C. above present (Deevey and Flint, 1957: Wright, 1968a). Since it was believed by Deevey and Flint and others that the effects of temperature were primary, the terms for this period of climate change reflect the supposed importance of this climatic parameter. Wright (1968a) notes that the interpretation of a "climatic optimum" preceding the Hypsithermal in North America cannot be justified. That the Hypsithermal was not a uniform'event either geographically or temporally is now becoming apparent. Wright (1976) notes that it is valid to identify a. Hypsithermal interval of continental dimensions but with rather indefinite temporal boundaries. He suggests that it lasted over a longer interval farther to the south and west than it did in the northeast. Watts and Winter (1966) present evidence that, in Minnesota, the Hypsithermal consisted of at least four intervals of dry conditions, each lasting several hundred years. Bryson (1983) also noted that this was_not a uniform climatic period: rather the Hypsithermal had a distinctly different midsection and was not constant throughout the range. Another interesting observation by Bryson is that the period from 7,000-3,000 y ILP. was a time of enhanced volcanic activity around the world and that this may have been an important influence on climate. Recent work of Dean t al. (1984) in northwestern 24 Minnesota allows an independent (non-palynological) look at climatic changes over the past 10,400 years. They present a sedimentological analysis of varved lake deposits from Elk Lake, Minnesota. Their results show that the mid-Holocene dry interval between 8,500 and 4,000 yIBJL was actually asymmetrical and that it actually consisted of two distinct drier pulses, separated by a more moiste interval. They conclude that: 1) amplitudes of climatic oscillations were greatest during the prairie period: 2) cyclic fluctuations were abrupt and persisted throughout the Holocene, being most clearly recorded within the two drier periods; 3) there is evidence for both gradual and abrupt, short term. climatic changes: and 4) climate stabilized in northwestern Minnesota around 3,500 y BJP. They suggest that the prairie period was drier than present, but evidence is somewhat equivocal as to whether it was colder or warmer. The recent work of Bartlein 2E 31. (1984) provides a less subjective approach to determining climatic changes as represented in palynological data. They use multiple regression models to establish relationships between modern vegetation, as represented by modern pollen spectra, and associated climatic parameters. They then apply these relationships to fossil pollen data. From this analysis they note several broad-scale vegetational changes that can be interpreted in climatic terms: 1) an early Holocene northward movement of spruce forest and later southward movement after 3,000 y B.P. 2) an eastward movement of the prairie-forest border into southwestern Wisconsin by 8,000y 25 B.P. and later westward retreat after 6,000 y B.P. Several climatic changes that were postulated include: by 6,000 y B.P. precipitation was less than 80% of present (in Wisconsin and Minnesota); after 6,000 y B.P. precipitation generally increased throughout the region while temperature decreased in the north and increased in the south; the time of maximum temperature varies within the midwest, being earlier in the north and later in the south. Two major assumptions required for this approach should be mentioned since a violation of them could present significant difficulties. These are that: 1) vegetation represented by the modern pollen data must be in equilibrium' with modern climate 2) variation in pollen data must be attributable to climate. Of significance to these assumptions is the recent the work of Davis (1983) in which she shows that some vegetation changes are not due to climate, but rather to differential migration rates. This means that not only will it not be possible to attribute all variation in pollen data to climate, but that some parts of the modern vegetation probably are not yet in equilibrium with climate. In spite of these limits, this study provides some indication of temperature and precipitation changes. A final factor that should be considered here because of its affects on vegetation and because of its link, at least on a regional scale, to climate, is fire. Many palynological studies indicate that fire has been a factor in the history of the vegetation being examined, This is 26 particularly true of the Prairie Peninsula region, though it has also beenaisignificant.factor throughout postglacial time in the region north of Lakes Superior and Huron (Terasmae, 1967). The importance of fire in the Prairie Peninsula has been mentioned by Transeau (1935), Borchert (1950), Cushing (1965) and Webb 33 31. (1983). Transeau felt that fire has favored persistence of prairie species but that it was not a factor in the origin of the Prairie Peninsula. In contrast, Cushing states that fire was important in pushing back the forest and maintaining the prairie-forest border. Webb gt El. (1983) note that, in southcentral Minnesota, the dominating local controls of the, prairie-forest boundaries were topography, soils and especially fire, which they assert was often set by Indians. They’also note that, though these are the proximal factors in controlling the exact timing and local expression of vegetation changes, climate is the ultimate cause for vegetation changes on a regional scale. This conclusion is quite interesting, however it is not really new since it is essentially the same conclusion, albeit much more refined, as wes reached by Cowles (1928) and earlier scientists. In a study of the vegetational history of the eastern Upper Peninsula of Michigan, Futyma (1982) notes several interesting events that pertain to the importance of fire. In this region the Hypsithermal is indicated by the peak abundance of Pinus strobus and the synchronous low levels of Picea and hardwoods from 7,000 to 5,000jy.lLP. By about 5,000 y. B.P. there was a regional increase in hardwood «’9 ’_(J 27 species. These deciduous taxa became the dominants in areas of loamy soil. Dominance of Pinus was maintained on drier, sandier soils. Futyma notes that the dominance of pines is not so much an adaptation to drought as it is to fire and that under the influence of the Hypsithermal climate, all sites experienced fires at a frequency sufficient to favor dominance of pines. Futyma (1982) suggests that temperature decreased between 6,000 y. B.P. and 2,500 y. B.P. in eastern Upper Michigan and that the resulting decreased moisture stress would have favored dominance by deciduous taxa on soils with good moisture holding capacity. He concludes that the vegetation on fine textured soils shows a greater response to climatic changes than does vegetation on sandy soils. This discussion of the late-glacial and Holocene vegetation history and the climatic changes that are hypothesized to have been driving forces during this time in the Great Lakes region should provide the background necessary for evaluating the unusual aspects of the vegetation of the alvars of Drummond Island. It is particularly important to note the coincidence (during the 6,000-3,000 y B.P period) of the strong eastward migration of prairie elements, in the Illinois, northern Indiana and southern Michigan region, with the final lowering of water levels in Lakes Michigan and Huron after the Nipissing high. ALVARS AND ALVAR VEGETATION. iglvar'gg g geomorphological and ecological term. Published use of the term "alvar" in describing a geomorphological setting, and sometimes the associated vegetation, can be traced back to the time of Linnaeus, from a report (1745) on a trip to the island of Oland, off the southeastern coast of Sweden in the Baltic sea (Konigsson, 1968). In the North American literature this term is poorly known but appears to have been used here by Beschel and' Catling gt gt, (1975). .Alvar has its origin as a Swedish.word, being variously defined in Swedish and Estonian dictionaries as a limestone region covered with thin soil and stunted vegetation (Saagpakk, 1982). The root of the word, "alv", refers to the subsoil or subsurface. Alvar is defined in,a recent dictionary’of ecological, evolutionary and systematics terms as a "plant community dominated by mosses and herbs occurring on shallow alkaline limestone soils" (Lincoln gt __l., 1983). Alvar is not used to describe any single plant community or association. Rather, it is used to describe a physical setting that is one of essentially flat limestone with thin soil, supporting only scant, open vegetation (Pettersson, 1965: Konigsson, 1968). Because of the unique 28 29 physical setting, alvars usually have an unusual flora associated with them. ZRosen (1982) and others frequently use "alvar" as an adjective in connection with the vegetation found on these limestone barrens. Alvar, then, refers to the physical setting as described above, and alvar vegetation refers to the unique plant assemblages that are characteristic of these areas. These plant assemblages will be addressed in detail following a discussion of the physical features of the North American and Swedish alvars. Description gt the physical features gt the alvars gt the Maxton Plains. As mentioned earlier, the bedrock of the Maxton Plains of Drummond Island is composed of dolomitic limestone. The surface of this substrate is quite flat and slopes to the southeast with gradients of one percent or less. Deposits of glacial till on the Maxton Plains are generally quite thin to absent, though there are numerous glacial erratic boulders distributed throughout. Soils on the alvar sites are also minimal, ranging in depth from zero to 15 cm. The lack of till may be the