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http://www.archive.org/details/cu31924003974148 


ane Mormeree Lime nce , omer H.H.Bennett,Photo, 
/ POTSDAM SANDSTONE, 


Stand Rock Dalles of the Wisconsin. 


GEOLOGY 


OF 


WISCONSIN. 


SURVEY OF 1873-1877, 


VOLUME II. 


Part I. HISTORICAL. 
II. EASTERN WISCONSIN. 
Ill. CENTRAL WISCONSIN. 
IV. LEAD REGION. 


ACCOMPANIED BY AN 7 


ATLAS OF MAPS. 


PUBLISHED UNDER THE DIRECTION OF THE | 


CHIEF GEOLOGIST, 


BY THE 


COMMISSIONERS OF PUBLIC PRINTING 


IN ACCORDANCE WITH LEGISLATIVE ENACTMENT. 


1877. 


SErrerT, GUeter & Co., MILWAUKEE, 


Davip ATwoop, MADISON, 
LITHOGRAPHERS. 


STEREOTYPER AND PRINTER. 


To His Excellency, the Hon. Harrison Luprneron, 


Governor of Wisconsin. 


Sir:—It affords me great pleasure to submit the following contri- 
bution toward the final report of the Geological Survey.of Wisconsin, 
begun in the year 1873, and still in progress. The manuscript for 
the remaining volumes is in part prepared, but the completion of 
certain portions is dependent upon field work now being prosecuted, 
and must await its conclusion. An earnest effort will be made to 
complete the series at as early a date as the proper execution of the 
work will permit. 


Most respectfully, your obedient servant, 


T. C. CHAMBERLIN, 


Chief Geologist. 
Bexorr, August 8, 1877. 


PREFACE. 


Tue Law, under whose authority the reports of the Geological Sur- 
vey are being published, determines the character of one volume, 
which, from its nature, will most appropriately form the initial vol- 
ume of the completed series. But as it involves general conclusions 
that can only be arrived at after the completion of field work, its ap- 
pearance must be delayed until that work is accomplished. It was 
not deemed advisable on this account, however, to defer the publica- 
tion of such portions as could be finished, and the present volume, 
although nominally the second of the series, appears first in the order 
of time. 

Although its size has been expanded beyond what was originally 
intended, and a large portion of its matter printed in a smaller type 
than is desirable, it has been found impossible to include all the ma- 
terial that has been gathered relating to the regions reported upon, 
and a considerable amount of manuscript relating to each of the dis- 
tricts has been necessarily omitted, and other portions condensed to 
an undesirable brevity. It is believed, however, that, notwithstanding 
this, a creditable degree of thoroughness and fullness has been attained, 
and that, by the assistance of the ample maps and profiles that accom- 
pany the volume, an adequate knowledge of the structure of any 
locality may be obtained. 

The law authorizing the survey requires the construction of a sin- 
gle map upon which shall be represented all the geological forma- 
tions of the state. A map based upon a scale of fifteen miles to the 
inch, is the smallest upon which this can be successfully accomplished, 
and this fact has determined the form and dimensions of the accom- 
panying atlas, whose sheets have the size requisite for such a map. 

A seale of three miles to the inch is the least that is at all adequate 
to the proper representation of the detailed mapping of the formations, 
and this scale has been uniformly adopted. for the more elaborate ge- 
ological maps. It was found that the surface of the state, on this 
scale, was readily and economically divisible into rectangles of the size 


vi GEOLOGICAL SURVEY OF WISCONSIN. 


indicated, and these constitute the Area maps of the atlas. Seven of 
these cover the territory reported upon in this volume. At least an 
equal number will be required for the regions yet to be reported upon, 
and these will be numbered consecutively with those now published, 
so that the whole series, when complete, may form a single portfo- 
lio. The contour lines of the topographical maps of the Lead region 
required the still larger scale of one inch to the mile, and five plates 
are devoted to them. 

It may be unnecessary to state that the construction of an ordina- 
ry surface map is no proper part of the work of a geological survey, 
and the geological corps cannot justly be held responsible for errors 
of a merely geographical nature. When it is considered that the 
original provisions of the law required the examination of more than 
13,000 square miles each year, it will be evident that no work of that 
kind was contemplated. But a correct geographical map is highly 
important to accuracy in the delineation of the formations sketched 
upon it, and hence the corps have labored under some annoying dif- 
ficulties growing out of the inaccuracies of the original government sur- 
veys, and of the maps in common use. To overcome these difficulties, so 
far as possible, the Area maps have been built up, township by town- 
ship, from the notes of the original linear survey of the government, 
and comparisons instituted with state, county, township and special 
maps, and with the observations of the geological corps. The townships 
and sections should be, setting aside the convergence of the meridi- 
ans and the trivial effects of sphericity, perfect squares, and cover the 
state with a symmetrical network of lines, but it will be observed 
that there are marked departures from this form in some cases, due 
to errors in the linear survey, and an effort has been made, by care- 
fully representing these on the maps, to restore the natural features 
to their true form and position. 

The areas mapped as Wet Lands are essentially those given on the 
government plats as marshes, but that term is not now properly ap- 
plicable to a considerable portion of the surfaces so designated, since 
most of them are so firm that they may be readily traversed by teams, 
and some are even cultivated with success in all except very wet sea- 
sons, and are, indeed, among the most valuable lands of the state. In 
the great majority of cases, except where they are fluviatile meadows, 
they represent extinct lakes, and hence their historical and geologi- 
cal significance is important. 

The survey has been put under great obligations by the kindness 
of citizens and corporations in rendering valuable aid in various ways 
in the prosecution of the work. In addition to the more specific ac. 


PREIACE. vii 


knowledgments that have been made in connection with the annual 
reports and in other appropriate ways, the corps desire to tender this 
general expression of their appreciation of the numerous courtesies 
of which they have been the recipients. 

It is dne also to those whose results do not appear in an individual. 
ized form, to call attention to the analytical work of Prof. W. W. 
Daniells, of the State University; of Mr. Gustavus Bode, of Milwan- 
kee; and of Mr. E. T. Sweet, recently of Madison; to the paleonto- 
logical identifications of Prof. R. P. Whitfield, of New York, and to 
the drafting of Prof. W. J. L. Nicodemus and Mr. A. D. Conover, of 
the State University. 

An expression of indebtedness is also due Prof. R. P. Whitfield, 
Ton. Geo. H. Paul, Prof. A. Salisbury, G. D. Swezey, J. H. Cham- 
berlin and C. 8. Bacon, for reading portions of the proof on subjects 
with which they are especially familiar. 

The provision which has been made by the commissioners of pub- 
lic printing for the publication of the work has proved wise and 
judicious, as well as highly economical. 

The mechanical execution of the work is the best witness that can 
be offered as to the skill and faithfulness with which the printers and 
lithographers have performed their respective tasks. The execution 
of large geological maps is confessedly a work of much difficulty, and 
great credit is due the lithographers for the obliging and liberal man- 
ner in which they have performed their work. In several instances 
they have exceeded the requirements of their contract. 


TABLE OF CONTENTS. 


Lerrver oF TRANSMITTAL, - = = = = = = © © « tt 
PREFACE, - = = = = = = = 8 = © 2 2 2 
PART I. 

HISTORICAL. 

PREFATORY NOTE, - - Bo = oe JR Se Oey. So 8) 


ANNUAL REPORT FOR 1873. 
BY I. A. LAPHAM. 


Law of the Survey — Organization of the Corps — Prof. Irving’s Party — Prof. Cham- 
berlin’s Party — Mr. Strong’s Party —Mr. Wilson’s Map — Practical Importance 
of Geological Knowledge — Mr. Edgerton’s Survey —Topographical Survey — 
Railroad Elevations — Elevation of Lakes — Elevation of Summits — Government 
Surveys — Catalogue of Minerals — Mineral Waters — Rain Fall — Relation of the 
Geological Survey to Agriculture — List of Maps Accompanying the Report, 5-44 


ANNUAL REPORT FOR 1874. 
BY I. A. LAPHAM. ’ 


Details of Progress — Prof. Irving’s Party— Prof. Chamberlin’s Party — Mr. Strong’s 
Party —Surveys in Oconto County by Maj. Brooks — Determinations of Latitude 
and Longitude by the U. 8. Engineer Department — Geodetic Survey under Dr. 
Davies — Mr. Ives’ Survey — Chemical Work — List of Maps and Sections Accom- 
panying the Report — List of Papers Accompanying the Report, - - 45-66 


‘ANNUAL REPORT FOR 1875. 


BY 0. W. WIGHT. 


Brief History of Previous Geological Surveys in Wisconsin — Reconnoissance made in 
the Northern Part of the State under the Personal Direction of the Chief Geologist, 
During the Latter Portion of the Season of 1875— Hamilton, or Lower Helder- 
burg — Artesian Wells — Mineral Springs — Acknowledgements, - 67-89 


ow 


x ‘GEOLOGICAL SURVEY OF WISCONSIN. 


PART II. 
GEOLOGY OF EASTERN WISCONSIN. 


BY T. C. CHAMBERLIN. 


ACKNOWLEDGEMENTS, - 93 
Extent or DistRIcrT, - - 94 
Previous Pusiications RELATING TO THE REGION, - 95 


CHAPTER I.— TOPOGRAPHY. 


Preglacial Features — Glacial Features — Postglacial Features — General Slopes — Pe- 
culiar Diagonal Valley —The Fox River — Its Commercial Importance — Origin — 
Rock River Valley — Peculiarities of its Course — Commercial Importance — Valley 
of Lake Michigan—Slopes and Dividing Ridges— Kettle Range — Elevations, , 

95-127 


CHAPTER II.— HYDROLOGY. 


DrartnaGE—The Watershed —The Mississippi and St. Lawrence Basins — Peculiar- 
ities of Streams of Walworth and Adjacent Counties— Of the Pike River — Of the 
Milwaukee River—Of the East Twin River — Of the Wolf, Oconto, Peshtigo and 
‘Menomonee Rivers — Of the East Branch of the Rock River — Relationship of some 
of the Streams on Opposite Sides of the Kettle Range — Geneva Lake and Big Foot 
Prairie — Delavan Lake and White River— Turtle Creek and Sugar Creek — Bark 
and Oconomowoc Rivers and the Branches of Cedar Creek — Rubicon River and 
Cedar Creek — Origin and Geological Relations of the Lakes of Eastern Wiscon- 
sin — Lake Michigan —Green Bay, Lake Winnebago and the Former Lake Hori- 
con— Lake Poygan — Lake Puckawa— Green Lake— Rush Lake — Lake Sha- 
wano — Lake Koshkonong — Glacial Lakes — Moraine Lakes — Minor Lakes — 
Their Beauty and Value—Geneva, Oconomowoc, Green, Elkhart, Rock, Brown, 
Clear and Delavan Lakes— Water Supply — Springs —Two General Systems — 
The Several Geological Horizons —Analyses — Source of Mincral Substances— Medi- 
cinal Character—Sulphur Springs—Chalybeate Springs—Travertine Springs—Trout 
Springs— Artesian Wells — Classified According to Source of Flow — Fountains at 
Fond du Lac — At Taycheedah — In Byron—In Oakfield — At Oshkosh — In Cal- 
umet—In Rushford, Aurora and Poysippi— At Watertown — At Palmyra — At 
Whitewater — At Manitowoc — At Western Union Junction —At Racine — At Mil- 
waukee — At Sheboygan — At Janesville — Possibilities of Obtaining Fountains at 
Other Points—The Three Districts — Elevations of Junction of St. Peters Nand- 
stone and Trenton Limestone — Water Power—Of Rock River—Of the Fox 
River— Of the Wolf, Oconto, Peshtigo and Menomonee Rivers —Of Milwaukee, 
Sheboygan and Manitowoc Rivers — Changes in Drainage, - 128-175 


CHAPTER JII.—NATIVE VEGETATION. 


Agricultural Indications — Natural Grouping of Plarts — Upland Vegetation, Prairie 
Group — Oak Group — Oak and Maple Group — Maple Group — Maple and Beach 
Group — Hardwood and Conifer Group — Pine Group — Limestone Ledge Group — 
Comprehensive Group— Marsh Vegetation — Grass and Sedge Group — Heath 
Group — Tamarac Group— Arbor Vite Group— Spruce Group — Black Ash Group— 
Yellow Birch Group — Distribution — Cranberries — Native Occurrence — Condi- 
tions of Success in Culture, - - - - = - 7 = 176-178 


TABLE OF CONTENTS. xi 


CHAPTER IV. —SOILS. 


Origin — Classes of Soils — Prairie Loam — Lighter Marly Clay Soils — Heavier Marly 
Clay Soils—Red Marly Clay Soils—Limestone Loam — Silicious Sandy Soils — 
Calcareous Sandy Soils —Humus Soils — Alluvial Soils — Analyses of Soils — Mag- 
nesian Character — Comparison of Soils and Vegetation, - 188-198 


CHAPTER V.— QUATERNARY FORMATIONS—THE DRIFT. 


Definition — Glacial Movements— Direction of Glacial Grooves—Trains of Bowlders 
from Archean Outcrops — Surface Configuration — Peculiar Phenomena at Burling- 
ton and East Troy — Fiords — Glacial Drift, Moraines, Kettle Range — ‘‘ Kettles” 
— Character of Range —Width — Material — Structure — Comparative Abruptness 
of Opposite Slopes — General Relationship — Summit Altitudes — Kettle Range, a 
Gigantic Moraine —Minor Moraines—Bowlder Clay or Till — Origin —Composition 
— Gravel Bowlders — Modified Drift, Champlain, Beach Formation A. — The 
Lower Red Clay — Character — Thickness — Elevations it Attains, and their Sig- 
nificance — Depression indicated — Beach Formation B.— Character — Thickness 
— Upper Red Clay — Character —Thickness — Beach Formations C. and D., and 
the Modified Red Clay — Description — Relations — Origin — Altitudes of the Beach 
Ridge — Terraces —Beach Ridge of Sand—Beach Ridge of Rock-Fragments — 
Terraces of Rock—The Three Forms United—Secondary Beach Lines — Gen- 
eral Movements —Encroachments of Lake Michigan — Dunes—Erosion and Deposit 
— Industrial Nature of the Drift I’ormations — Brick — Chemical Nature of the 
White Brick— Manufacture at Milwaukee, Racine, Ozaukee, Sheboygan Falls, 
Manitowoc, Kewaunee, Appleton, Neenah, Menasha, Clifton, Watertown, Water- 
loo, Jefferson, Ft. Atkinson, Edgerton, Whitewater, and elsewhere — Tiles — Pot- 
tery — Magnetic Iron Sands — Shell Marl — Peat — Origin — Details of Borings — 
Utilization, - 199-246 


ForMaTions oF EastERN WISCONSIN, - 247 


CHAPTER VI.— ARCHHAN FORMATIONS. 


The Mukwa Granite—The Berlin Porphyry—The Quartz-Porphyry of Pine Bluffs 
—The Quartz-Porphyry of Marquette — The Quartzites of Portland and Water- 
loo, - - 248-256 


CHAPTER VII.—LOWER SILURIAN. 


PorspaM SANDSTONE — General Character—Madison Sandstone — Mendota Limestone 
— Organic Remains — Method of Deposit —Extent — Sections and Local Deserip- 
tions — Lower Magnesian Limestone —General Character — Organic Remains — 
Area — Thickness — Local Descriptions - Economic Considerations — St. Peters 
Sandstone — Thickness — Structure— Transition Beds — Organic Remains — Meth- 
od of Formation— Extent and Local Descriptions — Economic Considerations — 
Trenton Group— Trenton Limestone —Subdivisions—Lower Buff Beds — Lower 
Blue Beds — Upper Buff Beds — Upper Blue Beds — Local Descriptions — Indus- 
trial Considerations — Galena Limestone — General Characteristics — ()rganic Con- 
tents — Thickness — Industrial Value — Distribution and Local Details — Recapitu- 
lation — The Cincinnati Shales and Limestones — General Character — Thickness 
— Life — Industrial Value — Distribution and Local Details — Table of Fossils of 
the Trenton Period, - - - - - - - 257-326 


xii GEOLOGICAL SURVEY OF WISCONSIN. 


CHAPTER VII[— UPPER SILURIAN. 


Curnton Iron Ore Derosrr—Age and Stratigraphical Relations — Formation at 
Iron Ridge — Analyses — Product — Furnaces — Formation at Hartford — In Stock- 
bridge— Near De Pere —General Conclusions — Niagara Limestone — Subdivis- 
ions — Mayville Beds —Character — Analyses — Life — Table of Fossils — Econ- 
omic Value— Distribution and Local Descriptions— Byron Beds — Character — 
Analyses — Fossils — Thickness — Distribution — Economic Considerations —- Trans- 
ition Beds — Lower Coral Beds — Nature — Organic Remains — Table of Fossils —~ 
Upper Coral Beds —Nature— Organic Remains — Table of Fossils — Distribu- 
tion — Local Details —Waukesha Beds — Character — Development at Waukcsha, 
at Pewaukee, in Genesee, elsewhere — Racine Beds—Extent and Relations — 
Local Details — Summation — Conclusions — Coral Reefs— Organic Remains — 
Table of Fossils — Guelph Beds — Nature — Local Details — Table of Fossils — In- 
dustrial Value of the Waukesha, Racine, and Guelph Beds — Lime — Analyses — 
Building Stone — Flux— Table of Fossils of the Niagara Group — Lower Helder- 
berg Limestone — Character — Analyses — Extent — Fossils — Formation in Fre- 
donia — Fossils — Analyses — Conclusions — Economic Considerations, 327-394 


CHAPTER IX — DEVONIAN. 


Hamitton Cement Rock — Nature— Composition — Analyses — Organic Remains — 
Description of New Species of Fish—Age of Formation — Local Descriptions — 
Economic Considerations — Investigations on the Hydraulic Properties of the For- 
mation, - 395-405 


PART IIL. 
GEOLOGY OF CENTRAL WISCONSIN. 


BY ROLAND D. IRVING. 


Inrropuction — Extent of District — Previous Investigations — Arrangement of Re- 
port — Acknowledgments 408-412 


CHAPTER I.—SURFACE FEATURES OF CENTRAL WISCONSIN. 


River Systems anp Generau Strrace SLopes—The Wisconsin River — Table of 
Altitudes of Water Surface of Wisconsin River —The Black River — The Rock 
River —The Fox River — Fall of Fox River. — Surface feeliefs — Watersheds — 
Baraboo Bluffs — Isolated Peaks and Ridges —Altitudes, Madison to Elroy — Elroy 
to Merrillon — Waterloo to Madison — Edgerton to Black Earth — Camp Douglas 
to Randolph—Tomah to Wausau — Amherst to Merrillon — Portage to Stevens 
Point — Stevens Point to North Line of Township 29 — Banomerrican ALTITUDES 
— Relations of the Topography to the Geology of the region — Vegetation and Soils 
— Praines — Marshes and Timber Land — Topographical Subdivisions — Résumé. 
Region of Crystalline Rocks — Central Sandstone Region — Limestone District, 

413-456 
CHAPTER II. —GENERAL GEOLOGICAL STRUCTURE OF CENTRAL 
WISCONSIN. 


Laurention System — Huronian System — Silurian Formations — Glacial Drift — Table 
of Formations - - - - - - 457-460 


TABLE OF CONTENTS. xiii 


CHAPTER III.—THE ARCHMAN ROCKS. 


The Main Archean Area — Considered in General — Line of Junction with Potsdam — 
Unconformability — Topographical Features of the Crystalline Rock District — 
Kind of Rocks — Bedding — Intrusive Granite — Weathering — Strike — Laur- 
entian — Huronian — Economic Importance — Local Details — In Upper Wisconsin 
Valley —In Yellow River Valley—In Black River Valley —Isolated Archean 
Areas — In General — Table of Isolated Archean Outcrops — Special Descriptions 
— The Baraboo Quartzite Ranges— The Marcellon Quartz-Porphyry — The 
Observatory Hill Quartz~Porphyry—The Moundville Quartz-Porphyry — The 
Seneca Quartz-Porphyry — The Marquette and Berlin Quartz-Porphyries — Com- 
parison of the Rocks of the Several Porphyry Areas —The Montello Granite — 
The Marion Granite Areas — Conclusions — The Necedah Quartzite - 461-524 


CHAPTER IV — THE LOWER SILURIAN ROCKS CONSIDERED IN GENERAL. 


Potspam SanpDsToNnE Serres — Mendota Limestone— Madison Sandstone — Two 
Names — Former Investigation — Surface Distribution — Boundary Between Pots- 
dam and Archean Areas — Between Potsdam and Lower Magnesian Areas — To- 
pographical Characters — Lithological Characters and Stratigraphical Arrangement 
— Sections — Analysis of Greensand — Discussion of Anomalous Relations of Cer- 
tain Portions of the Formation — Beds of Passage — Madison and Mendota Beds — 
Analyses — Fossils —Economic Contents — The Lower Magnesian Limestone — 
Name— Surface Extent — Topographical Characters — Lithological Characters — 
Stratigraphical Arrangement — Sections —Irregular Upper Surface — Fossils — 
Economie Contents — The Upper or St. Peters Sandstone — Name — Distribution 
— Topographical Features — Lithological Characters —Thickness — Economic Con- 
tents — The Trenton Limestone —Relations — Surface Distribution — Topograph- 
ical Characters — Lithological Characters — Buff Limestone — Blue Limestone — 
Fossils — Economic Contents — Building Stone — Flux — Galena Limestone — Lo- 
cal Details — Portage, Wood, Clark and Jackson counties —Juneau and Adams 
counties — Marquette and Waushara counties, and Green Lake county north of the 
Fox river — Sauk and Columbia counties — Dane county. - 525-607 


CHAPTER V—THE QUATERNARY DEPOSITS. 


Tur GuactaL Drirt — The Driftless region — Outline of the Driftless Region — Topo- 
graphy of the Driftless Area—Its Altitude—Surface Features of the Dnift- 
bearing Regions — Linear Topography—Roches Moutonées—Dnift Hills and 
Ridges — Kettle Range — Materials of the Drift— Bowlders — Gravel — Sand — 
Clay — Arrangement of the Drift Materials — Amount — Directions of the Glacial 
movement — Table —Origin and Directions of Travel of Erratics and Pebbles — Or- 
igin of Sand and Clay of Drift — Economic Contents of Drift — Conclusions, 609-636 


APPENDIX — MICROSCOPIC LITHOLOGY. 
BY CHAS. E, WRIGHT. 


Silicious Hornblende Schist — Granite — Argillo-chloritic Schist — Hornblende Rock — 
Syenite — Silicious Chloritic Schist — Chloritic Hornblende Rock — Syenitic Granite 
—Silicious Hornblende Schist-— Chloro-silicious Schist, - - 637-639 


xiv GEOLOGICAL SURVEY OF WISCONSIN. 


PART IV. 


GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 
BY MOSES STRONG. 


CHAPTER I.—INTRODUCTORY AND HISTORICAL. 


Territory Examined in 1873— Plan of Operations —Territory Examined in 1874— Pre- 
vious Publications and Surveys— Survey of G. W. Featherstonhaugh, 1834-35 — 
Surveys of Dr. D. D. Owen in 1839 and in 1847-8— Report of E. Daniels, 1854— 
Survey of Prof. J. G. Percival, 1854 to 1856 — Report of E. Daniels, 1858 — Report 
of Profs. Hall and Whitney, 1862 — Report of Rev. J. Murrish, 1872 — Topograph- 
ical and Geological Maps and Sections —Barometrical Observations — Information 
Derived from them — Elevations of Towns and other Localities — Acknowledg- 
ments, - - 645-651 


CHAPTER IJ.—TOPOGRAPHY AND SURFACE GEOLOGY. 


GENERAL FEATURES OF THE Country—Drainage—Situation of the Dividing Ridges or 
Water-sheds—Streams—Theory of the Formation of the Streams of the Lead Region 
— Process of Erosion — Formation of the Wisconsin River and its Tributaries — Re- 
sults of the Denudution — Diminution of Water in the Lead Region — Sinking of 
Streams in Grant County — Causes of the Decrease of Water — Springs and Wells 
— Springs of the West Blue Mound —Inorganic Salts Contained in the Water — 
Analysis — Prairie and Forest — Mounds — Sinks — Soil and Subsoil— Absence of 
Drift — Distribution of the Surface Soil and Rock — Peat — Brick Clay — Drift — 
Gravel Beds — Drift Clay — Erratic Bowlders of Sandstone, 652-667 


CHAPTER III. —GEOLOGICAL FORMATIONS. 


Potsdam Sandstone — Geographical Boundaries — Lithological Characteristics — Section 
at Lone Rock — Coloring Matter in the Potsdam — Hydraulic Shales — Localities of 
Fossils — Lower Magnesian Limestone — Geographical Boundaries ~ Lithological 
Characteristics — Varying Thickness—Localities of Fossils — St. Peters Sandstone — 
Geographical Boundaries — Lithologieal Characteristics — Terraces—Knobs—Ripple 
Marks — Varying Thickness — Upheavals — Concretions — Induration on Exposure 
— Quarries — Trenton Limestone — Geographical Boundaries — Lithological Char- 
acteristics — Carbonaceous Shale — Analyses — Section — Disappearance of the Blue 
Limestone — Ores — Minerals — Organic Remains —Galena Limestone — Geograph- 
ical Boundaries and Area — Lithological Characteristics -- Flint — Building Stone— 
Paleontology — Cincinnati Group—Geographical Boundaries and Area — Litholog- 
ical Characteristics — Section — Localities of Fossils, - - - 668-688 


CHAPTER IV.—THE LEAD REGION. 


Boundaries and Area — Explanation of Mining Terms — Mineralogy — Paragenesis of 
Minerals — Pseudomorphs — Present Condition of the Mines— Section of the Min- 
ing Openings — Beetown District — Potosi District — Fairplay District — Hazel 
Green District —Buncome Diggings— New Diggings District —Shullsburg Dis- 
trict — Benton District — Platteville District — Whig Diggings— Big Patch Dig- 
gings—Mifflin District — Centerville District — Blue River Paint Works — Highland 
District — Linden District ~ Dodgeville District — Porter’s Grove Diggings — Van 
Meter’s Survey — Mineral Point District —Diamond Grove Diggings — Calamine 
District — Wiota District — Monroe District— Occurrence of Copper in the Lead 
Region — Statistics of Zinc Ore — Statistics of the Production of Lead Ore in the 
Several Districts for each year since 1861; and the Smelting Facilities — Concluding 
Remarks, - : = - - - - - - - 689-752 


TABLE OF CONTENTS. XV 


ATLAS PLATES 


ACCOMPANYING THIS VOLUME. 


Nore. — As maps will accompany the other volumes of this report, it has been thought best to arrange 
and number the whole series as one set, for convenience of reference and binding, and hence the actom- 
panying atlas begins with Plate III. 


PLATE, 


Ti. 
IV. 
V: 
VI. 
VII. 
VITl. 
IX. 
X. 


XI. 


Map of Soils and of Vegetation of Eastern Wisconsin. 

Map of Topography and of the Quaternary Formations of Eastern Wisconsin. 

Map of Geology and Topography of the Lead Region. 

Map of Geology and Topography of the Lead Region. 

Map of Geology and Topography of the Lead Region. 

Map of Geology and Topography of the Lead Region. 

Map of Geology and Topography of the Lead Region. 

Area A.—Geological map of Kenosha, Racine, Milwaukee, Waukesha, Wal- 
worth, Jefferson, and parts of Rock, Dodge, Washington and Ozaukee counties. 

Area B.— Geological map of Fond du Lac, Sheboygan, Manitowoc, Calumet, 
Winnebago, and parts of Dodge, Washington, Ozaukee, Kewaunee, Brown, 
Outagamie and Waupaca counties. 


. Area C.— Geological map of portions of Brown, Door, Kewaunee, Outagamio, 


Shawano and Oconto counties. 


. Area D. — Geological map of Green, and parts of Iowa, La Fayette, Dane, Sauk 


and Rock counties. 


, Area E.— Geological map of Juneau, Adams, Waushara, Marquette, Sauk, Col- 


umbia, Green Lake and part of Dodge counties. 


. Area F. — Geological map of Wood, and parts of Clark, Jackson, Marathon and 


Portage counties. 


. Area G. —Geological map of Grant, aud parts of La Fayette, Iowa, Richland and 


Crawford counties, 


LIST OF ILLUSTRATIONS. 


LITHOGRAPHIC PLATES. 


Norz.—The chromo-lithograpbs were carefully reproduced from photographs. 


Puate I. View of Stand Rock, Dalles of the Wisconsin — Potsdam Sand- 


stone, - - - - eee ey 
Page. 


LA. False Bedding — Potsdam Sandstone — Dalles of the Wisconsin, Opp. 49 


JI. Map showing the Areas examined My the Several Parties, 1873- 


1876, Opp. 94 

JI A. Lucas Point, Green Lake, showing J a of Potsdam sandstone 
and Lower Magnesian limestone, - Opp. 91 
III. Iron Ridge Mine, - - = = = + Opp. 827 
IV. Topographical Map of Eastern Wisconsin, - - -— - Opp. 97 


V. Profiles elucidating Artesian Fountains in Eastern Wisconsin, Opp. 151 


VIL. Profiles elucidating Artesian Fountains in Eastern Wisconsin, Opp. 160 


GEOLOGICAL SURVEY OF WISCONSIN. 


Topographical Map of Milwaukee County, 7 

Diagram showing Glacial Movements in Eastern Wisconsin, 

Profile Section of Quaternary Formations along Lake Michigan, 

Map showing Outline of Eastern Wisconsin during the Cham- 
plain period, - ae 

Topographical map of Iron Ridge Mining Property, 

Profile Sections showing the Subdivisions of the Niagara Group, 

Profile Section through Artesian Wells at Western Union Junc- 
tion, Milwaukee and Sheboygan, - 

View of Milwaukee cement quarry, - - 

View of Roché a Cris Bluff, Potsdam sandstone, - - 

Archean. View of Devil’s Lake and Kirk’s Bluff, 

Map of Central Wisconsin, showing the Hydrographic Basins and 
principal Topographical Subdivisions, : 

Map showing the formations along Black river, Jackson county, 

Map of Isolated Archean Areas, - - - - 

Maps and Cross Sections illustrating the Structure of the Devil's 
Lake Gorge, - - - - 

Cross Sections in Sauk county, - 

East and West Sections in Columbia county, - - 

North and South Sections in Columbia county, - - 

North and South Sections in Dane county, 

East and West Sections in Dane county, 

Map of part of Wisconsin, showing glacial Drift and other Quat- 
ernary formations, - 

Geological map of the Four Lake Country of Dane county, show- 
ing the Directions and Effects of the Glacial Movements, 

View of bluff of Walena limestone near Cassville, on the Missis- 
sippi, - 

Outline map of the Lead region, exhibiting the Drainage and the 
Distribution of Prairie and Forest - - 
Map of Hendy, Davey, Sobey & Co.’s mine, - - 
Section through the Mining Districts of Beetown, Potosi and Fair- 
play, from the mouth of the Mississippi to the State Line, show- 

ing the Denudation, - 

Map of Linden mine, 2 . = 

View of Bluffs on the Mississippi, 

Section through the Mining Districts of Hazel Green, Besian and 
Mineral Point, from the State Line to the Wisconsin river, 
showing Denudation, - & 2 

Outline map of the Lead region, showing the ae Mining Dis- 
tricts andthe Furnaces, - - - 7 7 a 


FIGURES. 
REPORT ON EASTERN WISCONSIN. 


1. Geological Relations of Green Bay Valley, Bhs 


2. Striated Cone of Limestone, Pewaukee, - 


3. Trains of Bowlders from Portland and Waterloo Quartzite Outliers, - 


4, Peculiar Glacial Phenomena at Burlington, - = 


Page. 


Opp. 


Opp. 


Opp. 


Opp. 
Opp. 


Opp. 


Opp. 
Opp. 
Opp. 
Opp. 


Opp. 


Opp. 


Opp. 


Opp. 
Opp. 
Opp. 
Opp. 
Opp. 
Cpp. 


Opp. 
Opp. 
Opp. 
Opp. 


Opp. 


Opp. 
Opp. 
Opp, 


Opp. 


Opp. 


127 
204 
219 


223 
328 
336 


335 
395 
525 
407 


453 
493 
501 


507 
590 
579 
581 
597 
600 


608 
613 
643 
652 
731 


667 
726 
689 


663 


742 


Page. 


101 
200 
202 
203 


co DD EE 


TABLE OF CONTENTS. 


. Section of Kettle Range near Whitewater, 

. Profile Across Kettle Range, from Eagle Westward, 

. Profile Across Kettle Range near Whitewater, Showing Position of Kettles, 
. Map of Moraine in Towns of Herman and Theresa, 

. Section of Moraine in Town of Herman, - - 

. Map of Moraine in Beloit, - - - 

. Section of Drift Showing Gravel Bowlders, : 

. Sections of Drift near Milwaukee, - 

. Section of Drift near Manitowoc, - 

. Section of Drift near Racine, - - 

. Section Illustrating Drift Formation near Racine, 

. Diagram JNustrating Movements of Drift-Depositing Agencies, - 
. Profile Section Showing the Relations of the Mukwa Granite, 

. East and West Section through the Berlin Porphyry, 

. North and South Section through Pine Bluff, 

. Ripple-Marked Outlier, Waterloo, 

. Profile Section Showing the Relations of the Waterloo Cashak 

2. North and South Section through Portland Quartzite, 

. Section Showing the Relations of the Portland Quarizite, - 
. Section of Bartholomew’s Bluff, - 

5, Section Across Green Lake, - - - - 

. East and West Section near Ripon, - 

. Section near Stiles Showing Relations of St. Peters Sandstone and Lower 


Magnesian Limestone. 7 - 


. Contact of Trenton and Lower Magnesian Limestones, - 
. North and South Section near Ripon, - 

. Irregular Structure of Lower Magnesian, Nepeuskin, - 

. Section of Lower Magnesian Limestone, - - : 
. Secticn of Lower Magnesian Limestone, Mukwa, 

. Section of Lower Magnesian Limestone, Mukwa, 

. Relations of the Formations in the Town of Ellington, - 

. Coloration of the St. Peters Sandstone near Ripon, 

. Coloration of the St. Peters Sandstone near Ripon, 

. Relations of St. Peters Sandstone and Trenton Limestone, Magnolia, - 
. Subdivisions of Trenton Limestone, - - 

. Profile of Trenton Limestone near Beloit, - - - - 

. Section through the Iron Ore Deposit, Iron Ridge,  - = 

. Section at the Mayville Ore Bed, - - 

. Position and Relations of the Iron Ore at Hartford, 

. Cascade Falls near De Pere, - - - 
. Peculiar Structure of Racine Beds, Germantown, - 7 
. Stratification at Moody's Quarry, - - - 

. Relation of the Mound and Horizontal Limestone, Wauwatosa, - - 

. Profile of Leperditia Beds near Waubakee, - - 


REPORT ON CENTRAL WISCONSIN. 


. Specimen showing junction of Potsdam Sandstone and Archean Schists, 

. Vicinity of Point Bass, Wood County, *. - 

. Section Across Side Channel of Wisconsin River, near Point Bass, 

. Section Across Side Channel of Wisconsin River, near Point Bass, - 


Wis. Sur. —B 


xviii GEOLOGICAL SURVEY OF WISCONSIN. 


. Vicinity of Grand Rapids, - 

. Kaolin at Grand Rapids, 

. Junction of Granite and Hornblende Rocks. 

. Enlargement of a portion of Fig. 7, 

. Granite Vein at Grand Rapids, 

. Granite Vein in Gneiss at Grand Rapids, 

. Generalized Section, Grand Rapids, 

. Map of Localities at Conant’s and Stevens Point Rapids, 
. Sketch of Granite Exposures, * 


Granite Vein at Conant’s Rapids, 


. Quartzite Exposure on Rib Hill, Marathon County, 

. Map of Rock Exposures near Wausau, 

. Block Vein in Syenite, Wausau, - - 
. Rock Occurrences at the Falls of Rib River, 

. Faulted Veins in Granite, Yellow River, 

. Unconformability, Black River Falls, 

. Sketch of Original Structure and Erosion of Barahoo Ranges, 
. Surface of Quartzite Showing Curved Lamination, 

. Slaty Cleavage in Quartz Slate at Devil’s Lake, 

. Potsdam Bowlder-conglomerate and Sandstone on Archean Quartzite at Devils 


Lake, - 


. Sandstone and Conglomerate on Quartzite at Dorward’s Glen, 

. Unconformability, Sec. 23, Caledonia, 

. Map of the Lower Narrows of the Baraboo, 

. Section through West Bluff of the Lower Narrows, 

. Upper Narrows of the Baraboo, 

32. North and South Section. Upper Narrows of the Baraboo, 

. Veined Quartzite, - 

. Sketch of Possible Relations of Formations near Baraboo Ranges, 
5. Outlines of Roché a Cris and Friendship Mound, as seen from Pilot Knob, 
. Shape of the summit of Roché a Cris, 
. Diagram showing how an Area of « Lower Formation may be Entirely Sur- 


rounded by a Higher One, 


. North and South Section in Scott, 

. Profile Section across the Valley of the Wisconsin at Portage, 
. Section at Kingsley’s Bluff, Lodi, 

. Section across Valley of Wisconsin in West Point and Merrimac, 
. Sketch of the Western Face of Gibraltar Bluff, 

. Section of Gibralter Bluff, 

. Section across the Valley of the Wisconsin in Caledonia, 

. Section across the Valley of the Wisconsin at Prairie du Sac, 

. Section across the Wisconsin Valley from IIoney Creek Blut, 
. Section of River Bluff, north of Spring Green, 

. Map and Section showing the Relations of Eiky’s Limestone, 
9. Map and Section showing the Relation of Outcrop at Wood's, 
. Section in town of Burke, 

. Section across the Valley of the Black Earth Creek, 

. Outline of an Area of Trenton Limestone near Columbus, - 


DEER eee eee 
SOMANDAERWNHrF DOH ONHDS LO De 


bo 
rare 


TABLE OF CONTENTS. xix 


REPORT ON THE LEAD REGION. 


Page 
. General section of Platte River Valley, - - 657 
. Sketch of the upper part of the Blue Mounds, - 659 
. Sketch cf the Platte Mounds, - - 661 
. Sketch of a Terraced Hill near Lumberville, 669 
. Section of Calcareous and Arenaceous Shales at Grant River, 673 
. Section of Curved Strata at Grant River, 674 
. Sketch of Lower Magnesian Limestone at Welsh Mill, - 674 
. Sketch of a Hill in the Town of Mt. Pleasant, - - - 676 
. Upheaval of St. Peters Sandstone at Red Rock, - - 678 
. Section from Scale’s Mound to the State Line, - - - 686 
. Section of Openings (ideal), : - 690 
. Plan of Workings in the Beetown Mine, - - 696 
. Junction of E. and W. Veins with a Quartering Range, Adkinson Dieoinse, 698 
. Section of Meredith Mine, 699 
. Section of Vein, Black & Co.’s Diggings, - - - - - 703 
. Section of an Opening in the Williams Mine - - - 703 
. Vein-stone Breccia, Stopline Diggings, - 714 
. Section of the Barton Opening, - - 718 
. Section showing Connection of Flat and Pitching Sheets, Linden Mine 728 
. Section of Sheets in the Road Mine, 728 


. Plan of Evan Williams’ Diggings, “. - - 730 


PART I. 


HISTORICAL. 


ANNUAL REPORTS. 


-PREFATORY NOTE. | 


The administration of the survey, at its commencement, was placed 
in the charge of the late lamented Dr. I. A. Lapham, who brought 
to the work the fruits of a large experience, and the acquisitions of 
years of industrious observation upon the geology and natural history 
of the state. Under his able management, the survey continued the 
first and the greater portion of the second year. Annual reports for 
each of these years were duly submitted by him, but were not pub- 
lished. He was succeeded as chief geologist in February, 1875, by 
Dr. O. W. Wight, who held the position one year, and who presented 
a report for that year, which was likewise not published. In Febru- 
ary, 1876, the direction of the survey was placed in charge of the 
writer. Subsequently, provision was made, by enactment of the legis- 
lature, for the preparation and publication of the final report of the 
survey, and the foregoing annual reports were placed “in the hands of 
the chief geologist to be used in the preparation of his final report.” 
Under these circumstances, it has seemed to me the part of justice to 
publish, as nearly intact as possible, the reports prepared by my pre- 
decessors. Certain portions of a report of progress, however, necessa- 
rily relate to the administration of the survey, and to other matters 
of transient interest which have little subsequent importance, and 
would be inappropriate in a report of this character, and hence there 
arose a necessity for the revision of these reports for this volume. 
This, to me a very delicate duty, it was presumed would be esteemed 
a favor by those most intimately concerned in their publication, and 
it was freely proffered them. The revisal of the reports of Dr. Lap- 
ham was very kindly undertaken by his son, Mr. 8. G. Lapham, and 
they appear as they left his hands, with a few trivial changes made at 
his request. It should be considered by all, that these annual reports 
made thus early in the history of the work, and merely intended to 
show the progress and results of the survey, in accordance with legal 
requirement, cannot do full justice to tueir distinguished author, but 
it is hoped that they will éndécate the work accomplished under his 
administration, and if there be anything meritorious in the final 


4 GEOLOGICAL SURVEY OF WISCONSIN. 


results of the survey, a just and generous public will award a due 
measure of honor to the hand that organized and gave it direction at 
its inception. 

The like comity in relation to the revision of the report of 1875, 
extended to Dr. Wight, was declined, except the privilege of reading 
the proofs, but he has been kind enough to assure me that nothing has 
been omitted from his report that it is desirable to retain. 

The revision of all these reports has been closely confined to the 
elimination of administrative and duplicate portions, and everything 
of a geological nature has been retained, even though it were only 
provisional in character, and this has been done to the exclusion of 
portions of my own and of my associates’ manuscript. While pub- 
lishing thus fully and scrupulously the reports of my predecessors, it 
is but just to myself to disclaim any responsibility for the views pre- 
sented. 

Since these reports, besides being themselves the earlier annals of 
the survey, contain historical sketches, they are grouped together to 
form the opening historical section of the volume. 

The annual report for 1876, submitted by the writer, was promptly 
published, and hence no part of it will find a place in this volume. 

The annual reports of the assistant geolcgists, being their own in- 
dependent productions, were placed in their hands, and will be found 
incorporated in their reports upon the districts assigned them. 


» dy Cs 
Betort, August 6, 1877. 


WISCONSIN GEOLOGICAL SURVEY. 


REPORT OF PROGRESS AND RESULTS, 


FOR THE YEAR 1873. 


BY I. A. LAPHAM. 


As required by the act “to provide for a complete geological sur- 
vey of Wisconsin,” approved March 19, 1873, I now have the honor 
to report the progress made, and the results attained during the first 
year of the survey, and also to lay before you the maps, roiled and 
drawings necessary to exemplify thesame. The law reads as follows: 


An Acr to provide for a complete Geological Survey of Wisconsin. 
The people of the State of Wisconsin, represented in Senate and Assembly do enact as 
follows. * 

Section 1. The governor is hereby required to appoint, by and with the advice and 
consent of the senate, a chief geologist, who shall be a person of known integrity, thor- 
ough practical and scientific knowledge of the sciences of geology and mineralogy, and, 
upon recommendation of said chief geologist, the governor shall appoint one or mors 
assistants, not exceeding in number four, one of whom shall be a skillful analytical chemist 
and assayer; the said chief geologist and his assistants to constitute a geological corps, 
whose duty it shall be to make a thorough and complete geological, mineralogical and 
agricultural survey of the state, and topographical surveys of such portions as may be 
deemed by the corps to need them for the thorough completion of the work: Provided, 
That if the appointment of chief geologist be made during the recess of the senate, 
such appointment may be confirmed at the next session thereof. 

Srection 2. The survey shall have for its objects: 

1st. An examination of the geological structure of the state, including the dip, num- 
ber, magnitude, order and relative position of the various strata; their richness in mine- 
rals, metallic ores, clays, mineral waters, fertilizers, building stones and other useful 
materials, the value of such materials for economic purposes, and their accessibility for 


mining and manufacture. 


6 GEOLOGICAL SURVEY OF WISCONSIN. 


2d. Accurate chemical analyscs and assays of the various ores, clays, peats, mars, 
building stones, etc., discovered by the state. 

3d. A careful topographical survey of the lead region, for the purpose of ascertaining 
as far as possible, the amount of denudation, and the exact position of the mining 
ground at each locality; also careful barometrical observations on the relative elevation 
and depression of various parts of the state. 

4th. An examination of soils and subsoils, and observations upon the animal and vege- 
table productions of the state, with reference to its agricultural interests. 

Section 3. It shall be the duty of said geological corps, in the progress of the ex- 
aminations hereby directed, to collect such specimens of rocks, ores, fossils, minerals, etc., 
as may be necessary to exemplify the geology of the state. Sets of these specimens shall 
be deposited with the Wisconsin Academy of Sciences, Arts and Letters, and the State 
University, and with each one of the incorporated colleges of the state, and with cach 
of the normal schools: provided, application be made to the chief geologist before the 
commencement of field work. 

Section 4. It shall be the duty of the chief geologist and his assistants, on or before 
the first Monday in January in each year during the continuation of the survey, to make 
to the governor a report of the progress and results of the survey, accompanied by such 
maps, profiles and drawings as may be necessary to exemplify the same, which reports 
the governor shall lay before the legislature. 

Section 5. As soon as the progress of thesurvey will permit, the chief geologist shall 
begin, and on completion of the survey, shall complete a final report, including the re- 
sults of the entire survey, accompanied by such drawings and topographical maps as 
may be necessary to illustrate the same, and by a single geographical map showing by 
colors and other appropriate means the stratification of rocks, the localities of the beds 
of mineral deposits, and the character and extent of the different formations. 

Section 6. To carry into effect the provisions of this act, the sum of thirteen thou- 
sand dollars for each year, until the completion of said survey, is hereby appropriated 
to be drawn from the treasury on warrants from the governor, as needed; which shall 
be in full for all expenditures except printing of reports. The salary of the chief geolo- 
gist, and the salaries of the assistant geologists shall be fixed by the governor, and shall 
be for services actually performed, and time actually spent in the work. The balance 
of the sum hereinbefore appropriated shall be used in such manner as shall best pro- 
mote the purposes of this act. : 

Section 7. The survey shall commence by the first of June next, or as soon thereaf- 
ter as practicable, beginning with the counties of Ashland and Douglas, and the entire 
survey shall be completed within four years from and after its commencement, 

Approved March 19, 1873. 


ORGANIZATION OF THE GEOLOGICAL Corps. — Governor C. C. Wash- 
burn, by commission dated the tenth day of April, 1873, appointed 
the undersigned chief geologist under the provisions of this law. 

On the twenty-ninth day of the same month, Prof. Roland D. Irv- 
ing, A. M., E. M., Prof. T. C. Chamberlin, A. M., and Mr. Moses 
Strong, A. M., were upon the recommendation of the chief geologist 
appointed as assistants in the survey. Prof. W. W. Daniells, M. §., 
was also engaged to make such chemical examinations and analyses 
of ores and minerals as might be needed for the ‘survey. By an ar- 
rangement with the Regents of the State University, Prof. Daniells 


ANNUAL REPORT FOR 1878. 7 


is to have the use of the apparatus belonging to the Institution with- 
out additional expense. 

These gentlemen had, by previous study and training, qualified 
themselves for the special work required. Their elaborate reports 
herewith submitted will show that they have faithfully, efficiently, 
and satisfactorily performed the several duties assigned them; though 
the time between the close of the field operations and the day on 
which their reports must be submitted to the Governor is not suffi- 
cient to enable them to do that full justice to their work that could 
be desired. 

The assistants were each directed to organize a party adequate to 
the special work required; to supply themselves with the necessary 
instruments and outfit; to give their attention to all facts throwing 
light upon any of the special matters required to be considered by the 
law authorizing the survey; and, as it isobviously impossible, as well 
as unnecessary to visit every square mile in the country they were 
directed to so plan their routes as to be able to examine the localities 
of greatest importance to the material interests of the state; and at 
the close of the fieldwork, to prepare, as soon as possible, a detailed 
report of the results of their work with the necessary maps, profiles 
and drawings. Each party was supplied with skeleton maps, traced 
from the township plats of the government land surveys, upon which 
was laid down, from time to time, such additional information as 
could be obtained. These plats, it is well known represent “ town- 
ships”? six miles square, divided into thirty-six “sections ” of one mile 
square, upon a scale of two inches to one mile, which is sufficiently 
large to represent all but the minutest details of the geological sur- 
vey. Among the instruments brought into requisition by the sever- 
al parties were the aneroid barometer, miners’ compass, odometer, 
clinometer, pocket level, tape lines, etc. 


Pror. Irnvine’s Parry.—It was deemed advisable to assign to 
Prof. Irving of the State University, Madison, the duty of beginning 
the survey, by an examination of the Iron and Copper Ranges of 
Ashland and Douglas counties; and efforts were made to have the 
work begun as soon after the first day of June as possible. His party, 
consisting of Prof. R. D. Irving, Mr. Frank B. Jenney, Mr. Edmund 
T. Sweet, and Mr. James Munro, with a guide and a cook, though 
much delayed by ice in Lake Superior, were able to reach Ashland, 
and to commence the field-work of the Wisconsin Geological Survey 
on Monday the second day of June, A. D. 1873. 

In addition to the general instructions detailed above, Prof. Irving 


8 GEOLOGICAL SURVEY OF WISCONSIN. 


was requested to give attention to the question of the age of the red 
sandstone and accompanying shale of the counties to be examined; 
whether the Archean rocks are of different ages; and to the disturb- 
ances of the strata in the vicinity of the metal-bearing ranges, involv. 
ing important questions regarding the proper system of mining. 

His report, herewith submitted, will be found to contain ample de- 
tails of the beds of silicious magnetic iron ores forming what is 
known as the Penokee Iron Range, with numerous analyses of the 
ores, including all information necessary for a proper understanding 
of the extent and value of these important ore beds. Other details 
brought forward in this report, showing what had previously been 
done in exploring this interesting region; its topography, surface, 
general, special and economical geology; its agricultural features, 
timber, ete., will be found equally interesting and valuable. These 
explorations, made so early in the season, were not accomplished with- 
out the patient endurance of much suffering and hardship, arising 
from the clouds of musquitoes, and from unfavorable weather. 

Prof. Irving also made a partial examination of the iron ore beds 
at and near the Black: River Falls, in Jackson county. 


Pror. CuampBeriin’s Parry. — To Prof. Chamberlin was assigned 
the duty of surveying that portion of the state lying immediately 
west of the line of outcrop of the Niagara or Clinton group of rocks, 
from the south line of the state through the counties of Walworth, 
Jefferson, Dodge, Fond du Lac, Calumet and Outgamie to the south- 
ern limits of the crystalline Archean rocks in Shawano county; and 
upon his return route, to examine the outcrops of the lower strata lying 
west of that line. He would thus be led to examine the important 
iron beds, now so extensively mined at Iron Ridge, the artesian wells 
from which water flows so abundantly at Fond du Lae and elsewhere, 
and the highly interesting localities of quartzite in Dodge and Jeffer- 
son counties. He would also be in the midst of some of the most 
striking features of the glacial and modified “ drift,” with their “pot- 
ash kettles,” gravel hills and parallel ridges. 

On the twenty-third day of June, work was commenced by this 
party under the immediate direction of Prof. Chamberlin, aided dur- 
ing portions of the time by Messrs. L. C. Wooster, F. H. King, N. 
D. Wright, Samuel Shaw and G. L. Merriman. 

They reached Keshena, in Shawano county, early in September, and 
returned to Beloit by the last of that month. Some further explora 
tions were afterwards made by Prof. Chamberlin in person, us men- 
tioned in his report. 


ANNUAL REPORT FOR 1873. 9 


In Prof. Chamberlin’s report will be found much interesting and 
valuable information, stated in plain language, relating to the topog- 
raphy of the district examined by him; the drainage and water power; 
the distribution of vegetation, of marshes, of lands covered with oak, 
maple or pine forests, with a map showing the boundaries of these 
several divisions; the outlines of the several rock formations; the 
phenomena of the drift; the nature of artesian wells, and various 
matters coming under the head of economical geology. Special at- 
tention was, very properly, given to the subject of our peat deposits, 
which will increase in importance from year to year, as the forests 
disappear, and the cost of fuel becomes thereby increased. 

These, and the various other matters of much practical utility pre- 
‘sented in this report, will be read with much interest by the people 
of the state. 


Mr. Srrone’s Parry. — Special provision having been made for a 
careful topographical survey of the lead region, for the purpose of 
showing the denudation of the superior strata that so evidently has 
occurred, and the exact position of the mining ground at each locality, 
with reference to the particular rock-formation in which it is found, 
it was deemed advisable to assign one of the three surveying parties 
expressly to this work. Accordingly Mr. Strong, having made suita- 
ble preparations, commenced that work on the fifth day of June. 

For the purpose of securing the most general and complete view of 
the whole lead region during the first year of the survey, Mr. Strong 
was directed to give his attention to two lines, the one east and west, the 
other north and south through the middle of the district. This would 
lead him to construct a geological section from the Mississippi river 
eastward to Dane and Green counties, and another northward from 
the state line of Illinois, to the iron ores and quartzites of Richland 
and Sauk counties. This party consisted of Mr. Moses Strong, Mr. 
A. D. Conover, and Mr. J. W. T. Crawford. Mr. Strong’s previous 
training and skill acquired in the best scientific schools in this country 
and in Germany, and in the business of a mining engineer, enabled 
him to perform, with full satisfaction, the duties thus assigned to him. 

Special attention was to be given to the collection of all facts bear- 
ing upon the method by which the lead, zinc, and copper, were depos- 
ited in the veins or crevices; whether by deposition from above, 
injection from below, or by gradual infiltration from the inclosing 
rocks; these questions being deemed of the greatest theoretical and 
practical importance as showing the probable extent of these ores be- 
low the limits of present explorations. Also to ascertain whether 


10 GEOLOGICAL SURVEY OF WISCONSIN. 


there have been disturbances of the strata, centers of elevation, etc., 
questions of importance with regard to the downward continuance of 
the veins, and the proper method of drainage. 

Mr. Strong’s report will be found to contain much that is new and 
valuable in regard to this important and very interesting district. 
The local details, showing the present condition of the mines, and 
their capabilities of future production, cannot fail to be of great bene- 
fit to the state by making known in a reliable form the advantages 
that might be attained by a more vigorous prosecution of mining 
operations at many of the localities described. 

The extent, physical characteristics, mineral contents, and other 
important particulars of each rock-formation occurring in the district 
examined, are clearly stated. The discovery of fossils in the Lower 
Magnesian limestone shows that animal life was not entirely destroyed 
during the epoch of the deposition of this great member of the Lower 
Silurian series of rocks, and places it more directly in unison with the 
Galena (or Lead-bearing) limestone from which it is only separated by 
a comparatively thin layer of sandstone—the St. Peters. It thus 
being shown to have one more character in common with that rock, 
we may expect to find still more common features, such as the oceur- 
rence of crevices, openings, and the ores of lead, zine, and copper. 
Important facts are brought forward, bearing upon this question of 
the occurrence of metallic ores of economical value, in the Lower 
Magnesian limestone. 

Quarries of brown sandstone equal in beauty and value, and possess- 
ing in many respects the same qualities, with that so much admired 
from Lake Superior, are first publicly noticed in this report. 

Prominence is also very properly given to the layers of carbona- 
ceous shale, containing from fifteen to forty-five per cent. of bitumin- 
ous matter, which may, at some future time, be utilized in some way. 
It was found that this shale occupies a position between the Blue 
limestone below, and the Galena limestone above; and it thus be- 
comes a ready means of determining the exact position of the mining 
grounds, with reference to the geological formations. "We have here 
probable evidence of a considerable period of time during which vege- 
table life— perhaps in the form of sea weeds— predominated, and 
which may be regarded as an incipient effort towards the state of 
things that long ages afterwards supplied coal and oil to the world. 

” The history of former efforts in the production of copper at Mineral 
Point will be found interesting, and may lead to renewed efforts in 
that direction. 


With regard to the zine ores — consisting of the sulphuret (sphaler- 


ANNUAL REPORT FOR 1873. 11 


ite or blende) and the carbonate (Smithsonite, or dry-bone) often, 
though improperly, called calamine, a term rightfully belonging to 
the silicious oxide, that probably does not occur in the lead region — 
full details will be found in Mr. Strong’s report, showing the wonder- 
ful increase of production within the past two or three years. Woe 
have here a case where an ore, supposed for a long time to be worth- 
less, is suddenly invested with great value; and owners of abandoned 
mines, find themselves in the possession of unexpected wealth. It is 
to be regretted that the want of a cheap fuel in the lead region pre- 
vents the smelting of these ores within our own state. The construc- 
tion of a railroad from Milwaukee directly to the source of supply of 
these zinc ores, by cheapening the cost of transportation, might render 
the manufacture of spelter and zinc-white, a business of profit on the 
shores of Lake Michigan. 

It is proper here to call attention to the fact that Wisconsin lead is 
known in the arts as soft lead, in contra-distinction from hard lead, 
so called, that comes from the far west. The latter kind, separated 
mostly from the silver lead ores, is supposed to contain other metals 
as impurities; while the former is free from all deleterious substances. 
Doubtless the poisonous quality of some lead pipes used for the con- 
veyance of water may arise from the presence of arsenic, or other im- 
purities from which our lead is free. 

The very extended series of barometrical observations for altitude, 
made by Mr. Strong and his party, will have special value in tho 
mining region, not only at present but for all future time. 

Another highly important subject, the diminution of the flow of 
water from springs, and in the rivers and smaller streams is very 
properly presented, and many new facts mentioned. Although this 
falling off of the amount of water may be an advantage in working 
the lead, zinc and copper mines, allowing the miner to penetrate to 
greater depths before the steam pump or the tunnel must be resorted 
to, yet in view of other vital interests, this drying up of the living 
waters is to be deemed a disaster, which it should be the business of 
a wise and prudent government to check. Within the life-time of an 
individual, perhaps the change is not sufficient to be of much conse- 
quence; but within the life of the state, it will become a matter 
deserving the most serious attention. 

It is perhaps to be regretted, that the necessity of extending the 
geological survey over the whole state, with an area of fifty-six thou- 
sand square miles, renders it impossible to make such special surveys 
of each mining district as are wanted for the practical purposes of the 
miner, and seem to be expected in some localities. Such working 


12 GEOLOGICAL SURVEY OF WISCONSIN. 


plans can only be made by the mining companies, and landed propri- 
etors. Had this work been undertaken for each mining neighborhood, 
there would have been but little time or means left for the prosecu- 
tion of the survey in other portions of the state. 

It is deemed to be the proper business of the state survey to ascer- 
tain the dip, number, magnitude, and relative position of the various 
rock-strata; and, in the lead region especially, to make a careful top- 
ographical survey for the purpose of ascertaining as far as possible 
the amount of denudation, and the exact position of the mining 
ground at each locality. The miner is thus supplied with correct and 
tangible information to guide him in conducting his operations in 
prospecting for new ranges, by showing which are the mineral-bear- 
ing rocks, with their locality, dip, and thickness. This must be done, 
not only for the mining region proper, but for the whole state. 

It is the proper business of the miner, at the expense of the owners, 
and not of the geologist at the public expense, to search with pick in 
hand, within the limits thus defined, for mineral ranges, sinking 
shafts here and there until he meets with success, It then, and not 
until then, becomes the business of the mining engineer to make those 
minute and detailed investigations and surveys that are needed in the 
preparation of working plans, maps and profiles, showing the most 
proper and economical method of working the mines so discovered. 
Such survey and map should show the exact extent, location, and dip 
of the several veins, with their crossings; the present condition of the 
works; the proper system of drainage; the depth to which the veins 
may be supposed to extend; the contour of the ground; and many 
other items, varying, of course, with the peculiarities of each location. 

Such surveys and plans are necessary for the proper working of any 
mines, as has often been found at great cost; but they do not come 
within the requirements of the Jaw authorizing and defining the pres- 
ent geological survey of Wisconsin. Should such surveys ever be 
undertaken by the state, the work now being done by Mr. Strong, 
will be a necessary preparation for their proper execution. 

To indicate what is required by owners of mining property in the 
lead region. Mr. Strong has prepared a map of the Blue Mounds in 
Dane and Iowa counties, with the Brigham mines, showing the geo- 
logical formations in colors, in the usual method, and also the topog- 
raphy by contour lines, and the depth at which each rock would be 
reached from any point. With the accompanying explanations it will 
be found that this kind of map shows a very considerable amount of 
special information needed for practical purposes, and for deciding 
many important questions in regard to the proper working of the mines. 


ANNUAL REPORT FOR 1873. 13 


To Mr. James Wilson, Jr., of Cassville, the survey is indebted for 
a traced copy of his detailed and very valuable working map of the 
Muscalunge diggings in Grant county, showing in full detail the ex- 
act location, direction, and extent of all the drifts, adits, and shafts, 
with the depth of the principal shafts, and the local names by which 
they are known. This map will be of general interest as showing the 
intricate and complicated nature of these drifts in the lead region. It 
could only be constructed from surveys made at different times dur- 
ing the history of mining operations; for many of these drifts and 
shafts, having been abanduned, are now obstructed with rubbish or 
filled with water. To explore and survey them at this time would 
require a heavy outlay in clearing these passages; an outlay which 
would scarcely be justified, except for the purposes of the owner in 
recommencing the work of mining. 

The experience gained during the past year will perhaps enable us 
to do a greater amount of work hereafter. Much of the detailed in- 
formation collected does not properly come into a report intended 
more especially to show the progress of the work, and to give early 
notice of important discoveries. Our note books will again be called 
into service in the preparation of the final report, intended to em- 
brace the whole subject. 


Practicat Iwportance or GrotogicaL Knowreper. — The propri- 
ety of a more general diffusion of accurate knowledge of the simplest 
facts and deductions in modern geological science is evinced by the 
very positive assurances of numerous letter writers that coal is found 
—nhaving been dug out by badgers, or otherwise exposed —in this 
state, which is well known to be entirely underlaid by strata of date 
much older than the coal-formation. We found one party diligently 
boring into a stratum of soft green shale, just like — as he informed 
us —- the clay under which coal is found in Ohio and Pennsylvania. 
The slightest examination of the fossils found in this shale sufficed 
to show that it belonged to the Silurian age, and was deposited 
long before those peculiar conditions were brought into existence, 
which gave origin to the coal. We had here a practical illustra- 
tion of the importance of the study of paleontology, the index, 
by means of which any given formation wherever found, can at 
once be referred to its proper position in the geological series, and 
thus lead with unerring certainty to inferences of the greatest practi- 
cal importance. 

Other parties were found sinking shafts, or digging wells under the 
direction of “spiritual mediums,” or of persons skilled with the di- 


14 GEOLOGICAL SURVEY OF WISCONSIN. 


vining rod. Such persons can seldom be convinced of the futility of 
their labor by an appeal to the fossils. 


Mr. Epcerron’s Survey.— Mr. B. H. Edgerton, engineer, having 
been commissioned by the Milwaukee and Northern Railroad Com- 
pany to survey the northern extension of their road from Green Bay, 
an arrangement was made with him to report the results of such ob- 
servations as he might be able to make, that would forward the ob- 
jects of the geological survey. The line run was from near Green 
Bay, in ranges 19 and 20, very directly north to the Menomonee river, 
which it crossed at the head of the Big Quinnesec Falls. The list of 
elevations furnished by him shows the height of the ground above 
the level of Lake Michigan at the crossing of every section line, and 
the level of the surface of the water in the rivers over which the line 
was run. These latter are as follows: 


ELEVATION ABOVE 
Sec. | T. R. - 
e 
Michioasi. The Sea 
East Feet. Feet. 
Little Suamico ........eeceececceeees 26 26 19 144 722 
Pensaukee river ...-e. cece ec ee eceee 35 27 19 128 706 
North branch of Pensaukee .......... 23 27 19 139 17 
Oconto, above the falls...........-.6. 25 28 19 132 710 
Littlecvi ven’. ncsesnetei neces a ease isin oc 1 98 19 164 742 
North branch of Little river .......... 94 29 19 180 758 
Little: Peshtigo isis sesjon0se0sesaain sas 36 30 19 157 735 
Little Peshtigo lake............. «| 25 80 19 457 135 
A small lake on ...........0.. 24 30 19 159 737 
A creek (first sandstone found) 31 31 19 135 713 
Beaver creek, on.......... 13 31 19 139 7117 
Peshtigo river ..........- 26 32 19 162 740 
Middle inlet...... 18 33 20 192 770 
North branch «50% se04 ss0 5 33 20 211 789 
Wausaukan river......... 21 34 20 242 820 
Pike river.......... ihe hd 3.8 15 85 20 309 887 
Peminee-Bon-Won river ........ ze] $B8 37 20 415 993 
North branch of same .............0. 10 37 20 438 1,016 
Menomonee river.......--......0.005 7 38 20 472 1,050 
Highest ground (2 miles south of river)| 18 38 20 571 1,149 


No indications of the existence of workable beds or veins of iron 
ore were observed upon this route; if any exist they are further to 
the north and west. 

Mr. Edgerton reports as follows: “The geological formation of the 
country traversed I found to be much the same as indicated on your 
map, except that I did not succeed is discovering any evidence of the 
belt marked thereon as the St. Peters sandstone. The first cropping 


ANNUAL REPORT FOR 1873. 15 


out of the rock which we found is at the Oconto Falls, in section 25, 
town 28, range 19 east, where the Magnesian limestone makes its 
appearance in the banks of the river and adjacent bluffs. The per- 
pendicular fall here is about twenty-two feet, and the rapids which 
succeed make the whole fall of the river about sixty feet. 

“We first discovered the Potsdam sandstone in section 34, town 
31, range 19, where the bed and banks of a small creek are of this 
formation. It is a dark-colored loose stone, too soft to serve any use- 
ful purpose. At the falls of the Peshtigo river, in section 24, town 
32, range 19, this sandstone is of a firmer and finer texture, and may 
be found useful as a building material. It has also a sharp grit, and 
close grain, that renders it serviceable for grindstones, and I was told 
that at an early day it was used for sharpening edged tools. 

“In section 86, town 38, range 19, granite first shows itself, and 
with other metamorphic rocks, crops out from time to time until we 
reach the Menomonee river. It is a very abundant material at Pike 
river, in sections 15 and 16, town 35, range 20, and forms the bed 
and banks of the river at the falls. In section 34, town 37, range 
20, trap rocks' are found interspersed with the granite, along the 
banks of the Peminee-Bon-Won, but after leaving that stream until 
we reach the north branch in section 3 of the same township, no rocks 
appear on the surface except granite. At the crossing of the North 
Branch, trap rocks again make their appearance and are frequently 
seen in alternation with the granite, until we reach the crossing of the 
Menomonee river on section 7, town 38, range 20, at the head of the 
Big Quinnesec Falls; at which point the rocks are mostly granite, but 
a small area at the top is composed of trap mingled with some talcose 
rocks. 

“The granite of this region is mostly schistose in character and is 
frequently coarse and soft, so as to be of little use as a building ma- 
terial. It often abounds in seams, filled with feldspar, and other sub- 
stances; and quite frequently these seams cross each other at acute 
angles. 

“From the Peshtigo river I went westward as far as Thunder Lake, 
in section 15, town 32, range 18, and first discovered the granite in 
this direction near the line between ranges 18 and 19, and at the 
point between sections 13 and 18. 

“ At Keshena in town 27, range 15, or a little northwest from the 
village, the same rocks appear; and I judge that the line between the 
sandstone and granite follows about a northeasterly course to the Me- 
nomonee river, in town 36, range 21 east.” 


1These and the following rocks spoken of as trappean are metamorphic 


16 GEOLOGICAL SURVEY OF WISCONSIN. 


TovocrarnicaL Survey.— Much of the success of any geological 
survey depends upon the accurate measurement of the elevation of 
the country above some well known datum plane. For all such deter- 
minations in Wisconsin the level of Lake Michigan forms a conven- 
ient base from which to measure. The elevation of this lake above 
the sea was long ago determined, by the topographer of the early 
Michigan geological survey, under the direction of the lamented Dr. 
Douglas Houghton, to be 578 feet. Probably the first spirit level 
brought to Wisconsin was that of the late Hon. Byron Kilbourn, who 
in March, 1836, established the zero, at the lake level, to which all 
subsequent work of street grading, sewers, and the water-works of 
Milwaukee has been referred. It was also from this now well es- 
tablished datum plane that the surveys of the Milwaukee & Missis- 
sippi, the La Crosse & Milwaukee, and the Milwaukee & Horicon 
railroads were commenced; and it is to this zero therefore, that all 
work of the present geological survey will be referred. 

Since 1836, the level of Lake Michigan has varied, from 4 feet above 
this datum, in July, 1838, to 1.65 below in March, 1848, showing a 
total change of 5.65 feet; the mean being about one foot above the 
established zero. : 

These fluctuations have long been known to result from various 
causes, among them the effect of winds and storms; the annual change 
of the seasons producing high and low water, as in ordinary rivers; 
the variations, during different years, or series of years, as to wetness 
or dryness; and finally a regular (though very small) lunar tide, cor- 
responding with that of the ocean. 


Raitroap Exevations. —In the prosecution of any topographical 
as well as of any other survey of the state, it is apparent that advant- 
age should be taken of any work already done by others; and with 
this view, efforts have been made to secure, as far as can now be done 
the results of the several railroad surveys within the state, and the 
following list of stations, with their elevation above Lake Michigan 
and the sea will show what progress has been made in this direction. 

Every railroad station, the elevation of which is here given, becomes 
a bench mark from which our barometrical measurements of the rela- 
tive clevation and depression of various parts of the state, as well as 
all future surveys can be made, with definite knowledge of the abso- 
lute height above Lake Michigan and above the sea level. 

_ The level of Lake Michigan, thus definitely made known, will be 
found a convenient datum plane to which all future railroad surveys 
may be referred; this can be done without the use of negative quan- 


ANNUAL REPORT FOR 1873. 


tities, for no part of Wisconsin lies below that level. 
lication of the following list, it will not be difficult to connect any 
future survey with this, now well established datum plane, and thus 
aid directly in the development of the physical geography and topo- 


graphy of the state. 


ELEVATION OF RAILROAD STATIONS. 


17 
After the pub- 


ELEVATION ABOVE 
Stations. County. 

Lake The 

Michigan Sea, 
Ableman.......0..cccceeecees Sauk anwxade cease vier sends. wve 301 879 
Ackerville... 6. ...seecee eee Washington.................. 480 1053 
is des sdos ered Raven aero hmearha FROG asicacsa ess ny dais ave reusense sree s+ 180 758 
Allen’s Grove... ....eseeeeeeee Wealworthis = ccic-ssas seve chase 293 871 
AMET S tiase's.-.c.2 Saye n-etare easier POPta GO cssneie tia: sei sse eid: sie shoe sien eb 466 1044 
Amherst Junction............. POTS E waa ss eso ahidin wis dares ase aie ine 8 553 1131 
APpletOM wissen cis cecans Benes Oniawautia (C. & N. W.)...... 128 706 
AspplebOne i:s.ie.2dd0. cand ees ave Outagamie (M. & N.)......... 145 723 
OTD dare inp edsbas bed, ot drancics wake Ra LOWE Sis ascicscseseitiess eyeqnea se os iaes 154 732 
Arlington .........ec cece eee es Columbia ....... 2.0 ee ee eee ee 426 1004 
Auburndale ...........--.-+0- OOD excvora worewiore Cision mca ieceatoans 645 1223 
Augusta .....66 ceeeceeeeeeee Eau Claire ..........20200000- 395 973 
AVOCA ..ee cere eee be beeen ees OWE-sce scram eon anobemuaeens 117 695 
Baldwitt sscusciceecnscneecnes Sb. CHOTR a cccie: atvasecauersisaon-adanctcs 560 1188 
Balch’s Ranch.......--++++++- SW 00 ian eidheter cea essoutnals orice anante 389 967 
Bangor de pidewecnvaeienee hens Tai CLOSEE ain: i wie eardseserectsn arsnatnne 174 752 
Bara bOOis-sieesdaiiccucc scan ee Gaile acsicentiud apsostantuegs cine deuSare 984 862 
Bartonasdednscesoues<seaseows Washington...............4-. 320 898 
Beaver. ccaaracienire ease ome PUMEAUE d deasascimeucie accietcieanew suet eiue 379 957 
Beaver Datiiy...c0seaics sinwa vee. DOA GE's wiarsin:sieteses suewinie nercomie 340. 918 
Bearse Marsh..........-+-+00- CW OO! sya s.eedescoiiiaiia Sinatiane itera aeaeaaus 409 987 
Belgium ...... 0-2. ees cece eee OZAUKEE i ciniecerecene duatrase aieveauiteceve 153 731 
Beloit ... 3 fe ROCK: sctvasteav ou crmaubivanneecervosecalctnns 163 741 
Bellville | Jefferson’... 6.0.6 cee ee eee eee 248 826 
Berlin ...... .| Green Lake ............5 20005 184 762 
Black Earth . Dane ic veievivsieecnwdawaeeecue 232 810 
Black River... . Jackson: ticoes savaddacsdenaan 302 889 
Black River Falls JACKSON ss cesaceecce cwwenn oe 231 800 
Blooms ..... Sault vaiese. seta dadaaneaunand! 304 882 
Blue River Gran by) 2scaes spots coach etearsent aisears 85 608 
Boardman .....- Ste Crore uo siiiein erag ane dartiauearens 379 957 
Boscobel .........-- 34) Grant visss¢eeuasn seh deengtes 89 667 
Branch-Zalesburg ..-..- ..| Manitowoc - 158 736 
Brandom.:.siosa ousaveue. macani’s Fond du Lac . 421 1000 
Bridgeport... .....-eeeeeeeee Crawford . . 47 625 
NISEOL, ice cis goencdenevormieen tue totes Kenosha... 191 769 
Brodhead .....---.+e-eee cence Green ..... 220 798 
Brookfield Junction .....-...-- Waukesha 246 824 
Brooklyn... ....-eeseeeeeeeeee Green ..... 400 978 
Brown Deer.... ssceeeeeerees Milwaukee 85 663 
| Burlington .....-----..es sees Racine......- 203 781 
Burnett Junction ........+--++ Dodge ..--.++.- 299 877 
Cambria .......eecceeeee cere Columbia 1.2... sce e eee eee eee 284 862 
Camp Douglas Junction ......- UNEAM eevee ee eeee eee eeeees 356 934 
CatO is sc ca'eissas can weien eas Manitowoc ...----.- eee eee eee 946 82-4 
Calamineg:s.2s040% seewie taedoes La Fayette .....----- see eee 234 812 
Calvary ...... gue sine geass sibs Fond du Lac .......---- eee eee 362 940 
Cedarburg ........2+eseeereee Ozaukee 1... e cece cece ences 191 709 


Wis. Sur. —2 


GEOLOGICAL SURVEY OF WISCONSIN. 


18 
ELEVATION OF RarnroapD StaTions— continued. 
ELEVATION ABOVE 
. County. 
STATIONS iia The 
Michigan.| Sea. 
Cedar Greek, Ackerville ....... Washington........-..eeeeee- 480 1058 
Cedar Grove.... sseeeseeceees Sheboygan ..-.....eeeeeee eee 114 692 
Contraliayacxsccacex caus ness "Wi0Gdk7 wcll cistesincavsnuie wniaes 431 1009 
ChelsGaissanzacencdrases sas es Chippewaiss.ise cess awison geasrs 945 1523 
Chiltoti..ce.assveweeiw sas vasaes Galimet caren cateuwemewenrwere 269 846 
Clinton Junction.............. ROE achaiwbawaeginruaeaneee 363 941 
Clyniait,. ian csaccex cesses asexe< DOA G6 xnracaussawioraine esata 330 908 
Colby: cauusaane soavecsss aeens Chippewawewseccwnacinnescuas 715 1353 
Columbus::s20222000.ax ever sys COlMDIEs waisinccinganaarectersnerens 256 834 
Gounty Line.«sass% seven exe Milwaukee ...... cee cee eeeee 117 695 
Cross Plaiigecers cece scsecesxs DV BUTE ve cas ave wtasiceatn adeta lata me eoteraisCenese 280 858 
Dane ccorccreeeasex sees ened T)ATIG eo scarors sbenee ntptsterenauuarehaawn 481 1059 
Darieh, «ses eee exeee sts ee sree: Wall Wort iiss csetsratinana ranstosalassioetiss 367 945 
Darlirigton ssc 62a0. vs vaneres Vea Payette sc:o:0 x aieiscasy aise nsierees 224 802 
Deanvilles: cae syectes vas vanks IL) EAIUG ios wraeher os Rare arharaet pee eneela 305 873 
Dette. sans anewenassees soto Sheboygan vcs sisinis dais snaaiens 179 757 
De: Rorests22 sre .seeeorescass DatiGs caxcaue sues meee wae ars 341 919 
DelAVaN is e2curcraesseaees Woalworthiss.0..sumrecesxmcuvas 856 934 
Deperes ssscecivvs eusivs eed BrOwiles ancdansughat annaniines 9 587 
Dexterville: ..cc0csevesieverass WO0d. cax4ce00 exancam meee 417 998 
Dillltiatterse scace deve sens es2 4 Milwauke@:.xs.seecsasanenvac 107 685 
Dodgev Weis icsccccesescc saves TOWai.aciorn manner ancien aes 691 1269 
Dorchester ssavasaeescevacesss Chippewalis+ sae sxessesama xe $38 1416 
DOVER wwe snes taxes saecees oe DONG rca sses os oe ea oe wears 234 gif 
Dretickers scccne edie aeoueetexs O7aUkO: i530 aawcaseaanm a8 154 73 
GHEE ewes ese wean ce ene Calumet: sic0scnracnaacvarcassers 160 738 
Doyles — Otsego.........---24- Columbia, s<e060 sas sersimciare. 360 933 
Devils: Dakesa: fies eesssa5e55 AIC wicectte conc ntree nlomanitireies 390 968 
Maples saxesass eanseanences es Waukesha, osecasis av ecacenc ee 365 943 
Eagle Junction.............6 Waukesha: siccascistintcescicesciave 360 938 
Fast Madison..........-ee.065 Dan iiasia via nxt 50 4 be fereeacestes 268 846 
Bau Claires iene. ww eeeer cane Haar. Clait@s 5.5 4:0 vieieeceiare sens 266 844. 
HagertOn's:: nie x ocee esees yee ROCKS sicteseresaivears Aeiase these cocsealel overs 242 820 
Ehlers lids ee ee OZ KEE i sr thie 5 vere essccsiser assaueos 93 671 
HldOradO'rs:00 seceanes soceeands Sheboygan .........0e.eeeeeee 297 875 
Elkhart. Lake... s<scssccssesss Sheboygan ......-..eeseeeeeee 362 940 
ch OPilcc'seie corns eae eewsreaaxs Weal wortlia.iesovenaces scach.cvernsrarctvernte 413 991 
Filk. Mond s secon esd dcanses RATT snc soeve evseiaaceictavamiuarhaveornvens B51 929 
Elm Grovews sn ccwee cavexanses SWFELTURES INET sec avanaccncreroxecoiatsouontdinaiere 170 748 
Elm Groves sas cssccvaterarve. Weatakeshia s-sceiesocnvave viernes ave sisios 166 744 
BOY iene case rnae sear sareae UT CA asssvecerecsciceismevannanrmartenndeas 388 966 
Bearerile Sida iuaaitea ecscatteatae anit TROG kiss fa eshcwovexreuasehs oy acncbeh aieSeseeses 325 908 
Pairchild cs seaie ouceseeseaee ss Hani. CHANG wn enascercienines ovine 487 1065 
Fall Creeks icsaaaeiage saaad on ANT. CHAIR sistas cayeraseacas acsrtesaavirigcats 357 868 
Fall Rivers ssorsoseseanasasees COLI 8: cans wadacencnsiiek 290 985 
Payette: psvvg saan sae escc sev WralwOrthisvecccsscen aczgias aaa acest 283 861 
Fond du Lac............00006 Fond dwLaGes coesedecwarinses 168 746 
BOObVULS saisoancats een Sic core FROCK casas earn ainiscaieineiarese nue 6 288 816 
Forest House............200 0 Woanlktésha si:isenecavureeeyare « 240 818 
Forest Junction .............4. CRMC si actrecg a siidieioie le ase x emcee 250 828 
Fort Atkinson................. JOHCLION scccsieweaawel ew sheds 220 798 
Fort Howard ............00006 BrOWD s-tnidsnies seed tae ney eee 6 584 
Fox Lake Junction............ Dodge Oia resejéie sean saw -eewsn scien 305 883 
Hor: Rivetcsrassnees¢/etneace.sunsces Kenosha ............0005 re 200 7718 
Branksvilles scjssieire sec sts enecans RANG iivusasuys paseus enews 150 723 
Here Wor levers cc avert eGisiscecormaeias Ozaukee csccivmiaemeeanrnnr tes 206 784 
GEMESES, 6. sis Stig i-ddiaacarecousnvtr’s Weoaukeshaics cous sea ease atecs $25 903 


ANNUAL REPORT FOR 1873. 


19 


ELEVATION OF RAILROAD STATIONS — continued. 


ELEVATION ABOVE 
STATIONS. County. aa 
ake 
Michigan. The Sea. 
Gene aise sais sida leg xittesee ore eis "Walworth: ses snes sg ee este 274 852 
Genoar saeciatws.. se iMastaecor Wralworthicsissscwn sate sa istsareres 264 842 
Germantown ....-......+e0e- Washington....-........e0e0e 285 863 
GiffOrdSissaune bets das oe pee A eee Waukeshagsawsmageticmecates:s 297 896 
Gills Landing..............065 Wadpaliaceisisieewanewewane 183 761 
Gleason 222% oes ees wher waletonts MOnTOe: a xasencieniiniotirwowte 5506 353 931 
Glenbeulah..... ghitwinongleaatices Sheboygan.......seeeseeceeee 289 867 
Glendale asceudeavaws cihaie des MOnrOG:s. «xs sabe aaeeorensis 419 997 
ee Hopeesssccsewe cons save ne Milwaukee........-.2.0-e000- 112 690 
Grafton. « <ssecccmesenasewe dive OzaWkkee: sc ss ees hives saw ss ae ee 170 748 
Grand Rapids ss uaecenamse sien daeeties Wo0d)ssscceecrssevdsesdae ene 448 926 
Granville «.:2sceecnmwaws semis Milwatiken VE Teer e rr ree 168 746 
Gratiot: acc se cccsesenmoes ence et | Lay Fayette. ..... cc cccececeeee 205 783 
Green Bay ......-.-.2eee cree POWs sss es495 4h seS ase sa 6 584 
Green Bay Jct. (Merrillan)..... Jacksons sc caveas ce ee wees eases 865 943 
Greenfield)... i.0 ssceserreosees Mono sa2222000s0 2400500084 471 1048 
Gréen lake... ... sc esaiias cess Green Lake ....-.......0.005. 935 813 
Greenlead os nic iste ensromewews BroWiis cess weno sees aeees tase 141 719 
Hammond .....--2seeeeeceees Sts. Croikssceaccscteaears cares 525 1108 
Hanover Junction........--+-- Rock .ccissesste.steveseweses 209 787 
Plartlord :s si oeceswsase: aciaetees Washington .......2e.ee eee 408 986 
Hartland.......-ecse cree eeeee Waukesha ......-.. 00sec eres, 333 911 
Flartman......-.2..05 seeeee Colambia:.s<<ccsacceee ee vec 210 798 
Hayton ..--- eee eee e eee e eee ee Calumet ieee ness eerares ge seis 240 818 
Hersey.....-eeeeccereeceeeees Sti CrOiRaisauaes oe eetiera rads 588 1166 
Herseyville.....--- secre eeees MOnroG 435 oc odadeles ab eaectes 190 768 
Filbert as exes. ce steercenerend wen Calumet) sesiesaiéeceeesoen’ 950 823 
Hitchcock ..... 2-222 e eee eee IMGNTO@: a 2ckidpaee ake sid ek ones 364 942 
Horicon Junction ...........-- DOd Eis viccsscagicansecde deena 306 R84 
Hibbelton, «25 cece e sigeiecne wise JHeVSON, pursed oceadedaaies O11 789 
Fidson «iiss cece ceeds ce cows Sti CvOieaied cad aamed Saeed ey 128 706 
Hulls Crossing......+eeee cree Sheboygan.........eeeee eee 354 932 
Humbird...........0eee eee eee Clarks cscciworts eats soe swwnss 418 996 
Humboldt Junction ..........- Milwaukee.........-20e eens 61 639 
Jron Ridge ...--++seeeeeeeeeee Dodge. siirsa niacin tec eeeeees 845 923 
Jamesville ......sstsrvevccwaeies OK gainers teins hede eae 240 818 
Jefferson’ «ssc ste ew earawaeee Jefferson... cece cceccreeeeeee 921 799 
Johnson Creek.......2+-+-+0+5 TetersOnicasii ces iclavee deel ca 193 771 
Tada ccieva cosa shoes iat a aeonaaNe GreeienavowaWeeiea vsceweactetets 243 821 
JUnea 6c ese oe esa ceee eee aes Dodge-aa wes se veeisteciesienees 335 913 
Junction City....-..--see reese Portage... css seacesd ee caeees 572 1150 
Ransasville:s0cs ac eseanaces wets AGING: Stee sakes ow eee ke 240 818 
Kaukauna. ....--..02 ceeeeee Outagamie .. ......e eee eeeeee 80 658 
Kenosha ....---+++ ihegiemtaicetics paate Uaieegtana seinen nae ek eu a a 
mosha Junction........++-+- Ondshasscxctvesevesvcaaeees 
Ker estes ates gor $5Cs i i8s Seats Glithes wou cope Sine ONCE hE CARR eeeaS4 ne a 
uri ClbY sos eas cess ce de nes Olumbid sad eds eee sees as 3 
Keboure City sd poe teTaEe eee Milwaukee .. ...-..--..0-.0ee 10 588 
Kirkwood ....seeee cece ee ereee Gatiloausticceraehies are esas 286 864 
Unapp- eee ec ecee cece erecceeee| DUDN. cece ieee rere eter eee aee 349 927 
Knowlton... 2. cece ce ee eeeee Marathon. ........e-eceeeeeee 547 1125 
Koshkonong ...-.+eeeeeeeeees Rothksvcwusccaa dad ocean tas 949 827 
Tia: CrOssC. moon eee tas eae Tia. Cross@siicvavse ce wo teaiee cass 70 64e 
La Fayette.....--sseee cece eee MOnxG6 si weet eee wees eee 803 881 
Take siascowatecsar a ooeas kates Milwaukee we vine see eee cees 154 732 
Lake Side........:22seeeeeeee Waukesha .. ..-..eeeee eee eee 292 870 
Lamartine ....---..eeeeeeeeee Fond du Lac.........seeeeee 250 825 


20 GEOLOGICAL SURVEY OF WISCONSIN. 
ELEVATION oF Rartroap Stations — continued. 
ELEVATION ABOVE 
STATIONS. County. 
Lake The 
Michigan.| Sea. 

Lathanivcsteriieeen echisbee s Calime tevaihs woe eax e leew a 148 721 
Wai Al Oh: cnitensvernGlorern soma ta nig tee AU as gue Bini! sabi ate wiaolduane 820 898 
Ledgeville....csscreecseececes BroWitesse rierdampas ee senenes 96 674 
Tie@Mmonwelt .s.0ss04s eacw ea ese JUNCAU see ai eras epee rarer ces 316 894. 
LOROY se wecienwAvatnaes sone aeities Monroe’: ssnacedseawaredee tas 875 953 
Vie WASTON soa 2505 shes spaverietatin’s peek Columbidiesivces acadecesawres 231 809 
Dim aiieanitiaicen sneawngeind tee Rock cian Sewn ueukacnsueesiae 310 888 
Gini s eee ee eee nee JUNEAU = sadamayuasreetainctans 320 898 
Dan d Wert. evi. sccseisisiers sa sarnoceoxe Milwaukee ........ceceeeeaee 56 634. 
Little Chutes cee peeeieiaceeigrs Outagamie .........eeeeeeeee 144 722 
M18 WOU aa sears thanen sor esiexevabaviwiatonne IRAN GAN Supererenceatninddshas sreete deacons 315 893 
Tyrone Rok: esis scvivecesieareacevs Richi amd sicdrasauslercnnesssensraeateiae 126 704 
DOU tisrarspz aesvacivariciasastoiners Pease taeda Colum bidiwctwence genacemagtel an oar 271 849 
Lowell se-nnactsdenaaseisaaierts DOD GO acteriiisuie eine cteaiasliacaseele 247 825 
LOWOLY Scien’ Bota ecirseddumeae MONLOG! cs dows dene ameeranes 389 967 
LYONS) oaisiervaniteaieroreiacis Wealwortlt, 0 csensveuwensce ¢ 222 800 
adison, east .........eeeeeee DANO? eiccarcetsted tates arsine sa 268 846 
Madison: sccececcsccccssvidecace avanurecers I AT Os vse tticasereis rare naga ale anaes 275 453 
MA pM OMA is 6-sa.ns ovine oe vie 4 Rok sivigces weipicreiosaeen seein 340 918 
EMEAMAIWEA :osanacaveradtxarncacavadare crbstreeasers W aUpaea kissin ca enee ous 246 824 
Manitowoc .......-e-se0- eee Mamitow0c....---..20.08 sees 7 585 
Manville ...........cee eee eee Marathon: sci nesyseaacincn cone ee 713 1291 
Marslialll.,| sissecxsvasaceaearea exec eave Wan Gans vies anes dau tumleer tes 286 864 
MAUStOL: sivecssahinss Guid gatviavvesde04 JUN CAMs cnieaisinieds cnt daula ee0s 309 887 
Mazomanie .........e.ee eens DAaNCiiin tucatgenrcigne takeanoan 195 773 
McFarland ............2.000- Dane rat accnedtacsoiensl naa dts 289 867 
MCU EO 5:5 2:5: 6:0005 siecriece gn esaecelans Chippewas csccniseedewinten 842 1420 
COTE jays soseiccoss ie din teseverasbinanrciasone Outagamie................00. 192 770 
Mena Shiai cisseiats hs fosaze uvacana wipes Winnthaed:csissensecnaeennes 177 755 
Menomonie vs... esse eeeeeeees Din ws weesenirvaidumras y's waren cca. 3806 884 
MG TaD SGT syesrsseceue cal este 6 Lavsenena di hobs JACKROM washers seta ytigh aederacierhs secs 365 943 
Merrimac ....--. ee eee eee eee DU ciara sive tanaiasbaseen Yeagearee co 219 797 
Moquon......... sce cece ences Onauke: os: sia: on saecseaeisee sane 92 670 
Middleton.......... sce eeeee DGG stat canal ap naranctrentag lee coves 347 925 
Mill Oreck .............0.000, Wood visi cieiarscausieutaeunainee tose s 514 1092 
Min ye ctictesuecsinareaanuuva eG keesreis caeatesajienenensiaatansin bien case 293 871 
Milton Junction ........-..... TOG ts: sisecrenskniensicl ancestor net ccsacdes 299 877 
Milwaukee .............-..4. Milwaukee................... 5 583 
Mineral Point ................ OWA exe -avvicrstans esacerwiene a brisetvicsicas 357 935 
Minnesota Junction........... DOG G0 asoricgeecensiwreresaca availing 5 ate, duane 348 926 
MOny 08 ssc iste ce ctseseidierb quanecarninan GLOGM paisieeie ia enesiameintrire cnaacavas 492 870 
MOTIISOT: «sissies ws6's: sueieshasrinsctica ar Dari Oy ssiesisrcietasacrertearouiee Scvarpscecrs 387 965 
Mis0d a) sesso seiiacn: wrececsumecaes Grain ti Legececesvste oniatearemn.ecar case 109 687 
Nashotahtssecede rico cescettessie cece Waukesha .........ccccaeeeee 350 928 
Necriahs sxe cairns. sicisacareue sewed WMINCDALO ex = cee Ge4 8 6 byeceserten 170 748 
Nepeuskin (Rush Lake Junction)} Winnebago ................. 263 841 
ew Holstein ................ AMG: ss sve 5 Be Serdar aioe 351 929 
New Richtnond............... Db; CYOlR iss ay ta marersesicm aoe 411 989 
Northport...............00085 Weaupaed, os .eriie de ccceceeas 182 760 
North Prairie................. Waukesha ............0...., 363 941 
North Wisconsin Junction..... bs COIs seinnerwerricBc aman auc 295 872 
NOR Wat Yinieedarasiscicemeniciyoreyicastcatans MONKOC san 8909 HH eeieciaiesuiaieng 407 985 
Qalkk Greely ica ai ta diceecarenceeceaeae Milwaukee...............005. 86 664. 
Oa eRel er sia is sicasaca etareconaceseubtcnee Pond Git Latesorsscny vcanecag 810 888 
Oak wd ec%54.20%:0 cee ecevns sion Milwaukee................00. 105 685. 
Oconomowoc .......- 2.0. eee Waukesha ..............000, 983 861 
Ogdensburg ...........000005 Waupaca.......... wens drei ee 992 870 


ANNUAL REPORT FOR 1878. 


21 


ELEVATION oF RAILROAD STaTrons— continued. 


ELEvATIoN ABOVE 


STATIONS. CouNTIES. 
Lake The 
Michigan.| Sea. 
QRGC: ss ees ware inetowwigau eines Columbia: 01a s4sae ass euewe i 220 798 
Oosbburgyecs sces ces coe asa awe OZAUKEE «3+ sie sense aan eeaeeas 102 680 
Qrange sc: swertnacocises'sede s JUNEANY oeicecys oenenacsaneas 327 905 
Oregon Aciawennwcnsemes sees: Dan@asaccswsvneceroens seas 365 943 
Orford <4 906 a sitievs nee eee Rock tekcasc coo sek Guse ea here 313 891 
Oshkosh s</ostscswee sakes tony 4 Winnebago .......-- By sties ene 170 748 
Otsego. . ss. ese e cece eee ee eee Coltambias sixes secs since sce ees 360 988 
Pacis: it scadcecies vane oss Columbia: «ives asics enien eigen es 205 783 
Palmyra ......-s esse eee eee Jefferson. ci xses eed saiav nner her 260 838 
Pardeeville.........-s..eeeeee Columbia .......-. roe ers 232 810 
Penokee Gap -.---.-+s-eeseeee Ashland v1 sis scenes saenwets 713 1291 
Pewaukee: i063 sccacccsanadacs’ Waukesha .....+... eee ee eres 263 841 
Pine LakGscssweseaterea eed ¢ Waukesha ......-.---:00 ee eee 350 928 
Pleasant Prairie ........ «1... Kenosha s.ccsoa3 sired nae a ccheed shece 119 697 
PlOv er jen neciesnerinw saveitvnae s POTLARE foicvs cians Seah spencises ares acta 504 1082 
Plymouth ...........0.2-e000e Sheboygan ..........-,--.00e- 262 840 
PPOYER GE eo i6ia diese 6.8 bos savacedoonsenacds OLIN DUAY- cxsvsitn a Sciea aialeneraiersieiebevice 232 810 
Port wast apdlacsunncaceneaseeass W000 iecnacieaswestaienaeduatiatiage 388 966 
Port Washington ...........+- Dd pas steep a ee 87 665 
Prairie du Chien.............. Crawford ........... eee cece 41 619 
Princeton ......66 ceeeeeeeeee Green Lake ........--.---002 188 766 
Paoli Mts serene ons oss Rina Sivetsipinnie cd OU Che sik arared crannies eins 428 1006 
Racine (C. & N. W. sdeabacdl arises RAGING sian aaceus is ansuassneranetdieresasnaiard 40 618 
Racine Junction ............-. FRAGING s coae.phsvave Su ntaubidsadedeiaiorcnncaness 43 621 
Racine (W. U.)...-..0-seeeeee RACING aetcesncde ieinrn Giccerhioiaiiacoderdiet 5 583 
Randolph...........eceeeeeee Colin Did ia ecacsisiaredeginzerziscase wicsers 378 956 
Random Jake ..............+- Sheboygan ............e. eee ee 295 873 
Readstown ......2.se.eeeeeee VieiNONiie vac dcnegaatacaek toawe 155 733 
Reedsburg ......--.eeseeec eee Satile wcrc Giensdnen nce seen tau 800 878 
Reeds scorns pi sica exes clgebew 006 Sg Fond du Lac ........e.eeeeee 407 985 
Reed villesic cess seas a ce eee eee Manitowoc........ seiishorass Sere, 942 820 
Remin; a vvkiate ss aes in dauahacseaateaiete’y OO aise dcedsissicaiena cia wetss. od ws 403 981 
Richfield :seeenauneuseies eee Washington.............6.005 3881 959 
Ridsss aaisvscdseesunkants ons 5 Colin Didi 2s vend saan ae 352 930 
Ripon ....... annem Cumin s bye Fond du Lac .......--..--eee- 352 980 
Riverside: .cesxsis semen « coca y La Fayette ....--..es sees reese 208 786 
Roberts) 6. cencsaicscawedve se St: CHO i sis tnte dd wee dias oie es 462 1040 
ROCK ANG sce secs taiawee vies BrOWil. “erlscernouciatesehaanirs + 61 639 
Rolling Prairie ....-......---. DOO Peis wit irrui orice wae ls stele aa nies 363 941 
Rosendale. ..ccneee oecee ss Fond du Lac .....---+. eee 313 891 
Rosendale (west)....+-.-----+- Fond du Lac .......- eee eens 304 882 
Royalton......cccececeerceees Waupata: sesnsacnaecas eerie 259 837 
Rubicon ....0--. cece ese ceees Dod gen stessiawaaciceeseaX 4 440 1018 
Redd: ssid cccawaielecenen JACKSON esis stn ekinecietdtaea tates 403 981 
Rudolphiss.cseeeeswnncsas eae es WOM s.cesscccssundewneisane eater 562 1140 
Rush Lake Junction.........-- Winnebago ...--. eee eee eee ee 263 841 
Ritsk: wayseeinnesatee ke touhete ss ETI fouaivocalte syosossContas  sreaeibsancendes 331 909 
Saleiiisneanewnsewae Hetanien d Via, CYOSSC saiere: i area's a 2caorese 9050s 171 749 
Salem, soccxeuae daeegiwaaes bs Kenosha. ....-+.. edhauseenniaoe 198 776 
Sanderson......+eseeeeeeeeeee TIO ss sseys aeaictspnarestracese atncore <0s868 275 853 
Saukville sssciscexesacereaws 5 Ozaukee: ainineicscexauauiias tales’ 181 759 
Scandinavia ........---;se00e- wyaupas stan tadtoralreute cuisine ered 365 943 
Schleisingerville ...........-.- ane biahictrawneusi sive cuore 474 1052 
Schwartzburg Junction.......- Nei Setpiowee aie HEI Sa ees 66 644 
Geran tom os eains-aveesuriimmiessccunders JacksOn eras sntatssinxe aw ures lees 3 386 964 
Sheboygan ...... ss ee eeeeeeeee Sheboygan .....-.seeeeeeeeeee 7 585 
Sheboygan Falls.........+.+++ Sheboygan ......seeeeeee evens 85 663 


22 GEOLOGICAL SURVEY OF WISCONSIN. 
ELEVATION OF RaILRoAD Stations — continued. 
ELEVATION ABOVE 
STATIONS. CouNTIES. 
Lake The 
Michigan.| Sea. 
Sherwoddsaawass avvilaviswwweels Cavin Gb sa aces ecoencnuasecsvdvenced vars 258 831 
Shopiere ........ cece ee ee ev eee DC lraieccvat headed doraces i tedateasa tienes 366 944, 
SPAPBiics anesueduls aad ayetioeens MOD TOG) ras soivai activa wscecvients 215 793 
SPOMGeR sc :egaye.w's actrs oie bye acagreters Marathon....,..0..2c005 sees 730 1308 
eonng CYEGKS ies cviuracewas we aravat Callie tis. inrscta is coir starencert aoa apsice 248 826 
Springfield ..............0008e Walworth.............cee eee 270 848 
Spring Green...........eee eee Seat lca sos Aidorbb Suerayasaver’ wicks ave 144 722 
State Tans secsissacecugaoroineiecnva esis Racine, C. & N. W......-..... 90 668 
State Tie: ossacessrersceceisiece’eacaieasace Racine, C., M. & St. P......... 90 668 
State Line.......0..ee ce eeeee La Fayette...............005. 475 1053 
Sb: CU OUd enisvstaranvsrarvares onteceiticecave Sheboygan...........-...0006- 349 927 
Stevens Point.......-......4-- POP gE. wisisia eernaclanwsiaawiens 508 1086 
St. Prangis.c.u nasesteasaaaes Milwaukee .......+++--+0s.... 65 643 
SOUPhtON.. .owresmaee siamese Dame tees caysectna luted atecnemei cae 279 857 
Simimitt:.caesiase wa tue ved. Bond du. LaGiinaissin ni sexisen-an aac 398 976 
Sd PEAIIGs sso easiecaresoek eines aieince acs pane anny a elaya kava seh dees gpa aes 356 934 
TVCIIO: avsosseneres vatsedecesasesececaroueve-scecare||, IDAIRG sina tn aia cahsras¥eiiew Oia anges have 820 
Taycheedah .........+.2es0e05 Fond a TAGs jrcccghewiasaa ed aicts 173 751 
Thienville.........-.-eee eee Om aTlce es sisca asdisserordarene deatervenos ets 88 666 
Tomah...... Us ressaestineisicsd gs Sains anaes Monroe: siis-c-iscsessdssrers tareteveieusie 383 961 
Troy Center ............2.004. Wealwor tht wc:ettscesictteiawts aac 295 873 
Truesdell o222cc0cce00b oes ees Kenosha ...........ccccceeees 101 679 
Tunnel City (Greenfield) ....... ONTO astutehce Bioratons res Seneiaralareeyus a 483 1061 
Turtle Creek.........-..0.000. ROCK, «2:4 thernre-srerowsloicienenia nrc 273 851 
AO axe seater ana wae re vice OAM ER a sens stctecvesineno recede wianacs 117 695 
Union Grove:.......+.seeeeeee TRACHIG wiisrorareviseiorouatssassemaretenetnesuei 182 760 
Union Center........2.....04. JUIN CALS shacestionetacvekachioret esp ekexareun ante 366 944 
Valley Junction, Wis. Val- M 
wie R. & W.W.R.B.C: COIR e ed ako aye pee aes 354 932 
Qe eee e cere cece nee e ences SHELOV PAN «6.0.2 cee sven eave 
Waterl0Ovnsienineseey sua xeeasas J | Shebose Bi acsiisatats aiosiants eaten nod an a 
Watertown Junction .......... JOMEISON ac dsnidasnnaacsenluaetecers 243 821 
WialreM ene wirerevairreiceinsiaternets MON TOG vs sec-isccangay scpcsco stereo tae 448 1026 
Woarkau ...6-. sees ee ecee evens Winnebago.......,..0...000.. 474, 1052 
Weakeshainnesecnesamnaasg sis Waukesha ..........-.e00c- 295 803 
Wannakee css sans eiesemaeas Da nee acca e hein eicetnad aie ace B45 923 
‘Waupaca Se scar Tere or ee eer ear Waupaca fats anchaGhaniaeaises tote 814 892 
Waupunve ences sii sieutrasamnbe Dt a0 ccrcasceadeoiceor cea iocn 314 892 
Wiad Balsicinteiistsireiacsiecanesiien Marathon..............00.... 643 1221 
Wauwatosa .......-.-...c0e0- Milwaukee................... 713 651 
IW ata eles possteinacexssansts Gtaneiie fe larding Crawford...............00000, 60 38 
Weedens Crossing............. BUSHOR GAM woes ceceeees nua sve 115 6 3 
Wiest DOr sccscacaiscs-sieceina aie sos hippewa.......-seee. eos l 993 oe 
West Madison................ Danenraniathssctoena le 275 150 
‘Western Union Junction....... Racine................... ne 144 853 
Westport. s+sesesesereccn Ua ah ae 
CVAUWC RU oe ae anid eouee een Waupaca.......-.... 20000, 
White Fish Bay ..... 20.00... ieee ee es i 761 
Whitewater. cass vieessanen Walworth............0000000° 2 651 
WAlkON gia oda ete s sah bales SPICHOI cadk eee eh 819 
WHISON siccccn ected med Seka gsi Sheboygan............00000., 1 8 1096 
Walt ON eu  oceniawasicdiearaaeg GLO keke aba 02 780 
WAN BOR ad snaked aumacanie: kis DaHB siccdc wacacie commen co 414 992 
Wan dsORicts aieqantiewaincactieiparts RaGh@tascsllstcccmaeaee Ct 804 882 
Winona Junction ............. La Crosse.......0.0000 179 157 
romewon, rer ere AUMEA shades pyweegs eae cad 338 Hi 
Oodand...... eee eee eee DON BO sa csisxizcien carte ee ca were 373 951 


ANNUAL REPORT FOR 1873. 