result of wave action and flow patterns associated with the great fluctuations in lake levels that alternatly inundated and.exposed Drummond Island through much of the early Holocene. There are several smal l, but topographical ly significant, ledges or scarps (1-2 meters in height) which face northward and which extend in an east-west orientation, 30 roughly conforming to the north shore of the island. Since the bedrock surface slopes gently to the southeast, these ledges have a damming effect on water drainage. Another feature of the bedrock that is important to the hydrology of the Maxton Plains is a prominent jointing pattern. These nearly vertical joints are filled with degraded dolomite and soil and can be several centimeters wide at the surface and likely extend to a considerable depth. The significance of the joints can be easily recognized since rows of trees, shrubs or grasses that are much more luxuriant than the surrounding vegetation are usually associated with them. These joints provide an. important source of water that can be seen by observing the road surface in the early morning where it crosses a system of joints. Even through extended dry periods the soil and rock surface adjacent to a joint is usually quite damp, whereas surface areas between the joint sets are dry. The elevation of the alvars of the Maxton Plains is only slightly higher than that of Lake Huron, which is 580 ft. The alvar sites range in elevation from approximatly 585 ft. to 625 ft. with the most extensive areas at 590 ft. to 615 ft. Fire appears to be an occasional factor in the history of the Maxton Plains region. A Michigan Department of Natural Resources Information Circular (1947) reports that a large fire occurred on the Maxton Plains about 1925. In a compilation of the history of Drummond and the surrounding islands, Ashley (1978) noted a Wu.forest fire that swept 31 the island..." on 25 June, 1820. The extent of this fire is not known. Present evidence of past fires include pieces of charcoal in the soils, especially near upland edges, and burn marks on dead stumps, both along the edges and in the open alvars. Frequency of fires, however, is not known. Also unknown is what influence Indian cultures have had on this area. A physical factor that perhaps should have been considered is frost action but evidence to demonstrate the significance here was not pursued. Alternate freezing and thawing can have a major influence on the rock, soil and plants of a region. Soils gt the Maxton Plains alvars. Methods. Composite soil samples were collected on 19-21 July 1983 from all alvar sites where vegetation was sampled. In site #29-2 (see Figure 18, Appendix AJ soil samples were taken adjacent to each vegetation sampling plot so that the variability of soil parameters within a site could be assessed. Samples were stored in sealed plastic bags until returned from the field. Soil depth was measured by probing each 1/4 M2 plot at the corners and center with a calibrated steel pin. The pin was driven into the soil until it reached bedrock. Soil moisture was measured as percent of fresh weight after drying 24 hours at 100° C. Organic content is measured as percent of soil dry weight after 32 combustion at 550° C. for four hours. Organic content may be overestimated because of the high carbonate component of the soils. Soil pH was measured using an Orion 199 A pH meter after soaking equal weights of fresh soil and distilled water (20 g.) for one hour. Soil texture was determined by the Bouyoucos method of suspending a sample of soil (50 g.) in water and measuring the amount of soil remaining in suspension after 40 seconds (silt and clay) and two hours (clay) with a calibrated hydrometer. Results. The soils of the alvar sites are quite thin, with . average depths ranging from 4.7 cm. to 12.9 cm. The soils are dark brown to black in color with high organic contents, ranging from 12.8% to 27% ash-free dry weight. The average soil texture is a silt loam. Soil samples have high sand and silt fractions and a very minor clay fraction. Soil pH is circum-neutral with values ranging from 6.5 to 7.1. Table 1 presents measured soil parameters for all sites. Table 2 presents the range of variation for moisture, organics and pH measured in site #29-2. Summary gt the climatic data for Drummond Island. The climate of the Maxton Plains region was characterized from weather records (Michigan Dept. of Agriculture Weather Service, East Lansing, Michigan) from De Tour Village, at the eastern tip of the Upper Peninsula. It 33 Table 1. Summary of soil data.for the eleven sites where vegetation has been sampled. Summary of Soil Data for the Maxton Plains Alvars Percent Percent Mean Soil Texture Site Moisture Organics gt Depth Sand gilt Clay 28/29-1 13.67 27.04 7.0 8.77 38 58 4 28/33-1 8.38 23.74 7.0 9.25 44 51 5 29-2 8.23 18.11 7.0 9.73 54 41 5 33-2 11.49 23.75 7.1 7.55 34 60 6 33-4 9.54 32.75 6.8 7.57 32 63 5 34-1 7.07 17.95 6.8 4.67 24 72 4 34-2 10.29 18.75 7.0 12.90 44 49 7 34-3 7.59 17.96 6.5 10.35 36 56 8 34-5 6.26 16.35 6.9 6.75 20 77 3 36-6 8.94 12.76 7.0 9.24 40 48 12 36/31-1 7.69 15.96 6.9 9.99 36 61 3 collection date: sites: 18 July 1983 19 July 1983 20 July 1983 21 July 1983 29-2: 28/28‘1 34-2, 34-3, 36/31‘1 34-1, 34-5 34 Table2. Soil data from site #29-2 showing variability of measured soil parameters. Variability of Soil Parameters Within a Site. Sample Percent Percent Number Moisture Organics pt T1-#1 5.90 13.98 7.1 T1-#2 6.94 14.53 7.0 T1-#3 7.22 18.07 7.1 Tl-#4 8.53 19.37 6.9 T1-#5 8.49 19.69 7.1 T2-#1 7.79 19.79 7.0 T2-#2 7.37 18.52 7.1 T2-t3 9.46 20.62 7.2 T2-#4 12.04 21.08 7.0 T2-t5 5.29 12.48 7.1 T3-#l 5.40 14.11 7.1 T3-#2 6.45 18.26 7.1 T3-#3 10.26 21.56 7.1 T3-#4 9.69 17.21 7.1 T3-#5 10.94 24.02 7.1 T4-#1 9.02 18.68 7.0 T4-#2 7.57 14.48 7.1 T4-#3 10.94 19.32 6.6 T4-#4 6.65 14.00 7.1 T4-#5 8.30 15.01 7.1 T5-#1 8.09 16.69 7.0 T5-#2 7.89 15.52 7.1 T5-#3 7.50 16.50 7.2 T5-#4 5.11 13.35 7.1 T5-#5 11.40 27.53 7.0 T6-t1 6.88 16.75 7.1 T6-#2 10.16 23.71 7.1 T6-#3 9.93 22.74 6.0 T6-t4 8.08 17.99 6.3 T6-#5 7.63 17.92 7.1 Mean 8.23 18.11 7.0 Soil samples were collected on 18 July 1983. 35 should be noted that the De Tour weather station is located immediately adjacent to the water. Therefore temperatures recorded may be more moderated than those on the Maxton Plains. Precipitation should not be so affected. Table 3 presents mean annual temperatures (min., max. and mean) and precipitation for 1964 through 1983, as well as a 20 year average for these values. The coldest month is February with a mean temperature of -9.24°C. The warmest month is July with a mean temperature of 19.09°C. The value T.max./Ppt. is a relative measure of moisture availability. A larger value indicates higher than average temperatures and/or lower than normal precipitation. This value,. however, utilizes annual precipitation which will obscure summer drought conditions if winter precipitation is high. Further, heavy winter snows are of little importance in recharging the soils, considering their shallow depth and the bedrock substrate. Table 4 summarizes climatic data for the critical period, June through September. In this table, Tmax./Ppt. is calculated using temperature and precipitation values for the critical period. Using these values the dry summers of 1966, 1976 and 1983 are obvious. The summer of 1983 was very warm, the warmest on record for the 21 year period, with an annual mean maximum temperature of 11.6°C., 1.1°C. above the average. The mean temperature for July 1983 was 22.6°C., 3.S°C. above the average of 19.09°C. Precipitation in 1983 was below normal with 731.3 mm. recorded at De Tour. Precipitation during 36 Table 3. Summary of the climatic data for De Tour village from 1964 to 1983. SUMMARY OF CLIMATIC DATA FOR DE TOUR VILLAGE 1964-1983 MEAN ANNUAL MEAN ANNUAL TEMPERATURE PRECIPITATION YEARS Tmax.C. Tmin.C. TmeanC. Ppt.mm. Tmax./Ppt. 1964 11.4 -.27 5.565 786.9 .0145 1965 10.2 -.47 4.865 831.3 .0123 1966 10.6 .42 5.510 630.4 .0168 1967 10.0 -.77 4.615 757.9 .0132 1968 10.0 -.03 4.985 865.1 .0116 1969 10.7 .35 5.525 731.0 .0146 1970 10.6 -.13 5.235 909.8 .0116 1971 10.7 .20 5.450 831.8 .0129 1972 9.4 -.86 4.270 762.0 .0123 1973 11.2 1.95 6.575 750.1 .0149 1974 10.0 .26 5.130 745.5 .0134 1975 11.4 1.20 6.300 691.1 .0165 1976 10.5 -.23 5.135 590.3 .0178 1977 10.5 .83 5.665 851.9 .0123 1978 10.0 .26 5.130 725.2 .0138 1979 9.4 .23 4.815 935.5 .0100 1980 10.1 .22 5.160 564.4 .0179 1981 11.1 .94 6.020 581.2 .0191 1982 10.3 -.10 5.100 797.8 .0129 1983 11.6 1.70 6.650 731.3 .0159 20 YR. AVE. 10.485 .285 5.385 753.53 .0142 MEAN MONTHLY TEMPERATURE (C.) FOR: FEBRUARY (coldest month) -9.24 JULY (warmest month) 19.09 37 Table4. Summary of the climatic data for the critical period of June through September. SUMMARY OF CLIMATIC DATA FOR THE CRITICAL PERIOD JUNE-SEPTEMBER MEAN MAX. MEAN YEAR TEMPERATURE (C.) PRECIPITATION (mm.) Tmax./Ppt. 1964 22.15 292.8 .0756 1965 21.00 402.2 .0522 1966 23.22 157.0 .1479 1967 22.22 267.2 .0832 1968 22.32 385.5 .0579 1969 22.50 320.0 .0703 1970 23.28 493.2 .0472 1971 22.35 277.6 .0805 1972 21.35 344.9 .0619 1973 22.48 325.9 .0690 1974 21.65 308.5 .0702 1975 22.68 286.9 .0790 1976 23.35 225.3 .1036 1977 21.00 383.1 .0548 1978 21.15 389.9 .0542 1979 21.30 350.2 .0608 1980 22.05 232.0 .0950 1981 22.82 234.6 .0973 1982 21.10 307.2 .0687 1983 25.40 220.6 .1151 20 YR. AVE. 22.26 310.2 .0718 38 the critical growing period was the second lowest on record for the 20 year period with 220.6 mm. measured, 89.6 mm. below normal. Signs of drought conditions were well developed in August, with dead Picea glauca trees and severely damaged Populus tremuloides and Juniperus communis individuals. The only grasses and other herbaceous plants that werenot severely damaged by the dry conditions were associated with joints in the bedrock. With weather conditions as such, the 1983 season was not an ideal one for characterization of the vegetation. The late season species were the most severely affected by the drought and thus, the least accurately represented in the analysis. Comparison.gt the Maxton Plains alvar setting with alvars gt other regions. The physical features described above for the alvar sites of the Maxton Plains are very similar to features of the alvars of Ontario, Canada, as well as to those of Oland and Gotland, Sweden. Catling gt gt.(1975) described the vegetation associated with several alvar sites in southern Ontario. These sites include Manitoulin Island and the Bruce Peninsula which, togeather with Drummond Island, are located along the Niagara escarpment. Other sites in Victoria, Peterborough, Hastings, Lennox and Addington Counties (Ontario) are situated on limestone, along the contact lines between Ordovician and Precambrian strata. It is not surprising that the sites Catling gt gt. (1975) 39 described from Manitoulin Island and the Bruce Peninsula are very similar to those on the Maxton Plains since they all have a similar dolomitic limestone substrate and are located in relative close proximity, thus likely sharing a similar postglacial history. The sites along the contact lines are similar to those on the Maxton Plains in that they are also situated on limestone plains and have been greatly influenced by deglaciation events and lake level fluctuations (Harrison, 1971; Chapman and Putnam, 1966). The Great.Alvar of Oland, Sweden is quite similar to the alvars of Drummond Island in several respects. Pettersson (1965) notes that the islands of Oland and. Gotland are composed of calcareous Cambro-Silurian strata. The limestone bedrock outcrops in many places on Oland, with the most extensive areas being on the southern part of the island where the Great Alvar (or Stora Alvaret) is located. The bedrock dips to the east-southeast with a shallow gradient. A scarp system runs roughly north-south and faces westward. The scarps serve to dam surface drainage and form shallow lakes and fens. Glacial till deposits are very thin and soils are poorly developed over much of the Great Alvar. Areas of exposed bedrock are not frequent on the Great Alvar but there are local exposures. It is assumed that till cover on southern Oland was originally very thin and that it was later worked by wave action, which removed all but the coarse material which was deposited in beach ridges (Rosen, 40 1982). These beach ridges demonstrate the influence of the Baltic Sea on landscape development. There is also a prominent joint system developed in the bedrock of Oland. The bedrock is limestone and therefore much more soluable than dolomite. The joint system is much more developed on Oland than it is on the Maxton Plains and, in fact, displays characteristics of karst topography. The joints on Oland are important in the hydrology of the region in that water drainage follows these systems underground (Konigsson, 1968). When filled with soil, these joints can also provide an important source of water during dry periods (Rosen, 1982). 131a.pattern similar to that.on the Maxton Plains, narrow strips of trees, shrubs and harbaceous plants. can be seen growing along these structures (Pettersson, 1965; Konigsson, 1968). The climate of Oland can be compared to that of the De Tour Village area. From Table 5 it can be seen that the mean annual temperature at De Tour is only 1 - 1.5°C. lower than that measured at Ekerum, near the Great Alvar. The moderating effect of the Baltic Sea can be clearly seen by comparing the mean temperatures for the coldest month (February) and the warmest month (July) for the two localities. Pettersson (1965) notes that Oland lies in the rain shadow of the southern Swedish uplands and thus is sheltered from the moisture-bearing Atlantic fronts. Most of the moisture that is received by Oland and the east coast of Sweden comes from the south and the east. Because of the low elevation of Oland (S7 mJLS.l. maximum) much of the 41 Table 5w Comparison of climatic data for De Tour‘Village and Oland, Sweden. COMPARISON OF CLIMATIC DATA FOR DE TOUR VILLAGE AND OLAND, SWEDEN MEAN TEMPERATURE (C.) MEAN PRECIPITATION (mm.) ANNUAL FEB. JULY ANNUAL APR.'SEPT De Tour (1964-1983) 5.4 -9.2 19.1 753.5 441.27 Oland-Ekerum (1921-1950) 7.0 -1.8 17.1 463 * 249 ** (1969-1971) 6.5 -2.8 17.0 * precipitation measured at Skogsby (1965-1979) ** precipitation measured at Skogsby (1968-1980) Climatic data for Oland from Rosen (1982). 42 moisture-bearing air passes over. This can be seen by noting that the annual precipitation value reported from Oland's Skogsby Ecological Station is only 61% (463 mm.) of that reported from De Tour (753.5 mmJ. Another significant difference between the two localities is that Oland, being at approximatly 57° N. latitude will receive longer daylight hours during the summer months than will the Maxton Plains at 46° 05' N. These climatic variables show that, though mean annual temperatures are comparable, there are major differences in temperature extremes and precipitation. Pettersson (1965) notes that the precipitation and temperature conditions on. Oland are irregular and that they can cause great annual differences in the occurrence of many species. Similarly, the weather conditions on tflu: Maxton Plains are also variable and a comparable affect on the vegetation can be expected. Maxton Plains alvar vegetation. Introduction. The vegetation of the Maxton Plains is primarily dominated by coniferous forest. On well drained sites Picea glauca, Populus tremuloides, Abies balsamea and Thuja occidentalis dominate, while on poorly drained sites I. occidentalis, Populus balsamifera, Fraxinus nigra and Larix laricina dominate. The vegetation of the remainder ofthe 43 island is a mixture of northern hardwoods and boreal forest (Stephenson, 1983). The grass and sedge dominated alvar sites occur both as distinct openings in the forest and as a more:or less continuous band of varying width, extending eastward for several kilometers from the southwest end of the Maxton Plains on Potagannising Bay, (see Appendix A for a map of the alvar sites of the Maxton Plains). The vegetation of the alvar sites is interesting in several respects. The distribution pattern of the vegetation in a site is usually predictable because of the nature of the rock substrate. Since the bedrock surface slopes gradually to the southeast and since the lowland boundary is usually sharply defined by a scarp or ledge. oriented.roughly perpendicular to the slope, the southern edges of the alvar sites are usually poorly-drained wetlands dominated by Qgtgt’ssp.lor lowland forest. The upland edges are not as sharply defined. They are gradual, usually with a transition zone dominated by Populus tremuloides and sometimes Picea glauca. Juniperus communis is an important understory dominant. This transition zone is quite variable in width, ranging from approximately 20 m to 100 m or more. Sometimes these upland transition zones are dominated by a zone of young Populus tremuloides. These broad zones of young aspen have the appearance of having encroached relatively rapidly. The zones of encroachment are of particular interest in the investigation of vegetation changes on the Maxton Plains. Features of the bedrock are also likely important in defining the position of these 44 upland boundaries. The dolomite exhibits a network pattern of vertical joints which range in width from less than 1 cm to 3 cm across at the surface. Individuals of ttggg gtgggg, Juniperus communis, Shepherdia canadensis and other woody members of the upland transition that become established and persist in the Open alvar are usually associated with a joint. Another feature of the bedrock that is also probably important in determining vegetation patterns is the tendency of the dolomite to fracture along horizontal planes, more of less parallel with the bedding, forming slabs of rock that - are variable in thickness and size. There may be several layers of these slabs, each separated by a thin band of degraded dolomite, above the unweathered bedrock. It seems likely that this exfoliation is a result of frost action, as moisture gradually penetrates zones of weakness in the rock. The degree of development of this horizontal fracturing and slab formation may be related to position on the slope. It appears that this feature is most strongly developed in low, poorly-drained areas. In better-drained areas, such as the upland transition zone, frost action seems to result in smaller and thinner, irregularly shaped dolomite fragments. This variation, however, may not be entirely due to drainage, as there are lithologic features of the rock that may also be important. Spaces between these rock slabs are filled with degraded dolomite and thus are important as- 45 potential zones for rooting. The nature and position of the upland transition zone may also be related to these structures. Between the more or less abrupt lowland wet edges and the broader upland transition zone is an open, treeless area usually dominated by §22£22212§ bersrglseia and Schizachyrium scoparium, both C4 grasses, and Eleocharis compressa. The vegetation and history of these grasslands are the primary foci of this study. The same physical features that appear to be important in determining the nature of the upland transition flora are also likely important in the open alvars. For example, the importance of the joints in providing a source of moisture can be. easily observed since the tallest and most luxuriant growth is associated with a joint. There are frequent, small, shallow, rectangular depressions (as much as 10 cm deep and several dm across) distributed