23 
Exrvation or Rartroap Stations — continued. 
ELEVATION ABOVE 
StaTIONs. CouNnTIES. 
Lake The 
Michigan.| Sea. 
Woodman.....-...e.eeeeeeeee Grants cieavateceenciovies es 73 651 
Woodworth Kenosha... se cee cece eee ee eee 170 748 
Worcester. . . Chippewa 1038 1616 
Wright's...... Jackson 353 -981 
Wrightstown. . ..| Crawford 48 626 
Wyocena...... .-| Columbia, . 249 827 
Zalesburg ... al Wi aaaabopsens viele pe fwewcesevine 158 736 
ELEVATION OF LAKES IN WISCONSIN 
Beaver Dam pond.......-..--- DOdgE: acvscseedeneeresaeeces 282 860 
Bonner’s Lake.........---+-- Racin swe ck ance vested 200 778 
Cranberry... +. ee eee c ee eee Jefferson ....-.cceecccececees 269 847 
Crooked. .... 0.0 eee eee eee eee Waukesha ....-+-..eceeeeeees 288 866 
ous ee eee LIK weenie ku clase Nearness 390 968 
Jase aia oeabess oes evees A ae tien Bae alt fe 
lkbeat (Station) .......-..... ACHOVORN is sents seis vnewetees j 

Fox (Junction Station) ........ DOdGE senwcieeeakhe teense es 805 883 
Width .. 0.22 eees es Dane sts panera i B24 902 

Geneva (R. R. Bridge)......--- WONtles wetgackan sige Yeem 
Grea ie Station, <«. 2.6 sce Green Lake ........-.-+ 2000s 235 813 
Haymarsh.....-+eeeeeeee eee ee PGI le ssocins eon csr crsuare yes Wismreneea tase 620 1198 
Holdens....-+-escs secre cece | Walworth saciaicancs3 28h-eeewns 325 903 
Floricon -. ++ eee cere cere eee Dodge .---+-.-erecereeeeeees 277 855 
Keegus... secs eccc cece ececcee Wratti@SWaiieeisasdaoas sd iaesie-eie 2 376 954 
Kegonsa (Ist)..---.+--+-+-+--- Dane LLAbe ee ee KRey ETERS S * 260 762 
* Koshkonong....--.-++eeeee eee Jefferson... eee cess eee ee eee eee 184 851 
La Belle ..--+-- eer eeccet eevee Leese pea aneawnaclees a Be 

i Deserk «x acca cin ae Veuir!  .  e a ere e 
ea Pies : ie cr chea rich daisies Bayfield .........ceeeeeee cree es eae 

AEN), cave wetness Dane. weanwenseenheswase res 
Menta ¢ ne ) nopiled Wea at oa Milwaukee ........sccceecccclooecs ay an 

eiherai mina ca aMaasiats 4S Watie: eyacccmsaawayeee sed cies ) 

Muon & a ee use tee. Tiss cagirceetan ayes tees 328 906 

cccsen'd wicheieee. goheMvaesee GG Waukesha .....--scccerecece 
lees mpeg slbg Risk Mars te AS Waukesha .-...cccsccsecveecs 804 882 
Nashotah, upper. ---+--+erse+- Waukesha ........cccceceeeee 290 £68 
Narnah bine. @ssutsy ams re ocr Waukesha ......2..eeeeeeeeee 289 867 
Oconomowoe «.-+seee sree eres Waukesha .........ccceeceees 282 860 
Pewaukee... see eee creer eeeeee Waukesha ..........eeeseeees 263 841 
Pike wo. cece cece reece ceeeeee Washington........2seeeeeeee 416 994 
POWETS cee ee cree e eee ee ee tteee Kenosha .....seeeeeeeee eens 260 838 
Pucawa.-cceccseeeeeeeeeeeees Green Lake ........-..0ceee0- 206 784 
Random ...-eeeeereeceeeeenes Sheboygan ...-..seeeeeeeeeee 295 873 
Rush ..cecceece cece eeeerreee Winnebago ...--.seeeee eee eee 263 841 
Shawano ..--.-- i Sek MORIN Ghawan0. ssssceeseceeeeceeee 221 799 
Gilver..eceee eee e eer eer ee teeee Waukesha ......-. 02 see cece ee 278 856 
Spring ..-ee eer sees eres eeees Columbia .......eeeeeeeeeeeee 205 783 
Superior .... eee eee e eee cere ee Ashland, os4c:0s cv ntasresemiamnns 22 600 
Trout ...ceceeeeer ce ceeeeeete TAN COM: ss ele: aie 2ecerece vt orn besinelans 961 1539 
NWVUL sec e rec cn cece ce eneeeeeee Fond du Lac .... sees cece eens 450 1028 
Waubesa (2d) .-+--+++++eeeees Dane ceeeeceeeseeeeeeeeeeees 261 839 
ING « = 2.5 58 ¥ wa ierpdin gs Ses weerese mre se RACiiGs sae-cadlasauereccqeesey v's 190 768 
Winnebago ...-+-. sees e cere Winnebago ......ee eee ee eens 162 749 


24 GEOLOGICAL SURVEY OF WISCONSIN. 


ELEVATION OF SUMMITS, MOUNDS, HIGHLANDS, Erc. 


ELEVATION ABOVE 
Lake 

Michigan. The Sea. 

State Line of Illinois — 
On the line between Ranges 18 and 19 (Genoa) ........--.---- 262 840 
© O& N.. W. RB. RB. Glar0n) vsesacses meee seecancss 849 927 
- “ C., M. & St. ID hegre tint eahtanariiacee vac eenieen 90 668 
Near Warren, Ill........cccc cess ve ceasenserc cena eeeeseens 475 1053 
Head of Montreal river (Owen)......--.e sees reece eee eee ee ee eee 1150 1728 
St. Croix and Brulé Portage (Owen).....--.-- cess cere cere ee ees 674 1252 
Mount aren (OWED): sccsae ewer scnsesnanecrosnages eae 607 1185 
Maiden’s Rock (Owe )s....3000 002 cess areeeeoierearaeeecgnees 443 1021 
West Blue Mound (Whitney)........... see eeee ee eee e eee ees 1151 1729 
East Blue Mound (Whitney).....-.-0 00. cece eee eee eee ener ees 1000 1578 
Platte Mound (at base.553)..0cc0ssssencssreceensanaeeee aries 703 1281 
Sinsinewa Mound (base 866)....-.. cece cece cence ence eee e eran 591 1169 
Sinsinewa Mound College ......--.eeereeee cece eens eee ee neees 462 1040 
Penokée Gap.vcscecsasace sents eemestyccciaaneretieaienadnes 713 1291 
Government Hill (Waukesha Co.)........0.ee ese eeeeeee Loess 669 1247 
Lapham’s Peak (Washington Co.)...-.... sees ence ee ee enc enee 824 1402 
Elephants Back (Kilbourn City....... 6. e cess cece ee er ee erences 555 11383 
Buena Vista, Sec. 23, T. 22, R.9 Ho... cc cece eee cnc eee neeeee 605 1183 


Government Survers. —It is very generally known that the adii- 
rable system of surveys into townships, six miles square and sections 
of one mile square, with their boundary lines running due north and 
south and due east and west, adopted for the survey of the government 
lands of the United States, though exceedingly well adapted to the 
purposes for which it was chiefly intended, that of disposing of these 
lands, is altogether too crude and inaccurate for any scientific purpose. 
There are offsets occasioned by the spheroidal shape of the earth, that 
could not be avoided, but there are also many other irregularities arising 
from various causes which prevent the construction, from these surveys 
alone, of an accurate map of the state. Among these causes may be 
mentioned the necessity, often occurring, for making surveys of public 
lands to meet the wants of settlement and improvement before the 
principal or governing lines can be run. Some townships have been 
resurveyed in a neighboring state, revealing gross irregularities, only 
to be accounted for by a want of honesty on the part of the surveyor; 
how many similar cases exist in Wisconsin can only be known wheu 
the country becomes fully occupied, and the lines of the public survey 
retraced. 

While some tiers of sections are double the usual width! others are 


1Tn range 9, towns 21 to 30, inclusive. 


ANNUAL REPORT FOR 1873, 95 


contracted to a quarter of thein proper size’. Some section lines in- 
stead of running due east and west, or due north and south, are found 
to make considerable angles with these cardinal directions. Almost 
every section, when accurately remeasured, is found to show either an 
excess or a deficiency of the normal quantity of six hundred and forty 
acres. Railroad engineers discover these inaccuracies while running 
their lines with the theodolite, and connecting them with the section 
lines. One who, under instructions, followed a section line over a 
level country, was afterwards censured for the curves he had intro- 
duced at almost every mile of the road, where only a straight-line was 
intended. 

On the official plats of the surveys of the public lands, now depos- 
ited in the office of the secretary of state, at Madison, we often tind 
the north line of a township varying considerably from the true east 
and west direction; while the south boundary of the next township 
(which is the same line) shows no such variation®. Again, the east 
line of one plat differs from the west line of the next in the same 
manner. In all such cases there are no means, short of actual re- 
survey, of determining which is correct, nor what changes are required 
in the form of the subdivisions, or the direction of their boundary 
lines, to make them conform to these unexplained irregularities. 

If we plat one of the banks of the Mississippi or Menomonee rivers 
by the Wisconsin surveys, and the other, upon the same map, from 
those of Iowa and Minnesota, or of Michigan, we shall find that these 
rivers have in some places a wonderful breadth, while at others the 
two banks will be brought so near together as to leave scarcely room 
for a trout brook. 

Considerable progress has already been made in an attempt to trace 
all these irregularities; to show the offsets upon the correction lines, 
and to construct a diagram or skeleton map which shall correctly rep- 
resent the surface of the state. This work must be done before any 
correct map of the state can be made. Such maps are found to be 
matters of necessity in all civilized countries; large amounts of money 
and many years of labor having been expended to secure this object 
in Great Britain, France, and many other countries. 

The proper corrections to be made in the lines of the public land 
surveys can only be ascertained and applied after a complete geodetic 
survey shall be made, such as is now being prosecuted by the general 
government, under the direction of the coast survey and of the engi- 
neer department. Such survey contemplates the accurate determina- 
tion of the latitude and longitude of numerous prominent points 


1Tn town 16, range 1 to 11 east. 2 Notably townships 1 and 2 in range 9 east. 


26 GEOLOGICAL SURVEY OF WISCONSIN. 


which are to be connected, and made the basis of a system of triangu- 
lation, covering all the ground to be surveyed. 

The engineer department of the United States army have in charge 
the survey of the lakes, which reaches into this state along the shores 
of Lake Superior, Lake Michigan and Green Bay, and also other mili- 
tary and geographical surveys in the west. The work of the lake sur- 
vey will be available, so far as it goes, for the purposes of the state 
survey, and it is exceedingly desirable that it should be extended so as 
to embrace a larger portion of the interior. At my suggestion Gen. 
Humphrey, chief of engineers, has authorized the determination of 
the position of points on the base line of the land survey (the south- 
ern boundary of the state) and others on the fourth principal meridi- 
an, and on the “correction lines;” these being the governing lines 
of the public land surveys, their exact determination becomes of the 
greatest importance. Should the congressional appropriation for these 
objects be continued, other work of the same kind will be done. 

If such a survey could be extended over the state of Wisconsin, and 
properly connected with the land surveys, it would accomplish all that 
could be desired in this direction. It was found that congress, while 
making provision for extending the coast survey across the continent, 
so as to form a geodetic connection between the Atlantic and Pacific 
coasts, required also the determination of points in each state in the 
Union, which shall make requisite provision for its own topographical 
and geological surveys. Under this authority, the officers of the coast 
survey have already taken observations for determining the position 
of Madison and La Crosse, and arrangements have been made for the 
further prosecution of the work, which will be in charge of Prof. J. 
E. Davies, of the University of Wisconsin. In addition to the general 
benefits of that survey, it will be the means of training a number of 
young men in the methods of this important kind of work, thus mak- 
ing it the source of educational advantages. 

Other important surveys have been made by the general govern- 
ment within our state. Among them, perhaps the most valuable are 
those made a few years ago under the direction of Gen. G. K. Warren, 
of several of the larger rivers, inéluding the Mississippi so far as it 
forms our western boundary, and portions of the St. Croix, Chippewa, 
Black, Wisconsin and Fox rivers. Of these, maps were constructed 
on a scale of two inches to one mile (same as the plats of the govern- 
ment land surveys), showing not only the margins of the rivers, with 
the islands and sand bars, but also the boundaries of the bottom Jands 
and the position of the adjacent blufts. Copies of these detailed and 
costly maps have been furnished for the use of the state survey, and 


ANNUAL REPORT FOR 1873. ye 


add very materially to our knowledge of the minute topography of 
the state. They will also soon become still more valuable as a means 
of showing what changes are annually taking place along the course of 
these important rivers. * 

With the public land surveys, thus tested and corrected, together 
with the railroad surveys, and the barometrical measurements of 
heights by the geological survey, we shall have abundant material for 
the construction of a very full and correct topograpical map of the 
state. 

It is therefore to be hoped that means will not be withheld for the 
vigorous prosecution of these important surveys on the part of the 
United States government. All such work is of the greatest practi- 
cal importance in the more correct determination of the boundaries 
of real estate, thus, perhaps, preventing future litigation, neighbor- 
hood quarrels, and uncertainty as to the ownership of property. 


Minerars.— The following enumeration of the mineral species 
heretofore found in Wisconsin, has been made up from observation, 
and from various sources of information; and though it is, doubtless, 
far from complete, either in the number of species existing in the 
state, or in the enumeration of localities, it will serve as a beginning 
towards the more complete mineralogical survey contemplated. 


CATALOGUE OF MINERALS.? 


I. Native ELemMents. 


Gold. — Gold is said to have been found in several places in the northern part of the state. 

Silver. — Native silver is found associated with copper in boulders of the drift, having 
been transported from the copper veins of Lake Superior. Itis said to occur in veins 
on the Montreal river; and, associated with lead, in Ashland county. 

Copper. — Copper has been found in limited quantities in regular veins on the Montreal 
river and at. several other places in Ashland and Douglas counties. In the form of 
drift boulders it is often found, especially in the eastern half of the state; the masses 
vary from a few ounces to several hundred pounds; the largest, found near Hustis- 
ford in Dodge county, had a weight of 487 pounds. 

Tron, — Meteoric iron has been found in Washington county on the farm of Louis Korb, 
in masses varying from 8 to 62 pounds. They are, apparently, all fragments of one 
meteorite which must have exploded when very near the surface of the ground. It 
has been analyzed and described, and samples sent to collectors under the name of 
the ‘‘ Wisconsin Meteorite.’ The presence of nickel, and peculiar Widmannstiitlian 
figures leave no doubt of the meteoric origin of this iron. 

Native Sulphur. — Sulphur, resulting from the decomposition of marcasite, has heen 
found in the lead mines at Mineral Point, Shullsburg, etc. 

Graphite (Plurnbago, Black Lead). — Graphite is said to have been found in the northera 
portion of the state. 


1A list of all the minerals known at the close of the survey to occur in the state will be given ia 
another volume of the report. 


98 ~ GEOLOGICAL SURVEY OF WISCONSIN. 


II. Sutpuips, ARSENIDS, ETC. 


Galenite (Sulphuret of Lead). — Extensively mined in the southwestern counties of the 
state. Occurs in small quantities in many other localities. 

Sphalerite (Blende, Black Jack). — Abundant and now extensively mined in the lead 
region. 

Chalcocite (Sulphuret of Copper). — At Mineral Point, and other places. 

Niccolite (Arsenical Nickel). —Found in very small quantities in Douglas county, 1873. - 

Pyrite (Cubical Iron Pyrites). — At Mineral Point, etc. 

Chalcopyrite (Copper Ore). —At Mineral Point, Mt. Sterling and other places, but not 
in workable quantity. 

Marcasite (Iron Pyrites, Mundig).— With ores of lead and zine in the lead region; 
masses in drift clay near Lake Michigan, and elsewhere. 

Tetrahedrite (Gray Copper Ore).— Lett Hand River, Douglas county. (Owen.) 


If]. Oxyeen CompounpDs. 


Cuprite (Red Copper Ore). — Left Hand River, Douglas county. (Dana.) 

Water. Natural waters in the Archean and Sandstone regions are usually soft and nearly 
pure; in other portions of the state, hard, or containing lime and magnesia from the 
limestones. At Sparta, Waukesha, etc., the water of certain springs and wells is 
found to possess medicinal virtues. At Fond du Lac, Sparta and Watertown, the 
iron tubes through which the water flows become highly magnetic. 

Hematite (Red and Specular Iron Ore), — Iron Ridge, Hartford, Depere, etc., in small 
grain; flax seed ore. Used with Lake Superior ores at Milwaukee and other places. 
Penokee Iron Range, Ashland county, Wood county, etc. 

Menaccanite (Titanic Iron Ore). —In small quantities near Baraboo, Sauk county. Jn 
trap rocks, Lake Superior. (Owen.) 

Magnetite (Magnetic Iron Ore).—Penokee Iron Range, Ashland county, in great abund- 
ance; also at Black River Falls, Jackson county, and other places. It is found in 
the form of sand on the shores of the great lakes, 

Limonite (Brown Iron Ore). — Ironton, Sauk county, supplying an ivon furnace. In less 
quantities at various places, resultmmg from the decomposition of marcasite. Bog 
ore in Wood county and elsewhere. 

Wad (Oxide of Manganese).—In small quantities in the lead region, and other placcs; 
also the variety asbolite or earthy cobalt. 

Quartz. — Crystalized quartz is found in various places. In the form of grains it con- 
stitutes the sandstones, often pure and white. Its varieties, amethyst, carnelian, 
jasper, chert, etc., are often found. Quartzite occurs in extensive ridges among the 
Archean rocks. 

Amphibole (Hornblende, ete.).—Abundant in the Archean rocks. Variety, tremotite at 
Lac de Flambeau. (Norwood.) 

Garnet. — Lac de Flambeau river, four miles above the mouth, and other places in 
Archean rocks. (Norwood.) 

Epidote.—Associated with copper ores in Ashland and Douglas counties. 

Phlogopite (Rhombic Mica).—On the Eau Claire river, four miles above the falls, in 
large plates. (Dr. Littel.) 

Wernerite (Scapolite). — Twin Falls, of the Menomonee River of Green Bay. (Fcstor 
& Whitney.) 

Labradorite. — An ingredient of trap-rocks; upper rapids of the Bois Brulé river of Lake 
Superior. (Owen.) 

Albite (White Feldspar).— Common in boulders of Archean rocks, 

Orthoclase (Potash Feldspar).— Common in Archean rocks, By decomposition forms 
Kaolin (Potter's Clay). 


ANNUAL REPORT FOR 1873. 29 


Tourmaline. — Outlet of Lac de Flambeau. (Schooleraft.) 

Cyanite (Kyanite). — Lac de Flambeau. (Dr. Norwood.) 

Laumonite. — Copper veins on the Montreal river. (J. P. Hodges.) 

Chrysocolla (Silicious Oxide of Copper). — Wisconsin, with carbonate of copper. (Danx.) 

Prehnite. — Accompanying copper ores, Lake Superior. 

Tale. — Ableman, Sauk county, in quartzite. 

Glauconite (?,) (Green Sand). — Forming layers in the Potsdam and Upper sandstone 
Madison, Janesville and numerous other places. 

Sapronite (Thalite, Owen). — Black river (of Lake Superior). Three miles above Kettle 
river. 

Kaolinite. — Grand Rapids, Wood county. Potter's clay at Wenasiia and elsewhere. 
Brick clay at Milwaukee, Watertown, Port Washington, Sheboygan, etc., making 
brick of a light cream molok, Pipestone (Catlinite) in Barron county on lands be- 
longing to the Cornell University. There are also clays so largely consisting of 
silex in minute grains as to be useful as polishing powders, 

Apatite (Phosphate of Lime). — In the Potsdam sandstone and in Galena limestone the 
fossil Lingule are composed of phosphate of lime. 

Barite (Sulphate of Barites. Heavy Spar).— Abundant in the lead region; Mineral 
Point, Shullsburg, etc. 

Celestite (Sulphate of Strontia).— In drift clay filling a crevice in limestone, Wauwatosa 
near Milwaukee. 

Anglesite (Sulphate of Lead).—In small crystals, lining cavities in galenite at Mineral 
Point. 

Leadhillite. — At Mineral Point. (Owen.) 

Gypsum. — At Sturgeon Bay. Also among the lead mines. 

Melanterite (Sulphate of Iron, Copperas). — In the lead mines, formed by the decompo- 
sition of marcasite (iron pyrites). 

Calcite (Calcareous Spar, Tiff). — Common in the lead region. Fine crystals (scalene 
dodecahedrons) at Shullsburg. Coarse stalactites in Cleveland’s Cave, Dane coun- 
ty. Tufa deposited from springs incrusting moss, leaves, sticks, etc., at numerous 
places. Travertine (called marble) in Sauk and Richland counties. Hydraulic 
limestone has been found in some localities. 

Dolomite. — Most of the limestones of Wisconsin contain magnesia, and are properly 
dolomites. 

Siderite (Carbonate of Iron). — Penokee Iron Range, Ashland county; rare. 

Smithsonite (Carbonate of Zinc, Dry Bone). — At Mineral Point, and other places in the 
lead region. Extensively mined for the manufacture of zinc. 

Cerussite (Carbonate of Lead, White Lead ore). — At Mineral Point, Blue Mounds and 
elsewhere in the lead region. : 

Hydrozincite (Calamine, Zinc bloom).—- At Linden in a concretionary fibrous crust on 
Smithsonite (Whitney). 

Malachite (Green Carhonate of Copper).—In minute quantities in connection with 
other copper ores, Mineral Point, etc. 

Azurite (Blue Carbonate of Copper).—At Mineral Point; Left Hand river, in minute 


* quantities. 
IV. Hsaberenas CoMPOUNDS. 


otroleum. —Some layers of rock in the lead region are highly bituminous, burning 
with a flame when heated. 
Asphaltum.— Some small cavities in the Devonian limestone near Milwaukee, and 
also east of Fond du Lac, contain mineral tar. 
Peat i is found underlying very many of the bogs and swamps; sufficient to be of econo- 
mic value whenever the forests are destroyed and coal becomes scarce. 


80° GEOLOGICAL SURVEY OF WISCONSIN. 


The following species have been found in the mining region of 
Lake Superior, in Michigan, and may therefore be found in similar 
localities in Wisconsin: 


Donieykite (Arsenical Copper). Datolite. 
Algodonite (Arsenical Copper). Pectolite. 
Whitneyite (Arsenical Copper). Chlorastrolite. 
Argentite (Sulphuret of Silver). Apophyllite. 
Bornite (Purple Copper ore). Natrolite. 
Covellite (Indigo Copper). Analcite. 
Cerargyrite (Horn Silver). Chabazite. 
Fluorite (Fluor Spar). Harmotome. 
Melaconite (Black Oxide of Copper). Stilbite. 
Gothite (Oxide of Iron and water). Heulandite. 
Manganite (Gray Oxide of Manganese). Serpentine. 
Wollastonite (Tabular Spar). Genthite. 
Pyroxene, Delessite. 
Pseudomalachite. 


Mrinerat Waters. — Mineral waters being included among the 
numerous objects to be investigated by the survey, a beginning has 
been made in the collection of facts and information in regard to 
them, and arrangements made by which it is hoped that all desirable 
information will be at hand, ready for the final report. 

Mr. Gustavus Bode, of the firm of J. H. Tesch & Co., Milwaukee, 
having already analyzed a number of these waters, arrangements were 
made with him to furnish corrected copies of his work for the use of 
the survey, and to make such further analyses as should be deemed 
advisable. 

The accompanying table will show in the most compact and conve- 
nient form the chemical composition of twenty-three of the waters of 
our springs, wells, rivers, and lakes: 


ANNUAL REPORT FOR 1873. 31, 


ANALYSES OF THE WATERS OF WISCONSIN, 


oo fa |e | slo [a H ! S| on la. 
¢ |3 |a g|ee@ [2 |e | 4 E)e | & 
Dil & op rr : on ae laa & » | mM Ai 

Sussrancus | ~3| 3 A132 aa oi |e cI eel a 

IN ms) 3 | 8. S| B | &s|- m | 84 Qa 

SE aes me e As! Aid aes By » pe S| Gy 

1,000 Parts. e2 3 ed “3 A; ae ae Ze oa S a4 a8 
: g p eo Be oa 3 " 
Se| 26| $2) 3 | SE| Se] g8| Re] Bs] £| Be| Be 
21S |a |ElE |é6 la |e |8"| ele le 

Tas os «shay 

agnesia 

Soda .. 

Potash 

Lithia ..... “ 

8. Ox. of Iron]. . 

Alumina... 

Silica ....... 

Sulphur. Acid].... F : 

Nitric Acid..|..... SAO ssrcc as crcl laceistezanes patesarsp a ide ovate. 86a Sila coven fal] astcw coe fade sate 6 

Chlorine .... ; F ‘ ‘i ‘ R i: 0.003/0.012 

Carbon. Acid]..... 0.370/0.328]0.253/0.190)..... 0.176/0.177|0.163/0.166/0.160)0.151 

Org. matter .}..... [eee efecees [ene ee[eeeeefeceeeleveee trace].....[....- trace|....- 


Combined as 
follows: 
Chl. sodium . 

otassium . 
calcium... 
Sulph. Soda. 
otash 
IM€ «+00. 
magnesia - 
Nitrate soda. 
Bicarb. soda. 
Time. sera 
magnesia - 


8 
5 


32 GEOLOGICAL SURVEY OF WISCONSIN. 


ANALYSES OF THE WATERS OF WISCONSIN — continued. 


7 ¥ 
1 1 1 ' - n o - - ' ps 
4 a eS | Sls BOI a 28 
S 2 = ad rt a 3 os & L 2 
a ae ee ila \e 
wl |. |e |B |e} es 1 el dg |g | ae 
age [cee os qa |2 | 238 |g | 3H 
SUBSTANCES, a Y o |B A | 1s Gals S g 
mld00ranns. |a@ |= |F |e |CSlF | oa ie ae a. a 
a%/2 ) 2 | ce] 25| 28] 25) Zl 23) E28) ae 
eae “| 2 B2| €$| ye) S83] «v) 46 3 a 

2 £3|/ 82] 22/'85| 23) Sa) ga] 22] = 

Sle |4 |4 8 |e |e |e is |4 |< 
Eine ccotocasssas 0.096/0.108]0.082|0.09910.101/0.079/0.067/0.063)0.034/0.048/0.043 
Magnesia .....-.. 0.059|0.060/0.059/0.050|0.039|0.050|0.049]0.040|0.027/0.017/0.018 
DOC Misvexennnsiiseavcave dus 0.024/0.012/0.037/0. 02810. 025/0.015/0.005/0.061|0.043/0.002/0.005 
Pobashh:. cccscocovececs call oe sores heetev as [teniarets [loaleinn [aterensl| ocareia| a dara |'ae args hemnsane le senate | oieacace 
Lithia...... Bede icwval oasis ve) aces ees  ieaaaeee-Irosesecaee | acsenee seas a¥all a a's) ai] cinderay gy haa dia sats iene rove 
Sesqui Ox. of Iron.]|...-- 0.002/0.006}0.002}..... 0.004}..... wee ee (0.002]..... 0.005 
Alumina .........)- 055 0.002)..... 0.002)..... OS O08 lsccewal seals tice vis [pecan | a cea 
DHLICAL wseceieucctveratraences 0.014}0.017/0.026/0.014/0.016/0.016)0.055/0.013)/0.015/0.016)0.013 
pulpharic Acid. .. .|0.009)0.023/0.016]0.009|0.009|0.010)0.009/0.049/0.013/0.005)0.028 
RELIG) ACLs iz svar a0 fw tace ol om sideline tase [a auiere se iataisre-all pene see:|ieS ere wil race a wis os permet [PScacoeane 
Chlorine...... . .{0.008]0.002/0.007/0.007)0.011}0.002/0.002/0.045]0.004/0.003/0.007 
Carbonic Acid 0.1490. 147/0.147|0. 1383/0. 129|0.139)0.103/0.090/0.095/0.053/0.037 
Organic Matter ...}....e)eceecleneceleeeer[eceecfeoece trace|....- Os QE heccerecetcosinve 


Combined as fol- 


lows: 
Chloride of Sodium.}0.013/0.004/0.012/0.012/0.018/0.004/0.004/0.074)0.006|0.006|0.009 
' potassium ...... ss sigslehs Pree sagan tee a ls | teu sein 
IthiUiwsse oes 
calcium ........ 
Sulphate of Soda. . 
* "notash s22.aeaes 
BUC cprwow lanes tid 
magnesia....... 
Nitrate of soda ... 
Bicarbon’e of Soda. 
Tine is geerewis wees 0 
magnesia....... 


SiN Cane tissesesceneeers 
Alumina ........- 
Organic Matter... 


Though we have none that can properly be classed as “salt water,” 
nearly every one contains a small quantity of chloride of sodium 
(common salt), varying from a mere trace up to 0.423; the mean 
(omitting No. 3 as exceptional) being 0.052. It is believed that no 
salt bearing strata exist among the rocks of Wisconsin, and conse- 
quently that the production of salt can never become one of the re- 
sources of our people. 

A few only of these waters contain potash in small quantities, in 


* A more complete analysis of the water of the Bethesda spring will be found in the report un 
Eastern Wisconsin, and of the Sparta well in the report of Mr. Strong in a subsequert volume. 


ANNUAL REPORT FOR: 1873. 33 


combination with chlorine. Epsom salt (sulphate of magnesia) is 
found only in two; sulphate of lime is equally rare, being only found 
in two eases. The very small amount of alumina is remarkable, 
where there is so much clay in the soil. The occurrence of chloride 
of lithium * and nitrate of soda is also an interesting variation in the 
composition of these waters, being only found in the well at Water- 
loo. Possibly the proximity of this locality to the quartzite (and 
perhaps other Archzean rocks) may have something to do with this 
variation. 

The absence of nitrogen, ammonia, the bromides, iodides, ete., will 
be remarked by persons familiar with the composition of mineral 
waters. 

In seeking for the cause of this unusual absence of mineral matter 
in our spring waters, we must remember that the geological history 
of Wisconsin differs essentially from that of other countries. A large 
proportion of the state is underlaid by rocks of Archean age, an age 
the furtherest remote from the present, while the remainder is almost 
exclusively occupied by Silurian rocks, they being the oldest of the 
fossil bearing series. It thus appears that during all the ages of the 
Carboniferous, Permian, Jurassic, Triassic, Cretaceous and Tertiary 
periods, Wisconsin continued to be dry land, subject to the abrading 
and purifying action of rains and frost. This is still further attested 
by the wonderful amount-of denudation our strata have sustained, and 
which it is made the duty of the survey to investigate. While the 
Alleghany and Rocky mountains were being uplifted from the depths 
of the sea, Wisconsin stood firm, always above its waters, always con- 
tributing of her substance for the accumulation of the sedimentary 
rocks of the adjoining states — contributions which she still continues 
to make. 

During all these vast periods, each occupying an incalculable length 
of time, rains have continued to fall, the waters have continued to 
percolate through the soil and porous rocks, dissolving and carrying 
away all soluble substances. It is not therefore wonderful that by 
this time the waters of the state have an unusual degree of purity. 
Waters percolating through our limestones and sandstones can now 
absorb but small amounts of earthy or alkaline salts. 

The waters now examined are chiefly from the southern and south- 
eastern portions of the state, where the several magnesian limestones 
prevail; and hence they contain, as before stated, as chief ingredients, 
the carbonates of lime and magnesia, resulting directly from the de- 

* By a typographical error, the quantity of lithium in the Waterloo water has been 


overstated; it is correctly given in the table above. 
Wis. Sur. —3 


34 GEOLOGICAL SURVEY OF WISCONSIN. 


composition (aided by free carbonie acid) of these magnesian lime- 
stones. Whether the Archean rocks further north will afford waters 
of a different class, as seems probable, remains to be determined in the 
further progress of the survey. 

Waters percolating through the drift that so completely covers and 
conceals the rocks, are also found to contain chiefly lime and magnesia 
with smaller quantities of soda, chlorine, iron, ete. These elements 
are most usually combined with carbonic acid, and are the product of 
the solution of magnesian limestone almost everywhere existing in 
the form of boulders, gravel, or calcareous sand. If we take a lime- 
stone pebble from one of these springs, it will usually be found soft 
and much decayed upon the surface by the action of the waters, and 
it would be wonderful indeed if such waters should not contain lime, 
or if such rocks should not, in the course of ages, be dissolved and 
carried away. As the carbonate of magnesia is always associated with 
the carbonate of lime in the rocks, so it is in the mineral waters. In 
general, the waters are found to partake of the character of the rocks 
and soils through or over which they percolate or run. 

The figures in this table show the number of parts in one thousand 
parts (by weight) of the water, which consist of solid matter that re- 
mains when the water is evaporated. If we do not care to consider 
minute differences arising from changes of temperature, and the spe- 
cific gravity of the water, we have only to multiply the figures in thig 
table by seven, to find the number of grains in one pint; this product 
being multiplied by eight will show the number of grains in a gallon. 
The table shows, without any change of the figures, the number of 
ounces in a cubie foot of the water. 

This decimal system of stating the results of chemical analyses is 
adopted in all cases except in regard to mineral waters, where we of- 
teu find only the number of grains in a pint, a quart, or a gallon. 
Americans were the first to adopt in currency and coinage this simple, 
convenient, easily comprehended and labor-saving system, and we 
should not be the last to apply it in other cases. Its benefits are in- 
ternational. If we give the number of grains of solid matter in a 
gallon of water, we use a language understood, perhaps, at home, but 
not anywhere else; but if we say there are so many parts in every 
thousand parts of water, we state a fact in a manner that is under- 
stood in every part of the world. There will be ten grains in every 
thousand grains; ten pounds in every thousand pounds; ten grams 
in every thousand grams; and the Frenchman, or the men of 
any other nation, will not have to search the encyclopedia to find the 
value of a grain or the size of a gallon in Wisconsin. No matter 


ANNUAL REPORT FOR 1873. 35 


what the system of weights and measures may be in any other coun- 
try, the decimal system is the same in all. The general tendency of 
our times is towards simplicity and international uniformity, espec- 
ially in coinage, weights and measures, and hence the adoption of the 
decimal system should be encouraged in all proper ways. 

Many of these waters, as well as many others not included in the 
table, are now known from the best of all tests, actual experience, to 
possess valuable remedial qualities, and they are annually resorted to 
by great numbers of invalids, who, with judicious treatment, are al- 
most always benefited. 

These analyses were all made by Mr. Bode, except No. 1, Rich- 
mond’s, at Whitewater, made in 1873, by Dr. J. E. Garner, of Mil- 
waukee, and No. 6, the Oakton Spring, at Pewaukee, made in 1872, 
by Dr. J. V. Z. Blaney, of Chicago. 

Comparing these results with the analyses of other mineral waters, 
we are at once impressed with the small amount of mineral matter 
our waters are found to contain, only four having more than one part 
in one thousand; the average of twenty-two (No. 3 being omitted as 
exceptional) showing a mean of 0.657, or about two-thirds of one part 
only, in one thousand. 

The slightest inspection of the table will show that the carbonates 
of lime and magnesia constitute the most prominent and important 
ingredients of these waters. These, with the carbonate of soda, pres- 
ent in many of them, bring the mineral waters of the state into the 
class of alkaline waters, and they are arranged in the table in accord- 
ance with the relative quantity of these salts, those having the most 
being placed before those having less. The average in the whole 
number (twenty-three) is 0.365, or a little more than one-third of one 
part in a thousand, and more than half of the total average total quan- 
tity of solid matter in these waters. 

The purgative salts (sulphates of soda and magnesia) are found 
only in very small quantities, except in one case; the mean of nine- 
teen waters (No. 5 omitted) being only 0.023. 

Of the twenty-three waters, ten only, or less than half, contain 
iron, varying from 0.001 to 0.012, the mean being 0.006. This quan- 
tity, though apparently so small, seems to have very useful medicinal 
effects, and it suffices to discolor objects over which the waters run. 
Iron rust is deposited so freely from the waters of the several artesian 
wells at Sparta, that they are not used for cooking or for washing 


purposes. 


Rat-Fart. — It is solely to the clouds that we are indebted for the 
supply of water, in the form of rain, hail and snow, to all our lakes, 


36 GEOLOGICAL SURVEY OF WISCONSIN. 


rivers, springs and wells. The underground rivers reaching from the 
Rocky mountains, or the highlands of Dakota, exist only in the im- 
agination. Heavy or continuous rains cause the water to rise in the 
non-flowing artesian wells, in the same manner and for the same rea- 
son that the water in lakes, rivere and ordinary wells rise under the 
same circumstances. In dry weather, or during continued cold 
weather, when the falling water ceases to penetrate the soil, the re- 
verse takes place, the waters of lakes, rivers and non-flowing artesian 
wells fall below their average height. Springs are subject to the 
same variation to a considerable degree; it is only those that have 
their sources at considerable distances that show but little or no vari- 
ation during the changing seasons. 

The mean monthly and annual amount of rain-fall, at any given 
locality is, therefore, an item of great importance that will often be 
needed in the prosecution of the survey, and hence I contribute the 
following table, the result of many years of patient labor. It will 
thus be made accessible to engineers, agriculturists and meteorolo- 
gists, who will often have occasion to use it. 

The table shows the monthly and yearly amount of rain and meltcd 
snow at Milwaukee, latitude 43° 3’ N., longitude 87° 56’ W. The 
observations for the years 1843-48 were made by E. 8. Marsh, M. D.; 
for 1855-59 and for 1872-73, by Mr. Charles Winkler; for all the 
other years by J. A. Lapham. 


TABLE OF RAIN-FALL AT MILWAUKEE. 


Monrns. | 1841.| 1843. | 1844.| 1845. | 1846. | 1847.| 1848. | 1849.| 1850. 
January ...| 0.80 |....... 1.67] 1.30] 1.92] 1.06] 0.91 | 1.20] 0.75 
February...| 0.33 |....... 0.35 | 1.73| 0.80] 1.25| 1.12] 0.87] 0.38 
March... 1 en 1.66 | 1.85] 1.24] 1.40] 1.94] 2.31] 2.85 
April...... eg eee 3.15 | 1.15 | 5.33] 2.12] 1.20] 3.24] 2.98 
Yi eens Ce catace 4.20} 0.78} 1.83 | 3.53] 3.60] 4.03] 0.28 
June...... Bet lawucane 5.34 | 3.22] 4.05] 1.75] 4.33| 3.73] 1.98 
duly cs, eas 3.72 | 0.86 | 5.05| 3.81] 3.18] 1.43] 2.70| 2.36] 1.99 
‘August.-...| 3.85 | 8-37] 3.85 | 0.80] 0.90| 1.42] 5.10 | 3.54] 9.08 
September.| 7.02 | 1.57] 0.99| 4.92 | 3.97] 2.85] 2.73] 1.95] 1.73 
October....| 1-23} 1.29] 1.74] 0.93 | 0.80 | 0.83] 3.50] 3.07] 1.00 
November.| 1.70] 2.79] 1.46] 0.24 | 1.68] 4.37] 2.50] 5.00 | 2.60 
December..} 4.03 | 0.85 | 3.04] 0.81] 1.96] 0.94] 3.89] 0.94] 1.48 
Babes oris Ieee asec bias os 2.87 | 6.07| 8.03] 3.57| 2.97| 5.46} 2.02 
Spring. .... Be6l wae 9.01 | 3.28 | 7.90| 7.05} 6.74] 9.63| 5.37 
Summer...| 13.70 |......- 14.24] 7.83 | 8.13 | 4.60 | 12.13 | 9.63] 13.00 
Autumn 9.95] 5.65] 4.19} 6.09| 5.25] 7.55] 8.73| 9.99] 5.33 
Year .....- i ee 82.50 [20.54 | 25.26 | 22.45 | 33.52 | 31.09 | 26.41 


87 


ANNUAL REPORT FOR 1873. 


Tarte or Rarn-FaLu at MILWAUKEE — continued. 


. 2 ef es One cs (am) N . mor-or OOM 1919 ws on 00 re 
3 SISSS°CSSSSSS ||SSSR |S 3 BRASR SRR SZSRe || ASAE |B 
= SRE RAN a tes Bre a, ae 5 A Sea | Ea Se ES aes H ce | eae 
3 SAS Sa GHANA ATS || roo | = AAS ES ACI Sadar || cod Ws || c= 
= r= 

y Aararc an CANE |} co 5 ANRWM 9 Mem [oa] On it 
& SRI SSSRBSAS || RSH|S |B 2 ASSSSRESSARS ||RSBH || 5 
2 MMH eHMMASANAOO AIO || G0 @ MOANA SOMA SAMO SIA rr |] | 

5 1D OD WO OIN NWN | HRD 2 5 Woo OD onMenn inbYe) nN 
ee SSA ZSsesasas BESS IS is BSSSLRSSSSSRE tase & 
wn A et O19 og Hoda HH 12916 Sed || % AAA GANAM So || Eo e§ = 

= as lls 

xg DOBSAHMMOSS |1DROD || oa OHtotonmmM90NS il 
0 SHRSZIASERSE Sd || 0 S ZSRSSRRABLBS SSn8 ||S 
ee) SAAD FOMCIN MH | HAA [|S a) AMM CONHATOO HOI OD |] Heo 00 |] 3 
= &. aa = for) 
5 eo HMOnOMONM lH Rolla 5 00 CO Hh OOH A | Moan 
v4 SSezSSERR 38 BANDS |S iS ABSSaBCASARSA FSSA 8 
2 AM SOOANOAA GHA | Ora || ~% CHM MMM Het sS | iVcaa 2 
5 POSDDOODM NOD |] OMCOS |] Ht A 1d IQ =H ON OD HH aD roe || 2 
by SHLHAESSRSLS ASE [1S = SSS SRE SSSSSE SSS |B 

we a ss - jc 
2 SADIE GAIA || misao || 2 eS ACABASNONHA |More S 

‘ ee MmekneS¢s: |} ‘ca : 4 ORD HOHnAan»s 129M Ilo 
an BSR EC SESRS BBS : te SOFSHSYSSSAS Ot dow || dO 
®. LANWMIO GSONVDSA || sea || + cs AAD SANA OID gt || Sodus bs 
i SODPMOr MORAY || Minne lia i ADOHHORHMOOLE ingen’ a | aes 
a MSSSAGRLSERG 440960 || 63 s SRaSaSSSSRAH M8S5 |S 
~% THI CT S Mf IH || DOD || «@ MSA SiN HAAR ONO || 9 
4 > NNO || moog HOMO NORHAMNOD S00 
| SHRVRPHAANSS BSBA IS | S | SAVSASERSLRB || VRVS ||B 
iv) SCABSAsSMOMONAHNS |] HOCH [lO on CUD ACOH eH AOD rst |] Boo || 4 
© taal) = B Le st a & 
wo : eiath go redo yaat acmige, Gee eae : a Bodh fhe, Perey ange EM ce edeeaD Pakc grave. GE : 
fs] = B en ap oe a> sac te 58 tog : ies] SBS. e. sey ce. er 2 .2o re er . 
o Psa an Sh aetas eeyes iB : a BE eae aoa 2,85 3tf¢d : 
6 | sida jc.88808 S858 2 | 2 | seal i FSSERR Bees 

r ; ¢ o 2 
A | FSGRSESSESES FERS § | a | ESeRRESRESES BEES 8 
SHE425642540 Band Beedes542640 Baad 


f 


38 GEOLOGICAL SURVEY OF WISCONSIN. 


TABLE OF Rarn-Fatu at MinbwauKEE — continued. 


Mowrus. 1870.|1871.] 1872. |1873. | No. of) Mean, 

Cie Aid tase area natcasien 9.37| 3.14] 0.57] 2.89) 29) 1.73 
EEE SOO NE CE 1.32 | 1.32| 0.36] 1:50] 29] 1.86 
ee ere ESRD anes 5.01] 2.75] 0.80) 1.48] 30] 2-10 
Uta phn at ister 0.51 | 3.30 | 2.50] 2:70] 80] 2.68 
Beis tao 0.63 | 2.24] 3:10] 4:89] 30] 3.24 
SMe ects AG clothe oe 2:62 | 8.03] 4:42] 3:40] 30] 8.69 
Wi esa, aon eras 4.64| 1-84] 1.93] 1.82] 31] 3.20 
Drs pei etre Gites saeco 2.69 | 3.77 | 2164 | 5.26] 81) 2.82 
Begtsimbehavennansaucenenaswaance 2.10 | 0.60 | 8.87] 2.57] 81] 8.07 
De ete fica salentie nie 1.99 | 2.72] 0.82] 2:12) BL] 2.15 
ROVEUINER\. 5 <amancranvawentcenes 0.94] 2.40] 1:80] 140] 31] 2.31 
DECIDE enseraconu sew nen sa sie cc 1.79} 2.03] 1:00] 2.81] 81] 1.91 
WU sci gias osc ane ian eee Ran 6.48 | 6.25| 2.96| 4.80 |....... 5.00 
SON ada wae aston stato sss 6.15| 8.29] 6.40] 9.07 |....... 8.02 
Pree R icascssonasveniassawels 9.95 | 8.64] 8.99 | 10.48 |... 72. 9.71 
ANTHUTAN ait esenne casa cheine denne 5.03 | 5.72 | 11.49 | 6.09 |....... 7.55 
Repetto sk alll SA dS 26.61 | 29.14 | 28.81 | 82.34 ]....... 30.27 


This table shows that the rain in Wisconsin is generally very well 
distributed through the several months, seasons and years; the gen- 
eral average for thirty-one years being 30.27 inches, varying from 
20.54 in 1845, to 44.86 in 1858; the greatest amount in any one month 
was 9.03 inches in August, 1850, and the least 0.10 in January, 1857. 
The most rain upon an average falls in June; the least in February; 
the three months of summer have been supplied, upon the average, 
with the most rain, the three months of winter, the least; while the 
spring months have a little more than those of autumn. 

During nearly half the years covered by the table the rain-fall dif- 
fered but little from the general mean; while nine were considerably 
in excess, and eight were supplied with less than 28 inches. 

From the published results of observations collected by the Smith- 
sonian Institution, it appears that the average rain-fall at about 
twenty stations in Wisconsin, or on its immediate border, was about 
three inches more than at Milwaukee, 

The annual supply of falling water, as shown by this table, is 
equivalent to a sheet of water two and three-fourths feet deep, spread 
evenly and uniformly over the whole area of the state. The most care- 
ful investigations have shown that this is sufficient to account for the 
outflow of all our lakes, rivers and springs; the total quantity thus 
carried away being, in our climate, found equivalent to only about 
one-fourth of the total rain-fall. The remainder is evaporated, and 
thus returned to the atmosphere, either directly from the surface, or 
after having performed service in the growth of plants. The quantity 


ANNUAL REPORT FOR 1873. 39° 


of water absorbed by the roots of plants, with its mineral contents, 
and then evaporated from the leaves, is enormous. 

Rain water soon penetrates the soil and finds its way through 
crevices and pores of the more solid rock strata, down to very con- 
siderable depths, dissolving such substances as are soluble and carry- 
ing them to distant places. It is here we must look for the origin 
of all mineral waters, and for the cause of a large share of the de- 
nudation which in the lapse of many ages has become so very con- 
siderable. 

Knowing this annual quantity of water-supply and outflow, with 
the amount of mineral matter it carries, we lack only a knowledge of 
the amount of matter mechanically suspended in running water, de- 
rived from the loose soil and from abraded rocks, to be able to cal- 
culate the time required for the excavation of any given valley whose 
dimensions are known. 

The gradual decay and wearing away of rocks is not confined to the 
limestones and softer rocks, but includes many of the older and harder 
kinds, especially such as contain feldspar and similar minerals. Rocks 
are always penetrated with water and they hold in their pores an 
average of five or six per cent. by weight; a hundred pounds being 
capable of absorbing five or six pounds of water. As the clouds 
afford a constant supply which is continually removed in under- 
ground currents, springs and rivers, carrying with it the mineral 
matter taken up, we have a perpetually recurring cause of geological 
change. During the progress of water through the different rocks, 
meeting with different chemical elements, many chemical changes 
probably occur in the substances taken up, and it is only the final 
result of all these changes that we find in the mineral spring as it 
appears at the surface. Any considerable change of the course of the 
water among the rocks would, therefore, lead to changes in the com- 
position or combination of ingredients it contains. 

Water when pure has but little power to dissolve mineral matters, 
but when combined with carbonic acid, this dissolving power is very 
much increased. When waters holding these substances reach the 
open air they give off the excess of carbonic acid, and hence, by losing 
a portion of their dissolving power, become unable to hold them, and 
they are deposited forming a coating to sticks and stones over which 
they may run. 

If this depusit consists chiefly of lime, and accumulates with con- 
siderable rapidity, such springs are known as petrifying springs, or 
lime springs, of which we have many examples. The deposit often 
forms considerable conical mounds surrounding the spring; and moss, 


40 GEOLOGICAL SURVEY OF WISCONSIN. 


leaves, shells, sticks, etc., are often incrusted in such manner as to 
preserve beautifully their peculiar markings. 

In many cases the oxide of iron is thus thrown down, discoloring 
everything over which the water runs. The quantity of iron thus 
deposited does not depend so much upon the absolute quantity of 
iron in the composition of the water as upon the feebleness with 
which it is held in solution. Such springs are called chalybeate, or 
iron springs. 

Sulphuretted hydrogen, which gives the sulphur taste and odor to 
many springs, is supposed to result from the decomposition of or- 
ganic (animal or vegetable) matter — mostly of vegetable origin. Such 
springs are called sulphur springs, and we have several examples in 
the state. 

The rock strata are clearly shown, by the evidence of marine fossil 
shells and corals, to have been originally deposited in the waters of 
an ancient sea, from which they have been elevated to form our 
present continent; and it is not, therefore, wonderful that they should 
yield to the percolating waters those elements which we find in 
mineral waters. The supply might be supposed to diminish as ages 
pass by, but never to become exhausted. 

All natural waters may be regarded as “mineral waters ’’ — for 
none are absolutely pure. Indeed it is probable that pure water, such 
as can only be obtained by careful distillation, would not sustain 
either animal or vegetable life. Even rain water is found to contain 
minute quantities of salt, of ammonia, soda, lime, and organic matter, 
with traces of many other substances. It is mainly from the mineral 
matters dissolved in water that plants derive their solid materials con- 
stituting the ash. The silica, though small in amount in water, is of 
great importance to the growth of plants, especially the grasses, in- 
cluding the cereals, etc.; all our waters contain silica. 

Springs, whose sources are near the surface, are apt to contain mat- 
ters resulting from the decay of organic matter, and other deleterious 
material. Those which come from greater depths, and have passed 
over greater distance, are supposed to be of greatest value; the organic 
matter having been absorbed in passing through the soil and rocks. 
Such springs usually assume a temperature showing little change 
from winter to summer, and which correspond, with the mean annual 
temperature of the place. 

Several of these waters, notably those of Fond du Lac, Sparta, and 
Watertown, are known as magnetic; the iron tubes through which 
they flow, possessing the magnetic property in'a high degree. Whether 
this magnetic quality has any medicinal value remains yet to be de- 


ANNUAL REPORT FOR 1873. 41 


termined. A French savan has endeavored to demonstrate that the 
medicinal value of mineral waters is mainly due to their electrical 
condition; and the subject is well worthy of investigation by those 
most interested in it; and those who have the opportunity. 

There are, in this state, many other springs and wells, not included 
in the table above, that have been brought to the notice of the public 
for their medicinal virtues; among them the following, all at Wauke- 
sha: Hygiene, Mount Horeb, Barstows, White Rock, and Fountain 
Springs. 

Progress has been made towards the compilation of a list of all the 
more important springs, including those noted as petrifying (lime), 
chalybeate, sulphur springs, ete., and also such as are of sufficient 
capacity to supply ponds for the artificial rearing of fish. 

The investigation of mineral waters cannot be said to be complete 
without a determination of the gaseous matters they contain, for these 
may materially modify the medicinal or other effects of the solid in- 
gredients. This can only be done at the spring, with water taken at 
the moment it reaches the open air. 


Reiation or THE GEoLogicaL SuRvEY to AgRicuttuRE. — The law 
providing for a geological survey of the state of Wisconsin, includes 
also, and very properly, provision for some work for the special inter- 
est of agriculture; it being now generally known and admitted that 
these two subjects are so intimately related, that whatever is done to 
increase our knowledge of the local and special geology of any dis- 
trict tends, at the same time, to promote the interest of the farmer 
cultivating land in the same district. The underlying rocks are exam- 
ined as to their chemical composition, and surface arrangement or 
geographical extent; they are the sources from whence is derived the 
very soil into which the farmer annually intrusts his seed. Their dip, 
order of succession, depth beneath the surface, their porous or imper- 
vious nature; these are the data for deciding about artesian or other 
wells, often the only resource for a permanent supply of water for 
farm purposes; and as the forests become reduced in extent, the 
necessity for such wells will be gradually increased. The drift phe- 
nomena, gleaned from an extended and careful study of the loose ma- 
terials covering and concealing the more solid rocks, left here by the 
glaciers of the ice period, the study of which is so interesting to the 
practical and speculative geologist, have been the means of diffus- 
ing and spreading the soil over the rocky surface, commingling and 
mixing the various clays, sands, and pebbles, derived from the disinte- 
gration of the rocks, in such manner as to render them the best suited 


42 GEOLOGICAL SURVEY OF WISCONSIN. 


for the growth of vegetation. The mineral and other native resources 
are discovered and made known; they are the material for various man- 
ufactures, and their development creates a home market— the best of 
all markets—for farm products; thus deciding the great question, 
now so much agitated, relating to cheap transportation, by avoiding 
the necessity of any transportation of these products. 

The barometrical measurements of the heights and depressions, 
required of the survey, will show in many cases the sources of water 
supply upon which we are dependent for this life-giving element. 
These are taken as data in the topographical survey, which is to show 
the general contour of the ground, the extent, elevation, and slope of 
drainage basins, or river valleys; the amount and value of water power 
afforded by these rivers; the proportion of timbered, open, and prairié 
land; the uplands, the swamps, and marshes; all such detailed inform- 
ation is of importance to various interests, and especially to the agri- 
cnlturist. The geodetic survey, which has, through the instrumen- 
tality of the geological survey, been extended into Wisconsin by the 
general government, will also aid in the development of the topo- 
graphical features of the state, and will show with greater accuracy 
the exact position of the principal lines of the government surveys, 
from which are derived and established the boundaries of farm lands, 
thus often preventing litigation and neighborhood quarrels. 

It is further made the duty of the survey to search for and properly 
examine all mineral fertilizers that may exist in the state; to analyze 
the clays, peats, marls and other natural products useful, either in 
maintaining the richness of the soil or of restoring it when exhausted 
by the injudicious management of ignorant and selfish men. The 
soils and subsoils are to be made subjects of study, and observations 
are to be made upon the animal and vegetable products with refer- 
ence to their agricultural interest. Specimens are to be collected ex- 
emplifying the geology of the state, which are to be deposited with 
the various institutions of education, from which the youth of our 
state may hereafter acquire that more definite knowledge of our local 
geology which will enable them to prosecute their future labors in farm- 
ing with greater advantage both to themselves and to the country. 