throughout the alvars. These depressions tend to retain moisture longer and thus impart.a small scale mosaic pattern to the vegetation. There are occasional larger depressions, not associated with the scarps and lowland edges, that retain water for longer periods of time. These areas may be as much as a meter in depth and several tens of meters across. The species assemblages in these larger depressions may be very similar to those near the lowland edge of the alvars. Since the larger depressions support different species assemblages than the remainder of the alvar areas, the vegetation in these depressions is 46 excluded from all analyses and surveys of alvar vegetation. There are several areas with no soil. These "pavement" or outcrop areas are well developed in the large sites (site numbers 34-1 and 34-5) in section 34 (T43N, R6E) and in section 20 in the sites along the northwest shoreline. In such pavement areas vascular plants can grow only 1J1 association with joints. The areas between joints are usually bare rock. Wind-blown soil can accumulate along these lines of vegetation, allowing gradual colonization of the open areas. Various species of mosses will sometimes colonize the shallowest soil deposits. Many of the alvar sites contain inclusions or islands of trees, usually consisting of Picea glauca and Popul_t_1_s_" tremuloides but sometimes also including Thuja occidentalis or Abies balsamea. These tree islands are usuallyassociated with some kind of topographic or substrate irregularity. Typically there is a band of aspen encircling the margins of such tree islands. Floristic composition gt the alvars. The floristic composition of the alvars of Drummond Island is of interest primarily because of the unusual assemblage of plant species found there. Appendix A is a map of the Maxton Plains with all alvar sites numbered. Appendix B presents a checklist of the taxa found on the alvars. This listing also includes synonymies and notes on significant distribution patterns. Appendix C is an alphabetical listing of species by genus. Stephenson (1983) 47 noted that two major floristic elements contribute most of the vegetation cover in these areas. These are: 1) an arctic and/or boreal-cordilleran group and 2) a mid- continental group. A third element, though of lesser importance with regard to cover, consists of a southern and eastern group of species. In an attempt to look further at the biogeographic affinities of the alvar flora, the following references were consulted for information regarding distribution patterns: Gleason and Cronquist (1963), Fernald (1950), Hulten (1968). In this study the biogeographic affinity of a species is taken to be represented by the center of its present. distribution. It should be noted that there are several species with a significantly disjunct occurrence on the Maxton Plains. Disjunct northern species include: Carex scirpoidea and Trisetum spicatum. Disjunct midcontinental species include: Geum triflorum and Sporobolus heterolepis. Following is a listing of species according to biogeographic affinity. For a discussion of the importance and relationships of species and floristic elements in the vegetation see the discussion in "Vegetation Analysis". Species gt midcontinental affinity. Anemone canadensis Apocynum sihiricum var. cordiggrum Aquilegia canadensis var. hybrida Aster ptarmicoides gtomus kalmii garex crawei Qgrex merritt-fernaldii garex fichardsonii Carex umbe l l ata 48 Castil leg coccinea Cfisium hi 1 1 ii Comandra umbe 1 lata trucastrum ga l l icum Geranium bicknel 1 ii Geum triflorum gglygala.senega Ranunculus fascicularis thus aromatica thus glabra Bosa blanda Schizachyrium scoparium §cutellariaparvula _Stnilacina stel lata Sporobolus heterolepis §porobolus vaginiflorus Trichostema brachiatum Verbena.simplex Species primarily gt northern and cordilleran regions gt North Amefica. gster ci 1 io l atus garex virfiula Epi 1 obium ci 1 iatum Juncus dudle i guniperus horizontalis Ribes oxyacanthoides Rosa acicularis §gnecio pauperculus Shepherdia canadensis Sisyrinchium montanum Symphoricarpos albus Violanephrophylla Circumboreal species (some with interrupted distributions). Achil lea mil lefolium ssp. lanulosa Agropyron trachycaulum Arabis hirsuta var. pycnocarpa Arctostaphylos uva-ursi grtemisia campestris ssp. caudata Botryghium simplex gampanula rotundifolia garex scitpoidea Cerastium arvense Deschampsia cespitosa Juniperus communis tathyrus palustris Egg pratensis Potentil la anserina gotentilla.fruticosa Potenti l 13 norvegica 49 triglochin maritima Trisetum spicatum var.rmaltg Eastern and Great Lakes region. Amelanchier sanguinea Aster ptlosus var. pringlei Carex castanea Carex garberi (primarily Great Lakes region) Carex laxiflora gichanthelium accuminatum Eleocharis compressa Hypericum kalmianum (primarily Great Lakes region) Prunus pumila var. depressa ggunus virginiana Satureja glabel la var. angustifolia Saxifraga virgifiiensis (northern if synonym with g. nivalis) filidago nemoralis Solidago ohioensis (primarily Great Lakes region) Vitis riparia Zigadenus glaucus Species widespread within North America. Agrostis hyemalis Ambrosia artemisiifolia Antennaria neglecta Apocynum androsaemifolium Arenaria stricta Carex interior Qanthonia spicata Fragaria virginiana Geranium carolinianum Glyceria striata Li 1 ium phi l ade 1 phicum Silene antirrhina Solidago canadensis Veronica peregrina Vicia americana Species with g cosmopolitan distribution (or nearly so). gardamine parviflora var. arenicola tquisetum arvense Festuca ovina var. saximontana grunel la vulgaris var. lanceolata Pteridium aquilinum var. Iatiusculum Satureja'vulgaris 50 Introduced species. Agrostis gigantea gtenaria serpy l l ifo l ia tgrbarea'vulgaris ggntaurea maculosa Chrysanthemum leucanthemum Cirsium arvense Daucus carota Hieracium aurantiacum Hieracium pi lose 1 loides Hypericum perforatum ygdicago lupulina Phleum pratense Plantago lanceolata Poa compressa Potentilla recta Ranunculus acris Rumex crispus Taraxacum officinale ttagopogon pratensis trifolium hybridum trifolium pratense Trifolium repens Verbascum thapsus Veronica arvenSis Summary Total number of species: 118 Number of Species Percent of Total Midcontinental —""" — 26 "22 . 0 Northern 30 25.4 (Northern/Cord. 12 10.2) (Circumboreal 18 15.2) Eastern/Great Lakes 17 14.4 Widespread 21 17.8 (In North America 15 12.7) (Cosmopolitan 6 5.1) Introduced 24 20.3 From the summary of this listing it can be seen that the northern element is the largest with 30 species, followed by the midcontinental group with 26 species. Though the group of introduced taxa includes 24 species, it 51 will be seen in the011) IDNC 5131145 mum Low; (11:11:; West Rudd I'amp Transect 54-1 Nurth "runsect CHLORIDOID CHLORIDOID LUNG CELL; wow wow 1.0m; (rum: Fi be 164 Figure 15 Ternary diagrams representing the relationships between silica cell and long cell phytoliths and diatom remains. 165 Sporobolus and Schizachyrium s dominated alvar CHLORIDOID + DIATOMS PANICOID + POOID 28/33-1 Transect $1 CHLORIDOID + DIATOHS PANICOID ‘ POOID Nest Road Transect LONG CELL Alvars lacking :hese uominan:s LONG CELLS CHUJRIDOID t DIATOMS PANICOID + POOID 34—1 East Transect LONG CELLS CHLORIDOID + DIATOMS PANICOID + POOID 14—1 North Transect LONG CELLS :HLORIDOID ‘ DIATOMS PANICOID + POOID 166 east transect, whereas the diagram representing 28/33-1 trans. #1 shows considerable oscillation in the relationship between long cells and combined silica cells. In addition, the west road transect and 34-1 north both show unique trends in the silica cell-long cell relationship. If more was known regarding variability among the grass species of the ratio between long cell phytoliths and silica cell phytoliths then a meaningful interpretation of these results might be possible. This figure then is an example of a combination of morphologies that is rather uninformative. In this discussion several sets of ternary diagrams have been presented to illustrate some trends in thelopal phytolith data that are not readily apparent in the data table. These diagrams help to demonstrate the differences in the phytolith assemblages in the soils from the two groups of alvar sites. In addition, they illustrate a number of different patterns of vegetation change in the alvar-forest upland transitions. These conclusions will be summarized in the following section. SUMMARY. The following conclusions are drawn from the analysis of the opal phytolith deposits in the soils. 1) The alvar sites that lack Sporobolus heterolepis and Schizachyrium scoparium as dominants have not supported these species as dominants for a relatively long period of time, if ever. 2) The transects generally show less grassland influence, represented in the soils by a decrease in total grass opal, with distance into the forest. Each transect demonstrates unique details with respect to changes in opal phytolith content with distance into the forestw These details are the combined result of both differences in vegetation history between the transects and random variability of the opal content of the samples. 3) The opal phytolith assemblages in the transition soils _are generally quite similar to those in the soils of the Sporobolus and Schizachyrium dominated alvars, with regard to the proportional relationships between the phytolith morphologies. This is interpreted to suggest some degree of influence of this grassland community in the upland transitions examined. 4) Transects 34-1 east and 28/33-1 trans #l‘are located in transitionsthatappear tobe relatively more stable, as compared to the other two transects. 