It is now very generally admitted that the chemical analysis of 
soils does not lead to all of the beneficial results that were formerly 
anticipated from this source. The healthy growth of farm crops is 
dependent upon too many varying conditions, besides the mere quan- 
tity of plant-food that may exist in the soil, to enable the chemist to 
detect the cause of any given failure, by soil analysis. It was once 
supposed that we had only to analyze a soil before and after a crop 


ANNUAL REPORT FOR 1873. 43° 


has been, taken from it, to detect the substances that had been ab- 
stracted, and thus indicate what should be artificially supplied to 
stimulate the growth of the next crop; but such is the minuteness of 
the quantity of plant-food compared with the mass of the soil, that 
chemical science has not yet, except to a limited extent, been able to 
accomplish this task. Consequently no general effort will be made to 
analyze the soils of the state; but if any are found, that, from any 
special peculiarity or other reason, seem to require it, such analysis 
will be made. 

Geology. is now very properly included among the studies to be 
pursued in agricultural colleges, with a view to its special advan- 
tages in the proper cultivation of the soil—a cultivation which shall, 
without the least diminution of its annual product, perpetually main- 
tain its fertility. Every farmer should know whether his land is un- 
derlaid by rocks whose disintegration is beneficial or otherwise; 
whether these rocks are of the granitic kinds, or whether they consist 
of sandstone, limestone or shales. [He should also be able to deter- 
mine the nature of the pebbles, small and large, abounding in his 
fields, the gradual decay of which, from year to year by reason of ex- 
posure to weather changes — frost, rain, sunshine and alternate ex- 
posure to heat and cold — will add useful or useless, or even delete- 
rious qualities to the soil. Limestone pebbles especially, by their 
gradual disintegration, are of the greatest value by restoring fertil- 
izing substances to the soil that would otherwise soon be exhausted 
by continual cropping. If these pebbles are of such quality as to be 
thus beneficial, the land possesses additional value; if otherwise, a 
larger annual expense for fertilizers will be required. The system of 
farm management, suited to the one case, would require modification 
for the other. Hence it is sufficiently apparent that some knowledge 
of geology is quite essential to the intelligent farmer, and that it is 
wise to include it in a course of studies to be pursued in our agricul- 
tural colleges. 

The several reports to be made to the governor annually in Janu- 
ary, though chiatly intended to make known the progress and results 
of each year’s work, will be found to contain much that is of interest 
to the farmer. The publication and general distribution of reports 
of geological surveys always prove beneficial, by calling public atten- 
tion, in an official and reliable manner, to the resources and advan- 
tages of the district surveyed, for the agricultural, manufacturing 


and other interests. 


44 GEOLOGICAL SURVEY OF WISCONSIN. 


LIST OF MAPS 
Accompanying the First Annual Report of the Wisconsin Geological Survey, 1873. 


A map of the state (published by Silas Chapman) on a scale of six miles to an inch, 
showing in colors the boundaries and extent of the several rock formations so far as 
is known up to the end of the year 1873. On four sheets. 

A map of the Muscalonge diggings in Grant county, on a scale three chains (198 feet) 
to an inch. 

A map of Ashland county and another of Douglas county, on a scale of two miles to one 
inch, showing the geological features and mineral ranges in those counties; also a 
map of the Apostle Islands; to accompany the report of Prof. R. D. Irving. 

A map in two sheets on a scale of two miles to an inch, showing the geology and topo- 
graphy of the region surveyed by Prof. T. C. Chamberlin, from the state line in 
Walworth and Rock counties to Keshena, in Shawano county. Also two maps, on 
a scale of six miles to an inch (based upon Mr. Chapman's map); one showing the 
distribution of vegetaticn, etc., the other representing the areas occupied by the 
different kinds of soil in the same region. These maps accompany the report of 
Prof. Chamberlin. 

Geological Map of the Lead Region (in part) on six sheets, to wit: 

Ist. Ranges two and three east from three miles south of the state line to Min- 
eral Point, being townships No. one, two, three and four, in those ranges. 

2d. Townships four and five in ranges one to six west, inclusive. 

3d. Townships four and five in ranges one to five east, inclusive. 

4th. Ranges two and three east, in townships five to nine, inclusive. 

dth. Ranges two and three east, in townships ten, eleven, twelve and thirteen. 

6th. Ranges five and six east, from township five to the Wisconsin river in town- 
ship nine. 

Topographical Map of the Lead Region (in part) on two sheets, to wit: 

Ist. Ranges two and three east, in townships one to six, inclusive. 
2d. Townships feur and five in range one east, and ranges one to six west, inclusive. 

These maps are all upon a scale of one mile to an inch. 

A geological, topographical and subterranean map of the Blue Mounds and the Brig- 
ham Lead Mines, on a scale of one to twenty thousand. 

All these maps in the lead region accompany the report of Mr. Moses Strong. 


All of which is respectfully submitted. 


I. A. LAPHAM, 


MILWAUKEE, January, 1874, Ohiet Geologist. 


-Ursuovst Ay OF Jo SETTE ‘Surppeg ested Surmogs 


‘INOLSGNVS Wvdsl0d Senin amomageer 


REPORT OF PROGRESS AND RESULTS, 


FOR THE YEAR 1874. 


BY I. A. LAPHAM. 


During the past year the same parties have been in the field as in 
the preceding year, and in addition a party under the charge of Maj. 
T. B. Brooks, late of the Michigan Geological Survey, as will be men- 
tioned in a subsequent part of this report. I am glad to be able to 
state that the survey is progressing with reasonable rapidity; the 
amount of work done being considerably in excess of that of 1873. 

The first annual report of progress and results of the survey was 
deposited in the office of the governor on the first Monday in Janu- 
ary, 1874, with ample maps and illustrations, accompanied by the re- 
ports of the several assistants. It was found impracticable to com- 
plete the reports of explorations made by the several parties in 1873, 
in as full detail as is desirable, in time to be presented to the gover- 
nor on the day required by law. They were accordingly presented in 
an unfinished condition, with the expectation that additional matter 
could be annexed when prepared. By a law, approved March 4th, 
1874, it was provided that the manuscript report of the geological 
survey then made, with the maps and drawings, should be bound and 
preserved in the vaults of the office of the secretary of state at Madi- 
son; hence all such additional matter is necessarily excluded, and is 
herewith submitted in the form of supplementary reports. 

For greater convenience in binding and in future publication, it 
was decided to make all sections, drawings, and maps, so far as was 
practicable upon sheets of uniform size; and rules were adopted to 
secure uniformity in respect to the position of maps and profiles upon 
the sheets. 

Tracings from the township plats of the government land survey 
were furnished to the several parties as needed; and as before, they 
were greatly assisted by the published maps of the several counties. 


46 GEOLOGICAL SURVEY OF WISCONSIN. 


These are especially valuable as showing the location of the public. 
roads, usually from actual survey. 

The specimens collected during the year, for study and comparison, 
with the duplicates intended for the Academy of Sciences, University, 
colleges, and normal schools, now amount to a very considerable 
number, requiring much room and involving some expense for their 
storage and proper arrangement for convenient reference in making 
up the reports. 

Nearly five hundred townships (about one-third of the total area of 
the state) have now been examined, with more or less minuteness, by 
the several parties, as follows: 


By Prof. Irving in 1873, - - 45 townships. 
1874, - - - - 98 s 
By Prof. Chamberlin in 1873, - - Ke 
1874, - - - 180 * 
By Mr. Strong in 1873, - - - - 50 “ 
iev4, = = = = 66 * 
By Maj. Brooks in 1874, - - 17 ae 
By Mr. Ives in 1874, - = = . 4 ‘“ 


Several of the aneroid barometers purchased for the survey, having 
been found to be imperfect and useless, others of better quality, which 
have proved quite satisfactory, were obtained directly from the makers 
in London, England. 


Pror. R. D. Invine’s Parry. — Prof. Irving was directed to make 
such explorations and surveys as would enable him to construct a geo 
logical map and section along a line extending from the south part of 
Dane county, northward, through portions of Columbia, Adams, and. 
Wood counties, to Grand Rapids, and thence up the Wisconsin river 
to Wausau; the breadth occupied to embrace two or three ranges of 
townships; thence along the southern boundary of the Archean rocks 
in Wood, Clark, and Jackson counties, he was to extend his work. 
westward to the Black River Falls; the details of this important 
locality having been previously examined by him. This route would 
enable him to determine many important questions, in a portion of 
the state heretofore but little known geologically; especially in regard 
to the quartzites, conglomerates, and other rocks of the Baraboo 
river; the sandy region north of Portage; the kaolin beds; the 
Mosinee hills; and the reported localities of iron ores. As the iron 
ores of Lake Superior and the Menomonee region extend through 
considerable distances, it was hoped that there. might be a similar 


ANNUAL REPORT FOR 1874. 47 


range of ore beds extending eastward from Black River Falls; a very 
important question that might be determined, by the explorations 
thus to be made. 

Before commencing the field-work of the season, Prof. Irving pre- 
pared the supplementary report herewith submitted, embracing de- 
tails of results attained in 1873, which, for want of time could not, as 
before stated, be included in his general report for that year, now de- 
posited in the office of the secretary of state. This supplementary 
report, covering seventy-four pages of manuscript, with several maps, 
diagrams and sections, will be found to contain much additional mat- 
ter relating to the geology of Douglas, Bayfield and Ashland counties. 

The rocks in this part of the state are referred to five different per- 
iods, as follows: 


Ist. Laurentian — Granite, ete. 

2d. Huronian— Iron-bearing series. 
3d. Copper-bearing rocks. 

4th. Potsdam sandstone. 

5th. Quaternary — Drift, ete. 


Many facts and arguments are adduced to show that this is the 
proper order of arrangement, and ample details are given, so that geo- 
logists may judge of the correctness of these views. 

Prof. Irving has been able to show the existence of a synclinal axis 
extending in a southwesterly direction, through these counties, being 
the westward inland extension of the great trough between Keweenaw 
Point and Isle Royale, occupied mostly by the waters of Lake Super- 
ior. We thus have a more clear understanding of the different direc- 
tions assumed by the dip of the rocks at different localities, and are 
brought to a knowledge of one of those grand movements in the re- 
mote past, by which the solid rocks have been folded, contorted, and 
lifted to their present complicated positions. To understand these 
ancient disturbances of the strata is not only a matter of interest in 
speculative geology, but is also one of the greatest practical import- 
ance to the miner and to all having occasion to deal with these rocks. 

It will be seen that the Copper-bearing rocks are Pre-Silurian, 
though not as old as the Huronian. Prof. Irving’s conclusions on 
this point are that: 

Ist. “The beds of the Copper-bearing series and those of the Huro- 
nian were once spread horizontally over one another, including the 
whole series of tilted sandstone on the Montreal river; they were dis- 
turbed by the same force, and received their present tilted positions at 
the same time, as evinced by the entire conformability of the two series. + 


48 GEOLOGICAL SURVEY OF WISCONSIN. 


2d. “The horizontal sandstones of the Apostle Islands, and the west 
end of Lake Superior, were laid down subsequent to this tilting, and 
also to an immense amount of erosion; and the sandstones of eastorn 
Lake Superior were formed at the same time. These points are 
proved by (1) the occurrence of horizontal sandstones in immediate 
proximity to tilted sandstones and traps, in Ashland county; (2) the 
occurrence of the same in the Apostle Islands, within but a few miles 
of the tilted beds of the Montreal; (3) the actual contact of the hori- 
zontal sandstones with the melaphyrs of the Copper-bearing series in 
Douglas county; and (4) similar and additional facts observed by 
Messrs. Brooks and Pumpelly in the upper peninsula of Michigan. 

3d. “That hence the Copper-bearing rocks should rather be classed 
with the Archean than with the Silurian rocks.” 

Under the head of “ Economie Geology,” Prof. Irving discusses the 
questions regarding the probable existence of copper, silver, etc., with 
an account of the attempts heretofore made in mining for these metals. 

Accompanying this supplementary report, Prof. Irving has furnished 
for preservation, a transcript of notes made by him in 1873, on the 
iron ores and iron mounds at and near Black River Falls, in Jackson 
county, with the analyses of the ores, so far as they have been finished; 
these are to be used in compiling a final report, when the survey in 
that neighborhood is completed. From these notes it appears that 
there are no less than nine different beds of iron ore interlaminated 
with slates, crossing the river at various points, within a distance of 
less than two miles, and that there are seven prominent mounds, con- 
sisting chiefly, or largely of iron ores, with slates and quartz. Seve- 
ral analyses already completed, indicate 26 to 32 per cent. of metallic 
iron, associated chiefly with silica. The slates are supposed to be of 
Huronian age, resting upon gneissoid granite below, and covered un- 
conformably by the Potsdam sandstone. 

There are indications of a great lapse of time, and of very conside- 
rable erosion after these slates were hardened into rock and elevated 
to their present position, but before the deposition of the Potsdam 
sands. Specimens were obtained near the mouth of Snow creek, show- 
ing the junction of the sandstone with the Huronian slaty ore, in a 
very interesting manner; some of the horizontal and some of the in- 
clined layers being seen in the same hand specimen. 

These notes are accompanied by a map showing the occurrence of 
the mounds, and another showing the position of the iron beds along 
the river above the falls, with diagrams illustrating the same. 

Prof. Irving’s party took the field in the latter part of April, and 
continued until the portion of the appropriaticn allotted to this ser- 


ANNUAL REPORT FOR 1874. 49 


vice was exhausted in September. Some work had previously been 
done near Madison. The services of Mr. E. T. Sweet were again se- 
cured, and proved to be altogether satisfactory. On the 26th of June 
the party had reached Lodi, and soon after, Portage, where Prof. 
James H. Eaton, of Beloit, joined it in the explorations of the quartz- 
ites of Columbia county. He continued with the party until near the 
close of the season. At Grand Rapids the party had an interview with 
Prof. Davenport Fisher, of the Naval School at Annapolis, who had 
made and furnished to the survey an analysis of the kaolin of that 
place. In September Prof. Irving and Mr. Strong met in Jackson 
county, and by conference, were enabled to determine some results 
beneficial to the survey. 

Reference to the report of Prof. Irving, herewith submitted, will 
show the progress he has made, and the results, so far as they have 
been worked up, at the present time. In this report will be found 
much detailed information of local interest and importance, regarding 
the dip, thickness and economic value of the several rocks, and its 
publication cannot but be useful to the citizens of the state as well as 
to the scientific geologist. With the aid of the map and sections, all: 
these details may be clearly understood, even by persons not familiar 
with the science of geology generally. 

The interesting fact is pointed out that the boundaries of the prai- 
ries, as laid down upon the government plats, correspond, in a gene- 
ral way, with the boundaries of the geological formations — another 
instance of the bearing one study may have upon another. The na- 
ture of the soil, derived directly from the rocks, has much to do with 
the distribution of trees and other plants over the earth’s surface, and 
hence we find the native flora considerably modified by the rocks of 
the several geological districts. 

The artesian well at the state house, Madison, disclosed the Arch- 
wean character of the rock immediately below the Potsdam at that 
place, and gives probability to the suggestion that our whole state is 
underlaid by these rocks at no great depth. 


Wis. Sur. —4 


50 


GEOLOGICAL SURVEY OF WISCONSIN. 


REGISTER OF THE ARTESIAN WELL IN THE CAPITOL PARK, MADISON. 


| Above level of 
the Ocean 


We) 
to 
fox) 


918 


131 
122 
1203 


98 


89 


SOIL 
Top of well ...ccecceecrcee er eneeeeeeneene entrees 
Soil and Clay... .ssseecceeec cece ee reeeseeeecee ones 
DRIFT, 
Sand and boulders......++-++++eeeees Sa csisaetenieiie 
CTEM a sccis.siscace-avvsore op nieiecas ues SiS aS H chiara iaeegNe esos 
Clay and laminated rock .....+-+++seeeeeeeereeeeces 
Grayish-brown rock (boulder?)...+++se+e+seeeeeee eee 
Indurated clay (quite compact). ....+-.+eeseeeeeeeeee 
Rock (boulder?).....+..cseeeeee eres ee ceees siteisiencns 


POTSDAM SANDSTONE.* 


Sandstone gravel, quite loose, white and yellow, no ce- 
ment or coherence........++. + Docent reer e teens es 
Loose, white, uncemented sand, with layers of yellow 


White quartz sandrock of finer grain, mixed with a sub- 
stance resembling porcelain......-.0e+.eeeeeeereee 
Red clay-like powder, very slightly gritty, under high- 
est power appears to be mostly very fine quartz sand. 
Coarse, dark, reddish-brown powder, mostly very much 
rounded quartz grains, but mingled with some dark, 
opaque grains also rounded, belonging therefore with 
the mechanical rocks....0.c0 ccs evaesewsenmeeenes 


ARCH HAN. 


Dark grayish mixed rock, very hard to drill, coming up 
in quite large fragments all angular; carries patches 
of a greenish cleavable mineral; sp. gr. of rock, 2.76; 
hardness, 5; fuses at about 3 to a black bead. The 
included mineral (prehnite) is cleavable and semi- 
translucent, and fusible at 3.5 to 4 to a white enamel. 

Crystalline rocks (work suspended)....++.++..ss-e08- 


|. Be 
E Ag oe 
ge [ed 
ig BA 12,5. 
a la 
eRe | eee 348 
8 8 340 
60 68 280 
Ly 80 268 
17 97 251 
a 102 246 
20 122 226 
4 126 222, 
55 181 167 
74 955 93 
10 265 83 
495 760 —412 
30 795 —447 
9 804 —456 
143 80514|—4573 
ong) 98 | —480 
Is7 1015 —667 


The numerous artesian wells, though not always successful in 
affording water, show very important results in regard to the rock 


strata far beneath the surface. 


The recent discovery of native copper 


and silver in the well at Kilbourn City, at the depth of 516 feet, 


* Possibly this should stand next before the gravel, depth 80 feet. 


ANNUAL REPORT FOR 1874. 51 


must be deemed one of no inconsiderable interest, being the first in- 
dication of the existence of these metals (uncombined) in the central 
or southern part of the state. Whether they exist at this place in 
quantity sufficient to be profitably mined can only be determined by 
sinking a shaft to the depth indicated. The copper-bearing rock was 
exceedingly hard, and had a depth of eighteen feet. Until we know 
the dip of this rock, it will be impossible to ascertain its real thick- 
ness; if the stratum lies horizontally (which is not very probable), it 
has a thickness of eighteen feet; if it has a dip of 45° or more, its 
thickness is only thirteen feet or less. It is not improbable that 
when the proper trend of these rocks can be found, a search in the 
right places may lead to further discoveries of importance. The top 
of this well is 347 feet above Lake Michigan; Archean rocks were 
reached at 118 feet below; total depth of the well (December, 1874) 
840 feet. 

One of the first results of Prof. Irving’s survey of Dane county 
was the identification of a hitherto unrecognized layer of sandstone, 
far down in what has been classed as Lower Magnesian limestone; 
to this, in accordance with the custom of geologists, he has given the 
local name of “ Madison Sandstone.’ It is much used in and about 
Madison as a building stone. That portion of the Calciferous or 
Lower Magnesian limestone series lying below the Madison Sand- 
stone, and down to the Potsdam, forms the immediate shore of Lake 
Mendota (4th lake), and has with much propriety been named the 
“ Mendota Limestone” in the report. This explains some anamolous 
sections heretofore made, and introduces two new names into the local 
geological nomenclature. 

We thus find additional resemblance between the formations in 
Wisconsin and those in Missouri, where Prof. G. C. Swallow long ago 
recognized, and arranged under the head of “ Calciferous sandstone 
or Magnesian limestone series,” seven different members, which may 
now be parallelized with our strata as follows: 


MISSOURI. WISCONSIN. 
First Limestone, 190 feet. Buff Limestone, 50 feet. 
Saccharoidal Sandstone, 125 feet. St. Peters Sandstone, 100 feet. 
Second Limestone, 230 feet. Main Beds, 80 feet. 
Second Sandstone, 70 feet. Wanting. 
Third Limestone, 350 feet. Wanting. 
Third Sandstone, 50 feet. Madison Sandstone, 35 feet. 
Fourth Limestone, 300 feet. Mendota Limestone, 30 feet. 
Potsdam Sandstone. Potsdam Sandstone. 


Pror. T. O. Cxampertin’s Parry. — Before entering upon the field 
work, Prof. Chamberlin completed his report of the work done in 


52 GEOLOGICAL SURVEY OF WISCONSIN. 


1873, by sending a supplementary report, which, as above explained, 
could not be prepared in time to be bound with the matter previously 
reported by him. This supplementary matter is therefore herewith 
submitted, and will be restored to its proper place in the preparation 
of the final report, as contemplated by section five of the law author- 
izing the survey. 

In this report will be found many details with respect to the Lower 
Magnesian limestone, as it occurs in the northeastern part of the 
state, showing much the same general characteristics as in the south- 
western counties. It is interesting to note the occurrence of a con- 
siderable fault in the strata in the town of Ellington (T. 22, R.16 E.), 
such dislocations being rare in Wisconsin. To this we may attribute 
some very marked peculiarities in the hydrography of that vicinity. 

Wherever mining has been prosecuted in search of gold, silver, 
copper, etc., examination of the rocks gave little indication of the 
presence of these metals; and it has very often been the business of 
the survey to discourage the search for ores in places where they are 
not to be found. Copper-mining at Berlin and gold-mining at Win- 
neconne are among the projects thus discouraged. 

The quartzites of Portland, Dodge county, and some new localities 
discovered in adjacent portions of Jefferson county, are fully de- 
scribed. Several other outcrops of Archean rocks are described — as 
at Berlin, Mukwa and Keshena. 

The important subject of artesian wells is also fully discussed in 
this report, giving many details that will be of great value in the fu- 
ture operations of well-digging. , 

It was deemed most conducive to the public interest to direct Prof. 
Chamberlin to continue his survey from Beloit along and near the 
south line of the state to Lake Michigan, and thence northward be- 
tween his line of operations in 1878 and the shore of the lake. Though 
much covered with drift, it was hoped that a sufficient number of out- 
crops of rock could be found to reveal the general geological charac- 
ter of this district, and perhaps develop some new and interesting facts 
in regard to this portion of the state. Funds were supplied him for 
expenses of the field-work on the first of May, and the work com- 
menced soon afterwards. By the last of August this party was able 
to reach the extremity of the peninsula between Lake Michigan and 
Green Bay, at “ Death’s Door,” and to commence the return trip, in 
which some points of special interest were reéxamined, and many new 
localities visited. Active duties in the field were brought to a close 
in October. The services of Messrs. L. C. Wooster, G. D. Swezey, 
and J. H. Chamberlin were secured during portions of the season; 


ANNUAL REPORT FOR 1874. 53 


and Mr. F. H. King was engaged to continue his observations upon 
animal and vegetable life, such as are required by the provisions of 
the law authorizing the survey. Two thousand five hundred miles of 
travel with a team; seven thousand specimens of rocks, fossils, and 
minerals collected; these are justly deemed a good season’s work. 

Prof. Chamberlin’s report of his operations during the year 1874 
will be found to contain ample details of the geology of the district 
assigned to him. These will settle many questions as to the non- 
occurrence of coal and other useful minerals, which are dependent up- 
on the kind of rock found. The difficulty of determining the proper 
order of succession of the various strata, with their general dip and 
strike in a region where outcrops can be only here and there exam- 
ined, is very great. Hence, perhaps there may still remain some im- 
portant questions for future investigation; but sufficient has been 
ascertained, it is believed, to answer all the general objects and pur- 
poses of this survey. 

Attention is called, in this report, to the great valley diverging 
from the west shore of Lake Michigan towards the southwest, well 
marked by the waters of Green Bay, Lake Winnebago and the valley 
of Rock river; the rock ridge bordering this great ancient valley on 
the east; the very remarkable drift ridge, locally known as the potash 
kettles, extending from the south line of the state to the peninsula 
of Green Bay; the several systems of parallel drift ridges, some of 
them sharp and narrow, called hog’s backs; and the more level dis- 
tricts along the immediate shore of the lake. 

A very important and interesting deduction made by Prof. Cham- 
berlin, as a result of his explorations, is the fiord character of the 
peninsula of Green Bay; this being the result of intense glacial ac- 
tion, perhaps near the close of the great ice period. The glacier 
seems to have been concentrated upon Lake Superior by the converg- 
ing shore lines, and passing southward to Green Bay, was thence di- 
verted towards the southeast, plowing six or more great furrows, 
which are now indicated by bays on both sides of the peninsula. 
These valleys, or fiords, are continuous across this narrow neck of 
land, and may be traced on the charts of the lake survey upon the 
bottom of Lake Michigan, for a distance of twelve or fourteen miles. 

If the peninsula north of Sturgeon Bay was ever covered with 
drift, it has been entirely removed, perhaps by the abrading action of 
waves at atime when Lake Michigan stood at a much higher level 
than now; the rock surface being now covered only with a thin layer 
of soil, destitute of drift material. 

Some very remarkable facts relating to the course of streams are 


54 GEOLOGICAL SURVEY OF WISCONSIN. 


referred to as indicating changes that have taken place in the condi- 
tion of the land in remote times. 

The drainage is shown to be a proper medium between the slow- 
flowing streams and swamps of a flat country, requiring artificial 
drainage, and the rapid eurrents of highly inclined lands, causing ex- 
tensive erosions and the loss of the more fertile portions of the soil. 

Attention is given to the fact that large areas represented as marsh 
on the government plats are now dry and arable; that many of the 
streams have disappeared and become mere periodical runs; and that 
the volume of running water has been considerably reduced; facts 
undoubtedly due to the removal of the forests and the cultivation of 
the soil. 

Prof. Chamberlin, with the active and intelligent aid of Mr. Swe- 
zey, enters with much detail into the important subject of the distribu- 
tion of plants over the surface of the state, and accompanies his report 
with a map representing, as well as can be done, the principal facts as 
observed and recorded during the progress of the survey. Plants are 
arranged into fifteen different classes or groups, each of which oceu- 
pies certain localities to the exclusion of the others, and each indicat- 
ing some peculiarity of soil, geological formation, or climate. 

Under the head of Surface Geology will be found many important 
facts in regard to the soil and subsoils, of which he distinguishes 
eight different kinds, each with its peculiar qualities and value. One 
of these — the calcareous sandy soil, found near Elkhart lake — con- 
sists mainly of small crystals of dolomite or magnesian limestone, 
which, while having the appearance of being sandy and unpromising, 
is found to possess great fertility. 

The measurements along the west shore of Lake Michigan, intend- 
ed to show the progress that lake is making in wearing away its 
banks, are not only of interest and importance at the present time, 
but will possess value to those who shall come after us for many years 
in the distant future. They show a mean annual abrasion in Racine 
county of 3.33 feet; and in Milwaukee county of 2.77 feet. The 
rapidity of geological changes, made under our own eyes, is promi- 
nently exhibited in the fact above mentioned of a ravine having been 
formed near Racinewithin the past twenty-eight years, which is half a 
mile in length, one hundred and twenty feet wide and forty feet deep. 

The ample topographical details, including lists of elevations, will 
have their use in all future projects for the construction of canals, 
railroads, and for many other practical and useful purposes. 

Section two of the act to provide for the geological survey, among 
other objects and duties, very properly requires observations to be 


ANNUAL REPORT FOR 1874. 55 


made upon the animal and vegetable productions of the state, with 
reference to its agricultural interests. This duty has been assigned 
to Mr. F. H. King, under the direction of Prof. T. ©. Chamberlin, 
one of the assistants in the survey. Though this work is incomplete, 
it is deemed best to present herewith, for preservation and future use 
the two reports now prepared by Mr. King, which will be found to 
contain brief notes of very numerous and important observations 
made by him during the years 1873 and 1874, relating to the birds 
and to the Lepidopterous insects of the state. 

The notes upon the birds relate chiefly to their food, as ascertained 
by an examination of the contents of the stomach of the several spe- 
cies; this becomes important by showing whether they destroy our 
insect enemies or friends. It is only by such observations, made by 
persons who find pleasure in the pursuit, and who are to be relied 
upon for care and accuracy, that the truths of natural history can be 
ascertained and recorded. One hundred and two species of Wiscon- 
sin birds are mentioned, and facts of greater or less importance are 
recorded in regard to them. Fifty-four species of insects, injurions 
to one hundred and twenty-six species of plants, and seven species 
whose habits are such as to be deemed beneficial, are included in this 
report. 

Mr. King’s notes are to be preserved for use in making up a more 
general and complete work upon the animal and vegetable produc- 
tions of the state, which will embrace also such further observations 
as may hereafter be made during the continuance of the survey. 


Mr. Mosrs Strone’s Parry.— As early in the season of 1874 a8 
the weather became suitable for active operations in the field, Mr. 
Strong, with the aid of Mr. George Haven as an assistant, and John 
Cain as teamster, resumed the work of surveying those portions of the 
lead region not covered by him in 1873. The preceding winter bad 
been spent in preparing plats and collecting such information of the 
country to be examined, as would facilitate the field-work of the seu- 
son. The southern and eastern portions of the lead region were first 
surveyed, including the whole of Green county; and, after completing 
a few townships in the northeastern part of lowa county, he proceed- 
ed in August to carry out that portion of his instructions that con- 
templated the extension of his survey northward, through Richland, 
Vernon and Monroe counties to the southern limits of the Archean 
rocks in Jackson county. The northern portion of the lead region, 
and the much broken district extending from the great east and west 
watershed to the Wisconsin river, were next examined in detail. 


56 GEOLOGICAL SURVEY OF WISCONSIN. 


He was thus fortunately able to accomplish the whole of the work 
assigned to him at the beginning of the season, and to prepare his 
second annual report, with the necessary maps, sections and diagrams, 
within the time prescribed by law. 

The work of the past season is so intimately connected with that of 
the previous year, that it was deemed best to include the whole in 
one report; accordingly this has been done by Mr. Strong, so that the 
accompanying report gives one connected and comprehensive view of 
his work, and its results up to the present time. 

In this report will be found full details with respect to the district 
thus surveyed, arranged under the following heads: 

Previous publications and surveys; 
Topographical and geological maps and sections; 
Barometrical observations; 
Physical geography, and surface geology; 
The several rock formations; being the 
Potsdam sandstone, 
Lower Magnesian limestone, 
St. Peters sandstone, 
Buff and Blue (Trenton) limestone, 
Galena limestone, and 
Cincinnati group, 
All considered with respect to their geographical boundaries, litho- 
logical character, ores, minerals and paleontology; 
The origin of river valleys; 
Explanation of mining terms; 
Present condition of the mines; 
Statistics of lead, zinc and copper production; 
Explorations north of the Wisconsin river, and 
Prehistoric mounds of the lead region. 

Topographical maps accompany this report, embracing the entire 
lead region, on a scale of one mile to an inch, which is sufficient to 
exhibit, by contour lines fifty feet apart (vertically), the elevation of 
every point above the level of the sea. These maps also show the posi- 
tion of the public roads. Such maps have special value not only in 
respect to future railroad surveys, showing at once the practicability 
or impracticability of any contemplated route, and thus save the time 
and expense of a very large amount of preliminary surveys, but are, 
obviously, of great importance to the mining interest, as indicating 
the proper system of drainage, location of “levels,” ete. Geological 
maps are also furnished, constructed upon the same scale, showing the 
position of the several rock formations, by which the relation of a iy 


ANNUAL REPORT FOR 1874. BT 


particular quarter section of land to these formations can be seen, and 
its value with respect to mining prospects at once ascertained. The 
information from which these maps were constructed has been col- 
lected with great care, involving an immense number of barometrical 
observations, and a great many miles travel. 

From information contained in these two series of maps, it is easy to 
construct geological sections on any desired line. Those prepared by 
Mr. Strong, and accompanying his report, have been selected with a view 
of showing the “dip, number, magnitude, order and relative position 
of the various strata,” as well as the amount of denudation to which 
the country has been subjected. The amount of denudation thus 
shown, seems wonderful, but is accounted for when we consider the 
immense time during which the rocks have been exposed to the abrad- 
ing influences; being no less than the time occupied by the formation 
of the Devonian, Carboniferous, and all subsequently deposited rocks. 

The regularity and simplicity of the geological features of the lead 
region are quite remarkable; there being no sudden breaks or “ faults ” 
in the strata, no upheavals to any considerable extent; no intrusive 
rocks, breaking through the different formations; and the veins froin 
which ores are extracted do not penetrate the strata below the horizon 
of the St. Peters sandstone. 

The origin and nature of springs are not well understood, many 
crude notions being commonly entertained in regard to them; hence 
Mr. Strong has, very properly, adduced the facts to show that the 
springs near the top of the Blue Mounds have an abundant source of 
supply, even in the small area of the mound above. 

Though the lead region is supposed to have been exempt from the 
influence of the glaciers which have distributed so much drift mate- 
rial over adjacent districts, there are some facts still requiring explan- 
ation, particularly the one first noticed by Prof. Whitney, of the oceur- 
rence of blocks of St. Peters sandstone resting upon formations of 
later age. The boundary of the glacial drift through Green county 
has now been accurately traced. The occurrence of drift material in 
the valleys of the Mississippi and lower Wisconsin is rightly attrib- 
uted to river transportation from above. 

With respect to the several geological formations, much informa- 
tion is given in detail, systematically arranged, and not before pub- 
lished. 

Mr. Strong’s survey, and the experience of the past twelve years 
have given additional proof of the correctness of the views of Prof. 
J. D. Whitney, as set forth in his report, published in 1861. Among 
the most important of these views are the following: 


58 GEOLOGICAL SURVEY OF WISCONSIN. 


That the lead crevices, with their mineral contents, are not true 
veins extending indefinitely downwards, but partake of the nature of 
shrinkage cracks or joints, such as may be seen in almost all lime- 
stone quarries. 

That though the mineral grounds have considerable lateral extent, 
they reach only a short distance downwards. 

That the filling of the crevices with mineral matter was not from 
below by voleanic heat, but from above, and by precipitation from a 
solution. 

Much doubt and uncertainty still exist as to the origin of the 
metallic sulphurets, and as to the time when, and the special condi- 
tions under which they were introduced into these crevice joints. The 
occurence of a similar lead region in southeastern Missonri, and of 
another in the southwest part of the same state; the first in the Lower 
Magnesian limestone, the last in rocks of the Subcarboniferous age, 
would seem to indicate either that these conditions were repeated at 
three different times, or that they were brought about at a time sub- 
sequent to the deposition of the Subearboniferous limestones. 

Attention is directed to the fact that the valley of Sugar river, 
which constitutes the eastern boundary of the lead region, is much 
broader and deeper in proportion to the amount of water at present 
flowing in that stream than is usual; and hence the inference that at 
some time in the remote past, a large river found its channel along the 
course of the present Sugar river. With a breadth of stream of only 
about one hundred feet, it has a valley as broad as that of the Missis- 
sippi. In the future progress of the survey, additional light may be 
thrown upon this subject. 

The information contained in this report with respect to the pres- 
ent condition of the mines will have a practical value, and will con- 
tribute much towards directing the attention of capital and enterprise 
to that important industrial interest in our state. 


ANNUAL REPORT FOR 1874. 59 


The following table shows the amount of lead and zinc produced for 
the years named: 


Leap. Zinc. 
YEARS. 
Galenite, Smithsonite, Blende, 
Pounds. Pounds. Pounds. 
1360" as. Gaeiacnaninaieds ae Oat eatosl weenie eased 890000 |issveceevesecs 
1861 iieha eaten a laata cua Rape Nene oneal eae te. cc pe cao ane 266,000 |........eeeee 
1862 ga bape ahaa leases tape gaiermeinens yeas 17,037,912 |evess ee er ree ae ee ee 
1863 <2 cued sty ano denseecanes 15, 105, 577 15120, 000. Sissssacceee ces 
T1864. Sesaucegiaciwas woucecuen seta 13,014,201 85171385833 |ssassea veut ox 
W869: ova vinaicserrawadebenionn ta 14, 8387 ,895 4,198,200 |ccsccavcceeans 
TiO ewe vieay aemaneensieaion sa ak 14,029,192 HOt OEe licsnanesucuray 
L867 ass ueg aneweapeeacess cee ee 13, 820, 784 5, 181,445 841, 310 
1868 4546 MoM REM U RON Sea O edd 13, 869, 619 4,302 883 8,078, 435 
US69 vee e's eas Sn oe stem oewiowe ced 13,426,721 4,547,971 6,252, 420 
[S80 sss ces erowaenamnenetee ee ea 13,754,159 4, 429,585 7,414, 022 
1871 £61 4 Gee ay Ge ORAS eR TescsS 13,484, 210 16,618, 160 9,303, 625 
1872 ee ee ee ee 11, 622, 668 27,021,388 16 , 256 ,970 
1873) ccoraccctetiees pew eins e see 9, 919,734 18, 528, 906 15, 074, 664 
POUL, secs se ciscblaceuestaseer fa du 168 ,422, 672 97,080,704. 58, 221, 446 


It will be seen from the above that while the production of lead ore 
has been diminishing, during the past three or four years, that of zine 
ores is rapidly increasing. 

The explorations made north of the Wisconsin river, and outside of 
the lead region proper, were necessarily of a more general character, 
and the facts collected are represented upon maps on a much smaller 
scale. Those made in 187+ were confined chiefly to a single range 
(range two west) of townships, so that the entire extent of the 
Paleozoic rocks could be explored within the time and means appli- 
cable to this portion of the work. The most northern outlier of the 
St. Peters sandstone was found in the south part of township twelve; 
und the last occurrence of limestone (Lower Magnesian) in this range 
is on sections 10 and 15 in township seventeen. 

Here are found those high, continuous dividing ridges forming seri- 
ous obstacles to railroad construction, and from which fine views of 
the surrounding valleys may be seen. 

The search for oil at “ Oil City ’’ resulted only in a fine flowing ar- 
tesian well whose waters may be found to possess medicinal virtues, and 
a knowledge of the strata below, down to the Archsan rocks. Here 
the Potsdam sandstone has the unusual thickness of 844 feet. 

These explorations, being in a linc nearly parallel with the Missis- 
sippi river, will form a convenient base for the surveys to be made in 
1875, between that line and the river. 


60 GEOLOGICAL SURVEY OF WISCONSIN. 


The ancient artificial mounds, especially those of imitative forms, 
found within the district surveyed by Mr. Strung, have received a 
share of his attention. They were built in prehistoric times, by an 
extinct race. of people, whose existence here is believed to have been 
with that of the Mastodon. They thus form the connecting coeval 
link between the geologist and antiquary; the duties of the one cease, 
while those of the other commence with the epoch of the mound 
builders. 


Surveys iv Oconro County, sy Masor T. B. Brooxs. — Maj. 
Brooks, late of the geological survey of the state of Michigan, under- 
took to trace the Iron-bearing, and other rocks found on the east side 
of the Menomonee river of Green Bay, above Sturgeon Falls, across 
that river into Wisconsin, and to ascertain as far as was practicable 
their southern and western boundaries, where they are succeeded by 
granitic rocks. Special search was to be made with the aid of the 
“mining compass” and otherwise, for iron ores, but the money ap- 
plicable to this survey not being adcquate to the sinking of exper- 
imental pits, shafts, or drifts, such work was necessarily left to private 
enterprise, guided by the results of such survey as he should be able 
to make. A suit of specimens was to be collected and forwarded to 
the chief geologist, with a full report in detail, illustrated by the ne- 
cessary maps, sections and diagrams. All chemical analyses were to 
be made by Prof. Daniells, of Madison. 

Maj. Brooks commenced active operations in the woods with 
ample assistance aud supplies, on the 10th of August, and the work 
was continued fifty-six days. The weather, with slight exceptions, 
proved favorable; and the report of results will show that each per- 
son engaged must have done his whole duty. His camps were moved 
along the course of the river, from which he extended his observa- 
tions south to the outcrops of the granite, and west, as far as the 
“Great Swamp,” in range 17 E., town 40 N. He was thus able, 
though not without much exposure and difficulty, to accomplish all 
the objects proposed, and in a satisfactory manner. 

It is gratifying to know that his report, now being prepared, will 
show that the Iron range extends across the Menomonee into Wis- 
consin, and that there is a strong probability that it will hereafter be 
found to contain, within this state, workable beds of ore. 

The rocks examined, as in other portions of the Archean regions, 
were found to be quite local in extent, and often gradually passing, 
by insensible degrees, from one to another, rendering it very difficult, 
if not impossible, to distinguish the different kinds. and to classify 


ANNUAL REPORT FOR 1874, 61 


them under appropriate names. Efforts have been made to overcome 
this difficulty by chemical analysis, and also hy microscopic examina- 
tion of very thin sections, prepared with great care and skill. In this 
way it is sometimes found that rocks, having the same general ap- 
pearance to the eye, are made up by the aggregation of very different 
minerals. The specimens of rocks and minerals sent in were col- 
lected and transported with very considerable labor. They are all 
numbered, and the exact locality from which they were obtained prop- 
erly designated. They will be of much use in the further prosecu- 
tion of the survey, and will, at its close, be distributed to the institu- 
tions entitled to receive them in accordance with the law. 

One of the most serious difficulties met with by Maj. Brooks and 
his party, and which materially retarded the progress of his work, 
arose from the gross inaccuracies of the government surveys in that 
part of the state, and the careless and insufficient manner in which 
the lines and corners were established. Lakes were found having but 
little resemblance to their representation upon the plats; streams are 
made to run where none exist; swamps are laid down where excellent 
pine-lands yield an abundance of lumber; when a tract of land is 
“entered,” the purchaser may find his quantity or number of acres 
deficient, or largely in excess. It is matter of common remark 
among woodsmen in this region, that the Wisconsin surveys are 
much less reliable than those of Michigan on the opposite side of the 
river. Under these circumstances, it may be a question whether it is 
not the duty of the government to resurvey in a more thorough and 
accurate manner, the public lands in this region of the country before 
they become of so much value as to lead to endless trouble in attempt- 
ing to retrace the section lines. 

It is much to be regretted that the several stations of the United 
States lake survey were not connected with the lines of the public 
land survey. This would have afforded many points for correcting the 
maps projected from the land surveys alone. 

At the suggestion of the geological survey, Gen. A, A. Humph- 
rys, Chief of Engineers, directed that the latitude and longitude of 
certain points upon the fourth principal meridian, the base, and the 
correction lines, be ascertained with the utmost exactness. These, 
being the governing lines of the land surveys, are most important; 
and it is, therefore, extremely desirable that their exact position 
should be ascertained. 

As the first fruit of this application, the following determinations 
were furnished to the survey by Gen. C. B. Comstock, on the 17th 


of July, 1874: 


62 GEOLOGICAL SURVEY OF WISCONSIN. 


1. Intersection of the fourth principal meridian with the state line between Iinois 
and Wisconsin, lat. 42° 30' 26.1’; long. 90° 25’ 33.6". 

2, First section commer of the Wisconsin survey on the state line west of the fourth 
principal meridian, lat, 42° 30’ 26.4"; long. 90° 26’ 44.2”. 

3. Southeast corner of section 13, township 18, range 1 west, lat. 44° 1’ 49.6"; long. 
90° 25' 56”. 3 

4. Northeast corner of section 1, township 18, range 1 west, lat. 44° 4’ 26.6"; long. 
90° 25’ 56.7”. 

5, Southeast comer of section 31, township 21, range 8 east, lat. 44° 14’ 57.5"; long. 
90° 10’ 45.8", 

6. Southwest corner of section 31, township 21, range 3 east, lat. 44° 14’ 57.2"; long. 
90° 11’ 48.9”. 

Points Nos. 5 and 6 are on the correction line between townships 20 and 21, near 
Balch’s Ranch, on the Wisconsin Valley Railroad. 

On the correction line between townships 30 and 381, range 19 west, east of the St. 
Croix river. 

7. Southeast corner of section 34, township 31, range 19 west, lat. 45° 7’ 21.5"; long. 
92° 41’ 24.6", 

8. Southwest comer of section 33, township 31, range 19 west, lat. 45° 7’ 22.1"; long. 
92° 43’ 52.1", 


The following local bearings were determined: 


1. The state line between Illinois and Wisconsin, from its intersection with the fourth 
principal meridian, bears W. 16’ 17” N. to point No. 2 above. 

2. The fourth principal meridian, from the southeast corner of section 13, township 18, 
range 1 west, bears N. 11’ 10’ W. to point No. 4 above. 

3. The correction line between townships 20 and 21, from the southeast corner of sec- 
tion 31, township 21, range 3 east, bears W. 5’ 18” S. to point No. 6 above. 

4. The correction line between townships 30 and 31, from the southeast corner of sev- 
tion 34, bears W. 10’ 20” N. to point No. 8 above. 


In accordance with an act of congress, and upon application from 
the state geological survey, as explained in my last report, the super- 
intendent of the coast survey has made arrangements for the prosecu- 
tion, with suitable instruments, of geodetic surveys within this state. 
These will consist of the determination, by the accurate methods of 
that survey, of the geographical position of certain prominent points, 
and the measurement of a base line, from which, by a connected sys- 
tem of triangles, with sides ten to twenty or more miles in length, aa 
amount of exact knowledge of the geographical and topographical fea- 
tures of the state will be acquired, sufficient for the projection of a 
correct map. These surveys when completed and properly connected 
with the lines of the land survey will leave nothing to be desired. 

The work of the past season has been the determination of the lati- 
tude and longitude of Madison and La Crosse, and reconnoissance 
necessary for the selection of suitable triangulation stations, along the 
valley of the Wisconsin river from Prairie du Chien to Kilbourn 
City. This important survey is very properly placed in the hands of 


ANNUAL REPORT FOR 1874. 63 


Dr. John E. Davies, of the State University, and affords excellent op- 
portunities for giving instruction in the several branches of knowledge 
required for such work. 

Mr. Frank Ives, having spent much time in the valley of the Bois 
Brulé river, Douglas county, with his attention upon the geological 
features, was requested to make a report of the results of his observa- 
tions for the use of the geological survey. A copy of this report is 
herewith submitted. It will be found to contain much local infor- 
mation of considerable importance, which could not otherwise have 
been obtained except at a very considerable expense, owing to the 
wildness and unsettled condition of the country. 

The position of many of the rapids, falls, and lake-like expansions 
of the river is here first ascertained; the location of several, before 
unknown, outcrops of the Lake Superior sandstone, and the discovery 
of a range of possibly mineral-bearing trap rocks, in the south part of 
township 48, range 10 west, are among the items of importance in 
this report. Some remarkable drift ridges, extending across the val- 
ley, seem to indicate several successive stages in the decay of the 
ancient glaciers, each leaving traces of its work in the form of ridges, 
resembling, in many respects, the “terminal moraines”? of the mod- 
ern glaciers of the Alps. Above this most ancient or boulder drift, 
Mr. Ives recognizes two distinct epochs; one represented by the sand 
and fine gravel of the so called barrens; the other by the red, marly 
clay, so well known on the borders of Lake Superior. 

His observations upon the soil, climate and mineral productions, 
seem to be judicious and well worthy of the consideration of all who 
are interested in that portion of our state. 

Mr. Gustavus Bode of Milwaukee has furnished the survey with 
the analysis of ten springs and wells, made during the past year, thus 
affording additional knowledge of the character of the natural waters 
of the state. Of these, eight have the bicarbonates of lime and 
magnesia as their chief ingredients, supplied directly from the mag- 
nesian limestones abounding, not only in the solid rock, but in the 
gravel and boulders of the drift. The other two indicate the pres- 
ence of sulphuric acid, arising probably from the decomposition of 
iron sulphurets, by which these salts have been converted into sul- 
phates of lime and magnesia. They also contain the sulphate of soda. 
If these waters could be examined as they first issue from the ground, 
they would, doubtless, show the presence of gaseous matter giving 
them qualities not indicated by the analysis of the solid substances 
obtained. by evaporation. Several springs and wells are known to be 
highly impregnated with sulphuretted hydrogen, and, doubtless, we 


64 GEOLOGICAL SURVEY OF WISCONSIN. 


have many waters whose medicinal qualities are of great value, but 
not yet known and appreciated. 

It will be seen that the work of the several parties has been so dis- 
tributed over the state as to give the most general and correct view of 
the several rock-formations, and prepare the way for greater progress 
during the remainder of the time allotted to the survey. The most 
recent rocks —the Drift, Devonian and Upper Silurian came under 
the special consideration of Prof. Chamberlin; the Lower Silurian of 
the Lead region and the country immediately cet of it were inves- 
tigated by Mr. Strong; while the more ancient (Archean) has chiefly 
received the attention of Prof. Irving and Maj. Brooks. 

The chemical analyses needed for the survey have been, as hereto- 
fore, under the direction of Prof. W. W. Daniells, of the State Uni- 
versity, who has made a great number of full analyses, and numerous 
examinations, with a view to the determination of the value of cer- 
tain mineral products. 


Genera Grotocicat Mar.— With this report is presented a copy 
of Mr. Chapman’s sectional map of the state, on a scale of six miles 
to an inch, upon which is represented the geological features so far as 
they are known up to the date of this report. 


LIST OF MAPS AND SECTIONS ACCOMPANYING THIS REPORT. 


I. Pror. Irvine's SupPpLuMENTARY Report, 1873. 


I. General Map of Northern Wisconsin. Plate 4. 

II. Topographical and Outline Map of the Apostle Islands. Plate 5. 
Ill. Additional map for Plate 1— Ashland county. 
IV. Map of the Ashland Mining Company’s Location. Plate 8. 

V. Showing the occurrence of the Iron Mounds, in the vicinity of Black River 

Falls. Plate 6. 
VIL ee the Formations in detail along Black river, above the falls. 
ate 7. 


TI. Pror. Irnvine’s Report, 1874. 


VII. Map of Townships 5, 6, 7 and 8, in Ranges 8, 9, 10 and 11. 
VII. Map of T. 9, 10, 11 and 12, R. 8, 9, 10 and 11. 
IX. Map of T. 13, 14, 15 and 16, R. 8, 9, 10 and 11. 
X. Map of T. 17, 18, 19 and 20, R. 8, 9, 10 and 11. 
] (2) Map of T. 21, 22, 23 and 24, R, 7, 8, 9 and 10 E. 
X. (3) Map of T. 25, 26, 27, 28 and 29, R. 5, 6, 7and8 E. 
X. (4) Map of T. 21, 22, 23 and 24, R. 3, 4, 5 and 6 E. 
X.(5) Map of T. 21, 22, 23 and 24, R. 1, 2, 3and 4 W. 
Xl. Sections in central Dane county. Plate 2. 
XII. Grouped sections in Dane county. (Double sheet.) Plates 3 and 4. 
XIiIl. Sections in Dane and Columbia counties, 


XXXII. 
XXXIII. 
XXXIV. 

XXXYV. 
XXXVI. 

XXXVII. 


XXXVIII. 


LIV. 


ANNUAL REPORT FOR 1874, 65 


JII. Pror. CaamBerzin’s Rerort, 1874. 


Geological Map, T. 1, 2, 3 and 4, R. 17, 18, 19 and 20. | 
Geological Map, T. 1, 2, 3 and 4, R. 21, 22 and 23. 
Geological Map, T. 5, 6, 7 and 8, R. 19, 20, 21, 22 and 23. 
Topographical Map of Milwaukee county. 
Geological Map, T. 9, 10, 11 and 12, R. 19, 20, 21 and 22. 
a “1,18, 14, 15 and 16, R. 20, 21, 22 and 23. 
Si “1.17, 18, 19 and 20, R. 21, 22, 23, 24 and 25, 
ne “  T. 21, 22, 23 and 24, R. 23, 24 and 25. 
. “ TT. 21, 22, 23 and 24, R. 19, 20, 21 and 22. 
a “*  T. 25, 26, 27 and 28, R. 23, 24, 25, 26 and 27. 
Profile of Drift Formations. 
Map of Subsoils. 
Map of Post Tertiary and Recent Formations. 


IV. Mr. Srrona’s Rerort, 1874. 
Geological Map, T. 1 and 2, R. 2 and 3 W. 


. Topographical Map, T. 1 and 2, R. 2, 3 and 4 W. 


Geological Map, T. 1 and 2, R. 1 E. and 1 W. 
Topographical Map, T. 1 and 2, R. 1 E. and 1 W. 
Geological Map, T. 1 and 2, R. 4 and 5 E. 
Topographical Map, T. 1 and 2, R. 4.and 5 E. 
Geological Map, T. 1 and 2, R. 6 and 7 E. 
Topographical Map, T. 1 and 2, R. 6 and 7 E. 
Geological Map, T. 1 and 2, R. 8 and 9 E. 
Topographical. Map, T. 1 and 2, R. 8 and 9 E. 
Geological Map, T. 1, R. 4, 5 and 6 W., and T. 2, R. 4 W. 
Topographical Map, T. 3, R. 4, 5 and 6 W. 

Geological Map, T. 3, R. 1, 2 and 3 W. and R. 1 E. 
Topographical Map, T. 3, R. 1, 2 and 3 W. and R. 1 E. 
Geological Map, T. 3, R. 4 and 5 E. 

Topographical Map, T. 3 and 4, R. 4 and 5 E. 
Geological Map, T. 3 and 4, R. 6 and 7, E. 
Topogrophical Map, T. 3 and 4, R. 6 and 7 E. 
Geological Map, T. 3 and 4, R. 8 and 9 E. 


. Topographical Map, T. 3 and 4, R. 8 and 9 E. 


Geological Map, T. 6, R. 6 W. 
a “ TT. 6 and 7, R. 4 and 5 W. 
a “ 7. 6 and 7, R. 2 and 3 W. 
“ T.6and 7, R.1 W. and 1 E. 
af “1. 6, 7 and 8, R. 4 E. 
ts “ 7.8, R.1, 2and 3 W, and R.1E, 
ie “ 1. 8 to 22, R. 2 W. 

Profiles (double sheet). 


LIV. (2) Ancient Mounds. 


LV. 


General Geological Map of the State, in four sheets. 


ADDITIONS. 


XXIV. (2) Geological Profiles. 

XXVI. (2) Map of Vegetation. 

‘XXVI. (8) Topographical Map. 
Wis. Sur.—5 


66 


GEOLOGICAL SURVEY OF WISCONSIN. 


LIST OF PAPERS ACCOMPANYING THIS REPORT. 


R. D. Irving’s Supplementary Report. 
R. D. Irving's Transcript of notes relating to Black River Falls. 
R. D. Inving’s Report, 1874. 

T. C, Chamberlin’s Supplementary Report. 

T. C. Chamberlin’s Report, 1874. 

F. H. King’s Report on Birds. 

F. H. King’s Report on Insects. 

Moses Strong’s Report, 1874. 

Frank Ives’ Report, Douglas County. 

J. H. Eaton's Report, Quaternary of Central Wisconsin. 


REPORT OF PROGRESS AND RESULTS, 


FOR THE YEAR 1875.1 


BY O. W. WIGHT. 


In compliance with a requirement of the act “to provide for a com- 
plete Geological Survey of Wisconsin,” approved March 19, 1873, I 
have the honor to report the progress made during the third year of 
the survey. 


Brier History or Previovs Groroaican Surveys 1x Wisconstn.— 
The first geological survey undertaken by the government of the 
United States was instituted by the appointment of G. W. Feather- 
stonhaugh, Esq., by the war department, with instructions to make a 
reconnoissance “of the elevated region lying between the Missouri 
river and the Red river, known under the designation of the Ozark 
mountains.” It was in the early part of the year 1834. In the win- 
ter of 1834-35, that gentleman visited the lead mines of Missouri and 
made a perfectly worthless report. The next year Mr. Featherston- 
haugh was employed by the government under the title of United 
States Geologist to explore the region between the St. Peters river 
and the Missouri, and to make a general reconnoissance of the north- 
west. He referred the whole series of Lower Silurian rocks in the lead 
region of Wisconsin and up the river to the falls of St. Authony and 


1The fullest opportunity has been offered the author of this report to revise. it for this 
volume, but not having been accepted, the delicate duty has devolved upon very unwil- 
ing hands. Certain portions of an annual report necessarily refer to matters of transient 
importance and are of little subsequent value. Such portions of this report have been 
omitted, viz.: A financial statement, a business account of the work in Oconto county, 
and an outline of the work remaining to be done. The law authorizing the survey, 
which has been previously given, and the reports of assistants prepared by themselves, 
are also omitted, as in the case of the reports of 1873 and 1874. I have deemed myself 
under obligations to publish everything of a geological nature, even where dissenting 


from the views presented. T.C. C. 


68 GEOLOGICAL SURVEY OF WISCONSIN. 


beyond to the carboniferous limestone. It is hardly possible to 
conceive of a graver blunder, or an exhibition of profounder ignorance 
in the domain of practical geology. 

A resolution of February 6, 1839, adopted by the house of repre- 
sentatives, reads as follows: “That the President of the United States 
be requested to be caused to be prepared, and presented to the next 
congress, at an early day, a plan for the sale of the public mineral 
lands, having reference as well to the amount of revenue to be derived 
from them, and their value as public property, as to the equitable 
claims of individuals upon them; and that he, at the same time, com- 
municate to congress all the information in possession of the treasury 
department relative to their location, value, productiveness, and oceu- 
pancy; and that he canse such further information to be collected, 
and surveys to be made, as may be necessary for these purposes.”? In 
pursuance of this resolution, the commissioner of the general land 
office appointed Dr. D. D. Owen to take charge of a geological survey 
of the Upper Mississippi lead region. Dr. Owen began his work, 
with 139 assistants, in September, 1839, and finished it the same 
autumn. Tis report, accompanied by maps, drawings of fossils, sec- 
tions, ete., was transmitted to the land office, April 2, 1840. It was 
printed without the maps in June of the same year. 

The senate ordered it reprinted, with the maps and drawings, in 
1844. Dr. Owen’s report contains the first scientific description of 
the lead region of Wisconsin. With a few mistakes, easily made in 
a hasty survey, without skilled assistants, the report determines the 
geological structure of the southwestern part of the state. | 

The general government authorized a geological survey of the Chip- 
pewa land district in 1847, and Dr. Owen was very fortunately selected 
to take charge of it. His preliminary report was furnished to the 
treasury department in April, 1848. THis final report was published, 
with a general geological map, including the whole state of Wisconsin, 
in 1851. Itis a monument of Dr. Owen’s industry and scientific 
knowledge. Professor J. D. Whitney, a most competent witness, truly 
says, speaking of his previous report, “There were probably few, if 
any, persons in the country, at that early period of our geological cul- 
ture, who could have executed the survey with the ability and energy 
which were displayed by this gentleman.” 

The legislature of Wisconsin passed an act, approved March 25, 
1853, under which Mr. Daniels was appointed State Geologist. His 
report, about fifty pages in length, bears no date, but was printed in 
1854. It repeats the views of Dr. Owen and is mostly confined to the 
lead region. About a year afterwards, Mr. Danicls was removed, and 


ANNUAL REPORT FOR 1875. 69 


Dr. J. G. Percival was appointed in his place, August 12, 1854. He 
held the office till his death at Hazel Green, May 2, 1856. Dr. Perci- 
val was in the field two seasons. His first report, of 100 pages, was 
published under his own supervision. He left a second report nearly 
complete, which was subsequently published in 1856. His work was 
mostly confined to the lead region, but the sccond season he made a 
“reconnoissance of the state for the purpose of forming a general idea 
of the geological arrangement.” At once scientist and poet, morbid 
and eccentric, Dr. Percival made accurate original geological observa- 
tions, but refused to hold intercourse with others from whom he might 
have received important information and valuable aid. 

In March, 1857, the Wisconsin legislature passed an act providing, 
that “James Hall, of Albany, N. Y., and Ezra §. Carr, and Edward 
Daniels, of Wisconsin, are hereby designated and appointed commis- 
sioners to make a geological, mineralogical, and agricultural survey of 
this state, embracing a scientific and descriptive survey of the rocks, 
fossils and minerals of the state; full and complete assays of the ores 
and minerals, also of the soils and subsoils, with classification and 
description of the same and their adaptation to particular crops, and 
the best methods of preserving and increasing their fertility. They 
shall also make a full collection of the rocks, ores and minerals, and 
whatever illustrates the economic geology of the state, and deposit the 
same in the rooms of the State University, or such other place as may 
be provided for the same, constituting a museum of practical and sci- 
entific geology. Said commissioners shall also make full collections 
of soils, native fertilizers, cultivated and other useful plants, constitut- 
ing a museum of practical and scientifie geology, and deposit the same 
as aforesaid.’ The act also provided that “the sum of six thousand 
dollars per annum, for the term of six years, is hereby appropriated, 
to be drawn from the treasury quarterly on warrant of the governor, 
and paid to persons entitled to receive the same; which sum shall be 
in full for salaries of commissioners, assistants, rent of room, and all 
other expenses incident to said survey, exclusive of printing the an- 
nual reports of said commissioners.” 

The survey thus authorized was not begun until the following year, 
1858. In that year Prof. Hall and Dr. Carr employed, at their own 
expense, Col. Charles Whittlesey, to explore the country between the 
Menomonee and Oconto rivers, “as a preliminary to more extended 
surveys to the northward.”’ In the spring of 1859, they made an en- 
gagement with Prof. Whitney to make a careful survey of the lead 
region. Prof. Whitney having been employed as chemist and miner- 
alogist in the Iowa survey, had become, to a certain extent, familiar 


70 GEOLOGICAL SURVEY OF WISCONSIN. 


with the upper Mississippi lead region. The Wisconsin legislature 
passed an act, approved by Gov. Randall, April 2, 1860, author- 
izing the governor to use that portion of the fund accruing under the 
law of 1857, from the signing of the act until the organization of the 
survey in 1858, to the payment of Prof. Whitney and Col. Whittlesey, 
and also making Prof. Hall principal of the geological commission. 
Col. Whittlesey explored the country, and commenced a report on the 
iron region of Lake Superior. Prof. Whitney completed his surveys, 
maps and reports of the lead region. An act was passed, approved 
April 15, 1861, authorizing and directing the governor of the state 
“to purchase of Prof. James Hall one thousand copies of the first vol- 
ume of his Geological Report of Wisconsin, confined mainly to the 
lead region, with the details of the geology, mineralogy, and mining 
thereof; and to contain between four and five hundred pages. The 
said volume shall embrace a chapter on the general geology of the 
state, and its relation to the surrounding states, and shall be the same 
size, and in all respects as to type, paper and binding, equal to the 
Iowa Geological Report, with all necessary maps and illustrations; 
provided, that the said one thousand copies, delivered at the capitol in 
the city of Madison, shall not cost more than three dollars each.” In 
1862, the said first volume of Prof. Hall’s report was published in 
accordance with the specifications of the law. Prof. Whitney’s re- 
port of the lead region occupies three-fourths of the volume. Both 
Hall and Whitney are masters in this field of science, and the work 
of both was well done. 

The next year the legislature, under the pressure and excitement of 
the war, repealed the law authorizing the geological survey of the 
state. Whereupon, Dr. Carr and Mr. Daniels abandoned the field. 
Not so Prof. Hall. He had a contract, under seal, with the governor, 
according to the provisions of the law, and claimed that the legisla- 
ture could not annul it. He continued his labor, and completed that 
portion of his work which had been assigned to him in its division 
among the three commissioners. The second volume of his report 
has been ready for publication more than a dozen years. Prof. Hall 
has made repeated applications to the legislature of Wisconsin for 
compensation, but in vain. We are informed that he has brought 
suit against the state, through ex-Chief Justice Dixon, for two thou- 
sand dollars (a year’s salary, under his contract), with accrued inter- 
est amounting to as much more. The second volume of his report, 
in manuscript, has in the intervening time been a loss to science and 
a loss to the economic geology of Wisconsin. It contains, we are in- 


ANNUAL REPORT FOR 1875. "1 


formed, the report of Col. Whittlesey on the iron region in the north- 
ern part of the state. 

“ Descriptions of new species of fossils,’’ made by Prof. Hall, ac- 
companying his report of progress to Gov. Randall, in December, 
1860, were subsequently embodied in the first volume of his report, 
published in 1862. 

The report of John Murrish, as commissioner of the survey of the 
lead district, made to Gov. Lucius Fairchild, and submitted with 
the governor’s message in 1871, contains many useful, practical sug- 
gestions by an experienced miner and intelligent man. Whilst this 
report does nut, in our judgment, successfully combat the scientific 
conclusions of Prof. Whitney, it exhibits comprehensive views, and 
gives valuable hints to explorers for mineral deposits. Doubtless, if 
the labors of experienced miners, like Mr. Murrish, and the labors of 
purely scientific geologists could be combined, better practical results 
might be obtained. 

Under the provisions of the present law, the geological corps was 
organized by the appointment of I. A. Lapham as chief geologist, 
and Prof. R. D. Irving, Prof. T. C. Chamberlin and Mr. Moses 
Strong as assistants. The commission of the first, issued by Gov. C. 
C. Washburn, was dated April 10,1873. The commissions of the 
assistants were dated April 30, 1873. 

For an account of work accomplished by this corps during the years 
1873 and 1874, the undersigned has the honor to refer your excel- 
lency to the brief reports of progress made by the chief at the close 
of those years, and the accompanying voluminous reports made by 
his assistants, together with maps, profiles, tables, ete. 

The commission of the undersigned bears date February 16, 1875. 
His predecessor was appointed by Gov. Washburn, in the spring of 
1873, after the adjournment of the legislature. Jlis name was not 
sent to the senate for confirmation during the session of the subse- 
quent legislature. It was therefore decided (so the undersigned is 
informed) by the judiciary committee of the senate, in the early part 
of the session of the last legislature, that the office of chief geologist 
was vacant. His Excellency, Gov. Wm. R. Taylor, did the under- 
signed the honor to send in his name to the senate, and the senate 
confirmed the appointment with singular unanimity. 

The assistant geologists, following a rule of courtesy under such cir- 
cumstances, offered to surrender their commissions. The newly ap- 
pointed chicf requested them to withdraw their resignations, and to 
continue their work. With this request they cheerfully complied. 


72 GEOLOGICAL SURVEY OF WISCONSIN. 


The resignation of Prof. Daniells, however, aS chemist to the survey, 
was accepted after due deliberation, and the undersigned appointed in 
his place Mr. Gustavus Bode, of Milwaukee, whose acknowledged 
eminence in his scientific speciality was a guaranty of peculiar fitness 
for the work entrusted to his care and skill. 

Mr. E. T. Sweet, who had been connected with the survey from the 
beginning, a trained geological observer, an experienced practical 
chemist, was employed in a general way, to be transferred from one 
field party to another, or to be detailed to the laboratory of the State 
University for special analytical work. 

Mr. Sweet has shown himself very efficient in connection with Prof. 
Irving’s party, in connection with the party of the chief geologist in 
making an extensive reconnoissance of the northern portion of the 
state, and in the labor of the laboratory. 

Mr. Charles E. Wright, of Marquette, L. 8., Michigan, a partner 
as mining engineer and iron expert of Maj. T. B. Brooks, with whom 
he was engaged on the geological survey of the upper peninsula of 
Michigan, was employed during two months in making explorations 
at Penokee Gap, on the Chippewa, Wisconsin, Pelican and Wolf 
rivers, under the personal supervision of the undersigned. His ex- 
perience among crystalline rocks, his knowledge of the Laurentian 
and Huronian formations, and his skill in detecting under the micro- 
scope the difference between crystallization by igneous action and met- 
amorphosis, made his services of especial value in a reconnoissance of 
the Archzean region of Wisconsin. 


Recownoissance Mave 1n toe Nortuern Part or THE STATE UNDER 
tue Prersonat Direction or tHe Curer Grotocist, Durine tHe Lart- 
TER Portion or THE Season or 1875.— About the middle of August 
the state geologist began an extensive reconnoissance of the northern 
portion of Wisconsin, for the general purpose of ascertaining the na- 
ture and amount of work to be done to complete the survey in 1876. 
The reports of the surveys made by Dr. Owen and by Messrs. Foster 
and Whitney, were carefully studied and extensive notes taken, for 
the purpose of having a sort of geological guide book of the region, 
and for the purpose of avoiding an unnecessary repetition of work 
already performed and recorded. Maps, camping materials, supplies, 
instruments, etc., were collected beforehand, and all preparations 
made for moving as rapidly as possible, and covering the greatest 
amount of territory in a given time. 

Mr. E. T. Sweet, a seasoned explorer, a good geological observer, a 
hardy and enthusiastic worker, who had had experience in the north- 


ANNUAL REPORT FOR 1875. 73 


ern wilderness of Wisconsin, was detailed from the field party of Prof. 
Irving, to accompany the chief geologist during the whole trip. 

Charles E. Wright, E. M., of Marquette, Michigan, a ‘highly edu- 
cated lithologist and mining engineer, who had had many years of 
experience among the crystalline rocks of the upper peninsula of Mich- 
igan, was engaged to meet the party at Ashland on the first of Sep- 
tember, and to continue with it till the close of the reconnoissance. 

For the details of the work accomplished, your excellency is refer- 
red to the reports, maps and sections of Mr. Sweet and Mr. Wright, 
which are herewith submitted. 

Among the objects designated in advance to be accomplished by 
the reconnoisance, were to observe the trap dykes (the Copper-bearing 
rocks of Mr. Sweet’s report) crossing the St. Croix river, and to ascer- 
tain their direction; to study the relation of these same dykes to the 
Potsdam sandstone and to the Lake Superior red sandstone; to collect 
facts bearing upon the relative age of the Potsdam sandstone and the 
Lake Superior sandstone; to investigate the relations of the copper- 
bearing conglomerate to the older and the more recent formations; to 
make a more careful and accurate geological section of Penokee 
mountain; to determine the general direction of that range, and the 
probable locality where it crosses the St. Croix river; to find, by long 
journeys northward and southward on the Chippewa, Black, Wiscon- 
sin and Wolf rivers, boundary points between the Huronian and Lau- 
rentian formations; to discover indications of mineral deposits; and to 
collect information in regard to roads, bridle paths, trails, and streams 
navigable for canoes, in order to enable the chief geologist to give in- 
telligent directions for conducting the survey in detail next season, 
with economy and efficiency. 

‘The numerous trap dykes crossing the St. Croix river were found 
to run in a general east-northeast and west-southwest direction, nearly 
parallel to each other. 

There are three trap ridges between Osceola Mills and the village 
of St. Croix Falls; whether these dykes, so called, are of the same 
age, is a problem to be solved by future examinations. 

Whether they are igneous in origin, or whether a portion of them 
areof igneous origin and another portion are not, can only be deter- 
mined by a more careful examination of their crystalline structure 
under the microscope. The Canadian geologists have made out, on 
the northern shore of Lake Superior, several systems of trap dykes, 
evidently of different eruptive periods; but the geological character 
of the region on the southern shore of the lake is so different in many 
respects from that of the opposite shore, that no trustworthy argument 


v4 GEOLOGICAL SURVEY OF WISCONSIN. 


can be drawn from analogy. It is snfficient to remark here provision- 
ally, that the apparent common lithological character and the same 
general trend of the trap ridges crossing the St. Croix river would 
point to the same geological era. 

A somewhat careful examination at St. Croix Falls enabled the ex- 
ploring party to determine that the Potsdam sandstone was deposited 
in the ancient Silurian sea at a period subsequent to the formation of 
the trap, whatever may have been its origin. The beds of the Pots- 
dam sandstone are horizontal over the uneven and tilted surface of 
the underlying igneous or crystalline rocks. 

Almost in contact with the trap, the sandstone contains numerous 
well preserved organic remains. Three miles north of Osceola Mills, 
a ledge of sandstone was found lying horizontal, unconformably on 
the more ancient formation. These facts incontestably prove, that 
this particular trap dyke was not erupted or upheaved through a 
superincumbent layer of sandstone. 

At Kettle river rapids was first found, in ascending the river, a red 
sandstone, having all the lithological characteristics of the Lake Su- 
perior red sandstone, in talus along the shore. The water in the river 
was extremely low, so that unusual opportunity was afforded for ob- 
servation. The slabs and fragments of the red sandstone were sharply 
angular, showing that they were im sitw or not far away. In the 
bank, forty or fifty feet higher, was a fine exposure of Potsdam sand- 
stone in a massive ledge. 

The party had neither the time nor the means at its disposal to 
make an excavation to ascertain by definite observation whether the 
Superior red sandstone existed in true formation beneath the Potsdaia. 
Such a fact, definitely settled by a competent observer, would be 
strong evidence that the former is, at least in part, older than the 
latter, 

At “Pine Island,” in the same rapids, the Superior red sandstone 
was found in ledge, bearing abundant angular fragments of the adja- 
cent trap, forming a brecciated conglomerate that is evidently kindred 
to the conglomerate that extends from Keweenaw Point, in Michi- 
gan, along the northern base of the Porcupine and Penokee mountains, 
west southwestward, till it is lost beneath the heavy drift of north- 
western Wisconsin. Everywhere this conglomerate is formed by 
fragments of the more elevated Huronian or trap ridges, carried down 
by the action of the elements and imbedded in the Superior red sand- 
stone. The ledge of conglomerate under consideration was found to 
be lower than the horizon of the neighboring Potsdam. Placing the 
conglomerate and the Superior red sandstone in the same geological 


ANNUAL REPORT FOR, 1875. er 


category, this fact goes far to strengthen, if not confirm, the conject- 
ure, advanced in the preceding paragraph. 

Another fact has considerable bearing upon the same point. The 
Superior red sandstone, wherever it borders on the trap ridges, shows 
that it has been tilted, broken up or crushed. It therefore appears, 
that the trap, whether erupted, or upheaved convulsively or slowly, 
encountered this formation in its ascent. On the contrary, as we 
have already seen, the Potsdam exhibits undisturbed horizontal bed- 
ding on the trap. One of two things necessarily follows: either the 
Superior red sandstone is older than the Potsdam, or the trap rocks, 
wherever they occur in conjunction with the Superior red sandstone, 
are younger than where they occur in conjunction with the Potsdam. 
The evidence is not conclusive, but it is strongly corroborative. 

Again, it is known that the Superior red sandstone has a much 
greater thickness than the Potsdam. In the region of Montreal river, 
its thickness has been computed at five thousand feet. By trigono- 
metrical calculation, Mr. Sweet has found its thickness to be about 
four thousand feet on the upper St. Croix. The Potsdam in Wiscon- 
sin is not over nine hundred feet thick. . 

Now it is evident that the Superior red sandstone must have been 
much longer in forming than the Potsdam. As the former does not be- 
long to a later period, a portion of it must certainly antedate the latter. 

Awaiting then, a longer and more careful study and more extensive 
and accurate collection of facts, it may be conjectured that the lower 
and thicker portion of the Superior red sandstone is synchronous with 
and the equivalent of the Acadian epoch of Dawson, in the Canadian 
survey, while the upper and thinner portion is synchronous with, and 
the equivalent of the Potsdam sandstone of the New York geologists, 
which is represented over a wide area of Wisconsin. The argument 
from paleontology has no bearing on this difficult question. The red 
sandstone of the Lake Superior region is without organic remains. 
The Potsdam of Wisconsin, while it is rich in fossils, contains no 
species that is identical with any species in the Potsdam of New 
York. The epoch of the formation is determined solely on strati- 
graphical grounds, by its relation to the underlying Archeean, and to 
the overlying Calciferous of the Canadian group, or the Lower Magne- 
sian limestone. 

The journey from the head of St. Croix river to Bayfield confirmed 
. previous information, that the country is covered with drift to such 
an extent as to make satisfactory geological exploration an impossi- 
bility. There is not an outcrop of rocks for fifty miles. Most of the 
region is destitute of living springs and streams. Numerous depres- 


76 GEOLOGICAL SURVEY OF WISCONSIN. 


sions in the drift are partly filled with water, forming lakelets without 
inlet or outlet. Some of these little lakes are large enough to be kept 
pure by the action of the winds and waves. The soil is sandy and 
barren, supporting only a stinted growth of “jack” pines and “ serub 
oaks.” Fire has killed the timber over wide areas, on which grass 
was growing, exhibiting before our eyes nature’s simple method of 
converting woodland into prairie. The reverse process is just as 
simple. When prairies are no longer swept over by fire, timber 
springs up, reconverting prairie into woodland. Grass, with fire as 
an ally, can beat timber. Timber can beat grass when it has no fire 
to fight. 

The same kind of “Jack” pine barrens, interspersed with prairie, 
extends from a short distance above St. Croix Falls to the basin of Lake 
Superior. Along the streams, on the “bottom” lands, there is a 
heavy growth of timber, including white pine, oak, poplar, and maple. 
Towards the sources of the streams flowing into the St. Croix from 
the Wisconsin side, are many fine forests, supplying vast quantities 
of lumber. In the basin of Lake Superior, the soil is fertile, support- 
ing great forests of Norway pine, some white pine, hemlock, maple, 
ete. The agricultural capabilities of the St. Croix valley are not very 
great. The farmer could look to the basin of Lake Superior much 
more hopefully for a reward of industry and enterprise. 

A new geological “section” of the Penokee range was made by the 
party at Penokee Gap, along Bad river, where the Wisconsin Central 
railroad crosses. For a clear description of the structure of this Hu- 
ronian formation, your excellency is referred to the special report of 
Charles E. Wright and the accompanying chart. 

. In the most conclusive manner, the unconformabitity of the overly- 
ing northward dipping Huronian, to the underlying southward dipping 
Laurentian, is made out. 

The undersigned is less reserved than Mr. Wright in expressing an 
opinion as to the value of the iron deposit in the Penokee range. 
Careful chemical analyses of good specimens of magnetic ore show 
that it is very rich in metallic iron, that it is free from titanic acid, 
that it contains very little phosphorus, that silica is not sufficiently 
abundant to seriously interfere with its reduction in the furnace. 

Well selected specimens have shown from sixty to sixty-cight per 
cent. of iron, of fine quality. To scientists it is not necessary to state 
that the richest possible iron ore is a pure magnetite which yields 
seventy-two and forty-one hundredths per cent. of metal. It is sim- 
ply a popular delusion that there are ores rich enough to yield sev- 
enty-five, eighty or eighty-five per cent. of iron, 


ANNUAL REPORT FOR 1875. qT 


It is an important fact, that Mr. Wright found, by microscopic ex- 
amination, the crystalline structure of the Penokee rocks, to be meta- 
morphic and not igneous. His authority on this point is conclusive. 

Whether the Huronian formation of the Penokee mountain extends 
westward to the St. Croix river, is a question of great interest, both 
in the scientific and economic geology of Wisconsin. Awaiting de- 
ductions from more detailed examination to be made by the survey in 
1876, the undersigned may here give the arguments in favor of such 
a conclusion, taken from the report of Mr. Sweet, who has had more 
experience in this part of the state than any other member of the 
geological corps: 

“T. The westward extension, and occurrence on the St. Croix river, 
of all the formations in their regular order, except the horizontal sand- 
stone formed north of the Penokee range, is a strong argument from 
analogy. We can not expect to find as well defined ridges nor as 
high ranges near the St. Croix as there are in the eastern part of Ash- 
land county, for the dip of all the formations gradually decreases to- 
wards the west. The dip of the Huronian schists at the gorge at 
Tyler’s Fork is 75° to the northwest, At Penokee Gap it is 66°, and 
ata point near Atkins Lake only 45° in the same direction, The 
conglomerates and sandstones, which have nearly a vertical dip to the: 
northwest at the mouth of the Montreal river, and the mouth of 
Tyler’s Fork, have but a slight dip on the St. Croix river. At Le- 
high’s on Bad river, the southward dipping sandstones have a dip of 
38° to the southeast; at Wilton’s the dip is 25°; at the St. Croix only 
14° to the southeast. 

“TJ. If the Iron-bearing belt extends westward as far as the St. 
Croix, it doubtless follows the southern boundary of the Cupriferous 
formation. It would, therefore, intersect the river some distance below 
the mouth of Snake river. Then in the neighborhood of a line drawn 
from Snake river to Penokee Gap, one would expect to find indica- 
tions of the formation.” 

Iron ore is reported, by explorers, to have been found in place, at 
several localities in the vicinity of this line. 

Explorers report it from near the southern end of Long Lake, from 
section 18, town 43, range 9 west, and from the northern part of Bur- 
nett county. Near the qoouth of Wood river, on section 19, town 38, 
range 19 west, are found on the original survey Plat the signs used to 
indicate rocks i situ, and the words “iron ore.’ 

“JII, The occurrence of small angular boulders of magnetic rock 
and iron ore, in the drift at numerous localities in Polk and Burnett 


counties,’’ is another strong argument. 


78 GEOLOGICAL SURVEY OF WISCONSIN. 


“TV. In Michigan and in all regions where magnetic iron ore is 
found, much reliance in exploring is placed upon magnetic surveys. 
Valuabie mines have been discovered by noting the abnormal deflec- 
tions of a delicate magnetic needle in passing along at right angles 
to the trend of formations. This method often succeeds, when the 
dip compass fails, Although magnetic surveys have not been made 
in the region under consideration, lineal surveys have, and the varia- 
tion at several points of each section recorded upon the township plats. 

“In the townships through which the Huronian belt would be ex- 
pected to pass, the difference between the maximum and minimum 
deflection to the east is much greater than in townships known to be 
distant from magnetic influences. 

“ For instance, township 37, range 20 west, the difference is 5° 39’, 
and township 36, range 20 west, the difference is 5° 30’. Numerous 
other instances might be mentioned. The fluctuations of the needle 
from a fixed point under ordinary circumstances, is not usually over 
one to two degrees.” 

It is only necessary to add here that the explorations in the Peno- 
kee range for the discovery of iron ore would, in the judgment of 
the undersigned, be more likely to prove successful, if they were 
confined to boring with the diamond drill into the northern brow of 
the mountain at right angles to the dip of the rocks of which the 
formation is composed. The better ores are softer; therefore have 
undergone more denudation than the harder ores; consequently the 
former are buried under surface debris, whilst the latter are exhibited 
in outcrop. By traversing the magnetic schists with the diamond drill, 
the quality of the borings can be constantly tested, and the true hori- 
zon of valuable ores can be accurately ascertained. 

The long journeys down the Chippewa river, from the crossing of the 
Central railroad to Eau Claire, up the Wisconsin river from Wausau 
to the mouth of the Pelican, up the Pelican to its source, and down 
the Wolf from a short distance above Post Lake to Shawano, were 
fertile in negative results, but afforded too few data to determine with 
any degree of accuracy, boundaries between the Huronian and the 
Laurentian formations in the wild Archzean region of the state. Ap- 
parently the Chippewa river traverses an area of Laurentian till it 
touches the Potsdam sandstone in its southeastward course. A Hu- 
ronian range is known to enter the state from the Michigan side, at 
and above the mouth of Pine river on the Menomonee, and to extend 
westward. At Post Lake dam, on the Wolf river, highly crystalline 
hornblende rocks were examined, which, with other indications, led 
to the conjecture, that the Menomonee Huronian range crosses in that 


ANNUAL REPORT FOR 1875. 79 


region. Similar indications were found on Pelican river, and to the 
northwest of Pelican Lake. 

The “Greenstone group” found between Jenny and Grandfather 
Bull Falls on the Wisconsin river, the quartzite near Wausau, and 
the silicious rock of Marshall hill, evidently Huronian, give additional 
points for determining the general direction of the Menomonee range. 
The southwestern termination of it, where it disappears under the 
Potsdam, would seem to be at Black River Falls. Between this 
range and the Penokee mountain range there is probably a nearly con- 
tinuous area of Laurentian. And between the Menomonee Huronian 
range and the irregular line of the northern edge of the Potsdam 
there is a continuous Laurentian belt. 

The geographical boundaries of these formations can only be deter- 
mined by more detailed explorations. 

It is a matter of great practical importance to trace the outlines of 
the Huronian and Laurentian formations in the Archean region of 
the state, for, judging from results obtained from the adjacent region 
of the Upper Peninsula of Michigan where exactly the same forma- 
tions exist, the Laurentian rocks contain no useful minerals, while 
the Huronian areas promise an abundance of iron, if not more pre- 
cious metals. 


Hamitton 0: 2c? —There is a region of Wiscon- 
sin, on the shore of Lake Michigan, beginning in the city of Milwau- 
kee, extending northward to the vicinity of the county line of Ozaukee, 
running inland half a dozen miles, shaped something like a segment 
of a circle, which has been placed by geologists in the Upper Helder- 
berg epoch, and has been called by one scientist in connection with 
the present survey of the state, the Hamilton formation. 

The undersigned, soon after he began studying the geology of Wis- 
consin, was led to doubt whether the region in question belongs to the 
Devonian age, as it must, if it is either Upper Helderberg or Hamil- 
ton. The proper place for a full discussion of the subject will be in 
the final report, after the geological survey of the state is completed. 
Yet it may not be out of place to give here, briefly as may be consist- 
ent with clearness, the reasons which have forced the present head of 
the survey to conclude, against his predecessors, against his associates, 
that the limited area under consideration is Lower Helderberg, and 
consequently belongs to the Upper Silurian and not to the Devonian 
' age. 
In North American Geology, following the nomenclature of Prof. 
Dana and the New York geologists, the proper place of the Lower 


80 : GEOLOGICAL SURVEY OF WISCONSIN. 


Helderberg is above the Salina and below the Oriskany. Of course, 
its stratigraphical relations vary in localities. The normal underlying 
formations will be wanting where, during one or more preceding 
epochs, emergence of the land had taken place and, consequently, the 
ancient ocean, having receded, was not there busy with its work of 
rock-making. 

For the same reason, in many localities, the normally overlying 
series are entirely wanting. The Lower Helderberg, like the rocks of 
any other period, are entirely wanting, where the dry land had ap- 
peared before that particular epoch. Over a large area of Wisconsin, 
for example, there are no rocks above the Archean, for the simple 
reason that this area has been an emerged portion of the continent 
since the primeval ocean first deposited the Laurentian and Huronian 
formations. Nowhere in the state do we find rocks of the Mamma- 
lian, Reptilian, or Carboniferous ages, because during all these long 
divisions of geological time, Wisconsin has been dry land. In other 
places on the globe, the seas have continued their labor of rock-making, 
but here the continent was finished long ago. In places portions of 
the continent have been upheaved during one or more periods, and 
then for a season submerged again by faster or slower subsidence. 
During the period of emergence, rock-making has ceased; with re- 
submergence rock-making has gone on again. Thus epochs are want- 
ing here and there, and the geologist has dynamical problems to solve 
more difficult than problems of lithology. 

The Lower Helderberg epoch takes its name from the Helderberg 
mountains in the state of New York, where the formation is com- 
plete. Beginning from below, its subdivisions are: (1) The Tentacu- 
lite or Water-lime group; (2) The Pentamerus limestone; (8) The 
Catskill or Delthyris shaly limestone; (4) The Encrinal limestone, 
and (5) The Upper Pentamerus limestone. 

In this connection, it is necessary to consider more particularly the 
lowest, or Water-lime division. In fact, the different subdivisions ob- 
served in the Helderberg mountains, scarcely appear outside of New 
York state. All of them but the Water-lime group disappear, even in 
New York, westward of Ontario county. - “This group,” says Mr. 
Vanuxem, in the New York state survey, “takes its name from its 
earthy drab colored limestone, from which all the water-lime in the 
district south of the Erie canal, with one exception, is manufactured. 
It consists generally of dark blue limestone, and usually of two layers 
of drab or water-lime stone; the two always separated by an inter- 
vening mass of blue. The group is well defined, and is readily recog- 
nized in this state and in Pennsylvania, by its mineral nature, its fos- 


ANNUAL REPORT FOR 1876. 81 


sils in particular, and by its position.” Mr. Vanuxem traced it in 
that early date to Fort Plain, Cherry Valley, Richford Springs, vari- 
ous points in Oneida county, Onondaga Valley, Syracuse, Auburn 
and Cayuga Bridge. It must not be forgotten, however, as Sir Wm. 
E. Logan points out (Geology of Canada, p. 363), that Mr. Vanuxem 
confounded this group, in part, with the upper portions of the under- 
lying gypsiferous series, which it closely resembles in lithological 
character. 

The Lower Helderberg formation extends over a wide region of 
North America. Becrafts mountain and Mount Rob, near the city 
of Hudson, are isolated monuments of this geological epoch. The 
formation extends, in a broken way, through Connecticut, Massachu- 
setts, New Hampshire, Maine, New Brunswick and Nova Seotia. 
According to Sir Win. E. Logan, there are outliers of Lower Helder- 
berg at Point Gaspe and near Montreal, at St. Helens Island, at Round 
Island, at Isle Bizard, at cuttings for the Grand Trunk Railway, be- 
tween Point Claire and St. Anne. The distinguished chief of the 
Canadian survey justly remarks (Geology of Canada, p. 358): “From 
these scattering outlying patches, it would appear that a considerable 
area in the Champlain and St. Lawrence valleys was once continuously 
covered with rocks of the Lower Helderberg group; while from the 
unconformable relation of these to the formations on which they 
repose, it is evident that, prior to the Lower Helderberg period, the 
older fossiliferous strata had suffered a great amount of denndation.”’ 

This group extends along the Apalachian mountains southward, 
through southeastern New York, New Jersey, Pennsylvania, Mary- 
land and Virginia. The formation is thicker on the Potomac river 
than on the Hudson. It thins out to the westward in the southern as 
well as in the northern portion of the range. 

The Water-lime division of the Lower Helderberg enters Canada 
opposite to Buffalo, and according to Sir Wm. E. Logan, “ can be traced 
pretty continuously, in a band varying from twenty to forty-five feet 
in thickness.” 

Although this language was used in the Canadian report of 1863, 
yet strangely enough, Mr. Newberry, in the recent Ohio report, says 
that the Water-lime group “had not been recognized beyond the limits 
of New York previous to 1869.” In that year Mr. Newberry dis- 
covered the Water-lime subdivision of the Lower Helderberg on the 
islands in the upper end of Lake Erie, and on the adjacent shore. 
“Since our first identification of the Water-lime,” he says (Geological 
Survey of Ohio, p. 137), “we have traced it over a very large area 
within this state, and have learned to recognize it almost at a glance 

Wis. Sur. —6 


82 GEOLOGICAL SURVEY OF WISCONSIN. 


by its prevailing lithological characters. We have also obtained its 
characteristic fossils from hundreds of localities. The result of our 
investigation has been to show, that the Water-lime, judged by the 
area it occupies, with its outcrops, is, in Ohio, the most important of 
all the Silurian strata. It underlies a broad belt of country on either 
side of the Cincinnati axis, from the lake shore to Hardin county. 
There the two belts coalesce, and the Water-lime stretches entirely 
over the arch, forming the surface rock for nearly a hundred miles 
east and west. Further south the margin of the Water-lime sweeps 
around the blue limestone area, exterior to and parallel with that of 
the Niagara. 

“South of the national road, and east of the anticlinal axis, the 
Water-lime forms a constantly narrowing belt, which passes through 
the counties of Madison, Fayette, Highland and Adams, to the Ohio. 
In parts of Adams and Highland it forms a feather edge on the flanks 
of the Cincinnati arch, beyond which the Huron shales rest directly 
on the Niagara. This shows that the sea in which the Water-lime was 
deposited reached but part way up the slope of the old Silurian 
island.” 

The same formation extends westward into Indiana. In western 
Tennessee it has been recognized in Stewart, Benton, Decatur, Hardin 
and Henry counties. 

Worthen, in the Illinois reports, refers to the Lower Helderberg 
epoch a silicious limestone directly overlying the Cincinnati, with no 
intervention of the Niagara limestone. “No beds of undoubted 
Niagara age,” says Mr. Worthen (Illinois Reports, vol. I., p. 127), 
“were ever deposited in southern Illinois, but in their place these 
silicious limestones, representing in part the age of the Lower Helder- 
berg limestones, and, in part, the Oriskany sandstone of the New 
York series, were deposited, resting directly upon the Cinein- 
nati group of the Lower Silurian.” “Again,” says Mr. Worthen, 
giving an account of the geology of Union county (Illinois Report, 
vol. IIL., p. 36), “ the Lower Helderberg formation is similar in its ap- 
pearance here to the outcrops of it, already described in the foregoing 
report on Alexander county, and it may be described as a thinly bed- 
ded, grayish colored, close-textured, silicions and cherty limestone, 
sometimes argillaceous and shaly, and again so flinty that it is dif- 
ficult to say whether the flint or the limestone predominates.” The 
flinty character of this formation at certain localities in New York 
was fully described by Mr. Vanuxem. 

Following the Lower Helderberg northwestward from Buffalo, 
through Canada, we find rocks with the same lithological characters 


ANNUAL REPORT FOR 1875. 83 


at the junction of Lake Huron and Lake Michigan, occupying the 
entire island of Bois Blanc, occupying most of the small peninsula 
west of St. Martin’s Bay, and skirting the Straits of Mackinac along 
the northern shore of the southern peninsula of Michigan. It over- 
lies the Salina formation, and, consequently, is in the exact strati- 
graphical place of the Lower Helderberg. Speaking of these same 
rocks, Dr. Rominger says (Geological Survey of Michigan, vol. L., p. 
28, of his division of the subject), “Taking into consideration the 
stratigraphical sequence, surmounted above by well characterized’ 
Upper Helderberg strata, underlaid below by beds of perfect litholog- 
ical resemblance to the Onondaga salt group, we may safely take the 
intermediate beds as contemporaneous with the Lower Helderberg 
group.” 

Now the formation, under discussion in the state of Wisconsin, has, 
so far as the underlying strata are concerned, the same stratigraph- 
ical relations as the Water-lime subdivision of the Lower Helderberg in 
New York, Canada, the Appalachian region (and westward to the 
Mississippi river), and on the islands and adjacent shores of Mackinac 
straits. The Salina or Onondaga salt group underlies it here as else- 
where.* 

As an exception to the general statement, if Mr. Worthen is cor- 
rect, not only the Salina, but other formations are wanting below the 
Water-lime in southern Illinois, down to the Cincinnati limestone. 
But in this limited region of Wisconsin, the underlying Salina is 
present, and crops out all around the Water-lime in a narrow cireular 
rim2 The ancient Silurian sea slowly receded from the Archean 
peninsula in northern central Wisconsin, with its outlying islands 
and reefs, depositing in turn the Potsdam sandstone, the Calciferous 
or Lower Magnesian limestone, the St. Peters sandstone, the Trenton 
limestone, the Galena limestone, the Clinton and Niagara groups, the 
Salina, and, finally, at the last point of emergence, the Water-lime base 
of the Lower Helderberg. 

There is a stronger argument from stratigraphy than that of the 
normal relations of the Salina and the Water-lime. 

If the formation in question is Hamilton, then the absence of the 
intermediate strata must be accounted for, and reconciled to the facts 
of local, as well as North American geology. Between the Salina 


1 Recent investigation has shown that the rocks here called Salina are themselves 
probably the Lower Helderberg. T. C. C. 

2Qn the maps published previous to the more careful investigations of the present 
survey,.the formation was represented as here stated, but upon confessedly imperfect 
evidence. It is now shown that this mapping was unwarranted. T. C. C. 


8+ GEOLOGICAL SURVEY OF WISCONSIN. 


and the Hamilton, there are the epochs of the Lower Helderberg and 
the Oriskany in the Upper Silurian age and the Canda-galli, Schoharie, 
Corniferous, and Marcellus epochs in the Lower Devonian age. 

During all that long period, thercfore, while the ancient sea was 
depositing, under different conditions, these half dozen formations, 
the little semi-circular patch of Wisconsin, under discussion, must ’ 
have been dry land, with the Salina for surface rock, and then must 
have become submerged long enough for the deposition of the De- 
vonian Hamilton, again to be emerged at the close of that epoch, and 
remain dry land to the present hour. And this submergence must 
have been just far enough, according to such a hypothesis, to leave at 
every point on its margin a semi-circular rim of Salina. It would be 
impossible to harmonize a supposition of this kind with the known 
facts of rock-structure of surrounding regions, or to make it con- 
sistent with the recognized laws of dynamical geology. It is much 
more rational to suppose that the land was slowly rising; that, con- 
sequently, the Silurian sea was slowly receding; that the last edge to 
emerge was the region in question; that during its own epoch the 
Sabie was deposited; that, emergence still slowly going on, the 
Water-lime of the Lower Helderberg, being next in order of time, 
was laid down over a narrower area, after which the ocean disappeared 
from our shores, leaving the territory where Wisconsin now is, hence- 
forth a part of the abiding continent. 

The paleontological indications for determining the age of the for- 
mation are far less satisfactory than the stratigraphical. There is no 
doubt that these rocks are of the same epoch as those mapped by Mr. 

tominger in the Michigan survey at the Straits of Mackinac as 
Helderberg. He says (p. 28, Paleozoic rocks), speaking of the pale- 
ontological evidence: “ Leperditia alta and Spirifer modestus are 
known as Lower Helderberg species. On such a meagre representa- 
tion of such a rich fauna, I would hesitate to base conclusions regard- 
ing the age of the formation.” Yet, as already stated above, he 
panelides ae stratigraphy that the rocks are Lower Helderberg. 
The undersigned, while investigating the lithological and stratigraph- 
ical characters and relations of the formation, has left mainly to 
others an examination of its fossils. Orthis plicata, Avicula rugosa 
and Tentaculttes, designated by Mr. Vanuxem as characteristic of the 
Water-lime group, have been found by the chief geologist at Humbolt 
Falls. Leperditia alta, a still more important characteristic fossil, 
has also been found. 

The most satisfactory paleontological evidence of this formation is 
Lurypterus remipes, which has not been discovered in the region. 


ANNUAL REPORT FOR 1875. 85 


It is only fair to state that Prof. Chamberlin, of the survey, has 
designated from this region Ichthyolites, Strophodonta demissa, 
Atrypa occidentalis, Spiriferina zigzag, casts of dermal tubercles of 
fish, and other organic remains, which he regards as characteristic of 
the Hamilton epoch; yet he marks a large percentage of these speci- 
mens as questionable, and does not take into account fossils that are 
clearly of the Water-lime period. The paleontological question can 
only be settled by a more careful and ample collection of organic re- 
mains than has hitherto been made, which shall be submitted to Mr. 
Billings, Mr. Meek, or some other great authority in this difficult 
branch of science, who can judge with ample knowledge and without 
prejudice. 

While acknowledging that paleontological evidence is of the highest 
value, and is of itself sufficient to settle the age of a formation, when 
unmistakable and clear, yet we are reminded that the fauna of Paleo- 
zoic time in the northwest differs greatly from the fauna of the same 
time in the east. For example, the Potsdam of Wisconsin, as said 
above, does not contain a single species identical with any species 
found in the same formation in New York. It is necessary to rely 
on the stratigraphical relations for determining its age. . 

The lithological evidence, which, ordinarily, is of the least value, 
and is often of no value at all, may, in this case, be regarded as of 
considerable importance. Prof. Dana’s brief description of the Water- 
lime as “a drab colored or bluish impure limestone, in thin layers,” 
is everywhere characteristic of this formation. Its lithological char- 
acter does not essentially change in different regions, which ordinarily 
makes lithological evidence in geological questions so unreliable. 

The undersigned, coming to the conclusion, mainly on stratigraph- 


1 This remark was probably not intended to convey the full significance which its lan- 
guage might seem to imply, but as it has been retained, it becomes necessary to state 
that it was evidently made under a misapprehension of the character of the fossils in 
question. At Dr. Wight’s request, I furnished him with a box of fossils collected from 
the formation, but as they had not then received systematic investigation, a portion of 
the labels were prudentially marked with an interrogation point in accordance with the 
habit of conscientious investigators, but there were a sufficient number not so marked 
to demonstrate the Hamilton age of the deposit. There were no fossils characteristic 
of the Water-lime period contained in my collection, and it is safe to say that none ex- 
ist in the formation. The entire collection of the survey, which is ample for the deter- 
mination of the age of the rock, has been submitted to Prof. R. P. Whitfield, a most 
eminent authority, who pronounces the fauna distinctively Hamilton, and fully substan- 
tiates the correctness of my position. See page 397. The question of the hydraulic 
properties of the rock, which is independent of its age, frst received my attention about 
one year previous, and would have been discussed in my annual report for that year, but 
for the delay in the analysis of specimens sent to the ¢hemist of the survey for that pur- 


poce, June 12, 1874, T.C.C. 


86 GEOLOGICAL SURVEY OF WISCONSIN. 


ical evidence, that the formation under consideration is the Water-lime 
group of the Lower Helderberg, predicted from the lithological char- 
acters of the rock, that the region would prove rich in hydraulic 
cement. He did not then know that any discovery of the valuable 
commercial properties of the rock had been made. An analysis of 
specimens furnished Prof. Gustavus Bode, chemist of the survey, con- 
firmed the conclusion and the prediction. The state of Wisconsin 
may be congratulated in a discovery that will add greatly to her re- 
sources, to her industry and to her commerce. 

In the meantime, Mr. D. J. Whittemore, E. C., chief engineer of 
the Chicago, Milwaukee and St. Paul Railway, a well known Wiscon- 
sin scientist, had made a long series of careful experiments to test the 
commercial value of the cement rock found in the Water-lime forma- 
tion under consideration. He has demonstrated that it produces a 
cement of better quality, consequently of higher value, than any 
cement now produced, either in America or Europe, except the Port- 


land. 
The following resumé of the results of his experiments has been 


kindly furnished by Mr. Whittemore himself: 


MILWAUKEE, December 23, 1875. 
Dr. 0. W. Wieut, State Geologist of Wisconsin: 

My Dear Sr: In compliance with your request, I herewith make a condensed state- 
ment of the principal results attained in my experimental mquiry as to the value of 
hydraulic cement, made from the recently discovered stone deposit in the vicinity of 
Washington street bridge, near this city. 

For the purpose of comparison, I selected from very many samples of commercial 
cements those that, after a few days’ trial, gave indications of good quality; therefore, 
you will bear in mind, that the average strength of the commercial cement experimented 
upon by me, is considerably above the general average of the cements in our market. 
In both manipulation and testing, I availed myself of every experiment that I could 
well devise to secure uniform treatment throughout my inquiry. 

I converted the natural Milwaukee stone into a cement by the usual method of calcina- 
tion and grinding, and experimented upon the product from single stones separately; 
also upon the mixed products of two stones selected from widely separated localities of 
the ledge, each submitted to varied degrees of torrification in the preparation, and all 
gave very similar results. This determines quite conclusively that within the limits 
hereinafter mentioned the deposit has a uniform character, a matter of much import- 
ance in determining its value. 

My experimental tests were directed to determining the following features, viz. : 

1st. To ascertain the tensile strength in pounds per square inch of mortar, composed 
’ of equal weights of cement and sand, at the age of ninety days, the last eighty-nine in 
water. 

2d. To ascertain the breaking strength of mortars of cement mixed with definite por- 
tions of sand, moulded into bars one inch square, and resting on supports three inches 
apart, and broken by application of weight in the middle. Age of mortars one hundred 
days, the last ninety-nine in water. 

3d. ‘To ascertain the crushing strength in pounds per square inch of mortars of 


ANNUAL REPORT FOR 1875. 87 


cement, mixed with definite portions of sand, at the age of ninety days, the last eighty- 
nine in water. 

4th. To ascertain the adhesive strength, in pounds per square inch of mortars com- 
posed of equal parts of cement and sand, to common brick, at the expiration of seventy 
days. 

The following table is a compilation of the average of all of my determinations, and 
is derived from over fifteen hundred individual tests: 


Tensile Breaking Crushing Adhesive 
Strength. Strength. Strength. Strength. 
Pica ( 
és é 1to1 |2 Cement |1 Cement | 1 Cement | 1 Cement} 1 Cement | 1 Cement 
Sar by and and and an an and 
65g Weight. | 1Sand. | 2Sand. | 1Sand. | 2Sand. | 3Sand. | 1 Sand. 
S) 
Average of Milwau- 
kee Cement....... 290 124 69 2.365 1,451 1,107 TY 
Average of Commer- f 
cial Cement....... 192 80 44 1,477 799 488 4514 


The strengths of the commercial cements are derived from the average of many tests 
of the number of brands represented below. 

For tensile strength, 14 brands of cement. 

For breaking strength, 6 brands of cement. 

For crushing strength, 11 brands of cement. 

For adhesive strength, 9 brands of cement. 

I desire to state that the average results attained by the Milwaukee product exceeded 
the maximum attained by the best of the commercial cements. : 

J have now under examination the product from a section of the Milwaukee ledge 
extending from the surface to a depth of thirteen feet, running through eleven layers, 
and its strength compares very favorably with the former determinations of the Milwau- 
kee cement. 

The rock from which the cement, experimented upon, was made, was selected from 
the banks and bed of Milwaukee river, between the west line of the east half of north- 
‘west quarter of section No. 5, town 7 north, range No. 22 east, and the east and west 
quarter line of section No. 4, same town and range. 

Yours Truly, D. J. Warrremorg, C. E. 


Artesian Wetts.— As an addition to accounts of artesian wells 
given in previous reports, the survey is indebted to the General 
Manager’s office of the Chicago, Milwaukee & St. Paul Railway, for 
the following: 


Dr. O. W. Wiext, State Geologist, 
Sr: I send you below an account of the different strata found in putting down three 


MitwavKeEE, July 6, 1875. 


artesian wells on our lines in this state. Yours Truly, Joun C. Gauur. 
ARTESIAN WELL AT MILWAUKEE. Feet. 
Blaxthh enicccalsvece oie Rusnavecs BU 6H SUE Balas reine Sed ahd eee wits neg emi Gvin gg Ree cetate Ss wees 170 
Lame rock ......:.eeeeeeees a stave ha 6: tye '6 ed ahapaver aj apa gp N Leura eC Terese fiajesahaie 267 
Shale......... scent Bain: Bia 3 58 Be ope a anievaleeesan le dialog oleae aiaieule aes Saleh edness 165 
Second Limestone ..-..--eseeeeeeecveee vg She kaye veleraiate Rina a eave Suto eames 253 
Sandstone full of water ...--.-scececs ecco cece tence ne te eee ne ee terrence 193 


Total depth........++++ Rr et heal ie NG a eas aad chy 1048 


88 GEOLOGICAL SURVEY OF WISCONSIN. 


AT WESTERN UNION JUNCTION. Feet. 
Plan basics ss eles tace) anshee ahe ei aad acalota taco ala a ete aeagte: eas ctasscovennyciaie: “Grenades accede hd tic 147 
Tet LOC ken asedacceraracavetertctaaleteroastemeweratanctethen ea Saistersg doa Siae wae Was Gk Geo ste 233 
EAL Gets cnc tane eaten tal center atercxetarshaecstatas Aah gual giana wie leis tases fever Gere lureracde we roncetieigtas 200 
Tene POC earcinextsiseciausietewerrntauciarsieletsicts Chain be Sn ieee Eee Meyier WeinGeniel ees see 285 
SANSONE aa eeuceyrvedaaanesaKs meas eadseuascrirnine BGuureeno nies areieravalepoays 1400 
Sandy lime sancsvasvewawescsenscenees eee eu esicewsetecearacies welsrsipaniataiaine 141 
Struck St. Peters Sandstone .........eese see reeves Misewaenuntaack waaweante 21106 
Depth of Well nsx seatwecivowessonees’ deisade PEveereUeKE HaemmNONA eee 31263 
AT MADISON. Feet. 
Hath scancsien ca niente es tA SRS OO SRR T TA es BEREAN sed aaRiee eee es 5 
SandstOve-cnscwew sadaaed deeded vareea seein a aeeean a waaadaneieweee ee 525 
Shall @icamarnsrae a sewie easeeGi RAs ANAES SANSA RTT ARSE REID SERS AWE CaN REINS 4 
Secorid, Sandstone «00.01 tc edwwr bowie aii cast nsawtwseeeneaean See eeaeee ; 185 
ra TOK: 5. saisvwaa tase sited de aaeis unRR CONG WEAR AO TD ROR EES ou be aR Bata wes 
Total depth..... ec SOT E MMSGRR OATES RRR Tae Ce er eee 795 


Water does not rise above surface of ground, but it supplies a large pump, without 
any apparent loss of volume. 