5) From these conclusions and the results of the aerial photograph study it is concluded that there must be a band 167 168 or zone that the upland transition can occupy. The position of the transition oscillates and is likely dependent on climatic cycles involving drought and fire. The degree of importance of fire is not known, though it has been recorded historically and is evidenced by charcoal fragments in the soils. 6) Finally it is concluded that ternary diagrams can serve to illustrate trends in the opal phytolith data that are not evident in the data table. Suggestions for further work that ifi needed £9 make opal phytolith deposits 2: greater utility paleoecologically. The following areas need to be investigated further so that opal phytoliths will be of greater utility in paleoecological studies. 1) Differential production rates of phytoliths between taxa. 2) Differential weathering rates between different sizes of phytoliths. 3) Variability of opal phytolith deposits within a site, perhaps as it relates to microtopographic variations. 4) The significance of the long cell : silica cell phytolith ratio and variability between taxa. 5) Finally, developing a greater understanding of the capacity'of phytolith.deposits to discern different plant communities, perhaps through comparisons of similarity calculations of vegetation types with similarity calculations of opal phytolith deposits. The Maxton Plains is an ideal setting for investigation of these areas because of the limited flora, the shallow soils and the lack of forest influence in the central part of the alvar sites. 169 LITERATURE C ITED LITERATURE CITED Ammann, GJL 1947. 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Speciman collection and preparation for critical light microscope examination of Synuraceae (Chrysophyceae). Trans. Am. Micros. Soc. 102: 68-76. Wilcox, BJL 1980. Insular ecology and conservation. Chapter 6 pp. 95-117. In: M.E. Soule and B.A. Wilcox (eds.), Conservation Biology. Sinaeur Associates Inc. Wilding, IuP. and IuR. Drees. 1968. Biogenic opal in soils as an index to vegetative history in the prairie peninsula. pp. 96-103. In: R.E. Bergstrom (ed.), The Quaternary of Illinois. Univ. Ill. Colege of Agr. Spec. Publ. 14. Witty, J.E. and E.G. Knox. 1964. Grass opal in some chestnut and forested soils in north central Oregon. Soil Sci. Soc. Am., Proc. 28: 685-688. Wright, HJL, Jr. 1964. .Aspects of the early postglacial forest succession in the Great Lakes region. Ecology 45: 439-448. . 1968a. History of the Prairie Peninsula. pp. 78-88. In: R.E. Bergstrom (ed.), The Quaternary of Illinois. Univ of 111. Coll. of Agr. Spec. Pub. 14. 177 Wright, H.E., Jr. 1968b. The role of pine in the forest history of Minnesota and adjacent areas. Ecology 49: 937-955. . 1976. The dynamic nature of Holocene vegetation. A problem in PaleoclimatologY: Biogeography'and Strati- graphic Nomenclature. Quat. Res. 6: 581-596. Yeck, R.D. and F. Gray. 1972. Phytolith size characteristics between Udol ls and Ustolls. Soil Sci. Soc. Am., Proc. 36: 639-641. 178 Appendix A Figure 16 Map of the state of Michigan. 179 Figure 17. Main map of the Maxton Plains of Drummond Island. Bruce Pt. ;;:;;::Eg 182::pewa 43w 20 “5. Es. -‘: Grand g . €31» Alvar Marsh [::] Forest E Small lakes (ilometers Miles '19 l Marias Lake Transects A= Transect 34-1 East B= Transect 34-1 North C= West Road Transect D= 28/33—1 Trans. #1 E= 28/33—1 Trans. #2 Dawson Lake Poe Point , H910 DRLK‘VOND ISLAND Raynolds Point 181 Figure 18. Map of the Maxton Plains with site nunbers. Poe Point a“ :5: ‘§ ‘ . hi ' , , "m“ C ppewa «@QZO \- Eh -J Marias Lake .. ‘ CZ) ‘0 M ”f S (2%) "E ‘5: ' Raynolds Point Sites studied in 1983 for vegetation composition T143N. 17.2%.— 28/29—1 33—4 34—5 28/33—1 34—1 36—6 29—2 34—2 36/31—1 33—2 34—3 3’ L) Colton Bay 183 APPENDIX B. A checklist of the taxa found on the Maxton Plains alvars EQUISETOPHYTA Equisetaceae Equisetum arvense L. POLYPODIOPHYTA OPHIOGLOSSIDAE Ophioglossaceae Botrychium simplex E.Hitchc. ‘ POLYPODIIDAE Cyatheaceae Pteridium aquilinum (L.)Kuhn. var. latiusculum (Desv.) Underw. PINOPHYTA PINIDAE Pinaceae, Picea glauca (Moench) Voss Cupressaceae Juniperus communis L. S; horizontalis Moench Thuja occidentalis L. MAGNOLIOPHYTA MAGNOLIIDAE Ranunculaceae Anemone canadensis L. Aquiligia canadensis L. var. hybrida Hook. Ranunculus acris L. B; fascicularis Muhl. CARYOPHYLLIDAE Caryophyllaceae Arenaria serpyllifolia L. A.stricta Michx. Cerastium arvense L. Silene antirrhina L. Polygonaceae Rumex crispus L. DILLENIDAE Clusiaceae Hypericum kalmianum L. S; perforatum L. Violaceae Viola nephrophylla Greene 184 Salicaceae Populus tremuloides Michx. Brassicaceae Arabis hirsuta (L.) Scop. var. pycnocarpa (Hopkins) Rollins Earharea vulgaris R.Br. Cardamine parviflora L. var. arenicola (Britt.) O.E. Schulz. Erucastrum gallicum (Willd.) O.E. Schulz. Ericaceae Arctostaphylos uva-ursi (L.) Spreng. ROSIDAE Grossulariaceae Ribes oxyacanthoides L. Saxifragaceae Saxifraga virginiensis Michx. (=S. nivalis L. Rosaceae Amelanchier sanguinea (Pursh) DC. Sragaria virginiana Duchesne Geum triflorum Pursh. Potentilla anserina L. g; fruticosa L. E; norvegica L. E; recta L. Prunus virginiana L. S; umila L. var. de ressa (Pursh.) Gl. Rosa ac1cularis Lind . S; blanda Ait. Fabaceae Lathyrus palustris L. Medicago lupulina L. Trifolium hybridum L. E; pratense L. 3; repens L. V1c1a americana Muhl. Eleagnaceae Shepherdia canadensis (L.) Nutt. Onegraceae Epilobium ciliatum Raf. Santalaceae Comandra umbellata (L.) Nutt. Vitaceae Vitis riparia Michx. Polygalaceae Polygala senega L. ?) 185 Anacardiaceae Rhus aromatica Ait. R; glabra L. Geraniaceae Geranium bicknellii Britt. S; carolinianum L. Apiaceae Daucus carota L. ASTERIDAE Apocynaceae Apocynum androsaemifolium L. S; sibiricum Jacq. var.cordigerum (Greene) Fern. Verbenaceae Verbena simplex Lehm. Lamiaceae Prunella vulgaris L. var. lanceolata (Bart.) Fern. §atureja glabefli (Michx.) Eriquet var. angustifolia (Torr.) Svenson Scutellaria parvula Michx. Trichostema brachiatum L. Scrophulariaceae Castilleja coccinea (L.) Spreng. Verbascum thapsus L. Veronica arvegsis L. V; peregrina L. var. xalapensis (HBK) St. John & Warren Campanulaceae Campanula rotundifolia L. Plantaginaceae Plantago lanceolata L. Caprifoliaceae Symphoricarpos albus (L.) Blake Asteraceae Achillea millefolium L. ssp. lanulosa (Nutt.) Piper Ambrosia artemisiifolia L. Antennaria neglecta Greene Artemisia campestris L. ssp. caudata (Michx.) Hall & Clem. Aster ciliolatus Lindl. A; pilosus Wild. var. pringlei (Gray) Blake 5; ptarmicoides (Nees) T. & G. Sentaurea maculosa Lam. Chrysanthemum leucanthemum L. Hieracium aurantiacum L. IL piloselloides Vill. hfih florentinum All.,IL caespitosa -—Dumortu, S; pratensg Tafisch., S; raealtum_Gochnat, floribundum Wimmer & Grab. see Voss and B6HIE5_1978) 186 Cirsium arvense (L.) Scop. S; hillii (Canbyi) Fern. Senecio pauperculus Michx. Solidago canadensis L. S. nemoralis Ait. S: ohioenSis Riddell. Taraxacum officinale Weber Tragopogon pratenSis L. ALISMATIDAE Juncaginaceae Triglochin maritima L. COMMELINIDAE Juncaceae Juncus dudleyi Weig. Poaceae Agropyron trachycaulum (Link) Malte (= A. caninum Linn. ?) Agrost1s gigantea Roth. A. hyemalis (Walter) BSP. Bromus kalmii Gray Danthonia cespitosa (L.) Beauv. Dichanthelflm acuminaflm (Schwartz) Gould & Clark (=Panicum impl1catum Schribner, P. lindheimeri Nash) Festuca ovina L. var. sax1montana (Rydb. ) Gl. Glycer1a striata (Lam.) Hitchc. Phleum pratensg L. Poa compressa L. P. —pratense L. Schizachyrium scoparium (Michx. ) Nash Sporobolus heterolepis Gray Trisetum spicatum (L. ) Richter var. molle (Michx.) Beal Cyperaceae Carex castanea Wahl. ‘S; crawei Dew. arberi Fern. interior Bailey laxiflora Lam. merritt-fernaldii Mackenz. richardsonii R.Br. scirpoidea Michx. umbellata Schkuhr. viridula Michx. eocharis compressa Sulliv. |9|9|9|9|9|9|9|9 M H LILIIIDAE Liliaceae Lilium philadelphicum L. Smilacina stellatan.) Desf. Zigadenus glaucus Nutt. Iridaceae Sisyrinchium montanum Greene 187 Appendix C. Alphabetical listing of species encountered on the alvars of the Maxton Plains. Achillea millefolium ssp. lanulosa * Agropyron trachycaulum * Agrostis hyemalis Agrostis gigantea Ambrosia artemisiifolia Amelanchier sanguinea * Anemone canadensis Antennaria neglecta Apocynum androsaemifolium Apocynum sibiricum var. cordigerum Aguilegia canadensis var. hybrida Arabis hirsuta var. pycnocarpa Arctostaphylos uva-ursi’ Arenaria serpyllifolia Arenaria stricta Artemisia campestris ssp. caudata * Aster ciliolatus Aster pilosus var. pringlei Aster ptarmicoides * garbarea vulgaris §otrychium simplex gromus kalmii * Qampanula rotundifolia Qardamine parviflora var. arenicola Carex castanea Carex crawei * Carex eburnea * Qarex garberi * Carex interior Qarex laxiflora ‘garex merritt4fernaldii Qarex richardsonii garex scirpoidea * garex umbellata * Carex viridula Castilleja coccinea gentaurea maculosa Cerastium arvense Ehrysanthemum leucanthemum Cirsium arvense girsium hillii Eomandra umbellata * Danthonia spicata * Daucus carota Deschampsia cespitosa * Dichanthelium acuminatum Eleocharis compressa * gguisetum arvense * Epilobium oiliatum Erucastrum gallicum gestuca ovina var. saximontana * Fragaria virginiana * 188 Appendix C (continued) Geranium bicknellii Geranium carolinianum Geum triflorum Glyceria striata Hierac1um aurantiacum Hieracium piloselloides Hypericum kalmianum Hypericum perforatum Juncus dudleyi * Jun1perus communis * Juniperus horizontalis * Lathyrus palustris Lilium philadelphicum Medicago lupulina Phleum pratense Picea glauca * Plantago lanceolata Poa compressa * Poa pratensis * Populus tremuloides * Polygala senega Potentilla anserina Potentilla fruticosa Potentilla norvegica Potentilla recta Prunella vulgaris var. lanceolata Prunus pumila var. depressa * Prunus virginiana * Pteridium aquilinum var. latiusculum Ranunculus acris Ranunculus fascicularis Rhus aromatica - Rhus glabra R1bes oxyacanthoides Rosa acicularis Rosa blanda Rumex cr1spus Sature'a glabella var. angustifolia Saturela vul aris Saxifraga v1rg1n1ensis Schizachyrium scoparium * Scutellaria parvula Senecio pauperculus * Shepherdia canadensis * Silene antirrhina Sisyrinchium montanum Smilacina stellata Solidago canadensis * Solidago nemoral1s Solidago ohioensis Sporobolus heterolepis * Sporobolus vaginiflorus * Symphoricarpos albus * 189 Appendex C (continued) Taraxacum officinale ghuja occidentalis * Tragopogon pratensis Trichostema brachiatum grifolium hybridum Trifolium pratense TPifolium repens griglochin maritima Trisetum spicatum var. molle Verbascum thapsus Verbena simplex Veronica arvensis Veronica peregrina Vicia americana Viola nephrophylla yitis riparia Zigadenus glaucus * * Indicates species that.were prepared for opal phytolith reference materials. APPENDIX D Results of vegetation sampling. Table 12. Results of vegetation sampling for site 28/29-1. Site 28/29-1 Sporobon hetero Zepis Eleocharis compressa Senecio paupercu has Poo compressa Hieracium‘piloselloides Sohizachyriwn scoparium Agropyron trachycaulwn Carex umbellata Ambrosia artanisiifolia Achillea millefoliwn Carex crawei ‘ Phleum’pratense Campanula rotundifo Zia Aster ptarmicoides- Bromus kalmii Scutellaria parvula Fragaria virginiana Geranium oaro Zimlanum Danthonia spicata Carex garberi Juniperus communis Juncus dudleyi Deeohcmpsia cespitosa. .Rammculus fascicularis Botriohium simp Zea: Veronica arvensis Tam officinale Carex richardsonii Poa‘ pratensis Geum triflorum Diohanthe Ziwn accuminatum Lathyrus paiustris Castilleja coccinea Arenaria stricta 190 rel. rel. imp. cover freq. cover freq. val. rank 36.7 93.3 42.0. 14.1 56.1 1 18.8 60.0 21.5 9.1 30.6 -2 7.6 90.0 8.7 13.6 22.3 3 5.4 73.3 6.2 11.1 17.3 4 2.3 53.3 2.6 8.1 10.7 5 4.1 23.3 4.7 3.5 8.2 ' 6 1.3 36.7 1.4 5.6 7.0 7 2.3 23.3 2.7' 3.5 6.2 8 .3 26.7 .3 4.0 4.3 9 1.0 16.7 1.1 2.5 3.6 10 1.7 6.7 1.9 1.0 2.9 '11 .5 13.3 .5 2.0 2.5 12 .4 13.3 .4 2.0 2.4 13 .5' 10.0 .5 1.5 2.0 14 .3 10.0 .4 1.5 1.9 15 .3 10.0 .- 1.5 1.8 16 .6 6.7 . 1.0 1.7 17 .2 10.0 . 1.5 1.7 17 .4 6.7 . 1.0 1.5 18 .4 6.7 .5 1.0 1.5 18 .4 6.7 .4 1.0 1.4 19 .2 6.7 .2 1.0 1.2 20 .1 6.7 .2 1.0 1.2 20 '.1 ‘ 6.7 . 1.0 1.1 21 .1 6.7' .1 1.0 1.1 21 .1 6.7 . 1.0 1.1 21 .1 6.7 . :1.0 1.1 21 .5 3.3 .5 .5 1.0 22 .4 3.3 .5 . 1.0 22 . 3.3 .3 . .8 23 . 3.3 .1 .5 .6 24 .1 3.3 .1 . . 24 <:.1 3.3 0.0 .5 .5 25 <.1 3.3 0.0 .5 .5 25 *87.6 660.0 99.8 99.6 199.4 Table 13. Results of vegetation sampling for site 28/33—1. Site 28/33-1 Sporobolus heterolepis Pba compressa Senecio pauperculus“ Eieooharis compressa Hieraciwn p75 LoseZ-Zoides Agropyron trachycaulum Fragaria virginiana Achillea millefolium Garex‘umbellata Phleum‘pratense SbuteZZaria‘parvuZa Ranunculus fascicularis Ambrosia artemisiifblia Bromus kalmii Sbhizachyrium scoparium Botriohium'simpler Deschampsia cespitosa Hypericumrperfbratum Gare: crawei maraxucum officinale Pba pratensis Chrex'richardsonii Chrez'garberi CbrastiuM’arvense Geranium carolinianum Danthonia spicata Chrex'merritt-fbrnaldii Juniperus communis Aster‘ptarmiooidea Juncus dudleyi smilacina stellata Dichanthelium'-acum£natum Sisyrinchium4montanum Lathyrus palustris Chetilleja coccinea 191 97.3 819.8 100.0 99.8 199.8 rel. rel. imp. cover freq. cover freq. val. ra fi_ 42.8 96.7 44.11.11.8 55.9 1 8.4 93.3 8.6 11.4 20.0 2 6.5 86.7 6.7 10.6 17.3 3 10.3 53.3 10.6 6.5 17.1 4 3.4 76.7 3.5 9.4 12.9 5 3.8 73.3 3.9 8.9 12.8 6 6.0 36.7 6.2 4.5 10.7 7 2.5 30.0 2.6 3.7 6.3 8 2.4 26.7 2.4 3.3 5.7 9 1.6 16.7 1.7 2.0 3.7 10 .4 26.7 .4 3.3 3.7 10 .4 23.3 .4 2.8 3.2 11 .3 23.3 .3 2.8 3.1 12 ' 1.1 13.3 1.1 1.6 2.7 13 1.3 10.0 1.4 1.2 2.6 14 .2 20.0 .2 2.4 2.6 14 .9 13.3 .9 1.6 2.5 15 .6 13.3 .6 1.6 2.2 16 1.0 6.7 1.0 .8 1.8 17 .2 13.3 .2 1.6 1.8 17 .6 6.7 .6 .8 1.4 18 .5 6.7 .5 .8 1.3 19 _. 6.7 .4 .8 1.2 20 . 6.7 .2 .8 1.0 21 . 6.7 .1 .8 .9 22 .3 3.3 .3 .4 .7 23 . 3.3 .2 . .6 24 . 3.3 .2 . .6 24 . 3.3 .2 . .6 24 .1 3.3 .1 .4 .5 25 .1 3.3 .1 . .5 2S .1 3.3 .1 . . 25 .1 3.3 .1 . . 25 .l 3.3 .1 .4 . 25 <.1 3.3 0.0 .4 .4 26 192 ‘Table 14. Results of vegetation sampling for site 29-2. Site 29-2 Sporobolus heterblepis. Eleocharis compressa Senecio pauperculus Poa compressa Hieracium piloselloides Hypericum perforatum Ambrosia artemisiifblia Ranunculus fascicularis Danthonia spicata Geranium carolinianum: Cerastium arvense Chrex’orawei Scutellaria parvula Fragaria virginiana Botrichium simp Zea: Sbhizaohyrium scoparium Carex’umbellata Juniperus commie Epilobium'ciliatum rm officina Ze Prunella vulgaris Sisyrinchium montanum Veronica arvensis Agropyron tmchyoaulwn Browns kalmii Phleum pratense Juncus dudleyi Polygala senega re1. rel. imp. cover'freq..c6Ver freq. val. rank 46.9 96.7 43.3 14.3 57.6 1 22-3‘ 83.3 20.6 12.3 32.9 2 14.0 90.0 12.9 13.3 26.2 3 10.6 96.7 9.8 14.3 24.1 . 4 1.8 40.0 1.7 5.9 7.6 5 1.5' 36.7 1.4 5.4 6.8 6 1.1 33.3 1.0 4.9 5.9 7 .8 33.3 .7 4.9 5.6 8 2.0 20.0 1.8 3.0 4.8 .9 .4 20.0 .3 3.0 3.3 10 ~.7 16.7 .7 2.5 3.2 11 1.4 10.0 1.3 1.5 2.8 .12 .9 13.3 .8 2.0 2.8 12 '.6 13.3 .5 .2.0 . 2.5 13 .1 13.3 .1 2.0 2.1 14 .7 6.7 .7 1.0 1.7 ~15 .7 '6.7 .6 1.0 1.6 16 .4 6.7 .4 1.0 1.4 17 .3 6.7 . 1.0 1.3 18 .2 6.7 . 1.0 1.2 19 .2 3.3 . .5 .7 20 .1 3.3 .1 .5 .6 21 .1 3.3 .1 .5 .6 21 .1 3.3 .1 .5 .6 21 .1 3.3 .1 .5 .6 21 .1 3.3 .1 .5 .6 21 .1 3.3 .1 .5 .6 21 <.1 3.3 0.0 .5 .5 22 108.2 676.5 99.9 100.3 200.2 193 Table 15. Results of vegetation sampling for site 33-2. Site 33—2 Sporobolus heterolepis Sbhizachyrium scoparium Eleocharis compressa Pba compressa Chrex crawei Fragaria virginiana Danthonia spicata Senecio pauperculus Hypericum perforatum Hieracium piloselloides Agropyron trachycaulum Cbmandra umbellata Chrex'umbellata carer richardsonii Arctostaphylos uva-ursi Aster ptarmicoides Bromus kalmii Prunella vulgaris Juniperus communis Deschampsia cespitosa Cbmpanula rotundifolia Achillea millefolium Chrex scirpoidea Ranunculus fascicularis PbegaZa senega SbZidhgo nemoralis Amelanchier sanguinea Aster'ciliolatus Lathyrus palustris Festuca ovina Sisyrinchium'montanum SbuteZZaria parvula rel. rel. cover freq. cover freq. 25.7 100.0 37.4 13.4 8.8 43.3 12.8 5.8 4.6 40.0 6.7 5.4 2.8 60.0 4.1 8.0 4.0 43.3 5.8 5.8 2.9 53.3 4.2 7.1 2.3 53.3 3.3 7.1 1.4 60.0 2.1 8.0 2.1 33.3 3.1 4.5 1.5 36.7 2.1 4.9 1.0 30.0 1.5 4.0 1.3 20.0 1.9 2.7 1.8 13.3 2.7 1.8 71.3 16.7 1.9 2.2 1.6 10.0 2.4 1.3 .9 16.7 1.4 2.2 .7 16.7 1.0 2.2 .3 16.7 .5 2.2 .9 6.7 1.3 .9 .3 13.3 .4 1.8 .3 10.0 .4 1.3 .3 10.0 .4 1.3 .7 3.3 1.0 .4 .1 10.0 .1 1.3 .1 6.7 .2 .9 .4 3.3 .5 .4 .2 3.3 .3 .4 .2 3.3 .2 .4 .1 3.3 .1 .4 <.1 3.3 0.0 .4 <.1 3.3 0.0 .4 <.1 3.3 0.0 .4 imp. val. 50.8 18.6 12.1 12.1 11.6 11.3 10.4 10.1 7.6 7.0 5.5 4.6 4.5 4.1 3.7 3.6 3.2 2.7 2.2 2.2 1.7 1.7 1.4 1.4 1.1 .9 .7 .6 .5 9.4 .4 .4 r 1 1 HODGQO‘U‘hHUNI—‘E 13 14 15 16 17 18 18 19 19 20 20 21 22 23 24 25 26 26 26 68.6 746.4 99.8 99.3 199.1 194 Table 16. Results of vegetation sampling Site 33-4 Sporobolus heterolepis Eleocharis corrpressa . Senecio pauperculus Pod compressa Hieracium‘piloselloides Carex umbe Z-Zata Agropyron trachycaulum Danthonia spicata Sbhizachyrium scoparium Scutellaria parvula Ambrosia artemisiifblia Fragaria virginiana carer crawei Aster ptarmicoides Juniperus communis Deschampsia cespitosa Aster pilosus Garex'garberi Cbmandra umbellata GeraniuM'caroZinianum Rosa aoicularis Taraancwn officinale Achillea millefolium Campanula rotundifolia Arenaria stricta Bromus kalmii Epilobium'ciliatum Ranunculus fascicularis Hypericum perforatzm Hieracium'aurantioum for site 33-4. rel. rel. imp. cover freq. cover freq. val. ran}:~ 33.7 96.7 45.1«-15.1 60.2 1 16.9 60.0 22.6 9.4 32.0 2 2.9 76.7 3.9 12.0 15.9 3 1.4 63.3 1.8 9.9 11.7 4 1.9 50.0 2.5 7.8 10.3 5 3.1 33.3 4.2 5.2 9.4 6 1.6 36.7 2.2 5.7 7.9 7 1.8 16.7 2.5 2.6 5.1 8 1.7 16.7 2.3 2.6 4.9 9 .3 26.7 .4 4.2 4.6 10 .6 23.3 .8 3.6 4.4 11' .9 20.0 1.2 3.1 4.3 12 1.4 13.3 1.8 2.1 3.9 13 .6 13.3 .8 2.1 2.9 14 1.4 6.7 1.8 1.0 2.8 15 .9 10.0 1.2 1.6 2.8 15 .4 13.3 .6 2.1 2.7 _16 1.6 3.3 2.1 .5 2.6 17 .2 10.0 .3 1.6 1.9 18 .1 10.0 ..1 1.6 1.7 19 .4, 6.7 .5 1.0 1.5 20 .1 6.7 .1 1.0 1.1 21 .4 3.3 .5 ..5 1.0 22 .3 .3.3 .4 .5 .9 23 .1 3.3 .1 .5 . 24 <.1 3.3 0.0 .5 . 25 <.1 3.3 0.0 .5 . 25 <.1 3.3 0.0 .5 .5 25 <:.1 3.3 0.0 .5 .5 25 <.1 3.3 0.0 .5 .5 25 74.7 639.8 99.8 99.8 199.6 195 Table 17. Results of vegetation sampling for site 34-1. lSite 34-1 Sporobolus heterolepis Pba compressa Sbhizachyrium scoparium Carex scirpoidea Juniperus horizontalis Eleocharis compressa Senecio pauperculus Danthonia spicata Hieracium piloselloides Arctostaphylos uva-ursi Prunus pumila Cbmandra umbellata‘ Aster pilosus Agropyron trachycaulum Artemisia:oampestris Arenaria stricta Fragaria virginiana Hypericum'perfbratum campanula.rotundifblia Ambrosia artemisiifblia Taraxacum officifiale carer crawei Bromus kalmii Lichanthelium’ acuminatum Achillea4miZZebeium Cares: merritt-fernald 'i Prunella vulgaris solidago nemoralis Potentilla fruticosa Deschampsia cespitosa Rhus aromatica .Zigadenus glaucus Cbrastium'arvense Juniperus communis rel. rel. imp. cover freq. cover freq. val. ran§_ 418.1 65.6 25.7 10.1 35.8 1. 4.4 56.2 6.3 8.6 14.9 2 5.4 31.2 7.7 4.8 12.5 3 4.4 40.6 6.2 6.2 12.4 4 7.0 12.5 10.0 1.9 11.9 S 5.4 28.1 7.6 4.3 11.9 5 2.4 50.0 3.4 7.7 11.1 6 3.2 40.6 4.5 6.2 10.7 7 1.7 40.6 2.3 6.2 8.5 8 3.4 15.6 4.8 2.4 '7.2 9 1.7 18.8 2.4 2.9 5.3 10 1.0 25.0 _ 1.4 3.8 5.2 11 1.3 18.8 1.9 2.9 4.8 12 .9 15.6 1.3 2.4 3.7 13 .9 15.6 1.2 .2.4 3.6 14 1.0 12.5 1.4 1.9 3.3 15 1.0 12.5 1.4 1.9 3.3 15 .9 12.5' 1.3 1.3 3.2 16 .7 12.5 1.0 1.9 2.9 17 .1 12.5 .2 1.9 2.1 18 .1 12.5 .1 1.9 2.0 19 .6 6.2 .9 1.0 1.9 20 .3 9.4 .5 1.4 1.9 .20 .5 ' 6.2 . 1.0 1.7 21 .2 9.4 . 1.4 1.7 21 .4 6.2 . 1.0 1.6 22 .4 6.2 .6 1.0 1.6 22 .2 6.2 .4 1.0 1.4 23 .2 6.2 .3 1.0 1.3 24 .6 6.2 .2 1.0 1.2 25 .4 3.1 .6 .5 1.1 26 . 3.1 .4 .5 .9 27 .2 3.1 .3 ,5 .8 28 . 