Miyerat Sprines.—In addition to the analysis of Wisconsin 
spring waters given in previous reports of the survey, two are especi- 


ally noteworthy. 
Prof. C. F. Chandler, Ph. D., Chemist to the New York School of 


Mines, gives the following analysis of the water of the Beloit Iodo- 


Magnesian springs: 
Grains in 1 gallon. 


Chloride of Sodium............+s000. Se ee re er eee 0.3362 
Bromiderol Sodiiitiv. swcownwsecewenkaee se eawete navaeew eacdreeceine.ciecie oo. trace. 
Todideof Sodus. dsassis nnereunewes swareeedew BERTIE eine e Reewecoaecos 0.0049 
Bi-carbonate- Of S00a: sacsie. neve acese avee rae mawreaaewswdiecicss wet-cueaeaie gees 0.1406 
Bi-carbonate of Macnesiais vsis.ecs vse sea see ries 66 608 de eet oe vende caren oan 12.2803 
Bi-carbonate of Lime............. iA etapa A ieieiaee eral ceive abelian aaa eons 14.5196 
Bi-carbonate of Ir0ninci<isessasanesacskas oes aaderd cevcies a 
Sulplaterot Linens cveee neweisamaweamaraseeust aie seecudwwesewencen aes 
Sulphate of Potash 

Phosphaiteof Sodaiiewiss, wazrosnscegcteesaetenien carerect suasere asavecdiacess eenaowrionro onsen 
ALUMI ae o's 255 x ans Wes satetain ese wes ais ve a Risia eines o.gcsce. nacannresoseunie eiever siete eee « 

DUCA ais arslc:. ae: a wltaisrn wpe wa ny ae BE Ns Sig BLO ior leva vevn sp cdtersubunlavalatavadsiacabonns 

Organic: Matter’ sayes mwienadrs wets isk is dias ciscaeanre doe am odeasioaerwen 


é 


Prof. Gustavus Bode, Chemist to the Wisconsin Geological Survey, 
gives the following analysis of the water of a very remarkable ar- 
tesian well at Sheboygan: 


1 Struck small flow. 
4 Found 15 feet limestone in the eandstone. 
§ Sandstone again to bottom mixed with red rock. 


ANNUAL REPORT FOR 1875, 89 


One gallon, U.S. measure, contains: — 
Grains. 


Total quantity of Salts sirecaiiaae weenie enya veceae ede sd¥arah aadteses 657.8833 


Consisting of: 
Bi- eon of que 


Chloude of hacen EONS HET RoE EE 94 XK Mea ACEG Waepeeen ate Deikow ents ce 
Bromide of Sodium. . 
Iodide of Sodium. . 
Sulphate of Magnesia 
Sulphate of Lime. . 
Chloride of Calcium . 
Sulphate of Iron........ 


AcKNowLEDGMENTS. — The State Geologist has to thank in this 
formal manner, the officers of the Chicago, Milwaukee and St. Paul 
Railway, the officers of the Wisconsin Central Railway, the officers of 
the Wisconsin Valley Railway, the officers of the Chippewa Falls and 
Western Railway, the officers of the West Wisconsin and the North 
Wisconsin Railway, the officers of the Green Bay and Minnesota Rail- 
way, for free transportation of men and materials in behalf of the sur- 
vey. The Wisconsin Central and North Wisconsin have even put 
trains at the disposal of the chief geologist, free of cost, in order to 
facilitate and expediate his work. Such generous liberality cannot be 
too highly praised. Acknowledgments are also due to Captain Knapp, 
in command of a steamboat on the St. Croix river, not only for free 
transportation of the party of reconnoissance, but for services in pro- 
curing proper boats for ascending the river above the falls. Captain 
Vaughan, of Ashland, also laid the survey under especial obligations 
for putting his tug boat at the disposal of the undersigned and his 
party. Hotel keepers everywhere in the state have shown their sub- 
stantial good will to the survey, by keeping men who were working 
in the field at reduced rates. The American Express Company, 
through the friendliness of its general manager in this state, Mr. An- 
tisdel, has carried packages for the survey free of cost. 

In these various ways large expenditures of money have been saved 
to the state, and the chief geologist has been enabled to accomplish 
much more than would otherwise have been possible. The people all 
over the commonwealth have expressed, both verbally and by letter, 
great interest in the survey, and are looking forward with hopefulness 


of results to the time when its final reports shall be published. 
O. W. WIGHT, A. M., M. D., 
Chief Geologist. 


MruwavKeEx, December 30, 1875. 


‘SUOISOUITT UVISOUBBYW! JOMO7T pue SUC SpUeG UIeEpSs}o0g jo uopounl Surmoys 


"SAWV1 N3SZHYHO 'LNIOd SVONT 


PART IL. 


GHOLOG Y 


EASTERN WISCONSIN. 


BY T. C. CHAMBERLIN. 


ACKNOWLEDGMENTS. 


It is fitting that I should acknowledge in a preéminent degree my 
obligations to the lamented Dr: Lapham, under whose direction as 
chief geologist the earlier part of the field work, which forms the ba- 
sis of this report, was performed. In addition to the inestimable value 
of such direction to a young geologist, there was ever at my disposal 
and furnished to my needs, a large fund of information concerning 
local formations and the unwritten history of previous investigations. 
While nothing will be found reported without specific mention that 
has not been a matter of personal observation, it is impossible to dis- 
cern in how far that observation has been enriched by such assistance. 

My acknowledgments are also due to those who have been associa- 
ted with me as assistants during the progress of the work. Of these 
especial mention is to be made of the accurate and efficient aid of Mr. 
L. C. Wooster, who assisted in the field work of each season; of Mr. 
F. Ii. King, who sustained that relation with equal acceptance during 
two seasons, and of Mr. G. D. Swezey, whose botanical observations 
are especially to be noted. Efficient assistance was also rendered for 
shorter periods and special service by Messrs. N. D. Wright, Samuel 
Shaw, S. E. Lathrop, G. L. Merriman, J. H. Chamberlin, and W. C. 
Stevens, and in office work by W. F. Brown, I. M. Buell, C. 8. Bacon, 
C. 8. Douglas, and others. To Prof. R. P. Whitfield I am also in- 
debted for valuable suggestions in relation to paleontological ques- 
tions. . 

For the innumerable courtesies that have been received from citi- 
zens in the prosecution of the work, and that in many instances have 
been of the utmost value, I desire to express my most sincere thanks. 
It would be exceedingly gratifying to me to be able to make specific 
mention of these favors, and such acknowledgment has been made so 
far as possible in the manuscript annual reports, but the list has now 
swollen to such dimensions as to preclude its publication here. A 
very just legal acknowledgment has been made in the provision of the 
law of publication and distribution, which entitles all who have as- 
sisted in the prosecution of the survey to a full set of the reports, and 
the fulfillment of that provision will give me the utmost pleasure. 


EXTENT OF THE DISTRICT. 


The district described in the following chapters consists of the 
counties of Rock, Jefferson, Dodge, Green Lake, except that portion 
lying on the left bank of the Fox river, Winnebago, Outagamie, that 
portion of Waupaca which lies on the left bank of the Wolf river; 
those portions of Shawano and Oconto occupied by Paleozoic rocks, 
and all the counties lying east of these, consisting of Door, Kewau- 
nee, Brown, Calumet, Manitowoc, Sheboygan, Fond du Lac, Wash- 
ington, Ozaukee, Milwaukee, Waukesha, Walworth, Racine and Ke- 
nosha. It constitutes a belt averaging about sixty-five miles in width 
and more than one hundred and eighty in length, the extreme width 
being eighty-one miles, and the extreme length a little over two hun- 
dred. It includes nearly twelve thousand square miles. The area 
lies throughout its entire extent, adjacent to Lake Michigan, and might 
appropriately be termed the Lake Border Region, were it not that it 
includes so large an area whose drainage is tributary to the Mississippi. 


PLATE, I 


Showing the Areas cramined 
by the several parties of the Survey 


FOOO OE KK 


Scale 70 miles=t inch, 


MAP 


1873-1876. 


Lines of reconnotssance 
Boundaries of districts examined 


RTO 


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4 $ = 
So, WE 
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THe Minvarknn Larne & Fac Oa 


PREVIOUS PUBLICATIONS RELATING TO THE REGION. 


The following is a list of all publications relating in any specific 
way to the region, that have come to my knowledge. And as the na- 
ture and limits of this report preclude, for the most part, specific ref- 
erence to the contents of these publications, either in commendation 
or criticism, it is hoped that this mention will be accepted as an ac- 
knowledgment of the credit due their authors: 


Report of a Geological Reconnoissance, made in 1835, from the Seat of Government, by 
Green Bay, in the Wisconsin Territory, to the Couteau de Prairie. By George W. 
Featherstonhaugh, Washington. 1836. 8 vo., pp. 168. 

On the Existence of certain Lacustrine Deposits, in the vicinity of the Great Lakes, usu- 
ally confounded with the Drift. By I. A. Lapham. Am. Jour. of Science, 2d Se- 
ries, vol. 8, p. 90. 1847. 

On the Geology of the Southeast Portion of Wisconsin, not heretofore surveyed. By I. 
A. Lapham. Included in Foster and Whitney’s Report on the Geology of the Lake 
Superior Land District. Part 2d, pp. 167, et seg. Washington. 1852. 

Geological Formations of Wisconsin. ByI.A. Lapham. Transactions of Wisconsin 
State Agricultural Society. Vol. 2d. 1851, pp. 122, et seq. 

A Geological Map of Wisconsin. By I. A. Lapham. 1855. 

Report of a Geological Survey of Wisconsin, Iowa and Minnesota, and a portion of Ne- 
braska. By D.D. Owen. Philadelphia. 1852. The chapters relating to this dis- 
trict are by Col. Whittlesey. 

Annual Report of the Geological Survey of Wisconsin. By James G. Percival. Madi- 
son. 1855. Ditto, 1856. 

Annual Report of the Geological Survey of Wisconsin. By Edward Daniels. Madi- 
son. 1857. 

Report of Progress, on behalf of the Geological Commission of Wisconsin. By James 
Hall. Executive Message and Documents. 1859. 

Descriptions of New Species of Fossils from the Northwestern States. By J. H. McChes- 
ney. Chicago. 1859. 

On Drift Cavities, or Potash Kettles of Wisconsin. By Chas. Whittlesey. Proceedings 
American Association for the Advancement of Science. Vol. 13. p. 297. Spring- 
field. 1860. 

Report of the Superintendent of the Geological Survey of Wisconsin. By James Hall. 
January 1, 1861. Executive Message and Documents. 

Report of the Geological Survey of Wisconsin. Vol. 1. By James Hall. Madison. 
January, 1862. 

On the Fresh Water Glacial Drift of the Northwestem States. By Charles Whittlesey. 
Smithsonian Contributions to Knowledge. Washington. December, 1866. 


96 GEOLUGY OF EASTERN WISCONSIN. 


Geological Survey of Wisconsin. 1859-1863. Paleontology. By James Hall. 

Relations of the Niagara Group. By James Hall. Report of Regents of University of 
New York. 

On Western Boulder Drift. By E. Andrews. American Joumal of Science. Part 2. 
Vol. 48. 1869. 

A New Geological Map of Wisconsin. By I. A. Lapham. Milwaukee. 1869. 

The Glacial Features of Green Bay, of Lake Michigan, with some Observations on a 
Probable Former Outlet of Lake Superior. By N. H. Winchell. American Jour- 
nal of Sciences and Arts. Vol. 2. July, 1871. 

United States Engineers Reports on the Surveys of Fox and Rock Rivers. 

Geological Report of Michigan. 1869-73. Dr. Rominger on Paleozoic Formations. 

Catalogue of Plants Found in the Vicinity of Milwaukee. ByI. A. Lapham. 1838, 
12 mo. pp. 23. 

On the Plants of Wisconsin. By I. A. Lapham. Proceedings American Association for 
Advancement of Science. Vol. 2. 1850. pp. 19. Also published in Transac- 
tions of Wisconsin State Agricultural Society. Vol. 2. 1852, pp. 375, et seq. 

Notes on the Woods of Wisconsin. By P. R. Hoy. Transactions Wisconsin State Ag- 
ricultural Society. Vol. 2. 1852, pp. 419, et seg. 

The Grasses of Wisconsin and the Adjacent States. By I. A. Lapham. Transactions 
Wisconsin State Agricultural Society. Vol. 3. pp. 397, et seq. 

The Forest Trees of Wisconsin. ByI. A. Lapham. Transactions Wisconsin State Ag- 
ricultural Society. Vol. 4, pp. 195, et seq. 

Additions to the Flora of Wisconsin. Transactions Wisconsin State Agricultural So- 
ciety. Vol. 5. 1858, p. 417. Also vol. 6, 1860, p. 258. 

Map of Wisconsin, Iustrating Distribution of Timber, ete. By J. W. Hoyt. Transac- 
tions Wisconsin State Agricultural Society, 1860. 

Fauna of Wisconsm. By I. A. Lapham. Transactions Wisconsin State Agricultural 
Society. Vol. 2. 1852, pp. 237, et seq. 

Notes on the Ornithology of Wisconsin. By P.R. Hoy. Transactions State Agricul- 
tural Society. Vol. 2, 1854, p. 341. Also, the same, with additions in Proceed- 
ings Academy Natural Sciences. Philadelphia. Vol. 6. pp. 304, 381, 425. 1854. 

Quadrupeds of Illinois, Wisconsin, ete. By Robert Kennicott. Patent Office Reports. 
1856, p. 52. 


PLATE, IV 


showing the 
Salient Topographical 
vand. 
Drainage Features 
of 


EASTERN WISCONSIN 
Scale ,35 milessI inde. 


Tuy. Mawar Leto & Exon Ca. 


GEOLOGY OF EASTERN WISCONSIN. 


CHAPTER I. 


TOPOGRAPHY. 


When Eastern Wisconsin first emerged from the ocean, it doubtless 
presented an essentially plane surface, having a slight inclination to 
the east and southeast. The irregularities which it now presents are 
due to subsequent changes, the results of three classes of agents, act- 
ing at different times and under different conditions. 

1. During the long ages between the emergence of the land and the 
drift period, the streams were cutting their beds deeper and deeper 
into the rock, and rendering the former level surface more and more 
irregular. The softer rocks were more readily eroded than the harder 
ones, and this helped to increase the unevenness. There was a ten- 
dency of the streams, as far as the slope favored, to follow the less 
resisting belts of soft rock, and as these run in a northerly aud 
southerly direction in this region, the main streams had that direction. 
The little streams gathered into the larger ones in a manner not un- 
like that by which the branches of a tree are united into the trunk. 
The unevenness of surface produced by erosion of this nature pos- 
sesses a certain kind of system and symmetry readily recognizable. 
As this erosion occupied the time preceding the Glacial period, we 
may conveniently designate the features produced by it Pre-Glacial. 

We have the best example of this kind of surface configuration in 
the Lead region, over which the drift forces did not act, and which 
has not been resubmerged, so that we have the results of this class of 
action pure and simple. As we proceed eastward into the region of 
drift action in the central part of the state, these features arc 
modified more and more by the results of glacial action, until in east- 
ern Wisconsin they become wholly obscured, except in their grander 
outlines. 

Wis. Sur. —7 


98 GEOLOGY OF EASTERN WISCONSIN. 


2. The modifications of the surface constituting this first class of 
topographical features were produced by running water, those of the 
second class, which were produced next in order of time, were formed 
by ice in the form of glaciers, it is confidently believed, and by the 
agencies brought into action through their melting. The work of the 
ice was two-fold: first, in the leveling of the surface by planing down 
the hills and filling up the valleys; and second, in the creation of a 
new uneven surface, by heaping up in an irregular and promiscuous 
manner the clay, sand, gravel and bowlders it had formed, thus giving 
the surface a new aspect. 

Among the features produced by the action of the ice, are parallel 
ridges sometimes miles in length, having the same direction as the ice 
movement, hills of rounded flowing contour sometimes having a lin- 
ear arrangement in the direction of glacial progress, mounds and 
hummocks of drift promiscuously arranged on an otherwise plane 
surface, oval domes of rock (roches moutonées), sharp gravel ridges, 
often having a tortuous serpentine course, transverse to the drift 
movement, peculiar depressions known as “ kettles,’ and half sub- 
merged rock gorges, known as fiords, all of which will be considered 
more fully in describing the minor topographical features of the re- 
gion, and in discussing the Quaternary formations. 

' The melting of the ice mass gave rise to swollen lakes and flooded 

rivers, which eroded at some points and filled up at others, and so 
still farther modified the face of the country. All these peculiarities, 
being the result, directly or indirectly, of the ice action, may be de- 
nominated Glacial features. 

3. Subsequent to the Glacial period, the wearing action of the 
streams was resumed, but under somewhat new conditions. In addi- 
tion to this, there occurred a depression of the land toward the north 
of several hundred feet, attended by an increased volume of water in 
the lakes, by which nearly one-half of the district was submerged. 
The advancing waters of this period leveled down many of the surface 
irregularities, and while the land was submerged the “red clay”? was 
deposited which still further leveled the surface. After the land 
arose again from the water, the streams resumed their cutting, and as 
the clay was soft, they rapidly eroded deep, wide gorges, leaving 
abrupt terraces on either side. The results of the these agencies pro- 
duced peculiarities in the surface contour that may, following out our 
plan, be called Post-Glacial features. 

To the three agencies, lake action, ice and running water, assisted 
slightly by winds, the topographical peculiarities of the district are 
chiefly due. There is no evidence of violent eruptions, upheavals or 


TOPOGRAPHY. 99 


outbursts. There was indeed the gradual elevation and depression of 
the surface and probably some little flexure of the crust, and there 
are at two or three points, indications of faulting; but in general, the 
region has been free from violent agitation, and owes none of its sali- 
ent topographical features to such causes. 

Having thus briefly considered the general methods by which the 
present aspect of the country was produced, we may now more satis- 
factorily examine its special features, and if the reader will have re- 
course to Plate TV of this volume, and, for minor details, to the 
accompanying atlas, it will relieve us mutually of the wearisomeness 
of mere elementary geographical details, while it contributes to a 
clearer and more vivid understanding of the subject. 

No part of Wisconsin can properly be said to be mountainous, nor 
does it, over any considerable area, sink to a dead level. It presents 
the golden mean in a gently undulating diversified surface, readily 
traversible in all directions by the various highways of commu- 
nication. The eastern district under consideration contains the more 
level portions of the state, but presents at the same time much of di- 
versity and many most interesting topographical features. 

Setting aside minor details, the state presents two general slopes, 
a short, abrupt declivity northward to Lake Superior, and a long, 
gentler incline southward. Through the center of this southward 
slope there extends a moderate elevation-—a low anticlinal axis — 
giving a southeasterly and southwesterly inclination to the strata on 
either side. The district under consideration is wholly confiued to 
the southeasterly slope. 

The symmetry and simplicity of this system is however traversed 
in a peculiar manner by @ diagonal valley occupied by Green Bay 
and the Fox and Wisconsin rivers. This feature of the general sur- 
face of the state enters, in an interesting way, into the topography of 
our district, and from its commercial importance demands attention. 
This valley, including its extension into Michigan, is occupied by the 
waters of Green Bay for about one hundred miles, with an average 
breadth of about twelve miles. The bay projects into Wisconsin 
about seventy miles beyond Porte des Morts at the extremity of the 
peninsula, and about forty-five miles beyond the mouth of the Me- 
nomonee river, which forms the state boundary. 

This valley is abruptly limited on the east side by precipitous rocky 
cliffs rising from 100 to 200 feet above the Bay. From the crest of 
these cliffs, the land slopes toward Lake Michigan. On the opposite or 
west side of the valley, the surface rises very gradually for 20 to 30 
miles, beyond which the slope becomes somewhat steeper. The Bay 


100 GEOLOGY OF EASTERN WISCONSIN. 


has a trend of about S. 35° W. Following up the valley in this direc- 
tion, it presents the same characteristics, bounded by an abrupt wall 
of rock on the east, and gently sloping upward to the west. It rises 
somewhat rapidly, so that when Lake Winnebago is reached, an eleva- 
tion of 1694 feet, canal survey, or 162 feet, railroad survey, has been 
attained. This lake strikingly resembles Green Bay in the nature of 
its eastern and western shores. Its trend, however, is nearly due north 
and south, and if we follow on in this new direction, the valley leads 
up over the watershed between the Mississippi and St. Lawrence. ha- 
sins, into the valley of Rock river. This extension of the Green Bay 
valley will be noticed farther on. 

For the present, however, we are considering the diagonal valley — 
the topographical and drainage basin — which has its extension in the 
valley of the Upper Fox river. Like the preceding, this portion of the 
valley has its more abrupt slope on the south side, but this is far less 
conspicuous than before, nor do we find the same broad, level tract on 
the opposite side. These differences are due partly to the fact that 
the valley, in this portion, crosses the geological formations obliquely, 
whereas, in the lower portion, 7¢ followed their trend, and partly to 
the fact that here the drift movement was across the valley from east- 
ward to westward to a considerable extent. This valley undoubtedly 
had an existence before the glacial epoch, and during that period it 
was probably more filled than eroded. 

The Fou river, in this portion of its course, has a much less rapid 
descent than between Lake Winnebago and Green Bay, a circumstance 
greatly favoring its improvement and navigation. The Upper Fox 
descends 40 feet in an air-line distance of about 60 miles, or a little 
more than 100 miles along its meanderings, while the Lower Fox de- 
scends 162 (1694) feet in half that distance. 

The valley leading south from Lake Winnebago, which has been 
alluded to as an extension of the Green Bay valley, and, as will here- 
after be seen, is in many respects entitled to be so considered, rises 
140 feet in 15 miles. These facts, supported as they are by many 
others of similar import, show that the diagonal valley under consid- 
eration is not a fanciful conception, but a well characterized, if not 
obvious, fact. 

The commercial importance of this valley in presenting suitable 
conditions for the establishment of water communication between the 
Mississippi and the great lakes, has awakened a deep interest among 
leading citizens of this and adjoining states, and public attention 
has been so thoroughly turned:toward it, and the prospect of realiza- 
tion is so good, and so immediate, that so far as the people of the state 


TOPOGRAPHY. 101 


are concerned, it would need little discussion here, even if the limits 
of my field comprehended its entire extent and brought the whole 
of the subject under consideration. But it deserves to be here record- 
ed for the information and guidance of capitalists abroad, that for a 
moderate expenditure this remarkable natural feature can be made to 
yield an important avenue of transportation. 

In this connection the attention of capitalists is invited to the facts 
given subsequently in relation to the water power of the Lower Fox 
river, bearing in mind that grain bearing vessels will offer return 
transportation at the most reasonable rates, thus placing manufactur- 
ing establishments in the inost advantageous relation to the thousands 
of miles of rich territory along the Mississippi and its tributaries, and 
the still other thousands of miles of shore line around the great lakes. 
The enterprise for the improvement of this channel of communication, 
under the auspices of the general government, is already (1876) far 
advanced. 

It has been already remarked that the valley from Green Bay to 
Lake Winnebago is exceedingly abrupt on the east, and very slightly. 
ascending on the west. The persistence of this peculiarity for so great: 
a distance points to some general cause. This is readily found in the 
nature of the rock from which the valley was eroded. The strata in 
this portion of the state dip to the eastward. Three groups of beds 
are concerned in the formation of the valley. The uppermost one, 
which forms the cliffs on the east side, consists of hard, thick-bedded 
magnesian limestone, belonging to the Niagara period. Beneath this 
lies a series of clays, soft shales, and limestones, very easily eroded by 
water, forming the Cincinnati group, and below this again is a hard, 
thick-bedded dolomite, known as Galena limestone, which forms the 
bottom of the valley and its western slope, as shown in the accom- 
panying figure : 

Fia. 1. 


. Niagara limestone. 1—2. Green Bay valley. 


oe 


4. Galena limestone. 2. Cincinnati shale. 


Tt becomes evident enough then, from these facts and from an in- 
spection of the valley, that it was formed by the wearing away ot the 
softer strata, leaving the harder ones above projecting in mural cliffs. 
This eroding action is still going on, and to some extent is greatly fa- 


102 GEOLOGY OF EASTERN WISCONSIN 


cilitated by numerous springs that issue from the upper surface of 
the clay and shale, keeping them soft and assisting in wearing them 
down. The dip of the rocks tended to keep the stream hard against 
the soft stratum, and so hastened its removal. 

There is abundant reason for believing that this process had far 
advanced before the glacial period, and had already formed so consid- 
erable a valley as to influence the glacial movement. During the 
latter part of that period, at least, the ice mass moved southward up 
the valley, modifying its sides and polishing its rock bottom in the 
most beautiful manner. Subsequently the valley was partially filled 
with red clay, without however affecting its general features. The 
stratigraphical relations of this valley are then most conspicuous. 
If, keeping this prominently ia mind, we follow up the valley, we are 
led southward from Lake Winnebago to what was formerly Lake 
Horicon, now drained to a marsh, where the head waters of the Rock 
river gather together and flow southward to the Mississippi. We 
have then crossed the watershed between the great St. Lawrence and 
Mississippi basins; and yet on the very divide itself we find the pe- 
culiar character of the valley still conspicuous. The watershed in 
the trough of the valley is, in round numbers, 200 feet above Lake 
Michigan, while on either side the surface rises to more than twice 
that elevation. 

The Horicon basin is only a repetition of that of Lake Winnebago, 
overlooked by the same line of cliffs on the east, and scarcely confined 
by the gentle rise on the west. Descending the Rock river valley, 
these features are still discernible, but become more and more ob- 
secured by the heavy drift accumulation of this region, until in the 
southern tier of counties they are almost entirely concealed by a great 
drift ridge, a glacial moraine, hereafter to be described, which 
stretches entirely across the valley and, combined with other elements, 
gives ita new character. The river has removed from the eastern 
side of the valley to a more central position, and from it there arise 
diversified undulating slopes on either side. 

The course of the Rock river through this valley is interesting and 
for convenience may here be considered, in lieu of its appropriate 
place. From Horicon marsh southward, it follows, as closely as the 
drift accumulations will permit, the ledge of N iagara limestone above 
mentioned until about opposite Oconomowoc, when it turns abruptly 
and flows to the northwest, until it reaches Watertown, where it bends 
again suddenly to the southward and follows this course, bearing 
westward, till it leaves the state. The sigmoid flexure thus formed is 
apparently due to drift accumulations. Were these removed, there is 


TOPOGRAPHY. 103 


little doubt that the stream would follow its course along the strike of 
the formations, at least as far as the moraine in Walworth county, 
Beyond that point the drift is so deep as to preclude any knowledge 
of the configuration of the rock surface. 

It is interesting to notice that this river, which has been following 
the trend of a soft, easily eroded formation —the Cincinnati shale — 
from which it is now forced by drift, passes across the Galena and 
Trenton limestones and makes its bed in the next lower soft forma- 
tion, the friable St. Peters sandstone, which it follows, until it leaves 
the state. . 

Considering the Rock river valley as an extension of that of Green 
Bay, the two forming one great excavated trough, the elevations it 
attains become matters of much geological and commercial import- 
ance. At the north, it finds in Green Bay the level of Lake Michi- 
gan and, as has been previously remarked, rises somewhat rapidly 
about 170 feet to Lake Winnebago. Throughout the length of that, 
lake, a distance of thirty miles, it is essentially level. From its 
southern extremity, the valley again rises about 140 feet to the wat- 
ershed, making its greatest elevation a little over 300 feet.1 The 
former Lake Horicon was 285 feet above Lake Michigan. From this 
point a gentle declivity brings the valley down to 150 feet, at Beloit, 
on the state line. It continues its moderate descent till it joins the 
Mississippi, where it is about 50 feet below Lake Michigan. This 
Illinois extension of the valley differs, however, somewhat widely in 
geological and topographical features from the portion in Wisconsin. 

The commercial importance of the foregoing facts is very consid- 
erable as now realized, but is far greater in its future possibilities. 
It furnishes important facilities for both land and water communica- 
tion. The sagacious proprietors of the Chicago & Northwestern 

' Railway early perceived this and located nearly 200 miles of their 
road in this valley, thus securing an easy grade along a line of im- 
portant towns, supported by an exceedingly rich agricultural region, 
and possessing some of the finest water powers of the interior. 

Water communication is utilized to some extent, but the great pos- 
sibilities in this direction lie yet undeveloped. In the year 1866, a 
survey of this valley from Fond du Lac to the Mississippi was an- 
thorized by the general government and executed by Col. James Wor- 
rall, under the direction of Gen. J. H. Wilson, having for its object 
the determination of the practicability of establishing a capacious 


1 All elevations in this report, unless otherwise designated, signify altitude above Lake 
Michigan, which, awaiting more accurate measurements, is considered 578 feet above 


the ocean. 


104 GEOLOGY OF EASTERN WISCONSIN. 


channel of water communication between the Mississippi and the 
northern lakes. Important facts developed by that survey may be 
found in Ex. Doc. No. 15, of the House of Representatives, 40th 
Congress, and should not be forgotten by an enterprising people. 

Returning from this digression, it is to be remarked that the diag- 
onal valley previously described, and this Rock river, Green Bay val- 
ley, unite at the north and join the great depression occupied by Lake 
Michigan. The bed of this great lake is excavated chiefly from the 
soft rocks of the Devonian age, and has its axis parallel to the strike 
of the formations. The western edge of the lake rests upon the Ni- 
agara dolomites, but the dip of the formation is greater than the 
slope of the lake bed, so that this formation is probably overlaid near 
the western edge of the lake by the upper formations. 

This great submerged valley possesses one of the main features 
that characterize the Green Bay valley, that of having a more abrupt 
slope on the east. At least this is true of the northern portion accord- 
ing to the lake survey charts, for which I am indebted to the kindness 
of Gen. O. B. Comstock. This, however, is not a conspicuous fact, 
and the eastern shore is far from being precipitous. The eastern line 
of Wisconsin would, if traced on the bottom of Lake Michigan, Mie 
almost wholly below the sea level. The extent to which Lake Michi- 
gan occupies the territory of the state and its nearly constant level, 
make its surface our most convenient datum plane in giving elevations 
and discussing topographical features. The clevation of the surface 
of the lake above the sea level, that has been adopted in the progress 
of the survey, is 578 feet. In the report of the survey of Rock river, 
576 feet is given, and Gen. Comstock informs me that the lake survey 
use at present 581 feet above mean tide at New York. The series of 
levels, now being run, will, when completed, give for the first time an 
accurate determination of the level of the great lakes. 

The erosion of the great valleys we have now considered left of 
necessity adjacent slopes and dividing ridges. North of the Fox 
river a very large area is included in a southerly and southeasertly 
incline, the drainage of which is tributary to that river. This is indi- 
cated clearly by the general conrse of the Wolf, Oconto, Peshtigo and 
Menomonee rivers and their branches. On the west side of Rock 
river there is a similar slope tributary to it. But the most conspieu- 
ous elevation in the district is the extensive ridge that lies immedi- 
ately east of the valleys of Green Bay and Rock river, and which has 
already been cursorily mentioned in the descriptions of those valleys. 

A glance at the course of the rivers of this region shows that the 
summit of this elevation is immediately adjacent to the valleys men- 


TOPOGRAPHY. 105 


tioned. Its average elevation above Lake Michigan varies from about 
400 feet, in the south and central portions, to 200 feet, at the north, 
while isolated points considerably exceed these figures. From this 
crest the surface slopes eastward to Lake Michigan, and onward under 
its waters down to and below the sea level. With an unessential ex- 
ception, this slope is everywhere underlaid by the Niagara limestone, 
to the dip of which, and the softness of the underlying shale, the 
ridge owes its origin. Indeed, the ridge is simply the projecting edge 
of the inclined Niagara strata. “At the south, where this eastward 
slope enters the state from Illinois, it is about forty miles wide. It 
retains this amplitude for upwards of 100 miles, extending in an 
almost due north course, beyond which it curves more rapidly to the 
eastward, and gradually narrows till the limiting waters of Lake Mich- 
igan and Green Bay on either side meet and mingle through Porte 
des Morts. But in fact it does not end here. As a submerged ridge 
it extends onward to Michigan, its crest appearing as a line of islands, 
stretching across to the peninsula east of Big Bay de Noquet, which 
presents similar features due to the same cause. 

Without destroying the truth of what has been said of this east- 
ward sloping rock-ridge, the region presents a secondary topographi- 
cal feature of no insignificant importance. 

It consists of a line of immense drift hills, superimposed upon. 
the terrane just described, and known as the Potash Kettle, or Pots 
and Kettles Range. As the term “ Potash” has now no special sig- 
nificance, it will be dropped from this report. At the south these 
drift hills rest directly upon the summit of the rock-ridge, their 
added height reaching an altitude of from 400 to 800 feet above Lake 
Michigan. To the northward, however, the drift moraine has a some- 
what more easterly trend than its indurated companion, and creeps 
down the eastern slope of the latter, until it ends in Kewaunee county, 
midway between the shore of Lake Michigan and the rock-crest that 
overlooks Green Bay. This modifies, somewhat, the simplicity of 
contour that would otherwise be presented, but owing to the great: ir- 
regularity of the drift accumulation, the streams find their way across 
it, and the drainage system of Lake Michigan is uot essentially affect- 
ed by it. In Walworth county a branch from this drift ridge extends 
westward, crossing the Rock river, beyond which it curves to the 
northward, and passes beyond the limits of my district. The effect 
of this upon the features of the Rock river valley has already been 
noted. 

These then are the sakent topographical features of the district, 
the great Lake Michigan basin, the Green Bay valley, with its two- 


106 GEOLOGY OF EASTERN WISCONSIN. 


fold extension in the Upper Fox and Wisconsin river valleys, and in 
the Rock river basin, and their attending slopes and ridges. 

If we descend to minor features, a large number of most interesting 
phenomena will be presented. As these, however, are chiefly due to 
erosion and to drift accumulations, they may most intelligently be 
considered in connection with the drainage system and the glacial for- 
mations. 

Elevations. The following elevations constitute a more specif- 
ic class of topographical data. They will be of great value in mak- 
ing estimates for Artesian wells, a subject which possesses very gieat 
importance in this region, and in locating preliminary lines of rail- 
road, in which respect they have already proved serviceable, and in vari 
ous other ways. The elevations of railroad stations, and in many 
cases of intermediate points on the line, are those furnished me by 
Dr. Lapham, from the railroad surveys. To the same source, also, I 
am indebted for the altitudes of the Oconomowoc lakes, and some 
other points. The elevations along the line of the proposed Chicago 
and Midland railroad are from the survey of Mr. F. J. Starin, who 
kindly placed the profiles at my service, which have proved of much 
use in other ways. Elevations on the Peshtigo river were gener- 
ously furnished by Mr. Paul Wood, civil engineer of the Peshtigo 
Company. A few have also been taken from other trustworthy 
sources. These being the results of actual leveling, by competent en- 
gineers, are a very close approximation to the actual elevations. The 
remainder are the results of observations with aneroid barometers, 
and are liable to more considerable errors, because the nature of the 
instrument does not permit so great precision, and more especially 
because of the fluctuations of the atmosphere, for which, in a series of 
observations made in connection with and subordinate to geological 
field work, it is impossible to make altogether accurate corrections. 
A very large number of observations were made which are not thought 
worthy of publication, because changes in the weather and other cir- 
cumstances rendered them unreliable, and in using those given it will 
be judicious to leave a liberal margin for variation due to changes in 
the pressure of the atmosphere, which could not be detected. The la- 
borious work of reducing the barometrical observations was chiefly 
performed by Messrs, L. C. Wooster, G. D. Swezey, J. H. Chamber- 
lin and C. 8, Bacon. The elevations for Milwaukee county are the 
results of a special and very full series of observations made by Chas. 
Lapham, which the importance of that region, as a railroad center, 
seemed to warrant. 


TOPOGRAPIIY. 


LIST OF ELEVATIONS ABOVE LAKE MICHIGAN. 


(For the clevation above the ocean, add 578 feet.) 


Ahnapee. T. 25, R. 25 E. Feet. 
Sec. 5, S. W. qr., - - 60 
Bank 8. of Ahnay ee, - - 60 
Three miles 8. W. of Ahnapec, - 122 
Angelica. ‘T’. 26, R. 18 E. 
Sec. 33, - - - - 285 
Ashford. T. 13, R. 18 E, 
Sec. 2, N. Line, - - 441 
2. average, - - - 516 
3, R. R. cut, - - 459 
11, N. E. qr., - - 498 
-18, center, - 466 
23, Elmore Village, 421 
23, Surface of Kettle Formation, 444 
24, W. side river, - 322 
Auburn. T. 13, R. 19 E. 
Sec. 8, center N. hf., - - 490 
New Cassel bridge, - - 438 
New Cassel depot, - 466 
Sec. 30, Five Points, - 468 
30, R. R. crossing, 409 
32, 8. E. qr., Milwaukee river, 376 
Avon. . 1, R. 10 E. 
Sec. 5, N. ei qr., - 272 
58.5. qr., stream, 192 
9, 8. W. qr., 320 
LB, - 827 
13, Robie of Gofant,. - 330 
18, 8. E. corner, - - 318 
22) S. W. qr., 245 
25, 5. W. ar., fouge, - 17 
Aztalan.T. 7, R. 14 
Sec. 7, 8. Ww. ar., - - 251 
Ww. Village, - - 276 
18, N. E. qr., - 297 
18, Marsh, 252 
20, 8. E. qr., river bank, - 226 
20, 8. E. gr., water level, 210 
Barton. (See Kewaskum.) 
Beaver Dam. T. 11, R B, 4 Es 
Sec. 2, near mid. W. 277 
~ 2, center 8. E. qr., See 268 
Es N. E. qr., 327 
Beaver Dam Lake, - - 282 
Sec. 7,8. W. qr., marsh, - 284 
8, near center N. W. qr., 300 
10, N. W. ar., ridge, - - 320 
Beaver Dam. T. 12, R. 14 E. 
Beaver Dam Station, - 340 
Sec. 84, mid. 8. E. gr., R. B., 317 
Belgium. T. 12, R. 22 E. 
Sec. 2, N. line, - 145 
3, s line, - - - 145 
10, N. line, - - 145 
10,8. line, - - - 152 
15, N. line, - - 152 
g2, N.line,  - - - 153 
28, N. line, - 156 
33, N. line, Deckers, - - 154 
Bellevue. T. 23, R. 21 E. 
Sec. 15, mid. W. line, - 136 
20, S. E. qr:, stream, - 28 


107 

Beloit. T.1, R. 12 E. Feet. 

Sec. 3, 8. W. ar. of 8. W. qr, 196 

6, near center W. line, 200 

6,8. W. corner, hill, 309 

10, E. line N. E. qr., - 152 

10, N. E. qr., : 180 

10, nent center, - 273 

10, Be E. qr. - 200 

10,8 ‘ line, SE. qr., 302 

17, near center, - - 314 

17, N. W. ar., - - 228 

18, 8. E. corner, - 225 

18, S. line, ee - 260 

19, center W. hf., - 264 

26, N. W. qr., - 193 

27, near center, - 197 

28, mid. 8. line, - 251 

28, Hyde’s place, - 233 

28, Summit, Hyde's, - 275 

9, N. E. qr., creek, 189 

30, 8. E. corner, - 167 

31, center, creek, 144 

33, pe lng, i ii ae 

qz., Hanchett’s quasry, 21: 

BS Be ‘of N, W. qr., 201 

34, mid. W. line, . 236 

35, 8. E. qr., - - 161 

36, near center 8. E. qr., - 176 

8. line College Campus, - 192 

Iodo-Magnesian apg 177 
Bloomfield. _T. 1, R. 18 E. 

Sec. 6, N.hf., 845 

35, N. E. qr., - - 254 

39, 8. E. qr., - - 264 

Genoa Station, - 264 
Bradford. T. 2, R. 14 E. 

5) Hill-W. of Fairchild, - - 325 
Brighton. T. 2, R. 20 E, 

Sec. 18, N. ht. - 250 
Brillion. TT. 20, R. 20 BE. 

Sec. 6, N. E. corner, - - 175 

6, mid. 8. linc 8. E. qr., 211 

7, Forrest Junction, - 250 

15, near mid. W. line, 255 

16, near mid. 8. line - - 249 

18, near mid. N. line, - 250 

13, near mid. 8. line, - 267 

19, mid. 8. line 8. W. q 250 

92° mid. W. line N. We qr, - 250 

23, near 8. W. aaa - 229 

25, W. line, - - «248 

26, mid, N. line N. W. dei, 227 

30, mid. W. ht., - - 230 

31, mid. W. hf... - 238 

Bristol. T.1, R. 21 E. 

Sec. 5, Branch of Eau Pleine, - 149 

Bristol station, - 191 

Sec. 8, N. W. qr., - - 214 

9, center,river, - - 147 

9, W. line, - - - 154 

Woodworth station, - - 170 

Sec. 12, center, - - - 128 


108 


GEOLOGY OF EASTERN WISCONSIN. 


List or ELEVATIONS ABOVE LAKE MicHiGan — continued. 


Bristol. T.1, BR. aL dl — (con-} 
Sec. 19, N. W. 4 

Brookfield. _T. 7 7 20 E. 
Sec. 7, N. 


1L.N.E. oo : 


Brookfield Junc., - 
Elm Grove station, - - 
Burnett. T. 12, R. 15 E. 
Burnett Junc., - - 
Lake Horicon, - - 
Burlington. a 2, R. 19 E. 
Sec. 5, N. E. 
Burlington slatton, = 
Sec. 4, mid. N. line N. E. Wr 
5 mid. 8. line, - 
6 mid. W. line, - 


8, mid. §. line, - 
17, lake, - 
Calamus. T. eve R. 13 B. 
Sec. 6, mid. N. line N. E. ar» 
7 mid. 8. ht., 
Loss Lake, = 
Sec. 18, center N. ie 
18, center, - 
18, near center, - - 
19, near center N. line, 
. W. ar., - 
23) N. i qr., stream, 
a7 N.E E- - - 
21, center hf., awamp, 
1, N. W. corner, 
a S. W. corner, marsh, 
34, N. W. qr., - 
35, 5. W. qr., 
35, 8. W. qr., ridge, - 
Caledonia. T. 4, R. 22 E. 
Sec. 5, Root river, - 


5, near 8. line, - - 
8, mid. 8. line, 
17, mid. 8. line, - - 


20; mid. 8. line §. E. Gy 
Franksville station, - 
Sec. 31, center, - 
33, S. W. qr., railroad, - 
34 E. bf, - 
35, E. ihe valley, - 
—T. 4, R. 2 3, E, 
Sec. 6, 8. lines - - 
a 8. line, - - 


18,8. line, - - 


27,N.E.qr, = : 


Calumet. T. 1% Re 19 E. 
Sec. 26, mid. N. line, - 
98) near W. aa, miei 
35, N. W. g 
Cato. T. 19, R. BE. 
Sec. 1, near mid. E. line, 
1, center Kettle Range, 
i. near mid. W. line, - 


Fet 


230 


Cato. T. 19, R. 22 E. oe 
Sec. 2, near mid. W. lin 
9, mid. N. line 8. E. a» 
Cato Corners, hill, 
Sec. 3,8. W. qr., stream. - 
3) near mid. W. line, 
4, near mid. W. line, - 
5, near mid. W. line, 
5S. W. qr. of N. E. qr., 
. W. qr. of N. E. qr., 
6, 8. E. qr. top of quarry, 
a near mid. W. line, 


7, N. E. qr. LowerCato Falls, 


oe Clark’s mills, river, 

32, mid. I. ht., - 

35, N. W. corner, 

35, center N. E. qr., Kottles, 


Carlton. T. 22, R. 24 BE. 
Sec. 6, E. Twin river - 
6 8. E. qr., Mroinpate river, 
20, mid. 8. linc, 
28, N. E. corner, - 
31, mid. 8, line, creek, - 
33, 8. line, Michicott river 
Casco. T. 24, R. 28 E. 
Casco village - - 
Stream EF. of Casco, - 
Sec. 7, Cowles’ creek, - 


9, - - 

13, mid, W. hf., hill, 

14, E. line, N. E. qr., 

14, near middle, - 
14, 8. E. corner, - 

14, S. W. qr., W. side hill, 
14,5. W. qr., high ridge, 
15, 8. E. qr., ‘stream, - 
16, average Jevel, 

17, level of upland 


Cedarburg. T. 10, R. 21 E. 
Sec. ri N, KE. qr. of N. W. qu., 
4, mid S. line, N. W. qr., 
Mud lake, 
Sec. 6, 8. W. corer, - 

8, N. W. corner - 
Grafton above dam, - 
Grafton station, - 

Sec. 26, mid. W. hf., - 
26, mid. E. line, - 
33) mid. E. line 
33) mid. 8. line, 
Cedarburg station - 
Cedar creek at R. R. bridge, 
Sec. 35, center W. hf., - 
35, N. W. qr., 
35, S. E. qr., - - 
Center. T. 3, R. 11 E. 
Sec. 9, stream and-marsh, 


32, N. E. qr., = - 
33, N. W. comer, - 
Footville-station, - - 


TOPOGRAPHY. 


List or ELEVATIONS ABOVE Lake Micuraan — continued. 


Centerville. T. 17, R. 23E. Feet. 
Sec. 8, mid. N. line - - 64 
3, creek, - 47 
10, near mid, N. line, - 63 
5, N. W. corner, = - - 66 
I Fish creek, - - 30 
1, N. E. corner, - - 60 
an N. E. corner, - 67 
98) center E. line, - 53 
33, N. E. comer, - 61 
Charlestown. T. 18, R. 20 E. 
Chilton station, 269 
Sec. 20, Hayton station, - 249 
Hayton village, stream, - 227 
Sec. 22, E. line (est.), - 242 
Chilton. T. 18, R. 19 E. 
Sec. ae general level, 336 
6, N. W. qr. (est.), 398 
oY mid. N. W. ar. (est.), 392 
98) N. E. qr. (est.), stream 669 
Claybanks. T. 26, R. 26 E. 
Sec. 29, N. E. qr., top of terrace, 87 
29, N. E. qr., bottom of terrace, 12 
Clinton. T. 1, R. 14 E. 
Sec. 2, E. hf, - 370 
2; 8. Ww. qr, - - 852 
9, center, - - 373 
10, N. W.qr., - - 362 
i putin dunenios, - - 364 
8, N. E. qr. 338 
clyman’ oT. 10, R. 15 E. 
Sec. 6, N. W. qr., creek - 227 
18, mid. E. line, marsh, 231 
20, near N. W.-corner, 258 
20, center, N. E. qr. of N. E. qr. 277 
28, Clyman station, - - 330 
Cold Spring. T. 5, R. 15 E. 
Three-qr. miles 8. "of HEDrON. 296 
Bark river marsh, 223 
Cold Spring village, - - 226 
Cold Spring a ‘pond, - 212 
Concord. T.7, R.16 E. 
Concord village, - - 287 
Sec. 30, 324 
Cooperstown. he a1, R. 228. 
Sec. 1,5. W. q 219 
11, mid. S. “ing stream, 184 
93. mid. S. line, - - 240 
24) mid. N. ht., 172 
25, N. E. ar., bottom of ledge, 69 
35, mid. 8. line, outcrop, - 266 
Dale. T. 21, R. 15 E. 
Medina station, - 192 
Darien. T. 2, R. 15 E. 
Sec. 24, S. W. qr., hill - 3898 
28, 8. E. qr., - - 363 
28, Darien station, - 367 
31, mid. E. line, - - 290 
31, 8. W. corner, - 341 
33, W. line, - - 290 
Delafield. T. 7, R. 18 E. 
Lakeside Station, - - - 292 
Pine Lake Station, 350 
Nagowicka Lake, - - - oF 


Pewaukee, - = 


Delavan. T. 2, R. 16 E. 
Sec. 2,8 


17, EK. hf., - - 
17, Delavan Station, 
19, N. W. os, - 
24, hill, - 
De Pere. T. 33, R. a1 E. 
Sec. 26, center N. ht., - 
98) ledge, - - 
Dover. 'T. 3, R. 20. 
See. 13, mid N. line, - 
17, N. W. ar., 
Eagle Lake, - - 
Sec. 25, S. hf., - 
Kansasville Station, - 
Sec. 28, - : 
Dover Station, 
Sec. 33, N. E. qr., - - 
Eagle. T. 5, R. 17 E. 
Sec. 12, near mid. N. line, - 
14, near ef vt corner, - 
14,N.E - - 


19, 8. a 

19, mid. a bai 

99" mid. W. hf, Eagle, - 
22, 


East Troy. | T. qi R. ‘18 E. 
Honey reek, 8. 7 village, 
a 4 18, R. 21 E. 


Eden. a 14, R. 48'E, 
Sec. 6, N. W. corner, 

22) center, - 

22,8. line, - 

24° S. W. ar., - 

25, N. hf., creek, 

25, N. W. qr., - 

97, N. E. ar., river, : 

27, 8. E. qr., 

97. N. line N. E. g 
Egg Harbor. T. 29, R. "36 E. 

1 mile 8. of Ege Harbor, 
Sec. 22, N. wae. 
27, N.W. SOrneN 

27, W. hf., - 

27, 5. W. ar., 

34° N. W. corner, swamp, 
Egg Harbor. T. 30, R. 27 E. 

Sec. 29, N. E. qr., 

Elba. TT. 10, R. 13 E. 
Sec. 1, mid. 8. line, 

6, S. W. corner, Cheeta 
Elba R. R. crossing - 
Sec. 16, N. line N. &. ar., 

16, 8. E. a. R. Rs - 
Danville, - 
Sec.25, 8. W. qr., - 


110 GEOLOGY OF EASTERN WISCONSIN. 


List or ELEVATIONS ABOVE Lake Miciiaan — continued. 


Elba. T. 10, R. 13 E.—(con.) Feet.| Franklin. T. 5, R.21E.—(con.) Feet. 


Sec. 27, N. E. qr., Crawfish, - 232| Franklin Villa 
Ns ge (hotel) 218 
, ’ = » 4N. line, ~ aM 
ime teen © Paw aes 
. 9, R. 15 E. , N. W. qr., brook, - 
Sec. on iad pe ee - - 302 8, near N. W. cor., road, 200 
Rock river N. of Watertown 211 3 cente ee gree oe 
Empire. T.15,R.18E. Smid, We lines. | 199 
Ssc,4, 6, Banner, Z 399 Oe Woe bus Ie 
13, N. W. qr., lowland - 368 a 
Erin. 7.9, RB. 18 B. : Omid. line N.Evar, 208 
See. 1, §. W.ar. of 8. E. qr, 668 Calvin its 
1, 6.0 or, hill : 674 a mad 8 hae Ne WY. 1S 
14, 8. W. corner, « B17 9. NW. adh em 
14; Lapham’s peak, 824 6° N line 8. W. 0 
Farmington. T.7, R. 15 E. 9, center § Wei coe aE 
Joimson’s Greek station, - 193 Sand, Wolo N Ew a 
ec 28, N. E. qr., - i ‘li ‘Ear... $ 
Farmington. |''12, B. 20 E. ast 10 Nine Bo ee Oe 
See, f° Wegk, cota, - 362 voteie i 
OS a oe Sa Oe ee ee 
9, near N. E. corner, 254 10 Ni, We come Wane ae 
a1 'N, E, eoine?, - : 930 10 mid WON. Wig, 13 
37, mid. & line, s ae si ae a fae N. W. qr., 173 
By. Wels. | é 411 10° mid. W. line’'S. W. ne 
83, N. W. comer, —- 277 1 mide Mies a? oe 
Forrest, 7. 15,R. 19 £. iit ie Te ee 
ec, 7, E. hf, Sh ‘ wid. BL line 
ree SP bersan river, be as eh Det line N. W. qr, ra 
9, 8. E. corner, sti 3 Smad. Wine 8 : ‘ 
13, center N. E. a 498 1? ae nN ee 
18, Ele N. Boge, - = 497 12 mid. Ni line N. Wear, 180 
, near E. - - id. N. Ii “hE NW 
eS 45 12, maid. N. line W. hf, N.W.gr., 199 
16, N. E. ar., ‘ 389 ied Wine WR * 8 
24, center Nhe, = - - 494 Teaith Wr line ee iB 
5, dy Woogr., si ye 5 2! anid N. Ime. F 
eee ar Wea é : a i oe N. line N. W. aqr., 158 
Forrestville. T. 26, R.¥ E. id anid, 3 lene & a 
Sec. Mi, mid, E. line 8. W. qr. 170 id aad The Nereis 38 
NE. nee ’ : y mid. NN. line, = : 
32) mid. ine (D : ne ve m4 N. line N. W. qr... 9 1d 
Fox Lake. T. 13, R. 15 E, NW be 
Binily Take, 2 <a ia WwW. corner, - 138 
. Bee, A mid line, : : a iy N ce Root river, 105 
4, mid. 8. line, 346 Te ee apes a 
a Teed Fe Bi me N. line N. W. ar., 182 
NW ae, 3 Ph i nm .N. line W. hf. N.W. qr.. 141 
17,8.Eear.” 293 ia wee 7 ie 
31; N. W. gr. of N. W. ar. 77 5 iid We line. 2 
al mid Weling NW oe’ = Bab Catto ee 
31,8.W.ar,  - - 881 ae i aa ee 
Franklin. T. 5, B21 E. aids Wee ae 
Sec, 3, N. line N. E. qr., - o BS Ceci ee Be 
3, angle, Loomis rd., E. of riv., 133 17. ond, NW, line.” a 
3, Root river, Loomis rd., 118 Ve det, Loomis Tpsdllin dae oe 
ow ieee in 1a ig ee & Franklin rds., 215 
3, W. line 8. W. qr, - 190 18’ N ln Roane ae 
4, Th wi corner, - 130 18, N. hc, ae a 
5,N. W. corner, — - 205 .W. lin i 4 
es a ae angle of rd., - 230 20 Ne oe et 0) 
ie 5) SA Yr ’ 2: 
,N. line, onrd, - 235 20, W. line, Loomis road, 206 


TOPOGRAPHY, 


List or ELevatTions ABovE LAKE MrcurGan — continued. 
Franklin. T.5, R. 21 E. 7m) Feet. 