3.1 .3 .5 .8 28 Table 17. continued. SLEQ 34-1'(cont.) carer umbellata symphoricarpos albus satureja vulgaris Apocynum'androsaemifolium Ph Zeum pratense Aster ptarmicoides Equisetum arvense Castilleja coccinea 196 rel. rel. imp. cover freq: cover freq. val. rank .2 3.1 .2 .5 .7 29 .1 3.1 .2 .5 .7 29 .1 3.1 .2 .5 .7 29 .2 3.1 .2 .5 .7 29 .1 3.1 .1 .5 .6 30 .1 3.1 .1 .5 .6 30 ‘<.1 3.1 0.0 .5 .5 31 <.1 3.1 0.0 .5 .5 31 70.2 682.9 100.1 99.9 200.0 197 Table 18. Results of vegetation sampling for site 34-2. Site 34-2 Pod pratensis Fragaria virginiana Trifolium hybridum Hieracium piloselloides Phleumypratense Pba compressa Cbmandra umbeZZata,- Chrysantheman leucanthemum Rosa aoicularis Arenaria serpyZZibeia Symphoricarpos albus Prunella vulgaris SbZidhgo oanddbnsis Achillea millefolium Apocynum androsaemifoliwn Hypericum perforatum Canpanula rotundifo Zia Tarmcwn officinale Aster‘giliolatus Amelanchier sanguinea Medicago lupulina Geranium carolinianum Satureja vulgaris Danthonia spicata cover 24.3 16.4 15.8 8.1 7.0 7.7 4.9 3.3 1.8 2.5 2.5 1.9 4.2 1.3‘ 1.2 1.5 1.3 .5 1.1 1.0 .6. .4 .3 .2 rel. rel. imp. freq. cover freq. val. rank 70.0 22.1 ~7.7 29.8 1 90.0 14.9 9.9 24.8 2 60.0 14.4 6.6 21.0 3 100.0 7.4 11.0 18.4 4 90.0 6.4 9.9 16.3 5 50.0 7.0 5.5 12.5 6 60.0 4.5 6.6 11.1 7 70.0 3.0 7.7 10.7 8 40.0 1.6 4.4 6.0 9 30.0 2.3 3.3 5.6 10 30.0 2.3 3.3 5.6 '10 30.0 1.7 3.3 5.0 11 10.0 3.8 1.1 4.9 12 30.0 1.2 3.3 4.5 13 30.0 1.1 3.3 4.4 14 20.0 1.4 2.2 3.6 15 20.0 1.2 2.2 3.4 16 20.0 .5 2.2 2.7 17 10.0 1.0 1.1 2.1 18 10.0 .9 1.1 2.0 19 10.0 . .5 1.1 1.6 20 10.0 .4 1.1 1.5 21 10.0 .3 1.1 1.4 22 10.0 .2 1.1 1.3 23 109.8 910.0 100.1 100.1 200.2 J Table 19. Results of vegetation sampling for site 34-3. Site 34-3 Danthonia spicata Hieracium piZoseZZoides Fragaria virginiana Arctostaphylos uva-ursi Pba pratensis AchiZZea millefoZiwn Comandra umbeZZata Hieracium aurantioum Pba compressa Chrysanthemum leucanthemum Phleum pratense Agropyron trachycaulum Satureja vulgaris Aster ciZioZatus Ccmpcomla rotundifo Zia PruneZZa vulgaris Trifolium hybridum Hypericwn perforatum Mbdicago ZupuZina symphoricarpos albus Bromus kalmii Carex umbeZZata Anemone canadensis Arenaria serpyZZifoZia Agrostis gigantea PopuZus tremuloides Chrastium’arvenss Taraxacwn officinale 17.1 12.2 11.1 15.1 8.5 6.9 4.9 4.5 5.2 4.0 3.1 1.8 1.3 2.3 1.8 1.0 2.6 .8 2.2 .7 .6 rel. rel. imp. cover freq. cover freq. val. rank 86.7 15.5 7.3 22.8 1 100.0 11.1 8.4 19.5 2 100.0 10.1 8.4 18.5 3 40.0 13.7 3.4 17.1 4 93.3 7.8 7.8 15.6 5 73.3 6.3 6.1 12.4 6 80.0 4.5 6.7 11.2 7 80.0 4.1 6.7 10.8 8 60.0 4.7 5.0 9.7 9 66.7 3.6 5.6 9.2 10 53.3 2.9 4.5 7.4 11 46.7 1.6 3.9 5.5 12 46.7 1.2 3.9 5.1 13 33.3 2.1 2.8 4.9 14 33.3 1.6 2.8 4.4 15 33.3 .9 2.8 3.7 16 13.3 2.4 1.1 3.5 17 33.3 .7 2.8 3.5 17 13.3 2.0 1.1 3.1 18 20.0 .7 1.7 2.4 19 20.0 .5 1.7 2.2 20 13.3 .6 1.1 1.7 21 13.3 .4 1.1 1.5 22 13.3 .1 1.1 1.2 23 6.7 .5 .6 1.1 24 6.7 .1 .6 .7 25 6.7 .1 .6 .7 25 ' 6.7 .1 .6 .7 25 109.8 1193.3 99.9 100.2 200.1 Table 20. Results of vegetation sampling for site 34-5. Site 34-5. Sp'orobo Zus hetero Zepis Hieracium piZoseZZoides Carer scirpoidea Hypericum perforatum Schizachyrium scoparium Poa compressa Danthonia spicata Agropyron trachycaulum Fragaria virginiana Carex wnbeZZata Campanula rotundifo Zia Senecio pauperculus Comandra umbellata- Arenaria stricta ‘ Apocynum androsaemifoZiwn ’ Prunus pumila Cerastium arvense ArctostaphyZos uva-ursi Aster ptarmicoides Carex richardsonii Bromus kalmii Synphoricarpos albus Rhus aromatica Rosa acicu Zaris EZsocharis compressa AmeZanohier sanguinea Juniperus horizonta Zis Juniperus conmunus Tragopogon pm‘tensis AchiZZea millefolium Deschampsia cespitosa Scutellaria parvula Ranunculus fascicu Zaris Potentilla fruticosa rel. rel. imp. cover freq. eager freq. val. rank 23.6 86.7 33.2 11.7 44.9 1 5.1 66.7 7.2 9.0 16.2 2 8.1 33.3 11.4 4.5 15.9 3 5.5 '50.0 7.7 6.7 14.4 4 5.0 46.7 7.0 6.3 13.3 5 3.0 63.3 4.2 8.5 12.7 6 3.7 46.7 5.2 6.3 11.5 7 2.0 46.7 2.9 6.3 9.2 8 2.5 36.7 3.5 4.9 8.4 9 1.8 26.7 2.5 3.6 6.1 10 .8 36.7 1.2 4.9 6.1 10 .9 33.3 1.2 4.5 5.7 11 1.2 23.3 1.7 3.1 4.8 12 ' 1.1 23.3 1.5 3.1 4.6 13 .7 16.7 .9 2.2 3.1 14 1.2 10.0 1.6 1.3 2.9 15 .4 16.7 .6 2.2 2.8 16 1.1 6.7 1.5 .9 2.4 17 . 10.0 .8 1.3 2.1 18 . 6.7 .6 .9 1.5 19 . 10.0 .2 1.3 1.5 19 .6 3.3 .9 .4 1.3 20 .S 3.3 . .4 1.1 21 .1 6.7 . .9 1.0 22 .3 3.3 .4 . .4 .8 23 .2 3.3 . .4 .7 24 .2 3.3 . .4 .6 25 .1 3.3 . .4 .5 26 .1 3.3 . .4 .5 26 .1 3.3 .1 .4 .5 26 <.1 3.3 0.0 .4 .4 27 <.1 3.3 0.0 .4 .4 27 <.1 3.3 0.0 .4 .4 27 <.1 3.3 0.0 .4 .4 27 71.1 743.2 99.5 99.2 198.7 Table 21. Results of vegetation sampling for site 36-6. Site 36-6 Fragaria virginiana Pba compressa Chrysanthemum leucanthemum Senecio pauperculus Hieracium'piZoseZZoides Hypericum‘perfbratum Phleum‘pratense PruneZZa vulgaris Achillea millefolium Pbajpratensis Carex richardsonii Amelanchier humiZis Danthonia spicata Carex umbeZZata ‘ Taraxacum officinaZe Agropyron trachycaulum Aster pilosus Rosa acicuZaris Cbmandra umbeZZata~ rel. rel. imp. .2239: freq. cover freq. val. 7.4 90.0 23.4 12.3 35.7 9.8 100.0 13.2 13.7 26.9 6.8 90.0 9.1 12.3 21.4 6.8 90.0 9.1 12.3 21.4 8.3 60.0 11.2 8.2 19.4 6.5 70.0 8.7 9.6 18.3 3.1 40.0 4.2 5.5 9.7 p 3.1 40.0 4.2 5.5 9.7 2.0 30.0 2.7 4.1 6.8 2.8 20.0 3.8 2.7 6.5 1.5 20.0 2.0 2.7 4.7 2.0 10.1 2.7 1.4 4.1 1.0 10.0 1.3 1.4 2.7 .9 10.0 1.2 1.4 2.6 .9 10.0 1.2 1.4 2.6 .6 10.0 .8 1.4 2.2 .6 10.0 .8 1.4. 2.2 .2 10.0 .3 1.4 1.7 .1 10.0 .1 1.4 1.5 mmqmmmbuwuwg 553(55'6 #0 h‘ u: a. 74.4 730.0 100.0 100.1 200.1 3‘ 201 Table 22. Results of vegetation sampling for site 36/31-1. Site 36/31-1 Sporobolus heterolepis Pba compressa Senecio pauperculus Hieracium piloselloides Phleum pratense AchiZZea miZZebeium Cerastium arvense Aster‘piZosus Fragaria virginiana Pba pratensis Agropyron trachycauZum Iribeium hybridum Carex’umbeZZata Eleocharis compressa Deschampsia cespitosa Rbsa acicuZaris Aster ptarmicoides Ranunculus fascicuZaris Danthonia spicata Carex merritt-fernaZdii ArctostaphyZos uva-ursi Arenaria stricta campanuZa rotundibeia Chmandra umbeZZata. Zigadenus gZaucus .RruneZZa vulgaris Chrysanthemum Zeuoanthemum lhraxqcum officinaZe Sisyrinchium montanum Agrostis gigantea smiZacina stellata Aster ciliolatus rel. rel. imp. cover freq. cover freq;val. rank 21.0 46.7 19.2 5.7 24.9 1 13.6 83.3 12.4 10.2 22.6 2 11.7 86.7 10.6 10.7 21.3 3 7.3 70.0 6.6 8.6 15.2 4 6.2 66.7 5.7 8.2 13.9 s 6.3 56.7 5.8 7.0 12.8 6 4.2 53.3 ’ 3.9 6.6 10.5 7 4.5 26.7 4.1 3.3 7 4 8 5.0 13.3 4.5 1.6 6.1 ' 9 3.3 23.3 3.0 2.9 5.9 10 2.4 30.0 2.2 3.7 5.9 10 3.5 20.0 3.2 2.5 5.7 11 2.4 23.3 2.2 2.9 5.1 12 4.3 6.7 3.9 .8 4.7 13' 1.9 13.3 1.7 1.6 3.3 14 1.3 16.7 1.2 2.1 3.3 14 1.2 16.7 1.1 2.1 3.2 15 .4 23.3 .3 2.9 3.2 15 1.7 13.3 1.5 1.6 3.1 16 .5 16.7 .5 2.1 2.6 17 2.3 3.3 2.1 ..4 2.5 18 .4 16.7 .4 2.1 2.5 18 .7 13.3 .7 1.6 2.3 19 .6 13.3 .5 1.6 2.1 20 .4 10.0 .4 1.2 1.6 21 .7 6.7 ..7 .8 1.5 22 .7 3.3 .6 .4 1.0 23 .1 6.7 .1 .8 .9 24 .1 6.7 .1 .8 .9 24 .2 3.3 .2 .4 .6 25 .2 3.3 .2 .4 .6 25 .1 3.3 .1 .4 .5 26 Table 22. Continued. Site 36131-1 (cont.) Equisetwn arvense Satureja vngaris Lathyrus palustris} Hypericum perforatum Artemisia campestris 202 rel. rel. imp. cover freq: cover freq: val. rank .1 3.3 .1 .4 .5 26 .1 3.3 .1 ,4 .5 26 .1 3.3 .1 .4 .5 26 <.1 3.3 0.0 .4 .4 27 <.1 3.3 0.0 .4 .4 27 109.5 813.1 100.0 100.0 200.0 203 Appendix E. Table 23. Species lists for sites surveyed in 1984. 01000001011010000110010011100011010000011011100001000101100110100010000100100000 IIIIt'llIIIlilil'lll'lDIOOIIIIOIIIOOIOI'IOIIIIIIIIOIDIIIOIIOII'lllllllllllllllll 01000111101010001100110000000101010010011000000001010011000100000010110000000000 OIIOIIOIIIf!!!'0'!!!OIIIIIOOIOIIIDIllill'lllllllIDIOIUIOIOIIIIlllllllltltlilllli 11000111000010001010000100000101000010011000000001010001010100001010000000000000 If!villi!!!001000.!!!"U'IO'I'O'DOI'O'OII'IO0'UIIIOOIOIIOIII'IIO'OIIIII'IOIIOIIIO 11000001110011001100010000000001001010111000100001100011010100011011100000000000 It!!!IIIIIIIOIODIOOD9'0IIOIOOIOOOI'll!IIIIOOOII'IIOI'III'IIIII'lilllllllllllllll 11000100100000101110010000001001000110011010111001010010011101001011000000101011 III!!!I!IIIIIIIOOOIDIDI9'00!!!I'llllllI'llllrllllllllllllllilIIIOIOIIOIII'OIIIIO 11000101010011101110010010001001000110011010101001110011010100001011110000100101 I00000IIIIII!!!00"!IIII'llllililllllllillil'I'DlllllrlllilllIIOOOOOIIOIOIIOIIOO 11000100100011100110010000001001000110011010101001010011010100001011000011000001 It'll!IIIIUIIOOIIIIIIOIIIDOOIIIOIII0010'!!!I'IIIIOI'IIIIOOOOIII'IIIIIIIIOIOIIIOO 11000100101011101110110000000101000010111000110011010011011100001011110000001000 I'D0IfII0"I'l'lillill'll'OIDIOIIIIOIIIll!!!IIIIIOIIIIII'IIIIIlllllillllllllilll 11000100010010101110010010011001000110011010010001010011010110001011100100000011 '0'OI!IO0'00!!!OIOODIIIIOIIIOIIIOOOIII'I'll!OOIIOOIDIOOIIOIODllltlltllllllrlllll 11000100100001001000010000000001000110010000000001010011010100001111000000000000 IIlI!'00OOIODI'IIDI'IOIIIIDIOOOOOIIIIIOIIIIIIIIDDUIIIIOII'IIIIllllllllllilllllll 10000l10100011001000010000000000000010001000000001010011010000011001000000000000 I?!I00"!I'll!!!'O'DIDOIOI'IIIOOOIIIODIllllllllllllll(I'll!!!It'llllllllltilllil 110011011111111110101100100000110001100110101.001010100110101111110110101101.1000... I'IIIIIIIIIIIOIDOOIDOIIOOOOIOOOIIIIIIOIOIIOIOIt'lllllllllllliOI!It'lllllllltllll 1111100101.0000111110110110000011011110011010110011010011000111001.011000110110001 I!!!)000000!!!000070009000!!!IDOIIIIII'OIIOOOOODIIIIOI'lIIIIIIlllllillllllllll'l 11001000000000101110110010000001000100011010111001010001010100001011000010000001 llllliililllllOOOIIIIOIOOOOOIIIOOIIOIOIIOIIIOlttlllllllllllllIIIIOIIIOOIIIIOIODI 1100l1010000101001100100100011010001000110101.01011010011011100001.011100010100001 III'IIOO'OI'IIl0OOOIOIIOOOIIIOI'I'IOI'OOPIIOOIOOOOIIIvilli!!!It!Illllltlllllill' 11001101100010101110111010000011010000011010100011010001010110001010010000100001 OOIOOIOOIO'OID000000!!!IOIOOOIOIOOOOII'IOOOOII'llillll'ltllllOIIIIIUIOOIII'I'IOU 11001001000000100000000010001000010100011010101011010001000100001011000010100001 00'!!!OOOIO'IIII'IIOOOOIOIOIIIIOOIDIIIIOIIII'!III!!!010000100r00Illllvlllllllilo 11001100010001100110010000000010000000000010101001010011001100001011000000110001 IllI00'0'00007IIIOOIIOIIOOI'IIIIOOII'lllllvoIIIIIIIIIIOIOIIIIIIIOillllllllllllll 01000001010010000000100010000010010000011010100001010001010110000011110100100000 It!!!I!IOOIIOIOIII00"!!!0'00000000'IlirllvlIllllllllllllllllOOOIOIIIOIIIIOIIOII 11001001000011101000010010000011000100101000101001010011010100001011000010100001 IIIllIIOIOOOOIOIIIIOOI"00!llllllilvllllllllllllllllI'llOOIIIIIIIIIIIOOIOII'IIOO 110011010101111011101100100010010101001100101010110100110101010010110100101.1000... Ill0'l0"!00101000'00000090I'lltillllll'llll'l'll'llvlllliIllIllIIOOUIIIIOIIIIIO 110111011100111011111100110011110101111111111110111110110111011110111101101.1000]. IIIll!I000"IfIIIIOIIOIII!IIDOIOIOI'I'IOOOOOIIIOIIIDOIIIIIDII0!!IDOIIIIOIOIIIIIO 1.1101100100000100000011001000100.1000100011000100011010011000101.001.011100000000001 I!!!IIliltilllllllll0"'0IIOOIOIIOOIIOIIIOIIDOIIIIDOI'lllllllllllllllllllvllllli 01000000110010100010010010000011000010011001100001100001000110000011000100010001 I'll!IIt'll!!!lili'l'l'IllicilllllllllillllIlllllllllllllllllll!Illlllllllllllll 11010101010010001010110010000010000010011000100001000001000110000011110100100001 lI'llillilltllI'lllllllllllIIIOII'IOIIIIIIII'llilllllllllllllIIIOIOOOIIIOOOIIIII 11000000010000000010000010000000000000010000100001010001010110001010000100110001 IIIIOIIOIOOIIID00000000I'll'l'llll'lllillllill'lI!!!I'llllltlIlllllll'llllllllll 11000000010010100110110011100010110000011011100001010001110110100011110100000001 III!0DI'IIOII'OllillllllillillliillI'lliilllllllllll'l'll'll'IllIlllllllllllllll 11000010011010000100110011000111010110011011100001000001011111001011001100100001 I'll!!!It'll!It!!!000001!!!IIIOOIIIIIIIOIIIIIIIIIIIIIllllllllIllIlllllilllllllll 1100010010000010011001001000101100011001101010000101001101111000lOllOOOOlOOOOMOl « a __ _ a _ _ u a 1 1 S ma 3 O a U 0 ud t C t C l [.1 a .1 a S u era d n a I u n b? no e n o T a I r a r. a e t l dha C .1 a F. ca a r. C e m n n3 1. 0 No.0 0 1 o u m 0 as P ucrn P 9 r m u m Ie . s a i.aci s n a i e t Y s r r 3 8m .1 lrvmsa S .1 av .1 .h a X e . S .P a .1 u la 03 [1 r. .1 d t a? a m m .1 m re V r. Tl oe fvs ul 3 E 1a .1 n 51a 5 u u1 m I u as ad a uu n .1 .1..O .1 or a a a omS m aTln Comu a C a 3 asc V m 1. .la iisammsraf r .3 f0 nel ea C a tus mu.nia alut SCSI _t e no.1 . u u 1C53.1U.1teunaV.1 t [88 .11 I1 nseu ta alceeucralwl ollna T1n1ha a 71C0: Stan C oYiesgscacevulassadi df efina .1059 at Pcrstelailn atear norPn 1. .1 riearlanisi fhltinneSid 1C8UV1I “.1 afoea Clnle la sapnalvne,1 tnsio u2t1.1eO OmaLetVtrvalic ecanmaeloraasYCPt oa uva rr.sdtacue silcae meil inlmaaomfimiselse 1 surca .lirs lamaesdgrintoplmascgltre ifootdialocvmnieitcmovlaagkoulrlermruduncasuenroeganuca lregt aedbaulrraluilioanirlltrolucaruelbpo ucr.19nrcrrruiamfieoolaPensimnafnr 1.1036? .ICY.1rrnnn.1CSYeCC05mUmrBaeerfliaPld mamv1m5ra.1 dC .1.1.laOtaDL.K lChfllUtassee H.193 m hiaea as rhss iorvl twbeirhreia eriu rils mvvbcls d Bilalenrsaaaavmr 33 n ica aiP alla aaesartxrcibrziamhah aaselmmuo f mmmmuss h r ret 111 ulmuu aossah immihaaaiiitaklnarfinagicmieeut aicPhruur amfliauuuuduus 0 Opt allllanull erilfceruug tiiscppe uiCC 11mrsuv1r1nmmrn mtatitaiuurliicfic rru 9 masliiiil .luu 1Yttsnnannessrr1 rsnm lutauudosanhebscriltrCCllseermamaoruattttISSdCC IpssoaonYYliroaamrrraU&6XXXXXXXXXX.18$S.1.1nhUhacsoauann eaarruppYUCUCCplgnnnneUU.Inn .1ooorlmeccebtnneeeebm deeeeeeep;;::taYssatcchoilctflaamcrreeciihiien" uuYeeeennnruu hrrrbeetoouaceettttromrrrrrrrrrrrsnrrrrmnusceuiusarquee PnnntldlaaaPlttttuuuenn C991mmnnPBSrrrrrsssiraaaaaaaaaaaaaeehirloaaellgprere891.11 .WLuuuaiehloooooooorrrtaa AAAAAAAAAAAAAAAAAAABBCCCCCCCCCCCCCCCCCCCDDDDEEEEFFGGGGnHHlJJJLLMPPPPPPPPPPPPPPRR 204 Appendix E. Table 23. Continued 00000100111101001100010000010100000 I!It'll!I!I'I'IlI'llfill'lllliili'lll 100010000101100000001000010000000000 0'l""""""'lllllll['Oll"""" 00000001101101101000000011100001010 III'llIII!IIIOIIIOIIIIIOIOIIOIIIOIII 000100001101100001001000010000000000 IIl'l'll0'I'l'lll'll'l'll'llllllllI, 100101001101000110010100010000000100 I!10"!0"I'l".I'lllll'lil'll'O'li' II0'I'llilllllllllllll0000000100900! 110010001101101000001000110100000010 OII01",ICUIIOUDOII'UII'IOIIII'0'0'0 100010001001001010010100000000000000 IllI'lllll'09'9000090'00020000,9009! 100000010000000000001000001000000000 " "" ' O " ' 0" """" ' """ ' "' O " 100100010000100000000000001000000000 ll0'00!llillllllillilllllil'lI900!!! 100010001111010011011101000000110000 IIl0"I'llI'lll'lllllllllIDOIDIDO'II 000110000111001011110000000001001001 0000'!IIIOOIIIOIO'IOOIIIIIIIIIIIDIO' 00010001111010000010101000000001000 IIl'l'll'll'l'l'll'l'llllI'llI'II'I' """""""""""'""""""' 001.001000111011000010.100000000000000 I!IllllllillllllllllllllllIOOOODOOOL 000010001111010001010100000000001001 IIIIOIIIOIIIIOIO'IIII'I'0.000.09'9'0 rnvoo0000001501.006.30OOnUcinuooooooonvooooooo ll""""'""'"""""""""" 00010000111101000001.0100000100001001 lllltillilOlllillllllllllllll00000.0! 100100001111010100010100000000001001 I,I""l0"0"""""""""""" 00000010011100000001.0000000000000000 IIIllil'tllil'llillltlIt'lllllilllil 000100100101101111010000000000000000 I'llililllI'll!!!)IIODIOIOIIIOOIIO'I 0"IOIIIOIIIIIIOODIIIIIOIIOIIDIOIIII 000000110111011011011101000010001000 000070000!It'llllilll'IIIIOOIDIOIIOI 000000111111001011011110000000000000 lll'll'll'IOIIIOIIIIIOIOOII'IIOI'0'! 000101001101001000010000000000001001 Site 1 2 3 4 5 6 7 8 9 n.n D Rhus aromatica Rhus glabra 4 #— peregrina giniens1s ybridum tense spicatum var. mo1Ie dentalis ium pra glochin maritima 1a occi folium repens if ‘r— Tr1folium h IrifOI Tri Satureja glabella var. an ustifolia Satureja vulgaris Trichostema brachiatum Taraxacum officinale m Zigadenus ggaucus Tragogogon pratensis __‘ Ribes oxyacanthoides Rosa acicularis Schizachyrium scoparium Scutellaria parvula Shepherdia canadensis Si1ene antirrhina Sisyrinchium montanum Smilacina stellata Sporobolus heteroTepIs Symphoricarpos albus Verbascum thapsus Verbena simplex Veronica arvensis Rosa blanda Senecio pauperculus Solidago canadenEis Solidago nemoralis Solidago ohioensis Rumex crispus Saxifraga vir Trisetum Veronica Vicia americana . —1—— Tri LEGEND TO SITE NUMBERS 1 . 1 673245678 ../...... 456666660 333333332 ..uasuunu 123456789 222222222 2 t i 8 415234152 ._....... 922333444 233333333 -.--.-.- 123456789 111111111 9 t .1 S 11 .. 2 493 .21234223 6.._._.// /00000788 532222222 sass-u..- 123456789 6 t i S 34-3 20- 10II 29-2 205 Appendix F. Notes on the sites surveyed in 1984. Site 5/6-2 20-1 20-4 32-5 33-3 35-7 36-2 36-5 36-7 36-6 Notes Appears to be wet for the most part; cutting on edges; poor quality, weedy. Has sporobolus and Schizachyrium on rise near rocks at north end. Very shallow soil, cobbles, some pavement in spots. ORV trail through site; some pavement; wet edge. Edge near road rather moist. ORV trail On south and southeast sides. Quite weedy; some aspen in middle of site; south side of road is better. Slopes down to north; many down trees; rather weedy. Edges are better that middle of site, disturbed. Much Hieracium; many down trees. Carex richardsonii and Schizachyrium around juniper and dead Picea in center; most of site weedy. 206 Appendix<3 Calculated similarity values. Table 24. Sorensen index of community similarity calculated for sites examined in 1984 Sorensen's index of community similarity 2 3 58 73 4 55 59 59 5 59 64 67 60 6 63 63 63 69 68 7 72 52 50 53 49 55 8 65 65 65 44 58 44 59 9 69 59 59 56 57 51 68 78 10 70 56 54 55 54 54 69 65 80 11 56 62 68 64 73 62 48 50 54 53 12 68 56 58 61 51 54 64 60 73 73 46 13 65 55 55 61 50 50 70 60 69 70 61 62 14 70 64 68 60 65 59 63 66 76 68 60 68 66 15 79 63 61 56 57 53 77 71 83 81 54 77 75 75 16 72 60 64 60 50 56 68 63 75 77 52 72 72 72 79 17 69 65 61 54 66 58 59 69 72 65 57 65 62 73 69 68 18 63 67 65 56 63 59 60 79 75 67 56 65 57 72 67 69 72 19 44 33 28 25 39 30 38 39 39 44 27 33 25 38 38 33 30 43 20 55 43 35 40 38 40 53 44 49 49 34 42 37 46 45 48 40 51 71 21 73 64 62 57 62 58 65 62 65 59 57 58 55 67 68 70 65 68 46 57 22 61 54 49 38 53 46 58 64 59 55 47 52 41 62 60 58 52 61 51 58 64 23 82 56 54 49 51 57 67 65 75 73 44 68 59 64 79 72 60 63 51 62 71 61 24 71 58 58 53 64 55 66 69 76 73 56 69 60 65 77 68 60 67 52 56 72 63 73 25 75 57 47 48 53 48 68 67 69 61 41 61 58 60 70 67 59 62 44 54 87 65 73 72 26 58 54 47 43 59 55 56 56 57 56 61 50 49 40 52 59 51 52 58 59 56 69 63 67 57 27 55 49 41 45 56 41 32 48 49 52 46 43 42 56 56 57 47 47 50 52 53 64 55 58 51 61 28 47 49 44 32 54 45 51 50 49 42 53 38 36 60 49 46 45 54 51 56 54 73 50 54 49 65 62 22_47 67 69 52 61 62 34 48 47 42 61 44 45 60 48 43 56 55 22 27 48 43 40 46 37 47 43 50 Site 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 Key to site numbers: site locality site locality site locality 1 5/6-2 11 29-4 21 34-6 2 30-2 12 32-1 22 35-7 3 20-1 13 32-5 23 36/31-1 4 20-2 14 33-2 24 36-2 5 20-3 15 33-3 25 36-4 6 20-4 16 33-4 26 36-5 7 27-24 17 34-1 27 36-6 8 28/29-1 18 34-5 28 36-7 9 28/33-1 19 34-2 29 20-8 10 29-2 20 34-3 207 Appendix G (continued) Table 25. Horn's index of community similarity calculated for sites examined in 1983. Horn's index of community similarity .80 .72 .83 .72 .82 .89 .66 .64 .67 .80 .73 .83 .94 .93 .71 .82 .83 .68 .70 .62 .67 .37 .35 .21 .34 .56 .22 .41 .68 .76 .88 .88 .68 .93 .63 .19 .21 .24 .14 .30 .52 .18 .29 .67 .16 .33 .38 .26 .49 .63 .34 .42 .62 .35 .66 Site 1 2 3 4 5 6 ‘77 8 9 10 HOW‘DQO‘UIth P'F‘ Key to site numbers: site locality 34-1 33-2 33-4 28/33-1 36/31-1 28/29-1 34—5 34-3 29-2 34-2 36-6 wamqmmowww I-‘O "‘11“11111111'1117113