Sec. 22, mid. W. line S. W. 
22, N. W. corner, - - 
29; W. line near N. W. cor., 


99} mid, W. line N. W. ar, - 
99° mid. W. line, 
95, mid. N. line N. E. qr, + 
25, mid. N. line, - 
25, mid, N. line N. W. ar, - 
25, N. W. corner, 
26, mid. N. line N. E. ar. - 
26, mid. N. line, - 


26, mid. N. line N. W. qr, - 
26, N. W. corner, 
27, N. line, Root river, - 
27, mid. N. line, - 
27, mid. N. line N. W. cay 
27, N. W. corner, 
27, mid. W. line N. W. ary 
27, mid. W. line, 
27, mid. W. line S. W. » 
28) N. W. corner, 
29, mid. W. line N. W. ay = 
29, N. W. corner, 
30, mid. N. line N. E. qr, - 
30, mid. N. line, - 
34, mid. N. line N. BE. qr, - 
34, N. line, Root iver, 
34 mid. N. line, - 
34, N. W. corner, 
35, mid. N. line N. E. a - 
35, mid. N. line, - 
35, mid, N. line N. W. a.» 
35, N. W. corner, ‘ 
36, mid. N. line N. KE. a, 
36, mid. N. line, - 
36, mid. N. line N. W. qr., 
36, N. W. commer, - 

Franklin. T. 20, R. 22 E. 

Sec. 1,5. W. one 


2 latest ne of Kettle range, 


- qr. sa 
19; mid, W. line, - 


Franklin. T. 22, ae 
Sec. 11, N. W. - 
Lb, center N. a qr., 
22,8. line 8. E. qr, - 
34, N. W. corner, creck, - 
34, 8. W. corner, - 
34, 8. E. qr., creek, - 
Fredonia. T. 12, R. 21 E. 
Sec. 1, N. E. corner, - 
12,8. E. comer, - - 
ns - - 
25, 8. E. corner - 
28, Waubakee_ village, - 
29, Quarry on N. side river, 
33) Milwaukee River, - 
35, S. linc S. W. qr., BR. B., 
Fredonia Station, - : - 
Fulton. T. 4, R. 12 E. 
' Newville Bridge, - - 


182 
175 
170 


112 

Fulton. T. 4, R. 12 E. (cou) Feet. 

Edgerton Station, - 242, 

Sec. 8, center N. line, - 251 

4, center N. hf., - 232 

5 center 8. line, - - 273 

5 8. line 8. E. qr., - 284 

6, N. W. ar., - - 240 

10,8. W.gr., — - - 219 
Geneva. T. 2, R.17E. 

Sec. 2,8. E. qr., - - 436 

5, 8. hf. 29. = - 445 

6, mid. K. line, - 415 

6, Elkhorn Station, - - 415 

9, center E. hf, - - 4u2 

a aie E. line, R. R., - 406 

oe - 418 

10 ae E ne, - 400 

10, near center, - - 423 

10, W.hf,  - - - 415 

ig N. W. corner, - 337 

14, near center, - 342 

, o. bf, - - 277 

25, W. line, - 333 

34, mid. E. line, - - 345 

36, Geneva Station, - 300 

Lake Geneva, - 282 
Genesee. T. 6, R. 18 E. 

Genesee Station, - - 825 

Saysville Mill Pond, - - 232 

Sec. 13, N. line, - - 827 

14, 8. W. qr., - 313 

15, mid. §. line, - 329 

21, N. E. qr., creek, 315 

21) mid. 8. line, - 331 

21, hill, - 350. 

25, mid. N. E. qr., 228 

25, center 8. W. qr., 225 

29,8. E.corner, - 359 

31, North Prairie Staton - 3863 

35, mid. §. line N. W. qr., 367 

Germantown. T. ae R. 20 E. 

Sec. 5, N. line, R. R., - 278 

6, N. E.qr., - 289 

9, N. line, R. R., - 313 

10, N. W. corner, - - 276 

10, center 8. hf., 297 

15, 8. E. qr., Menomonee River, 273 

16, W. line, 35 298 

1s, mid. line, R.R., - 318 

47, W. line, R. R., - 828 

18, W. line, R. RK. - 360 

21, N. line, R. R., - 286 

22, W. line, R. R., - 273 

22, center, - 275 

23, N. W. ar., RB. 301 

93) W. line, B. R., 295 

23) mid. S. line, R. R., - 293 

25, 8. line, R RR 248 

95, W. line, R. R.,  - - 278 

26, 8. E. qr. - - 813 

28, mid. N. line, 286 

30, mid. E. line, 8. E. qr., 276 

32; N.W. comer, - - 296. 

32) center, * - 284 

35, 8. W. comer, - - 319 


112 


List oF ELEVATIONS ABOVE 
Germantown. T.9, R. 20 E. —(con.) wee, 


GEOLOGY OF EASTERN WISCONSIN. 


Late MicHican — continued. 


Granville. T. 8, R 21 E. —(con.) Feet. 
Sec. 15, N. line R. R., - I 


Sec. 35, center 8. W. qr., - 9 

35, near S. W. corner, 314 

35, mid. 8. line 8. W. sy 270 

36, 8. line, R. R., - 198 

6, 8. E. corner, R. R, - 193 

36, center 8. W. qr., - - 195 
Gibson. T. 21, R. 3k 

Sec. 1 N. tine N. E. ar., - 63 

7, mid. N. Pa - - 96 

9, N. E. q - 160 

21; ee We. corner, 174 

ot E. line 8. E. qr., - 83 

26, : W. qr., Jambo Creek, 49 
Gillette. T. 28, aR 19 E. 

Sec. 1, Little River, - 164 

25, Oconto River above the falls, 132 
Grafton. T. 10, R. 22 E. 

Sec. 5, mid. N. ht., - 174 

8 S. line, R. K, - - 117 

9, near center S. hf., - il 

19, N. fs Gre Cae W. qr., 211 

20, mid R. R., 119 

20, mid. Eline N.E. qr., 150 

20, bank Lake Michigan, 119 

20, S. line, R. R., 130 

29° 8. line, R. RB. - - 96 

32, 8. line, R. - 97 
Granville. T. 8, R. 21 E. 

Sec. 1, mid. N. line, - 68 

1 N. line, river . - 06 

2, N. line, Cedarburg P. Road, 68 

2, mid. N. line, R. R., 83 

2, N. W. corner, - 89 

2, 8. E. qr. brook - - 74 

3, mid. N. line, - 15 

3, N. W. corner, = - 87 

4, mid. N. line, - - 100 

4, N. W. comer, - - 143 

5, N. W. corner, - 145 

6, mid. N. line, - 190 

6, Wetne Oe M. & St. P. R.R. 190 

6, mid. W. line, - 173 

6, N. line 8. W. ar. B. R. 186 

7, N.lne R. R. 169 

7. mid. N. line, 206 

7, N. W. corner, 169 

8, mid. N. line, - - 165 

8, W. line, Granville, - 167 

8, mid. W. line, - 184 

9, mid. N. line, - 125 

9, N. W. comer, - - 179 

10, mid. N. line, - 84 

10, mid. N. line, N. W. qr. 122 

10, . corner, 98 

10, Whittaker’s house, - 103 

11, N. line R. R. - 85 

11, mid. N. line, - - 79 

11, N. W. corner, 77 

12, N. line river, - - 54 

12, N. W. corner, 89 

13, N. W. corner, = - - 123 

13, mid. W. line, 166 

14, mid. N. line, - 99 

14, N. W. corner, - 119 


15, N. W. corner, 7 
16, mid. N. line, - 

16, N. W. corner, - 
17, N. line R.R., - 

17, mid. N. line, - 
17, N. W. corner, _- 

19, mid. N. line, N. E. qr., 
19, mid. N. line, - 

19, mid. W. line, N. E. qr., 
19, center, 


212 
190 


20, N. E. corner,water in E. br., 124 


20, mid. N. line, N. E. qr., 
20, mid. N. line, 

20, N. W. corner, 

21, N. line, M. & St. P.R. R. 
21, mid. N. line, 

21, N. W. corner, 

22, mid. N. line, - - 
22, N. W. corner, - 

22, center R. R., 

23, mid. N. line, 

23, mid. N. line N. W. qr., 
23, N. W. commer, 


160 
1 


115 
145 
135 


94° mid. N. line B. qr. N. E.ar. 135 


24, mid. N. line, N. E. qr.. 
24, N. line W.C. R.R., 
24, N. W. corner, 

24, W. line R.R.,  - 

24, N. line S. E. qr. R. R., 
24, mid. W. line 8. W. gqr., 
25, N. W. corner, - 
25, N. line R. R., 

25, mid. W. line, - 
25, N. line, - 

25 N. line N. W. R. R. bs 
25. mid. N. line, - 

25, mid. N. line N. W. qr., 
26, mid. N. lne N. E. ce 
26, mid. N. line, 

26, W. line 8. E. qr. R. R, 
27. N. W. corner, 

27, mid. N. line N. E. qr. 


97, mid. N. line W. hf. N. E.ar. 


27, mid. N. line, 

27, N. W. corner, 

98, mid. N. ges E. ar» 
98) mid. N. lin 

3) N. W. Soe 

99) 200 ft. W. N. E. corner, 


29, N. line, N. F. du Lac Rid, 


nd 
SOS 


mid. N. line, 

29, N. W. comer, 

30, mid. N. hne, 7 
30, mid. N. line N. W. qr., 
30, N. W. corner, - 
30, center, 

31, N. line, E. branch, 

31, mid. N. line 

31, mid. N. line N. E. ey 
31, N. W. comer, 

31, center, - 

31, mid. W. line S. E. a+, 
32, mid. N. line, - 


98 
112 


TOPOGRAPHY. 113 


List or ELEVATIONS ABovE Lake Micuican — continued. 


Granville. 
Sec. 33, mid. N. line e, 
33, mid. W. line, - 
33, center N. E. qr., - - 
34, mid. N. line N. E. qr., 
34, mid, N. line, - 
34, N. W. corner, - 
34, mid. W. line, - 
35, N. line R. R., 
35, mid. N. line, - 
35, N. W. corner, - 
36, N. lime W.C. R. R., 
6, N. W. corner, - 
W.lineR.R., - 


mid, N. line S. E. qr. R. R., 


3 ’ 
36, 
36, mid, N. line W. hf. 8. W. qr. 94 
a 58 


T. 8, R. 21 E.—(con.) ea 


8. E. qr., eeinarnonre Bt n, 66 


3 
Green Bay. T. 24, R 
Sec. 13. mid. 8. line, 
Le Outerop, - 
22, ae a near Franken, 
— T. 25, R. 22 E. 
Whitney s Bluff, - 
Sec. 16, On bluff, - - 
Greenbush. T. 1, R. 20 
Glenbulah Station, - 
Sec. 4, center, - - 
St. Cloud Station, - 
Sec. 6, N. E. corner, 
10, center, 
35, mid. W. line, plateau, 
36, center summit of ridge, 
36, near center, road, = 
Greenbush hotel, - - 
stream, 
Hill 8. of Greenbush, - 
Greenfield. T. 6, R. 21 E. 
Sec. 1, mid. Ww. line, 


By N. of center, ened. - 
By N, line, Mnekwonago road, 


Oe 


ar center, Poplar creek, 
nter, 


nter 8. W. ar - 


id. si ‘line, - - 
. W. corner, - 

id. N. line, - - 
. W. corner, 

id. W. line N. W. ar. pt oie 
id. W. line, 

. W. corner, - 


a 
SB 


~ 


$9 D> PP SLIUE, 
cee sl 


eA 


id. W. line N. Ww. es - 


E. 
BSE: 
< 
EF 
& 


WANA AIIAMD AHP AON 
BE 


d 
id. line 8. E. qr.,  - 
. line, Muckwonago road, 
id. W. line N. EB. qn, - 
line 8. E. qr., - 


& 90.90. 
e ae 


x N. W. cor., Root river, 


Greenfield. T.5, R. 21 E.—(con.) Feet. 
Sec. 8, W.lineS. E. qr. Muckw’ 'goR., 170 
"1738 


8, center N. W. qr., 


9, N. W. corner, - 200 
9; N. line §. E. qr., 141 
10, mid. N. line, - 135 
11, N. line N. E. qr. R. R., 90 
11, N. W. corner, - 112 
11, mid. W. line N. W. qr., 127 
WH mid. W. lme, - - 102 


aN mid. W. line 8. W. qr., 125 
12 center, - 84 
12 S. W. qr., Janesville road, 54 
13, mid. N. line N.E. qr. - 55 
13, mid. N. line, 90 
13, mid. N. line N. W. ar., 106 
18, mid. W. line N. W. qr., 93 


13, N. W. corner, 124 
13, mid. W. line, 119 
18, mid. W. line 8. W. qr., - 146 
13, S. line, Loomis road, - 137 
14, mid. N. line N. E. qr. - 137 
14, mid. N. line, - 158 
14, mid. N. line N. W. ar., - 170 
14, N. line R. R. grade, - 146 
14, N. W. corner, - 140 
14, mid. W. line, 92 


1 
14, W.line 8. W.ar., Janesville R. 202 
14, N. E. qr., Janesville road, 177 
14, 8. W. qr., Janesville road, i 
15, mid. N. line N. E. ar, ae 
15, mid. N. line W. hf. N.'E. qr., ce 
15, mid. N. line, 


Lb, mid. N, line N. W. qr., 140 
1, N. W. corner, - 145 
15, N. lime N. W. qr., Brook, 140 
16, mid. N. line N. . qr., 155 
16, mid. N. line, 170 
16, mid, N. line N. W. qr., 200 
16, W. line, Beloit road, - 225 
16, mid. W. line 8. W. qr., 183 
16, mid. W. line 8. E. qr., 215 
16, center, - 209 
16, mid. W. line N. E. ar, 183 
17, mid, N. line N. E. qr., 210 
17, center, 200 


17, 8. W. qr., angle Beloit road, 190 
17, W. line, Beloit road, 180 
18, N. line, Root river, - 149 
18, mid. N. line E. ht. N.W. qr., 156 
18, mid. N. line N. W.qr., - 161 


18, N. W. comer, - 193 
18, mid. W. line N. W. ar., - 212 
18, mid. W. line, 182 
18, mid. W. line 8. W. q. 212 


18, mid. W. line §. hf. gw. qr. ae 
19, N. line, Root river, - 

19, mid. N. line N. E. qr., 170 
19, mid. N. line, - - 230 
19, mid. N. line N, W. qr, an 
19, N. W. corner, - 214 
19, mid. W. line N. W. qr., 244 
19, mid. W. line, - 255 
19, W. linc 8. W. qr., Beloit road, 245 
20, mid. N. line 8. E. qr, - 178 


114 


GEOLOGY OF EASTERN WISCONSIN. 


List oF ELEVATIONS ABOVE LaKE Micuiean — continued. 


Greenfield. T. 6, R. 21 E. — (con.) Feet. 
Sec. 20, center, 159 
20, mid. line, Root river, - 148 

a1, inid. N. line N. E. qr., 217 

21, mid. N. line, - 221 

21, N. W. corner, . 180 

on; mid. W. line, - - 180 

on; mid. N. line 8. W. ar., 210 
On, center, - 240 

22) mid. N. line N. E. ar., . 174 

22? N. line N.E, qr., R.R. bridge, 172 

99° mid. N. line, - - 185 

99° mid. N. line N. W. qr., 199 

99° N. W. corner, 188 

99° mid. W. line, 220 

92) W. line, Janesville road, - 244 

29, center 8. W. qr., R. BR., 240 


22, N. line S.W.ar., i anesville R.., 200 


23, mid. N. line N. E. qr, 179 
23, mid. N. line, - ° 165 
93, mid. N. line N. W. o-, 181 
93) N. W. corner, 192 
23, mid. W. line N. W. as, 187 
23, mid. W. line, 180 
23, md. W. line S. W. qr., 196 
o4 N. line, Loomis road, 137 
24° N. W. corner, - - 137 
94, mid. W, line 8. av qr., 170 
24) N. line, 8. W. qi - 122 
94, W. line, N. oe tohs Loomis’ 
Roa d, 117 
26, N. line, Loomis’ Road, 180 
26, N. W. corner, - - 193 


26, mid. W. line, N. hf. N. W. qr..232 
26, mid. W. line, N. W. qr., - 220 


26, mid. W. line, - 227 
26) mid. W. line, 8. W.ar., 223 
26, center 8. W. qr., - 210 
26, center, - - 186 
26, N. E. qr., brook, - 160 
27, N. W. qr., R. R. grade, 195 
98° N. line N. E. qr., Janes- 
ville Road, 198 
28, N. W. corner, . 157 
98) W. line 8. W. qr., Root R., 141 
99° 8.E. qr., Janesville road, 199 
30, N. W. corner, 265 
30, mid. W. line N. W. qr., 254 
30, mid, W. line - - 234 


30, mid. W. line 8. W. qr., 229 
31, N. W. corner, - - 


31, center W. hf.N. W.qr., 233 
31, N. line 8. W. qr, Tall 212 
31, center brook, - 192 
31, mid. N. hf. 8. E. qr., - 192 


32, N. line N. E. qr., Janesville 


road, 224 
32, Hale’s ‘Corners, 211 
382, mid. W. line 8. W. qr., 195 


33, N. lne N. E. qr., Root R. 128 


33, mid. N. line, R. R., - 13% 
33, mid. N. line N. W. qr., 157 
33) N. W. corner, - 171 
34° mid. N. line N. E. qr. 152 
34, mid. N. line, - : 192 


Greenfield. 
Sec. 34, mid. N. line N. W. Gees * 
34, N. W. corner, 
34, near 8. line, Loomis ncaa, 
35, N. line, Loomis road, 
35, N. W. comer, - 
35, mid. W. line N. W. qr., 
35, N. Ww. ats pond, 
Harmony, T.3 a R.13E. 
Sec. 2, N. W. - - 
Hartford. _T. ib, "R. 18 E. 
Hartford Station, - - - 
Sec. 1, near N. W. corner, 
13, near 8. E. corner, stream, 
13, center, R. R., 
13, W. line, R. R., - - 
14, center, R. R., - 
14, Ww. line, R. R., - 
16, N. E. corner, - 
16, center E. hf., - - 
17, W. line, R. R, - 
18, center, R. R., - = 
12, W. line, R. R., 
21, center, R. R., - 
21, W. line, RR, - 
92° center, R. R., - 
92) W. line, R. R., - 
ce little W. of mid. of B. line, 


Hartland. T. 26, R. 17 E. 
Sec. 21, Hartland, - 
Hebron. T. 6, RB. 15 E. 
Cushman’s mill pond, - - 
Herman. T. 16, R. 29’E, 
Sec. 11, N. E. corner, 
12, mid. N. line, N. E.qr., - 
1, mid. 8. line, - 
26) near 8. line, stream, - 
26; 8. E. qr., aaa 
Holland. T. 13, R 
Sec. 1, N. ine iam - 
12 N. line R. B., - 
13, N. line R. B., - - 
16, 8. E. qr., bridge, - 
24" N. Jine R. R., - - 
95, N. line R. R. - 
26, Cedar Grove,’ - 
29; Ww. 


36, center E. line, 


Top of ‘terrace above Amsterdam, R. 


Bottom of — above Amster- 


dam, It. 
Holland. T. 21, "R. 20 E. 
See. 20, 8. E. qi - 
20, 8. Wea - 
Jackson. T. 10, ee 20 EB, 
Sec. 1, 30 rods W, of 8. E. Sommer, 
1; mid. 8. line, creek, 
1, Lee of creek, - 
‘is mid. 8. line S. E. qr., - 
6, center, R.R., - 
iN. line, R. B., - 
7, N. E. qr. - - 


T. 6, R. 21 E.—(con.) Feet. 


180 
156 


TOPOGRAPHY. 


List of ELEVATIONS ABOVE 


Jackson. T. 10, R. 20 E.—(con.) Feet. 
Sec. 7, mid_S. line S.W. qr., valley, oe 


30, N.E. qr., eae creek, 
ai mid. 8. line, - 

32; 8. E. qr., F itosls - 
32) N. W. commer, R. R., 


32, mid. N. line N. W.'ar., - 


33, mid. N. line N. E. qr, 

34, N. W. corner, - 

34 8. W. corner, - 

36, 8. E. qr, - - 

36, 8. W.qr,  - - 

Jacksonport. T. 29, R. 27 E. 

Ridge S. of Jacksonport, 
Racine Limestone, 


Coral beds hf. mile 8. of J acksonport, 


Sec. 33, S. hf. 

Janesville. T.3 R. 12 E. 
Janesville Fair Grounds, 
Janesville Station, - 

Jefferson. T. 6, R. 14 E. 
Jefferson station, 

Rock river at Ji efferson, - 

Mouth of Crawfish river, 

Sec. 9, 8S. E. qr., stream, - 
12; N. E. qr., hill, - 


15, near center W. hf., stream, 


fells = ar., 

17. qr., quarry, - 
18, center W. hf., nll, 
19, near N. W. corner, 

Johnstown. T. 3, BR. 14 E. 


Level of Rock Prairie, - 
Kewaskum. T. 12, R. 19 E. 
Sec. 5, N. line, R. R., 


20, ‘mid. E. line, stream, 
99° S. W. qr., R. R., 
29° mid. N. line, 
28, near mid. N. line, 
aN W. corner, - 
E. corner, - 
ve N.E. -, R.R., - 
35, R. B. - 
Kewaunee. Re 23, R. 24 E. 
Sec. 5, N. W. ar., ledge, 


14, Kewaunee ‘river at bridge, 


14, 8. W. qr., junction of 
Coral and Racine, 
20, mid. N. line, - 
26, Est., ere level, 
30, mid. SiG 
a, pele - 
31, N soak 
Koshkonong. 5, R. 14. 
Fort Atkinson station, 
Marsh below Fort Atkinson, 
Lake Koshkonong, 
Kump’s quarry, 
Sec. a center W. hf., - 
27,8. W. ar., 
31, N. E. a - 
34, N. E. g 
32, center N ‘hf. , valley, 


pper 


319 
273 
276 
327 
340 
300 
273 
208 
004 


Lake MIcnrGan — continued. 


Kossuth. T. 20, R. 23 E. 
Sec. 12, E. line | 8. E. qr, river, 


26, 8. E comer, 
36, S. E. q - 
La Fayette. 1 "3, R.17 E. 
Sec. 8, near center, stream, 


19, N. E. qr., 5 


31, N. E. qr., - 
31, 8. W. qr. 
La Grange. T. 4, R. 16 E. 
Sec. 1, nearly S. of hil. 
Heart’ Prairie, - 
Lake. T. 6, R, 22 E. 
Sec. 7, mid. N. line, - 
7, mid. N.line, N. W. a, 
7 mid. W. line, - 
i, mid. W. lhe, Ss. W. ar, 
7. mid. N. line, S. W. ar., 
7, W. of center, 
ts N. of center, 
i, center, N. Eq 
‘ae highest land i a ns 
8; . E. corner, 
8) mid, 8. line,’S. E. qr., 
cy N. W. corner, - 


8, W. line, Kinnickinie, 

3 mid. W. line, - 

8 mid. W. line, S. W. ay 
9, mid. N. line, N. W. qr. 
9, N. W. qr., angle in road, 
9, mid. line, roa 

9, mid. line, road E. ond Wi, 
9, 8. E. 


9, center 8. E. q 

10, N. W. qr. ban of lake, 
10. 8, E. qr., bank of lake, 
15, N. line, bank of lake, - 


15, center, 


house, 
St. Francis R. R. station, 


8. E. qr., 
17, N. W. corner, - 
18, mid. N. line, N. E. qr., 
18, mid. N. line, 


18, N. W. corner, - 

18, mid. W. line, N. W. sy 
18, mid. W. line, - 

13, mid. W. line, S. W. My 
19, N. W. corner, 

19, mid. W. line, 

19, W. line, 8. W. qr., ercek, 
19, mid. W. line, 8. W. qr., 


qr. 
9, near # lio,8. B. gr. R.R., 


15, N. line, N. W. ar, Chic. rd. 55 


15, 8. E. qr., Deer creek, R. R., 


18, N. line, N. W. qr., brook, 
18, mid. N. linc, N. W. Fs : 


115 


8, mid. N. W. line, N. W. ar., 58 


15, Chicago road, N. of school 
: 15, Gace road, 8. of school 


Sec. 16, mid. ee line, N. E. ar. of 


116 


Lake. 
Sec. 


GEOLOGY OF EASTERN WISCONSIN. 


List or ELEVATIONS ABOVE 


T. 6, R. 22 E. — (con.) Feet. 
20, N. W. corer, - 80 
20, mid. N, line N. E. a 109 
20, mid. N. line, 105 
20, N. line, railroad, - 86 
20, mid. W. line N. W. qr., 79 
20, mid. §. line 8. W. qr., 97 
21, mid. N. line N. E. qr., 72 
21, mid. N, line, - 78 
21, mid. N. line N. W. qr., 83 
21, N. W. corner, - 100 
92 N. line, Chicago Road, - 380 


22, center NE. qr., Chicago R'd, 82 
29! mid. line, Chicago Road, - 100 


92? 8. E. qr., Chicago Road, 90 
23, ae line, bank of lake, 30 
23) N ‘Tine, Lake Shore Road, 45 
23° mid. N. line, - 35 


23, W.line S.W. qr., Chi. Roail, 120 
23, N. E. qr., Lake Shore Road, 115 
23, N. line 8. ‘E. qr., Lake Sh. Rd, 75 


24 mid. line, bank of lake, 60 
25, N. line, bank of lake, 80 
95, N. W. corner, 90 
25, mid. W. line, - 102 
25. mid. line, bank of lake, 80 
26, mid. N. line N. E. ar., 87 
26. mid. N. line, 130 
26, N. line, railroad, - 113 
26, N. W. corner, 116 
26, mid. W. line N. W. qr., - 89 
27, N. line, Chicago Road, 124 
27, mid. W. line, - 122 
27, N. W. corner, 83 
27, mid. line, Chicago Road, 84 
27, center 5. E. qr., 95 
28, mid. N. line, - 88 
28, N. W. corner, 81 
99, wid. N. line N. E. Ty - 74 
29, mid. N. line, - 82 
Zh N. line, railroad, 97 

9, N. W. corner, 96 
30) mid. W. line N. W. a., - 118 
29, mid. W. line, 111 
29" mid. W. line 8. W. qr., - 184 
99, mid. S. line 8. W. qr., 137 
30, mid. N. line N. E. sis 129 
30, mid. N. line, - 113 
30, mid. N. line N. W. , - 127 
30, N. W. corner, 136 
30, mid. W. line N. W. Ts 165 
30, mid. W. line, 185 
30, mid. W. line 8. W. a, 178 
31, N. W. corner, 180 
31, mid. W. line N. W. a, - 190 
31, mid. W. line, 195 
31, mid. W. line 8. W. ar., 175 
32) N. line N. E. qr, - 122 
32, mid. N. line, 139 
32, N. line, railroad, 137 
32, N. W. corner, - 142 
32, mid. §. line 8. W. qr., 154 
33, mid. N. line N, E. a, 103 
33, mid. N. line, - 115 
33, mid, N. line NW: gr. 102 


Lake Micuigan — continued. 


Lake. T. 6, R. 22 E.—(con.) Feet 
Sec. 33, N. W. corner, 120 
34, N. line N. E. qr., road, - 98 
34, mid. N. line, - 90 
85, N. line, railroad, 111 
35, mid. N. line, 115 
35, N. E. qr., angle Chi. Road, 108 
36, N. line bank of lake, - 90 
36, mid. N. line W. ht, N. W. 
qr, - 110 
36. N. W. corner, - 93 
Lake Mills. T. 7, R. 13 E. 
Sec. I, W.ht., - 265 
3, center N. E. qr., 274 
8, near center N. W. qr., 327 
3, mid. W. line N. W. ar. 311 
3, 5. W. corner, 291 
4, center N. W. qr., 330 
4. flat, 315 
5 N. E. qr. hill 370 
6 8. W. qr., 398 
8, mid. 8. line, - 373 
Koshkonong Creek at Kroughville, 257 
Sec. 10, mid. W. line, 315 
Lake Mills villa; ge, 260 
Lake Mills ville, N. W. part, 277 
Rock Lake, - 250 
Sec. 18, mid. S. line, - 345 
19, 8. W. qr., creek, 288 
98" mid. S. line S. E. a.» 278 
31, 8. W. qr., creek, 272 
33, N. E. corer, - 363 
La Prairie. T. 2, R. 18 E. 
Sec. 13, mid. Ww. line, 271 
16, mid. W. line, - 242 
Lima. T.4,R.14E. 
Sec. 6, 8. E. qr., marsh, 243 
18, N. E. qr., 807 
14,8. E. qr, - 316 
18, near mid. W. line, 248 
21, 8. E. comer, - 301 
22, Lima station, - 310 
23, mid. N. hf., 305 
93) W. line, - 308 
30, E. line, - - 311 
Lima. T. 14, R. 22 E. 
Sec. 2, E. line 8. E. qr., highland, 129 
16, mid. E. line, 164 
20, center §. E. qr., 219 
26, center N. hf., - 119 
Hingham Mul Pond, - 192 
Lincoln. T. 25, R. od EB. 
Sec. 19, S. line outcrop, 23) 
20, 8. line 8. W. qr., 192 
92, mid. S. Tne 8 E. qr., - 197 
23, mid. §. line 8. W. qr. (est.), 168 
26, swamp, » td 
35, stream, - 98 
Linn. T.1, R.17E. 
Sec. 5, Moorfield’s lime kiln, - 388 
Geneva lake, 982 
Little ea T. 26, R. 19E. 
Sec. 2 - 144 
Lowell. Tt, 10, R. 14 E. 
Sec. 6,8. W.aqr., - 256 


TOPOGRAPHY. 


List oF ELEVATIONS ABOVE 


Lowell. T. 10, R.14E.—(con.) Feet. 

Sec. 7, near center W. ht., 236 

15, Lowell Nea - 241 

19, N. E. - 245 

30, center “he, R. R., 240 

30, near 8. line 8. E. a» tiatahi, 216 

‘Lowell Station, = - 247 
Lowell. T. 11, "R.A EL 

Sec. 26, 8. E. qr., ridge, - - 300 

30, near center W. hf 236 

31, near center W. ne - 266 

36, mid. §. line 8. E. w, creek, 240 

36, hill-top, 305 
Lynden. T. 14, R. 21 E. 

Sec. 1, mid. S. line S. E. qr,  - 262 

2, mid. 8. line §. E. qr., 264 

3, mid. 8. line, R. R., 224 

4 mid. 8. line, valley, - 245 

4, 8. E. commer, Onion River,- 211 

6, anid, Sine’. oy 299 

26, near center, 492 

27, mid. §. line, - 352 


28) nid. E. lineS. E. qr., sient 
30, near mid. W. line, 4 


30, 8. line N. E. qr., stream, 805 
35, N. E. corner, church, 316 
35, N. line, R. R., - 807 
Cascade River, below mill, 287 
Lyons. T. 2, R. 18 E. 
Lyons Station, - - 222 
Sec. 1, center E. line, R. Bo 207 
c near mid. 8. line, 291 
1, 8. W. ar., 194 
if near S. W. corner, 339 
2) S. W. corner, R. B., 200 
i, 8. W. qr., - 273 
8, mid. W. line, - - 285 
9, N. E. yr, - - - 228 
10, N. hf., - 220 
10, near center 8. Tae; - 366 
12; near east line, 355 
12, S. E. qr., brook, - 218 
23, mid. E. line, 321 
23, mid. E. line, 8. E. ee, - 305 
28) S. line 8. E. qr., : 319 


Magnolia. T. 3, R. 10 BE. 


Magnolia Station, 340 
Sec. 6, mid. W. line N. W. qr., 304 
6, mid. W. line, - 285 

6, S. W. qr., flat, 286 

6,5. W.qr., - 309 

6, S. W. qr., Allen’s Creek 278 

6,8. E.qr., - 360 

7, 8. E. gr., - - 433 

7,8. E. qr., road, - - 323 

7, 8. E. qr., top of ledge, 450 

9, N. W. Allen’ s Creek, - 292 

23, N. W. qr. 339 

26, S. W. ar., 384 

96, 8. W. qr., summit, - 441 

28, 8. W. ar. - 339 

34, N. W. qr, - 432 

Meo T. 19, R. 24 E. 

City, S. W. corner, - pe 


Station, - - = 


117 


Laxe Micurean — continued. 


Manitowoc. T.19, R. 24 E. == {oon,) Bee 


Sec. 5, near W. ‘line, 719 
6 center 8. W.qr., - 69 
7, N. W. qr., bridge, 3 
17, N. W. cor., Little’ Man’ woe, 15 
17, 8. W. gr., R. B., 44 
18, N.W. ar. §, Ban. RRs 51 
18,8. W. q i 60 
“LN. Wee, Ree - 83 
Manitowoc Rapids. T. 19, R. 23 E. 
Sec. 2, a . line 8. W. qr., 136 
3, near 8. B, vorner, - 153 
4. mid. E. line, 203 
4, mid. 8. line, highland, 213 
4, mid. N. line, R. R., 154 
5 mid. E. line, 158 
6, mid. EK. line, - 173 
10, near N. line §. E. sits, 60 
ii, near N. line, - 124 
12, near mid. W. line, - 1) 
12, mid. 8. line 8. W. qr., 68 
13, center N. W. qr., R. R., 68 
13, near 8. E. corner, - vit) 
19, N. Hh ots , top of Kettle’s, 166 
19, mid W. ayr., river, 108 
22, N. line N. W. qr, - 140 
oA, mid. E. line N. i qr,  -. 53 
95, N. W. qr. of 8. E EH. gr., R. R., 53 
32, center stream, 142 
34, mid. E. hf., N. shore Sil. a 150 
34, center 8. E. qr, - 129 
34, S. line 8. E. qr., 123 
35, near center, 111 
Maple Grove. T. 20, R. 21 E. 
Reedsville Station, 242 
Sec. 6, 328 
6, S. W. corner, - - 329 
7, Serpentine ridge, - 304 
12) 8. E. corner, 247 
29, mid. W. line. w. qr., 296 
30, near mid. W. line, 276 
32, near N. E. corner, 278 
33, E. line, 276 
34, E. line, 262 
35, S. E. corner, 240 
Maple Valley. 
Sec. 24, N. branch Little River, T. 29, 
R. 19 E., "180 
Sec. 24, Small Lake, T. 30, R. ‘19 E., 159 
25, Little Peshtigo Lake, - 157 
Marshfield. _T. 16, R. 19 E. 
Sec. 6, N. W. corner (est. ) - 402 
6, stream, - 3860 
6, S. W. corner, - 406 
6, S. E. comer, - 483 
14, 8. E. qr, Reichart Quarry, 357 
16, S. line, Maria, Hotel 865 
17, N line (est.), R. R., 371 
17, 8. W. corner, hill, - - 442 
20, near center, hill, - 450 
24, 8. E. qr., - - 424 
25, N. line, - 420 
30, S. W. qr., Steffer's quarry, 409 
Calvary station, - 363 
St. Cloud station, - 849 


118 GEOLOGY OF EASTERN WISCONSIN. 
List or ELEvations arovE Lake Micuiean— continued. 
Memee. T. 17, BR. 22 E. Feet. | Milford. T.7,R.14E.—(con.) Feet. 
Sec. 1, mid. N. line, - 175| Sec. 6,8. E. ar., outlet of lake, 228 
N, W. qr., 348 6, 8. E. qr., outerop, - 252 
8, N. W. corner, - 9348} Milton. T. 4, R. 13 E. 
14, 8. W. qr., river, 135 Milton station, - 293 
21, mid. N. line, - - 248] Milton Junction, 299 
21, center, streain, 175 Ridge 8. of Milton Junction, 318 
Menasha. T. 20, R. 17’E. Sec. 10, 8. E. comer, : - 216 
Menasha station, - 177 29° center E. ht., hill, = - 875 
Menomonee. T. 8 R. 20 E. , 8. E. qr., - 307 
Sec. 2, N. E. qr., outerop, 193 26, 8. E. qr., 803 
6, E. side N. E. ar. - - 259 30, N.E. ws 289 
8. outcrop, 290 30, N. W. 255 
8, 8. line 8S. W. qr, mall, - 834] Milwaukee. T 8 R. 2B. 
Menomonee Falls, - 238-226 Sec. 4, N. line, bank of lake, - 87 
Sec. 17, center N. ‘hf., 314 4, mid. W. line, 93 
19, N. ee qr., spring, 287 4 center, 88 
30; S. W. corner, 279 5, mid. N. line, Me 
Mequon. T. 9, R. 21 E. 5, N. W. corner, 
Mequon station, - 92 5, N. W. ar., Washington. Rd, : 
Thiensville station, 88 5, N. line 8. W. qr., 
Sec. 1, mid. N. line N. E. qr., 147 5, mid. line R. R., 84 
10, RB: Ris; 128 6, mid. N. line, - 107 
31, N. E. corner, valley, 154 6, mid. N. line, N. W. ar., 117 
31, N. W. corner, 252 6, N. W. corner, - 127 
32) N. line, 172 7, mid. N. line, - - 103 
35, R.R., - - 107 7, N. W. corner, - 95 
35, N.W. Or; RR - 97 8, mid. N. line, - 93 
— T. 9, R. 22 E. 8, N. W. corner, - 91 
Sec. > near N. EH. corner, - Ill 8, center N. E. qr., - 79 
5, 8. line, R. R., - 93 8, center, - - - 70 
6. mid, N. ge river, - 83 9, N. line R. R., 107 
8, 8. line, R. R., 98 16, N. line, R. R., 127 
17, S. line, R. R.. 94 16, mid. line, bank of lake, - 98 
20° mid. N. line, bank of lake, 110 16, mid. line., R. R., 94 
20, N. W. corner, 83 1% near mid. N. line, 94 
29° S.lime, ‘- - 112 17, mid. W. line, - 723 
32, 8. line, 76 1s mid. line, Washington Road, 91 
Merton. T. 8, R. 18 E. 7, N. W. corner, - 62 
Sec. 2, 14 mi. N. of MONEE, - 369 18, N. line, river, 52 
Lake Kessus, 376 19, N. line, river, - 49 
North Lake, - 309 19, mid. N. line, - 65 
High land E. of Pine Lake, 384 19, N. line, Good Hope, 90 
High land W. of Pine Lake, 345 19, N. W. corner, 120 
Ridge 1 mi. W. of Pine Lake, 359 19, W. line, N. E, ares plank rd. 70 
Valley 124 mi. a of Pine Lake, 318 19, mid. line, 8. E. qr., plank-rd, 75 
Metomen. T. 15, R. 14 E. 20, N. W. corner, 95 
Sec. 1, N. E. qr, River's quarry, - 3850 20, W. line, 8. Ww. qr., 42 
Reed's Corners station, 407 20; W. line, river, 45 
Brandon station, - 421 20; mid. W, line X, E. qr., 114 
Michicott. T. 20, R. 24 E, 20, center N. I. qr., 120 
River ie Michicott, 22 20; mid. line Wash, rd., - WW 
Sec. 4,8. W. qr., 60 21; N. line, M. L.S.& W.R. R., 85 
3 S. ht. of 8. E. qr, T. 21, 126 29, center N. E. qr. 7 
9, E. hf. of N. E. qr., , river, 11 9, W. line, river, 40 
22, N. W. qr., - 653 99° mid. N, lne 8. E. q 71 
82, 8. W. gr. T. 21, 108 30, N. W. ARR. & GB. rd, 60 
Milford. T. 8, R. 14, E. 30, mid. N. line, 65 
Hubbleton ttn - Q11 30, N. line; river - 40 
Sec. 21, mid. N. line, - - 260 30, N. W. corner, - 102 
94 N. E. corner, - - 232 30, center, - 50 
24, mid. S. line, 222 30, center, N. BE. qr., - - 55 
: 33) N. E. qr., quarry, - 284 31, mid. N. line, 50 
36, center N. hf, - 295 1, N. line, creek, - 4) 
—T.7,R, 14E. 31, mid. N. line N. W.qr., 59 


TOPOGRAPHY. 


List or ELEVations aBovE Lax Micuiaan — continued. 
Milwaukee. T. 8, R. 22 E. —(con. ) Feet. 


Sec. 31, N. W. comer, 60 

31) R. R. bridge, Milwaukee Ry 51 

Lindwurm station, 56 

Sec. 32, mid, N, line, - 60 

33) N. ihe bank of lake, - 80 

33, N. line R. R., - 3 

33, N. W. corner, - 73 

33, mid. W. line, . 74 

33; mid. N. E. qr., bank of lake, 75 

33. N. line, bank of lake, - 80 

33, mid, line, S. E. qr., - 75 
Milwaukee. T. 7, R. 22 = 

Sec. 3, N. line, - 95 

, N. W. corner, 92 

3, mid. W. line, 112 

3, center N. E. qr., bank, 105 

3, mid. line, bank, 108 

3, center 8. E. qr., ae 110 

4 mid. N. line N.'E. r, - 93 

4 N. line R. R., - 71 

4, mid. N, line, - 64 

4, W. line, river - 30 

4, center 8. W. qr., river, 21 

4, N. W. corner, 59 

5, N. line R. R., - 57 

5, N. line N. E. qr., - 59 

5, mid. N. line, 59 

5, N. W. corner, river, - 37 

5, W. line R. R., 98 

: 5, W. line, Green Bay ils 14 

5, center, - 1 

5, mid. line R, R. - 80 

5, mid. line, river, 36 

6, N. line, Green Bay road, 68 

6, mid. N. line, - 70 

6, N. W. oe - 66 

6, center N. E. q - - 81 

6, RB. R. & Green Bay road, 98 

7, mid. W. line, 98 

7, mid. line near 8. Tine 124 

8, mid. N. line, 94 

8, N. line, Green Bay road, 121 

8, W. of center, 155 

9, Humbolt seees - 61 

9, mid. N. lin - 84 

River at Hombolt B Bids, 15 

Sec. 9, mid. W. line N. E. qr., 60 

9, center, - 63 

9; mid, W. line R. R., 90 

10, N. line, bank of lake, - 102 

10, N. W. corner, - 90 

10, mid. W. line, - - 47 

10, mid. W. line, 8. W. qr., 78 

10, center N. E. qr., Lake Ave., 105 

10, mid. line, Lake Avenue, 83 

10, 8. E. qr., Lake Avenue, 98 

10, 8. line, Lake Avenue, - 88 

Mitchell. T. 14, R.20 E. 

Sec. 2, near mid. 8. line, - 580 

9, 8. E. corner, high hill, - 566 

10, S. E. corner, - 510 

21; mid. E. line, 491 

a7, N. W. qr., Stanley Creek; 391 


119 
Montpelier. T. 23, R. 23 E. Feet. 
Sec. 25, near center, 181 
25, mid. S. line 8. E. qr,, - 138 
Morrison. _T. 21, R.21 FE. 
Sec. 28, N. W. corner, Dry Run, - 237 
34, mid. W. line, stream, 240 
34) mid. §. line, - 284 
Mose). T. 16, R. 23 in 
Sec. 4,8. line R. R., 51 
5 mid. 8. line, ‘stream, 83 
5, 8. line 8S. W. 112 
16, mid. N, ling E. qr R. E 51 
16, N. line N. W. qr., pineati,. 56 
27, mid. N. line, 50 
Bank three- -qr. mile N. of pier, 48 
Mount Pleasant. T. 3, R. 22 E. 
Sec. 4, N. W. corner, - 150 
4, near mid. 8. line, 147 
9, near mid. 8. line, - 158 
12, N. E. qr, . 105 
1%, center, - - 1 
20, 8. ie qr; - - 158 
20, S.h - - 178 
W. U. tea, - - 1438 
Sec. 21, 8. E. qr., - 126 
22,8.E.qr, - 2 95 
23, EK. ht., - - - 120 
_ 25, N. W. corner, 141 
26, N. W. corner, - - 92 
28, mid. 8. sees - 129 
30, N.E. 168 
30, N. Wa ey ‘Windsor, 203 
— T. 3, R. 22 E. 
Sec. 5, S. line, 45 
19, S. E. corner, 80 
19, N. E.qr, - - 78 
20, S. line - 40 
21, Racine Junction, 43 
Vaughn’ s Quarry, - 58 
Horlick’s quarry, - - - 46 
Sec. 82, pepter, - 38 
32, "Si 40 
pene Lt “ip. 5, R. 13 E. 
Sec. 6, marsh, - - 305 
14, 8. W. corner, 335 
Mukwonago village, - 276 
Muskego. “"T.5, B, 20 E. 
Sec. 13, a E. line, - 205 
13, mid. 8. line, - 227 
33, near mid. 8. line, 191 
Muskego lake, - - 191 
Newark. T. 1, R. 115. . 
Sec. 1, N. E. qr., spring, - 258 
1,8. W. qr., 362 
3, N. W. qr., 328 
10, mid. W. line, - 342 
11,8. W.qr,  - 357 
11,8. W. qr., hill, = - 379 
13, W. line near mid.,  - 313 
18, §. E. corner, - 263 
13, 8. E. qr., flat, - 193 
14, N. a qr., - 805 
i 8. W. ar., 331 
15, 8. Ww. qr., stream, - 296 
16, 8. E. corner of 8. W. qr., 244 


120 GEOLOGY OF EASTERN WISCONSIN. 


List or ELEVATIONS ABOVE LAKE Micuia@an — continued. 


Newark. T, 1, R. 11 E.—(con.) wee 


Sec. 16, 8. W. qr., Coon creek, - 
20, mid, S. line, ridge, - 
24, N. E. qr., stream, - - 
25, center W. hf., - 
25, 8. E. qr., - 
28, N. E. ar., creek, - 
29, N.E. qr., quarry, - - 
31, center E. ht, - 
31, near center, - - 
31, W. of center, 
31, W. bt,  - - - 
32) center, - - 
33) near center, - - 
3) mid. W. line, - 
, 33, bottom of outerop, - 
34, center, ridge, - 
35, center, creck. 
New Berlin. 1.6, B. 20 B. 
Sec. 21, mid. N. hf, - 
22, general level E., - 
39 N. W. cores, Prospect hill, 
New Denmark. T. 2 2, R. 22 EB. 
Sec. 7, N. E.ar., Two Rivers, - 
ie N. line N. W. ar; 
28, near N. W. corner, 
35, 8. W. qr., Kettle range, 
New Holstein. T. 17, R. 20 i 
Sec. 30,8. W. qr, - 
32, N. W. corner, 
34, N. W. qr, - - 
Newton. T. 18, R. "23 E. 
Sec. 1, N. line, R. R., - 
te creek, 
4,8. line 8. E. ax, of 8. W. qr. 
12, N. line BR. R., 
18 N. line R. R., - 


23, N. hue Ri, Bis - 
26, N. line R. R., - 
27, creek, 
30, mid, W. ling, &; W.aqr., 
34, N. line R. R., - 
Norway. ‘T. 4, BR. 20 E. 
Wind lake, 
Sec. 8, N. line, - 
8, 8. line, - - 
18, 8. E.corner, - - 
; 19, 8. W. corner, 
Oak Creek. T. 5, R. 22 E. 
Sec. 1, N. line, bank of lake, 


, N. W. corner, - - 


mid, N. line N. W. qr, - 

, N. W. corner, - 

5, mid. N. line, 

5 mid. N. line, N. W. ar. 
Lake station, - 

5, mid. N. line W. hf. N. W. 


q., . 


Oak Creek. T. 5, R. 22 E.—(con.) Feet. 
Sec. 5, N. W. corner, 152 


5, mid. W. line N. W. a, 164 


5 mid. W. line, 161 
5 mid, W. line 8. W. i. 158, 
6, N. W. corner, 185 
6, mid. W. line N. W. as 205 
6, mid. W. line, 210 
7, mid. N. line N. E. a.» - 160 
7, mid. N. line, 175 
7, mid. N. line N. W. Os) = 170 
7, N. W. corner, 195 
7, mid. W. line N. W. e-, 180 
7, mid. W. line, 175 
8, mid. N. lne N. E. a.» - 138 
8, mid. N. line, 150 
8, N. line R. R., - - 147 
8, N. W. corner, - 155 
8, near mid. 8. line, - 129 
9, mid. N. line N. E. qr., 96 
9, mid. N. line, - ill 
9, mid.N. line N. W Bs 155 
9, N. W. corner, - 134 
10, N. line, Oak creeks, - 71 
10, mid. N’ line N. E. Py 80 
10, mid. N. line, 119 
10, mid. N. line, N. W. -» - 138 
10, N. W. corner, 82 
11, N. line, Oak creek, 45 
11, N. line, Chicago road, - 74 
11. N. line, R. R., 94. 
11, N. line N. W. qr., - Ill 
11, N. W. corer, 82 
11 center, Oak Creek station, 86 
11) mid. line, 107 
12) N. line, bank of lake, - 80 
12, mid. W. line N. E. qr., 84 
12. N. W. corner, - 65 
14, N, line, ee road, 108 
14; mid. N. line NX. W. Py 89 
14, N. W. corner, 105 
15, mid. N. line N. E. qr, - 91 
15, mid. N. line, . 96 
15, N. W. corner, - 102 
15, mid. N. line N. W. cr., 126 
1, mid. W. line 8. E. qr.,. - 88 
15, mid. W. line N. E. qr., 101 
15, center, - - 112 
16, N. line, Oak Creek, 77 
16, mid. N. line N. B. qr, - 7 
16, mid. N. line, - 91 
16, mid, N line’N. W. ar, - 118 
16, N. W. corner, 1k 
16, mid. W. line N. W. -, - 184 
16, mid. W. line, 136 
16, mid. W. line 8. W. ar., 122 
17, mid. N. line N. E. qr., 130 
17; mid. N/ line, R. R., - 199 
17, mid. N. line N. W. qr., 136 
17, N. W. corner, - - 140 
17, mid. W. line N. W. qz., 125 
17, mid. W. line, 130 
17, mid. W. line’S. Ww. qr. 140 
17, mid. W, line S. hf. $.W. qr., 155 
vd mid. 8. lneS. Wear, - 116 


TOPOGRAPHY. 


List or ELEVATIONS ABOVE LAKE MicHigan — continued. 
Oak Creek. T.5, R. 22 E.—(con.) Feet. 
160 


Sec. 18, N. W. corner, - 
20, mid. N. line N. E. E-» 
20; mid. N. line, 
20; N. line, R. BR. - 
20, mid. N. line N. W. qr. 
20, N. W. corner, 
20, mid. §. line 8. W. qr., 

1, N. W. corner, - 

92° mid. N. line N. E. Ess 
22, mid. N. line, 


93, mid, N. line N. Ww. qr., 
93, N. W. corner, - 
93) mid. line, R. R., 

93° mid. line, Chicago pat 
93) cent. N. hf, S.E. qr., 
26, N. line, Chicago road, 
26, mid. line, pineage road, 
27, mid. W. lin 

27; mid. W. tne’S, w. qr., 
93° mid. N. line, 

98) mid. N. line N. w. GTi; 
98) N. W. corner, — - 

98° mid. N. line 8. E. as 
98; center, 

98° mid. W. line N. BE. qr., 
29, mid. N. line N. E. es 
99) mid. N. line, - 


99) mid. N. line N.W. qr., R. 


29, N. W. corner, - 

99) mid. 8. line 8. W. aqr., 
30, mid. N. line N. E. a 
30, mid. N. line, - 

30, mid. N. line N. W. ar, 
30, N. W. corner, 

30, mid, W. line N. W. a.» 
30, mid. W. line, 

30, mid. W. line 8. W. qr., 
81, mid. N. line N. E. qr., 
31, mid. N. line, - 

31, mid. N. line N. W. qr., 
31, N. W. corner, - 

32, mid. N. line N. E. qr., 
32, mid. N. line, - 

32) mid. N. line N. W. ati, 
32) N. W. corner, - 

33; mid. N. line N. E. qr., 
33) mid. N. line, - 

33, mid. N. line N. W. qr., 
33, N. W. corner, 

34, mid. N. line N. E. qr., 
34 mid. N. line, - 

34, Pla N. line N. W. qr., 
34, N . W. corner, _'- 
34) mid. W. line N. W. qr., 
34, mid. W. line, - 
34, mid. N. line 8. W. qr., 
34, center, 

34, mid. N. line §. E. qr., 
35, mid. N. line N. E. Es 
35, mid. N. line, - 

35, mid. N. line N. W. a+, 
35, N. W. corner, 


Ch. 


- 125 
145 
116 


- 136 


' 
re 
con) 
or 


121 


Oak Creek. Te 5, R. 22 BE. eons)! Feet, 
Sec. 385, mid. W - line, ai 
35, mid, N. line'S. W. ar., 80 
35, center, 78 
35, mid. N. line 8. E. qr., 96 
36, N. W. corner, - 114 
36, mid. W. line, - 104 
36, mid. W. line 8. W. qr., 102 
36, mid. 8. line 8. W. qr., 118 
36, inid. 8. line, - 121 
36, 8. line, R. R. station, 117 
36, Chicago rd. on County ine, 110 
36, 8. E. corner, 130 
Top of ‘bank (Sec. 3L, T.5, R. 23 ), 80 
Oak Grove. T. 11, BR. E. 
Horicon Junction, - - 306 
Minnesota Junction, 348 
Rolling Prairie station, - - 363 
Juneau station, 335 
Oakland. T. 6, R. 13 E. 
Lake Ripley, - - - 239 
Red Cedar lake, - - 233 
Sec, 4,8. W. qr., - - - 266 
5, 8. half, - - 280, 
7, W. line N. W. ar., 271 
13, mid. W. line N. W. a.» 343 
16, 8. E. corner, - 330 
18, S. E. qr. of 8. E. qr., - 246 
19, near N. W. corner, 264 
19, center 8. E. qr,  - - 251 
19, S. W. ar., 234 
25, near N. W. corner, 363 
25, W. line N. W. ar., 270 
93) mid, E. line, - 253 
28, near mid. 8. line, 227 
30, S. W. ar., 257 
30, near center 8. W. Fs 253 
31, 8. W. ar., 214 
31, S. line 8. W. qr., - 210 
Oconomowoc. T. 8, R. 17 E. 
Lac La Belle, - - 273 
Oconomowoc station, - 283 
aoe T. 14, R. 20 E. 
Sec. 1, mid. W. line, : 500 
4, N. E. qr., cross roads, 458 
i. 8. W. qr., stream, - 453 
13, Long Lake, 443 
30, E. ht., pond, 413 
32) N. line, 518 
34, general level, - ~a0t 
35, N. hf., Canton, - 566 
Palmyra. T. 5, R. 16 E. 
Palmyra station, - 260 
Sec. 20, E. hf., - - 266 
20, N.W. qr. - 278 
22, 8. E. qr., - : 290 
93, N. E. qr., - - 271 
28, N. line, - 241 
29,8. E. qr. - 22) 
81, center, - - 221 
82, W. line, - - - 221 
Paris. T.7, R. 21E 
Sec. 18, center, prairie, - 191 
Pensaukee. T. 27, R. 19 E. 
Sec. 23, N. branch, Pensaukee road, 139 


GEOLOGY OF EASTERN WISCONSIN. 


List oF ELEVATIONS ABOVE 


Pensaukee. T. 27, R. 19 E.—(con.) Peet. 
Sec. 35, Pensaukee river, - 128 

Pewaukee. T. 7, R. 19 EB. 
Pewaukee Lake, . 
Mabtgree station, - - 


I. N. Stewart’s place, - 


Sec. 1, center, . 


12) highland, 

12) mid. 8. line, - 
13, mid. N. hf., - 
16, 8. E. qr., 

26, quarry, - 
26, ru teed crossing, - 


Pierce. au of R. 4 E. 
Gen. level, E. of Casco village, 
Sec. 28, center, high bluff, - 


28, ae 


33, Woe : 


rs miles 8. W. of Ahnapee, - 
Bank at Alaska, 
Sec. 20, N. W. qr., - 


Pleasant Prairie. 


31,8. E. corner, 
qT. 1, R. 92 B. 


Kenosha Junction, 
Pleasant Prairie station, : 
Eau Pleine river, near state line, 


Sec. 1, mid. N. line N 


EK. a.» 
1, mid. W. ei 

1,8. W. q 

2) mid. 8. “he, W. gr., 
4 near mid. N. line, 

4 near mid. 8. line, 

7, W. line, 

9, mid. N. line, railroad, 


18, Eau Pleine ic, - 
20, mid. 8. Aaa E. qr., 
24 N. E. - 
29, mid. ch ‘tine B B. qr., 
32) iid. 8. line 8. E. qr., 
32) center E. hf., railroad, 
33, S. E. corner, - 


35, 40 rods W. of mid., s. line, 


Pleasant Prairie. . 1, BR. 2S E. 


Sec. 18, 8. E. qr., 
18 


beach 1; 
. E. qr., beach TL - 
31,8. W. qr., beach IT, 


Beach I, near state line, 
Beach II, near state line, 


Plymouth. T. 2, R. 11 KE. 
anover Junction, 
Sec. b 8. W. qr., 


9, N. E. corner, railroad, 
98) mid. W. line, - 
33, N. E. corner, - 
35, mid. W. line, - 


Plymouth. 


Lake Mronrean — continued. 


T. 15, B. 21 E. 


Plymouth station, - 


Red 
Sec. 


Polk. 


Clay, E. of Plymouth, 

3, N. W. qr., 

16, 8. E. qr., stream, 
line, Onion river, _- 


E. qr., Ist Kettle Ridge, 


/8. 
2) 8, 
3S. line 8. E. qr., 
8. 


ve 
36, 8. E. one hill, 
7. 10, R oF. 


Cedar Creek village, - 
Cedar Lake, - 
Schleisingerville station, 
Ackerville station, 


Sec. 


Q 
8 

3 “Foo 
Pe cocomencrencooors” Cc 
ee 


DWHAIOAIAAD EH 
E. 


AE. 


6, mid, N. line N. W. qr., 
6, N. line N. E. qr., 
6, N, E. corner. - 


ee 
[=*) 
aa 


, E, comer, - 
.qr., Catfish riv er, 
eN. W. qr., 

qr., stream, 


Erenexe 


Le 


Ee 
o 


ae 


t Portland, 
mer, 


spore, 


8 iz 
444. 


BRS. 


. CO 
0-5 
Pelee 
er W. 
rin 
. W. ht., stream, 
mid. 8. ‘line, marsh, 
. N. line, 

W. 


“8 


S 
Oo 
i 


iNe) 
NIN 


27, N.wW. qr., Crawfish, 
27, top of conglomerate, 
29° center E. hf., 

29, near 8. line, - 

31, N. E. corner, - 
31, near mid. N. line, - 
31, N. W. corner, 

31, 8. E. corer, 

34) mid. N. line N. W. a, 
35, 8. W. qr. 

35, mid. EB. line, - 
36, mid. N. tine 8. W. qr., 


Preble. TT. 24, R. 21 E. 
Top of beach’ line, 1 mi. E. of Green 


B 
Sec. 


BY» 2 
26, mid. E. line, - - 


27, fork of roads, 

33) mid, of W. line, - 
34, N. W. qr., 

34, top of highland, - 
3A, center, highland, - 


hne, railroad crossing, 


N. We qr., marsh, 


5, 8. E. qr., gen. level of high: 


"Nena - 


157 


TOPOGRAPHY. 123 


List or Exzvations apove Lake Micurean— continued. 


Preble. T. 24, a 21 E. — (con.) Feet. 
- 189 


Sec. 36, N. E 8 
36, nid, N. EE - 180 
9, S. ht, T. 23, - 91 
Randall. ip. ‘i R. 19 E. 
Lake Elizabeth, | - - 196 
Sec. 18, Power's Lake, 265 
18, 8. E. corner, - - 282 
19, mid. S. line, - 289 
21, E. hf., RB. B., - 201 
35, mid. 8. hf, - 298 
36, 8. hé. of S. E. qr, - 3840 
Rantoul. . 19, R. 20 E. 
Sec. 4, mid. E. line (est.), 271° 
Hilbert Station, - - 250 
School house 8. of Hilbert, - 301 
Raymond. ‘T. 4, R. 21 E. 
Sec. 7, mid. W. line, - - 203 
18, S. W. corner, - 238 
OL, N. W. qr., - - 179 
36, N. line N. E. qr, - 89 
Red River. T 25, R. 23 E 
Mayville beds in N. part of town, | 163 
Sec. 20, S. E. qe.y = 186 
21, S. line 8. E. qr. 138 
21; 8. E. aes smooth thin beds, 1388 
92° 8. E. q 168 
99° mid. &. rite, highland, 249 
93) 8. line 8. W. qr., swamp, 176 
4. S. line 8. W. qr. (2), outcrop, 268 
27, N. W. qr., 203 
33, N. line N. E. qr., stvean, 125 
34, N. W. qr. N. line, stream, 144 
35, N. W. corner, highland, - 274 
386, N. E. corner, gen. level, 285 
Rhine. T. 16, R. 21 H. 
Elkhart Station, - 362 
Sec. ee mid. N. E. qr., - 341 
3, N. E. corner, - - 211 
13° center Hi. ht., R. R 316 
19, 8. E. qr., summit, 426 
24° E. line N. E. ar., 327 
33, 8S. W. qr., stream, - 3800 
Richie. 'T. 9, R19 E. 
Richfield Station, 381 
Sec. 3, mid. E. line, 413 
8, 20 rods W. of mid. E. line, 542 
4 mid. E. line, - 528 
10, mid. E. line, - 530 
1b, S. E. corner, - 430 
22, S. line, Bark river, - 367 
92, 8. E. qr, - - - 498 
26, N. E. qr., - 379 
36, N. E. corner, - 42! 
36, E. line of 8. E. qr, - 300 
Ripon. 'T. 16, R. 14 E. . 
Ripon Station, - - 852 
Cliff, W. of road, 341 
City, Falls under tressel bridge, 332 
Top of St. P., near limekiln, 351 
Top of Hill, W. of limekiln, 873 
St. Peters, W. of last, ee 
Coombs quarry, bottom, - 
Sec. 2, (ést.), S. E. corner, - 3809 
19, mid. W. line, - 304 


Ripon.. T. 16, R. 14 E.— (con.) Feet. 


3ec. 20, N. W. qr. of N. W. qr., - 327 
20, N. W. of center, quarry, 400 
20, little W. of center, 397 
20, near mid. 8. line, 350 
Aree WM Ge BT Uns 301 
ON. Bee We 381 
2i, foany 6. W. of Mr. ae 8, 364 
26, N. W.q 366 
98) N. ling E. qr., - - 370 
29, N. E. qr. near center, 350 
29, N. E. qr., top of Temmesanne, 370 
29) 20 rods 8. of last, 341 
35, S. E. qr., 364 
36, 8. E. qr., stream, - 343 
Rochester. T. 3 R.19 E. 
Sec. 2, mid. 8. line, - 208 
14; N. E. qr., river, 187 
15, 8. E. gs bluff, 276 
15, mid. 8 we 8. E. ar., 200 
Rock. T. 2, R. BE 
Afton - 206 
Sec. 7, N. BE. qr., gina. 306 
8, N. W. ar, R. R., "marsh, 265 
20, mid. W. line, Bass creek fat 183 
21, mid. W. line, 206 
Rockland. T. 19, R. D1 E. 
Saas ledge, - 300 
Sec. ren . ee , outcrop, 310 
lime, - 258 
Rockland” t 22, R. 20, E. 
Sec. 3, N. hf., - 22 
3, 8. E. qr. E. of east river, 30 
14, mid. E. line, base of ledge, 267 
24, mid. E. ht., level above lei 320 
Rosendale. T. 16, RB. 15 E. 
Rosendale station, - 813 
West Rosendale station, 804 
Rubicon station, - - 440 
Sec. 4, 5. W. qr., - 288 
, 8. W. gr., quarry, - 278 
23) N. W. qr., river, 271 
39) 8. E. corner, 845 


Russell. T. 16, B. 20 E. 
Sec. 31, W. line N. W. qr., Sheb. riv. a 
36, E. line 8. E. qr., hill, 


Salem. ‘T. 1, R. 20 E. 
Salem station, - 198 
Fox river station, - - - 200 
Fox river at head - 154 
Sec. 82, N. E. qi - 161 
Saukville. T. i, R. 21 Ei. 
Saukville station, - 181 
Sec. 2, HE. line 8. E. qr, - - 249 
26, N. E. qr., quarry, = - 212 
34, mid. 8. line, outcrop, - 187 
35, 8. line, R. R. crossing, 181 
Schleswig. 1. 17, R, 21 E. 
Rockville, ; - 286 
Sheboygan river under bildge be- 
tween Rockville and Kiel, - 272 
Kiel station, 333 
Sec. As N. E. qr., gen. level, - 295 
7, N. W. corner, gen. level, 350 
20° N. W. qr, - 309 


GEOLOGY OF EASTERN WISCONSIN. 


List or Eevations Above Lake Mrcnrean — continued. 
Sherman. T. 13, R. 21 E.— (con.) Feet. 


124 
Scott. T. 13, R. 20 EB. Feet. 
Sec. 9, Stanley creek, 324 
10, - 826 
19, Tamarac swamp, - 392 
27 mid. N. line, 328 
27, Stanley creek, - 284 
Scott. T. 24, R. 22 E. 
Sec. 7, W. ht, Cowles well, 124 
19, (est.), 222 
Scott. T. 2, R. 8. 
Top ot Mayville beds, - - 70 
Sec. 12, Outerep, Cincinnati, a 
Sevastopol. m7 28, R. 26 E. 


Racine limestone near Whitefish bay, 33 
Sandbank, R. 27, E., Whitefish bay, ae 


Sec. 10, 8. W. ar., gen. level, 27 

7 Ds e, 80 

20, bank, - - - 193 

21, N. BE. gq 133 

27,5. W. ae ’ (est. 3, ridge, 100 

98) mid. E. line, 116 

98, S. E. qr., stream, 56 

29, N. B ae = - 155 

33, 5. E. qr., hill, - 62 

Sheboygan. T. 15, R. 23 E. 

Sheboygan post- -office, 53 

Sheboygan and Fond du Lac R. is 
station, 

Lake Shore R. RB. station, - 7 

Lighthouse point, bank of lake, 46 

Sec. 4, near N. E. corner R. R.., 60 

4. mid. N. line, 85 


6, mid. 8. line, Shevoyean riv., ia 


6 §. E. comer, highland, 
7, center, N. ht., aie s quarry, 73 
9, 8. E. qr., Roth's quamry, 7 
River opposite quarry, 13 
Sec. 10, near center, - 55 
10, near center, R.R, crossing, 46 
10, Pigeon river above dam, - 16 
16, N. hf., rising to W., 25 
16, mid. 8. line, - 126 
1 near z cena highland, - 127 
30, N. E. qr., gen. level, 111 
33, 8. E. qr. of 8. E. qr., 58 
34, mid. N. W. qr., 62 
Sheboygan Falls. T. 15, R. 22 E. 

Decca Station, - 179 
Sheboygan Falls Station, - - 85 
School house, 118 
Sec. 2, mid. W. line N. W. a, 202 
11, N. E. corner, - 199 
12, mid. E. kne 8. E. qr., 122 
18, S. W. corner, - 190 
21, near center, saw mill, 139 
24, N. E. comer, 116 

27, mid. E. lne 8. E. im 
stream, - 93 
a6 near center, hill, - - 159 
5,8. W.ar., RB. R. crossing, 96 


5, 8. W. qr., Sheboygan river, 129 
eins T. 13, R. 21 E. 


Onion river, - - - 


212 


Sec. 25, quarter mile from White 
Cedar swamp, 
27, W. hf., highland, 
34) N. W. ‘corner, (est.), 

Shields. T. 9, R. 14 E. 

Sec. 32, eae - - : 

Somers. 22 KE. 

Sec. 1, tee gt ne 8. E. qr. 
os S. W. qr., Pike river, 
4, mid. N. line, R. R., 
4, mid. S. line, R. R., - 
9, mid. 8. line, R. B., 
10, mid. E. line, - 
16, mid. 8. line, R. R.,  - 
21, mid. 8. line, R. R., - 
28) mid. S. line, - 
34, center, - - 

Somers. T. 2, R. 23 E. 

Kenosha Station, - - 
Sec. 5, 8. W. corner, - 

7, 8. line, R. R., - - 

18, S. line, R. R., - 

19, center, R. R., 

19, S. line, R. R., - 
Prairie. ae 3, R. 18 E. 
ay s quarry, - - 

Sec. 5, 8. W. qr., highland, 

7 and 8, average, - 
8, 8. Ww. qr, - - 

17 and 18, average, - 

20, mid. W. line, 

26, E. hf, - 

27, 8. W. corner, stream, 

29, center, 

34, N. W. qr., stream, 

Spring Valley. ‘I’. 2, R. 10 E. 
Orford Station, 

Sec. 2, mid. KE. line, 


Sprin. 


nA, 
Ent 
26 
@ t 
Oo 
S 
VIA 
& 
a 


E. qr. 
. WwW. a of 8. Ww. qr., 
., stream, - 


EMzg 2 PAE 


ROR RA coco eor 


a 


12, center N. Th, - 
12, 8. E. qr., flat. : 

12, outcrop, - 

13, mid. N. line, 

15, 8. E. qr, - 3 
17,8. E. qr., stream, 

18, 8. W. qr., Taylor's Creek, 
19, N. W. corner, 

21; N.E. or, of NW. a R.R. 


on E. line of 8. E. q 

28, N. E. qr., 3 

33, 8. E te - 

34, N : , Galena lime- 


stone, - 
84, N. W. ar., summit, 


473, 
339 


TOPOGRAPHY. 


List or Exevations above LAKE MicHIGAN — continued. 
Spring Valley. T.21, R.13E.—(con. 0 ee 


Sec. 34, 8. line 8. W. qr., 
Stockbridge. T. 19, R. 19 E. 
Fork in roads going to Chilton and 
Sherwood, 


397 


Three miles ot of Stockbridge vil Aa 


lag 
Two miles a of Stockbridge village, 
One and a half miles N. of Sto 
Me village, - 
Four corners N. of Stockbridge vil 


lag 
Stockbridge = ine - 
Sec. 28, mid. N. line N. W. ar, 


Sturgeon Bay. T. 27, B. 26 E. 
Top of hill N. ve Sturgeon Bay vil- 
Ag - 
Sec. 5, santos Racine and Coral 
beds, - 
5, top of rock, - - 
5, valley, - - 
9, E. ht, ridge, - - 
9,8. Ww. qr., top of rock, 
9, 8. E. qr., top of rock, - 
Sugar Creek. T. 3, R. 16 E. 
Sec. 4,8. W. qr. W. line, 
5, Holden’s Lake, - 
5, mid. N. line, - - 
9, near center, - 
93) N. W. corner, creek, - 
36, mid. N. line, 


36, 

Summit. T. ve R. 175. 
Silver Lake, - - 
Nemahbin,- - - 

Sumner. T. 5, BR. 13 E. 
Lake Koshkonong, 

Sec. 7, center S. hf, ea 
18, near center, - - 


Taycheedah. T. 16, R. 18 E. 

Lake Winnebago, - = 

Sec. 5, mid. N. line N. w. qr., 
5 centre, - 
99° 8. W. corner, hill, - 
22, mid. N. line, - - 
25, N. line, hills, - 
25, N. line, valleys, - 
2), S: We qr. of 8. E. qs 
32, N. W. qr., R. R., - 


Trenton. T. 11, R. 20 E. 
Newburg, outcrop on river, - 
Sec. 6, mid. H. line, - - 


1 


25, N. W. qr., - - 
Troy. T.4, R.17E. 
Sec. 2, N. W. corner, - - 
10, S. E. corner, R. R.,  - 
11, E. hf. center, - 


383 
358 
214 


231 
399 


118 


313 


11, 8.W. qr., Castleman’ squanry, ae 


15, 8.E. qr, - 

22, R. R. crossing, 

27, centre N. hf.. 7 aes - 
33, mid. 8. line, h - 


. 


125 
Turtle. T.1, R. 13 E. Feet, 
Crest of hill’E. of Beloit, - - 405 
Sec. 5, level hee prairie, 217 
ry - 227 
NW ofS, Bats; 225 
13, 8.E - 323 
13, EL i ‘tne, W. a-, 306 
15, N. E. corner, 220 
16, center, - 223 
19, center, 202 
21: mid. g. line, - 228 
22, N. W.ar., - 270 
22, N. E. qr., - 280 
22, N. hf., mar Bi R. cut, 802 
92; bottom of Galena Exposure, 246 
22, summit of hill, 276 
, N. E. qr., - 280 
28, mid. E. line, - - 825 
29; near center, - 218 
31, N. E. corner, - 211 
31) N. of center, - - 188 
32) center N, ht, - - 229 
3) N. E. corner, - 266 
Two Rivers. T. 20, R. 24 E. 
Sec. 22, N. W. qr., = - 63 
pire at Neenot - 29 
. crossing near ae Rivers, - 14 
Utiea T. 1%, R15 
eat aaken. - - - 266 
ickett’s quarry, - - 242 
McFarland’s quarry, 264 
Fisk’s corners, - 259 
Flat E. of Rush Lake, 235 
Union. T.4, RK. 10E. 
Evansville station, - - - 325 
Sec. 1, N. W. corner, 321 
: 1, N. E. ar. of. N. E. qr, mill, 238 
2, N. W. corner, 336 
2,N.W.aqr, - 339 
2, N. W. qr., stream, 288 
4,N.W.ar, - 379 
5, N. E. qr., - 379 
6, N. W. nee R. R, 400 
6, W. hf., marsh, - 3877 
6,5. W. ne - 427 
Mya - 442 
10, W. hf., “Vion village 375 
12, N. W. qr., 412 
12, near ae - 298 
18, N. W. qr., stream, 293 
14, center E, ht., 339 
18, mid. W. line, stream, 382 
18, S. W. qr., flat, - 368 
19. 8. W. qr., - - 391 
mA N. W. corner, - 382 
, (est.) - 2 - 407 
36° k. qr, - B84 
26, near N. E. corer, - 3889 
29, center 8. hf., flat, = - 367 
0, 5. E. qr., well, - 402 
30; 8. W. ar., valley, 345 
30, near center W ne, 336 
31, N. E. qr., . 383 
31, N. E. qr., summit, - 423 
31,8. W.qr.  - - 299 


126 


List of ELEVATIONS ABOVE 


Union. T. 4, R, 10 E.— (con.) 
Sec. 33, near center stream, . 
34, near N. W. comer, - 

Vernon. T.5, R. 19 E. 

Fox river at Big Bend, - 
Sec. 10, mid. E. line, - - 
11, N. W. comer, - 

28) valley. - 
Washington. Mn 11, R. 22 B 
Se ee N. of Port Washington, 
HR of bank N. of Port Washington, 
W. of Port Washington, - 
Port Washington station, 
Port Washington, beach formation, 
Sec. 4, N. line, 
9, N. line, - 
9, center N. E. qr., - 
9, center, - - 
16, N. line, - - 
16, Sauk river, - 
30, center 8. E. Es» - 
32) center, - 
Waterford. T. 4, R. 195. 
Fox river above dam at Waterford, 
General level E. of Waterford, - 
Sec. 6, N. line, 
28, Vernon valley, - 
36, mid. N. line, - - 
Waterloo. T. 8, R. 13 E. 
Waterloo Station, - - 
Sec. 8, 8. W. qr., 
5, N. W. qr., - 
6, N. E. corner, - 
9, near mid. N. line, - 
9, mid. N. line, R. R., - 
9, center, creek, 
11, near center S. W. i - 
16, N. W. qr., marsh, - 
i, center W. ht., hil, - 
17, center, marsh, 
18, N. W. corner, - 
19, S. E. corner, - - 
23) center S. hf., hill, 
24 Crawfish marsh, - - 
95, N. E. qr., 
25, near ge E. hf., - 
27, 8. E. q 
99; near aakeey creek, - 
29, E.hf., - 
30, mid. N. line N. E. a, 
31, N. W. corner, 
31, S. W. qr. of 8. W. ats 
32, near center 8. hf., 
32, mid. E. line 8. E. Bo 


36, center, - 
Watertown. T. 8, R. 15 EB. 
Watertown J unction, - - 
Sec. 21, mid. E. line 8. E. es - 
Waukesha. T. 6, R.19 E 
Waukesha Station, s 
Waukesha School House, - 


Feet. 
352 
400 


268 
859 


225 
243 


Junc. of Niagara and Racine pulse 250 
336 


Sec. 13, mid. N. E. qr., - 


GEOLOGY OF EASTERN WISCONSIN. 


Laxe Micuraan — continued. 
Waukesha. T. 6, R. 19 E.—(con.) a 


See. i mid. E. line, hill, - 


N. W. ar., creek, 305 
Wanpms. No 13, BR. 15 E, 
Waupun Station, - - - 314 
Horicon marsh, - - 280 
Wauwatosa. T. yee aa a E. 

Wauwatosa Station, - B 
Sec. 1, N. line N. KE. qr., - - 71 
1, N. line N. E. ar, R. B., 72 
1, mid. N. line, - 80 
1, N. line W. hf. N. W. ar., 69 
1, center N. hf. 8. W. qr., 83 
3, N. W. comer, - 123 
3, mid. W. line, 121 
3, 8. \% post, W. line 8.W. qr., 178 
3, near & Ww. corner, - 193 
8, E. line, plank road, 85 
4, mid. N. ine, - 160 
4, center N. E. qr., - 167 
4, mid. W. cc - - 161 
4, center N. E. 145 
4, mid. line, oud ‘du Tae Rd., 167 
5, mid. N. line, 142 
5, N. W. corner, - 150 
5, mid. W.line N. W. qr, 140 
6, N. une, river, 115 
7, N. line, Menomonee river, 104 
7, N. W. corner, 159 
7, mid. W. line, 174 
8, mid. N. line N. E. He, 155 
8, mid. N. line, - 161 
8, mid. N. line N. W. qr., 122 
8, N. W. corner, - 163 
9, mid. N. line N. E. qr., 172 
s a N. line, - 203 
N. W. corner, - - 169 

10 mid. N. line, - - 157 
10, N. W. corner, - 186 
10, mid. W. line, - - 217 
10, plank road, W. line, 199 
11, mid. N. line, - 118 
11, N. W. corner, 136 
12, N. line, R. R. 80 
12, mid. N. line N. W. a5 - 110 
12, N. W. corner, 104 
13, mid. N. line, 114 
1, N.E. qr., R. ne and plank r'd, 100 
13, N. W. corner, - 125 
14, mid. N. line, - 150 
14, N. W. corner, - 180 
15, N. line, Fond du Lac vane. 192 
15, mid. N. line W. hf. N. E. qr., 186 
15, mid. N. line, - 206 
15, mid. N. line’ N. W. aes 199 
15, N. W. corner, 174 
15, mid. W. line, 176 
16, mid, N. line, - 174 
16,N. W. corner, - 164 
17, N. line, river, - 100 
17, N. W. corner, - 139 
18, mid. N. line, - 159 
18, N. W. comer, 199 
19, mid. N. line N. E. as 186 
19, mid. N. line, - 180 


PLATE, VIA 


TOPOGRAPHICAL MAP OF MILWAUKEE CoO. 
by Chas, Lapham. 


pham 


WAUKE E 


| 


Nee 
| ~ LG : ae r) 4 
fr pe GAL A eas ) 


| Ai Brae a ee / 
| = | s 4 A a . Sh owe : 
iF: 


GREENER LD | 
2 i fell ase Aunt i‘ 


Se es His — anes 
PRANK Iu x A ph 


— |—— = f i SS 
a . tS os at 


TOPOGRAPHY. 127 


List or ELEvatTiIons above Lake Mrcuigan — continued. 


Wauwatosa. T.7, R. 21 E.—(con.) Feet. 
Sec. ee mid. N. line N. W. qr, - 7 


N. W. corer, - - 
19, mid. W. line N. W. a.» 
19, mid. W. line, - 
20; N. line, river, - 
20, mid. N. line, 4 = 
20, N. W. commer, : 
20, N. line S. W. qr., R. B., 
21, mid. N. line N. E. oy 


21, mid. N. line N. “Ww. as 
21; N. W. corner, 

21 W. line, R. Be - 

a1 mid. line, R. R., - 
29° mid. N. line, - - 
99° mid. N. line N. W. E-, 
93 N. W. corner, 

29° mid. W. line, - 


228 
218 


gy’ near center 8. W. qr., pl.road, 141 


93) N. line N. E. qr., plank r’d, 148 
93) mid. N. line, - - 169 
93, mid. N. line, N. W. aqv.. 179 
93, N. W. corner, - - 150 
93) W. line on Holston road, 115 
24 N. W. corner, : 140 
24, W. line N. W. qr.,plankr’d, 136 
24, W. line 8. W. ., ‘Wauwa- 
tosa road, 120 
24, W. line N.E, qr., Lisbon’ , 123 
24, R. R., Lisbon plankroad, 104 
26, center 8. E. qr., - 94 
26, W. line N. E. qr., 43 
27, N. line, R. B., 64 
27, E. line, Spring road, 116 
28, W. line, g ring road, 172 
28) mid. line, Spring road, - 113 
98) mid. N. line, 107 
28, center 8. E. qr., - 90 
99, W. line, Spring road, 207 
29, mid. line, le road, 195 
30, mid. line, Spring road, 226 
30, center 8S. W. qr., R. B., 163 
31, center, 175 
32, W. line, R. RK. - - 161 
32, center, R. R., - 195 
33, W. line, R. RK. - - 169 
34, W. line, R.R., - 125 
34, center, R. R., - - 144 
Wayne. T. 12, R. 18 E. 
Kohlsville, river, - 409 
Sec, 34, a S. line 8. E. as 590 
36, - 517 
36, re 8. line S. W. qr., dll 
West Bend. T. 11, R. 19 E. 
Barton village, 8. side, 461 
West Bend Station, - - 314 
Sec. 2, mid. S. line S. W. qr, - 461 
5, W. line N. W. qr. - 505 
10 N. E. qr., - - - 353 
14, N. line N. W. ar., - 330 
17, mid. N. line, - - 517 
18, mid. N. line N. E. qr., 564 
Westford. T. 12, R. 13 E. 
Head of Beaver ‘Lake, - - 282 


\ 


Westford. T. ss R. 13 E.—(con.) Feet. 


Sec. 1,8. BE. gq - 314 
6, 8. ines. W. ar., - 3872 

i, 8. line 8. W. qr., - 375 

19, enter E. qr, - - 298 

N. W. qr., stream, - 412 

on near conten, - - 330 

- 276 

26, and W. 4 - - 292 

30, near N. line N. W. qr., 378 

31, N. line N. W. qr, - 382 


81) near beniee Es hf., hill, 412 


34) 8. E. q 827 
Wheatland. i "S, R. ‘19 B. 

Sec. 29, mid. E. hf. - 206 

29, near 8. W. Somes, - 270 

31, near 'S. E. corner, - - 280 
Wheatland. T. 1, R. 19 E. 

Sec. = ape level, - 231 

. E. comer, - - 287 

? s E. cecrner, 268 
Whitewater. | T. 4, R. 15 E. 

Whitewater Station, - 241 

Whitewater Normal Hill, - 307 

Whitewater creek, 228 

Whitewater lake, - - 317. 

Sec. 2,58. E. qr., - - 242 

2,8. W. ar., 259 

4 E. hf., - - 249 

4, W. hf., - 232, 

19, N. hf., - - 297 

Wilson. a 14, R. 92 E. 

Sec. 5,8. line 8. E. qr., R. R. cross’g, 115 

5, near N. line R. R., - 133 

6, N. W. corner, general level, 131 

6, mid. N. line, kettles, 114 

&, N. line R. R. - 115 

17, N. line, R. R., - 105 

20, N. line, R. R., - 102 

30, N. line, RB. R., 109 

31, N. line, R. R.,  - - 102 
Woodville. T. 20, R. 19 E. 

Dundas Station, —- 160 

Stream 3 miles E. of Sherwood, 256 


R. RB. crossing 214 m. E. of Sherwood, 292 
Highland E. of Sherwood, - 318 
bie htstown. 
edge, - - 240 
Wrightstown village, - Bd 
Sec. 1, 5. E. qr., “highland, T. 21, 
20, 331 


R. 

8, mid. 8. line T. 21, R. 20, 154 

85, mid. N. line T. 22, R, 20, 382 

35, mid. EK. line T. 22, R. 20, 292 

35, S. E. qr.. swamp, T. 22, R.20, 284 

Yorkville. T. 3, BR. 21 E. 

Sec. 10, 8. W. corner, Root Tver, 128 
11, 8. W. corner, 188 

11, mid. 8. line, branch Root R., 155 

12) 8. W. ar., Ives Grove, 20-4 


26, N. E. qr., 207 
27, N. E. qr., - Li7 
28, mid. E. hf., - 187 
29, 8S. E. qr., 164 
80, Union Grove, - 108 


128 GEOLOGY OF EASTERN WISCONSIN. 


CHAPTER IL 


HYDROLOGY. 


Drainage. On the average, about 165,512,000,000 barrels of water 
fall annually upon the district under discussion. Of this, about one- 
half is lost by evaporation and absorption, and the remainder runs 
away, constituting the drainage of the district. Were the slope of 
the surface much increased, the water would be discharged so rapidly 
as to do much permanent damage by erosion and the rapid removal of 
our fertile soil. Were its inclination much less, the drainage would 
be imperfect, and our noble water powers destroyed. In the golden 
mean presented, a mutual adaptation to the twin industries, agricul- 
ture and manufacture is fortunately secured. The drainage of the 
region forms part of two great systems, the Mississippi and the St. 
Lawrence. Perhaps one-fourth belongs to the former and the remain- 
der to the latter. 

The watershed between these systems is very peculiar. On the 
Illinois line, the divide is within three and one-half miles of Lake 
Michigan, and is only 160 feet above that body of water, while the 
surface to the west continues to rise by undulations to 400 feet and 
upwards. A little north of the state line, several of the streams, no- 
tably the White river, the outlet of Lake Geneva, flow to the north- 
east, and yet reach the Mississippi. 

From the state boundary, the line of the watershed pursues a north- 
westerly course, becoming more and more elevated till it passes the 
Kettle range at about 500 feet above Lake Michigan, whence it con- 
tinues still to the northwest till it suddenly drops 200 feet into the 
Green Bay and Rock river valley, whence it curves more to the west, 
until, on the highlands of Metomen, at about 400 feet elevation, it 
turns abruptly southward, giving rise to another anomaly. The 
streams that here flow east discharge into the Mississippi, while those 
that flow west empty into Lake Michigan. Following the watershed 
onward from this point, it gradually curves to the westward, descend- 
ing to the portage between the Fox and Wisconsin rivers, where its 
elevation is little more than 200 feet. From thence it pursues a 


HYDROLOGY. 129 


northward course to the highlands of Michigan. A section along the 
line of the watershed across the Green Bay and Rock river valley, 
would exhibit its peculiarities almost as conspicuously as if taken at 
any other point, and so, to almost the same extent, would a projection 
of the whole line exhibit the valleys, slopes and ridges that constitute 
the salient topographical features already described. It is evident 
then, that the present drainage systems are not the cause of these 
features. 

At some points the elevation constituting the watershed is so slight 
as to be scarcely perceptible. A notable example of this is found in 
Racine county, in the relations of the head waters of the Eau Pleine 
river, a tributary of the Mississippi, and those of the Root river that 
flow into Lake Michigan. Both have their rise in an extended marshy 
valley, so nearly level that it is at times very difficult to determine 
which way the water flows. On the county and state maps the divide 
is placed seven miles from the point where it was at the time of my 
visit. 

The Mississippi basin is represented in the district by the Rock 
river system, comprising that river and its tributaries, and the [linois 
river system, embracing the (Illinois) Fox river and the Ean Pleine 
river, with their branches. 

The St. Lawrence basin includes the Lake Michigan system, of 
which the principal streams are the Root, Milwaukee, Sheboygan, 
Manitowoc, Twin, Kewaunee and Ahnapee rivers, and the Green Bay 
system, to which the important Fox, Wolf, Oconto, Peshtigo and Me- 
nomonee rivers, with several minor streams, belong. 

A moment’s attention to the courses of these streams reveals many 
striking peculiarities, for most of which, upon careful study, there is 
an obvious cause. Some of these are worthy of special attention, not 
only from the inherent interest which they possess, but because they 
illustrate the dependence of such important features as rivers, which 
often determine the location and relations of great business centers, 
upon surface geology. 

Beginning at the south, the streams of Walworth and adjacent 
counties on the east first claim attention, and form an interesting 
group, most conspicuous among which are White river, Sugar creek 
and Honey creek. These streams all flow in an easterly or northeast - 
erly direction for a distance, and then abruptly turn south, uniting 
with each other, and at last joining the Fox river, which continues 
south until it unites with the Illinois river, through which its waters 
finally discharge into the Mississippi and the Gulf. All the group 
oceupy deep parallel valleys in the upper part of their course, and it 

Wis. Sun. —9 


130 GEOLOGY OF EASTERN WISCONSIN. 


is only when they debouch into the lowlands of the Fox river that 
they turn southward. 

The contour of the adjacent country forbids the supposition that 
these valleys were excavated by simple drainage erosion. Their di- 
rection corresponds to that of the drift movement to which they are 
undoubtedly due. They bear the distinctive marks of troughs, up 
which the ice mass moved from the northeast, as will be explained 
subsequently. On either hand there are vast accumulations of drift, 
heaped up in the form of an irregular moraine, or of rounded hills and 
parallel ridges. When the streams reach the lower land, they follow 
southward along the foot of the drift hills, in what was formerly, to 
some extent at least, the bed of an elongated lake. 

It is noticeable, also, that the numerous beautiful lakes of this re- 
gion fall into line along these glacial valleys, and owe their existence 
to the same general cause. 

The Pike river in Kenosha county is but an insignificant stream, 
but its course is very instructive. In the upper portion it flows in a 
meandering manner toward the lake in the direction of the general 
slope of the surface. But when within about one mile of the lake 
shore, it turns abruptly southward and runs parallel to it for about 
four miles. It formerly extended farther, but the encroachment of 
Lake Michigan cut across the narrow tongue of clay that separated 
the river from it at one of the bends just above Kenosha, and allowed 
the stream to discharge at that point. Dut the old gorge reénters the 
shore bluff farther down and again joins the lake at Kenosha harbor. 
Drs. Lapham and Hoy have both previously called attention to this 
interesting instance of lake encroachment. 

At the point where the stream now discharges, a sand bar is formed 
which turns it southward. With a single unimportant exception, all 
the streams, great and small, along the Wisconsin shore of the lake, 
so far as they have come under my observation, are turned to the 
southward, in a similar way, by an accumulating bar at the mouth. 
This fact has heretofore been remarked by several observers. 

It is noticed also that where piers are extended into the lake, the 
sand rapidly accumulates on the north side, forming “made land,” 
while that which collects on the south side is inconsiderable. 

These facts show clearly that the drift along the present shore is to 
the southward and would seem to warrant us in saying that there is a 
southward lake current along the Wisconsin shore. This furnishes 
the key to the explanation of the course of the Pike river. Formerly 
the lake stood relatively about 50 feet higher at this point than it now 
does and extended inland beyond the position of this portion of the 


HYDROLOGY. 131 


‘Pike river, and left its record in a low beach ridge. The Pike river 
seems, at that time, to have discharged directly into the lake, and it 
would appear that there was then as now, a southerly current which 
forced the stream southward by the formation of a bar and gave it 
its present course. The gorge it now occupies, it has since cut from’ 
the yielding clays. This little river then seems to teach us something 
of the past history of Lake Michigan, and since the present shore cur- 
rent is believed to be due to the prevailing direction of our winds, it 
perhaps also teaches us something of ancient meteorology. 

The course of the Milwaukee river is even more interesting. It 
originates chiefly in Fond du Lac and Sheboygan counties from a 
number of nearly parallel southward-flowing streams, which gradually 
unite to form the main river. At West Bend it turns abruptly east- 
ward. After passing Newburg it makes a rude sigmoid flexure to 
the north, and resumes its eastward course. When within about nine 
miles of the lake, it bends suddenly to the right and flows almost di- 
rectly south parallel to the lake shore for more than 30 miles, being 
distant from it at some points in its course less than two miles. It 
really then consists of three portions: the southward-flowing parallel 
branches, the eastward-flowing portion, and the main trunk flowing 
south as last mentioned. The course of the river in each of these 
three parts requires a different explanation. 

The parallel branches occupy so many valleys enclosed by the ridges 
of the Kettle Range which here develops a more than usual parallel- 
ism among its component ridges. At the occasional breaks in these 
ridges, the streams find the means of uniting. 

At West Bend, where by taking advantage of these interruptions 
the united stream has reached the east flank of the Kettle Range 
proper, its course is intercepted by an east and west valley, attended 
with “kettles” and serpentine ridges, and corresponding to the direc- 
tion of drift movement, in short, a glacial valley. This, the stream 
follows to the vicinity of Newburg, when it passes across to a parallel 
valley on the north. These two east and west valleys are entirely 
analogous to those in Walworth county, already mentioned; indeed, 
they belong to one system of topographical features, occupying more 
or less conspicuously the whole territory between them, and due to the 
same glacial action. 

Near the great bend, in the town of /’redonia, the stream reaches an 
ancient beach line, which marks the shore of the lake at the time of 
the deposit of the Lower Red Clay, yet to be described. The river 
follows along this beach line to its mouth at Milwaukee. The con- 
clusion can scarcely be avoided then that it owes its course to this re- 


132 GEOLOGY OF EASTERN WISCONSIN. 


lationship, and that the explanation is the same as that given for Pike 
river—and that the same inference as to a southward lake current is 
justified. 

We have a similar phenomenon in connection with the east mem- 
ber of Two rivers, or the Last Twin river, which marks, though 
much less definitely, the western limit of the Upper Red Clay, follow- 
ing in a similar way the sandy beach deposit, that marked the shore 
line of the lake at the time of its formation. It would seem then that 
as far back as we can trace the history of the lake, by these means, it 
has had a southward-flowing shore-current along the Wisconsin side. 

The courses of several other streams belonging to the Lake Michi- 
gan system are to be explained in a similar way. 

The upper portions of the Wolf, Oconto, Peshtigo and Menomonee 
rivers are essentially similar to each other. Rudely parallel among 
themselves, they flow in the direction of the general inclination of 
the surface, exhibiting nothing peculiar while they are passing over 
the region of the granitic and other Archean rocks, but after en- 
tering upon the territory underlaid by Paleozoic formations, their 
several directions become exceptional. 

The Oconto river, after flowing parallel to the Wolf for thirty-five 
miles, turns at a right angle to the east, and flows directly to Green 
Bay, while the Wolf river continues straight on its course for thirty 
miles, when it turns with equal abruptness to the west, afterwards 
more gradually to the south, and then east, and at Lake Winnebago 
its current is reversed and flows northward, so that after a circuit of 
about 140 miles, it reaches the mouth of the Oconto and mingles with 
its waters, which have only traveled thirty miles since the rivers part- 
ed company. 

The distance between the Wolf and Oconto where this divergence 
takes place is only about twelve miles, more than half of which is oc- 
cupied by Shawano Jake and its outlet, and only drift accumulations 
of no very considerable magnitude make up the divide. 

The Ifenomonee and Peshtigo rivers make similar abrupt changes 
in their direction. 

By referring to the map, showing the geological formations of this 
region, the explanation of these anomalies becomes at once apparent. 
It will be seen that the boundaries of the formations are zig-zag, or 
step-like, and that the rivers follow the softer formations along the 
face of these steps. 

The Wolf rwer, from Shawano south, follows along the nearer or 
more remote cliffs of the Lower Magnesian limestone, its bed lying in 
the soft Potsdam sandstone, until in the town of Ellington, along the 


HYDROLOGY. 133 


line of an apparent fault, the limestone is brought athwart its course, 
and it turns to the west, still following the face of the Lower Magne- 
sian cliffs, until they turn southward in the town of Mukwa, when the 
river curves in the same direction, and at length in the bed of Poy- 
gan lake and the basin of the: Fox river, it finds its way across the 
obtrusive formation. Its waters then reverse their course and flow 
back along the face of the projecting cliffs of the Niagara limestone 
for a hundred miles, when Porte des Morts allows thei to escape into 
the great lake, at a point not half the distance from their source that 
they have traveled. 

The Oconto river, on the contrary, on encountering the resisting 
Lower Magnesian limestone, turns sharply to the east and flows along 
the north face of the formation for some distance, when it forces its 
way across it, forming the beautiful falls of the Oconto, and keeps 
directly on its course to the bay. The falls are occasioned by a soft 
shaly stratum near the middle of the formation, there being hard, 
heavy bedded layers of dolomite above and below. The softer stratum, 
being more easily eroded, permits the water to undermine and throw 
down the heavy beds above it, thus keeping tbe face of the cliff verti- 
cal and causing the falls to slowly recede. The perpendicular fall is 
about twenty-two feet, with a considerable descent upon the rapids 
above and below. 

The deflection of the Menomonee river to the eastward (town 33, 
ranges 21 and 22 E.) is to be attributed to the barrier interposed by 
the same formation, though in this instance it is far less conspicuous, 
as the formation does not immediately adjoin the river on the south, 
nor does it anywhere in the vicinity project in mural cliffs, according 
to its habit, to the southward. Yet its influence on the drift accumu- 
lations is apparent, and it is none the less the cause of this deviation 
of the river from its general course. At Grand Rapids the river 
crosses the formation, the rapids being due to the same cause as the 
falls of the Oconto. The shaly stratum is here harder, however, and 
the layers above less massive, making the resisting power of the two 
portions less different, so that the result is a series of rapids instead 
of vertical falls. Immediately on passing this barrier, the beautiful 
river recurves to the south, indeed to the west of south, and follows 
the horizon of the St. Peters sandstone, having the Trenton limestone 
on the east, until within about eight miles of its mouth, where it 
crosses the latter formation by a succession of rapids. It is true that 
between the Grand Rapids and those last mentioned, neither the St. 
Peters sandstone nor Trenton limestone appear as obvious barriers, 
the channel of the stream being excavated in drift, but there is good 


134 GEOLOGY OF EASTERN WISCONSIN. 


reason to believe that the original surface of the drift, which controlled 
the direction of the stream, was determined by these underlying 
formations, and that they are none the less truly, though remote- 
ly, the governing influences. This view of the case is supported by 
the unquestionable facts relating to the similar detour, though 
in an opposite direction, of the Peshtigo river at a point nearly op- 
posite. 

Although perhaps more than usually winding in its minor features, 
the general course of the Peshtigo river is exceptionally direct, and 
almost exactly southeast. The only noteworthy deviation is that to 
which attention is now called. From the outlet of Lake Noqueba, its 
course is nearly due south until it crosses the western edge of the 
Lower Magnesian limestone near the third correction line, when it 
immediately sweeps round to the north of east, and flows nearly at 
right angles to its general course for about nine miles, approaching 
the Menomonee within less than three miles, when it reverts to its 
southeastward course. 

Throughout this northeasterly course, it is flanked on the south- 
east by a wall of Trenton limestone and St. Peters sandstone, the for- 
mer appearing at points in naked ledges left projecting by the disin- 
tegration of the latter. The present bed of the stream is excavated 
below the horizon of these formations, and lies in a trough cut from 
the Lower Magnesian limestone, for the greater distance. But the 
dip of the formations to the eastward is greater than the descent of 
the stream, so that it is finally enabled to surmount them at Potato 
and White rapids, when it returns to its original direction. 

The controlling influence of this barrier is also shown to the south- 
ward in the courses of the “ Little river” of the Peshtigo, and the 
“Tittle river” of the Oconto. 

Perhaps the conjecture may be ventured that the Peshtigo and Me- 
nomonee rivers, before the drift period, united near their point of 
nearest approach on the west side of this limestone barrier, and passed 
it through a common, but now drift-filled and concealed, channel, for 
it is abundantly evident that they did not then pass it, at the same 
points they now do, and this vicinity appears to present the lowest 
point to which the western edge of the Trenton limestone is depressed 
within the basin of these rivers. 

On the flats below the village of Peshtigo, the tortuous course of 
the river reminds us of the Asiatic Meander. 

If the limitations of our space allowed us to go more into detail, 
and to examine the minor streams, we should find equally instructive, 
though less conspicuous, phenomena. We can find room for only one 


HYDROLOGY. 135 


example, that of the Last Branch of the Rock river, which joins the 
main stream in Horicon marsh. 

This river has its source in a broad, deep valley, extending from the 
southeast to the northwest (about N. 30° W.) for a distance of up- 
wards of 20 miles. In the towns of Wayne, Theresa, and Lomira, the 
width is from one to two miles between the foot of the hills that rise 
somewhat abruptly on either side. The valley is occupied very ex- 
tensively by marsh. Branches from the north and south unite near 
the center and form the main stream, which taking a direction nearly 
at right angles, and pursuing a serpentine course among the parallel 
north and south ridges of this region, finally discharges its waters 

‘into Horicon Marsh, thus forming a rude italic 7, the upper portion. 
being formed by the branches first mentioned. These branches are 
not large, nor is the area drained by them considerable. The valley 
which they occupy may be traced onward to a northward connection 
with the valleys crossing the ledge in Byron. 

It is scarcely credible that this valley with all its peculiarities was 
due to the unaided erosion of the streams occupying it. Though par- 
tially filled with drift accumulations, it is really channeled from the 
Niagara limestone, which distinguishes it from the class last under 
consideration, where the essential condition was two formations of 
different resisting power. In explaining its origin we must again 
have recourse to glacial action. We find that the drift movement was 
southward along the axis of Lake Winnebago, but on surmounting 
the ledge on the east and south, it turned somewhat eastward and fol- 
lowed down the slope of the surface and dip of the rocks, eroding fur- 
rows that have a southeasterly trend. One of these is the valley in 
question, which is doubtless more extensive and well defined than the 
adjoining ones, because it lies south of Lake Winnebago, that is, more 
nearly in the line of heavy glacial action. The angle in the ledge just 
north of it doubtless contributed to the same result. 

Relationship of some of the streams on opposite sides of the 
Kettle Range. One further feature relating to certain streams and 
their attendant topography deserves notice. It consists of a certain 
peculiar and definite correlation between the streams on the east and 
west sides of the great dividing drift ridge. 

Where an extended ridge-like watershed exists, it is to be expected 
that streams on the opposite sides will rise near each other and flow 
in opposite directions, at right angles to the ridge, but in the present 
instance they are arranged én pairs, and connected across the summit 
by more or less well defined valleys, so that the relationship cannot 
be looked upon as being merely fortuitous. 


136 GEOLOGY OF EASTERN WISCONSIN. 


My attention was first called to those in Walworth county some 
years since by Dr. H. Hunt, of Beloit. The fluvial pairs and the 
essential facts are briefly as follows: . 

1. Geneva Lake and Big Foot Prairie, in Walworth county. The 
bluffs on either side of Geneva Lake rise upwards of 100 feet above 
its surface, but at its head the valley extends westward, though much 
narrowed, and joins the more elevated level area, known as Big Foot 
prairie, whose present drainage is southwestward, the watershed being 
on its margin next Geneva Lake, and less than two miles from it. 
The surface is more elevated on either side of the prairie, which bears 
evidence of having formerly been occupied by a lake. 


2. Delavan Lake and the White river, in Walworth county. The 


valley of Delavan Lake is very similar to that of Lake Geneva, but 
it lies on the western slope. From it a well defined valley extends 
across the divide and connects with the valley of White river, but the 
elevation of the summit is greater than in the previous instance. 

3. Turtle creek and Sugar creek, in Walworth county. The head 
waters of Turtle and Sugar creeks are connected by a narrow band of 
marsh, bordered on the south by a line of bluffs, and on the north by 
amore gentle ascent. Its whole aspect is that of a fluvial flat. 

4. The Bark and Oconomowoe rivers and the branches of Cedar 
creck, in Washington county. These streams constitute a double pair, 
each of the rivers rising in a marshy valley in very close association 
with the headwaters of Cedar creek, the elevations separating them 
being very slight. 

5. Rubicon river and the northern branch of Cedar creek, in 

Washington county. Between Cedar lake and the headwaters of the 
Rubicon river lies an elongated marsh, occupying a notable depression 
in the otherwise elevated ridge. 

These facts naturally suggest the question, Did the streams on the 
east side formerly flow across the present summit, or was the reverse 
the case; or, again, are these facts to be otherwise explained? In 
answer, it is to be remarked, in the first place, that the watershed in 
question is either formed by, or is closely related to, the great drift 
ridge previously described, and that this, as I shall hereafter attempt 
to demonstrate, is a moraine, formed as an accumulation along the foot 
of an immense sheet of moving ice. If this can be clearly pictured to 
the mind, it will at once become evident that the waters from the melt- 
ing ice mass must find their way across the accumulated drift, and as 
the amount of water discharged must have been immense, deep valleys 
would be ent at intervals of no great distance. This is probably the true 
explanation of the initial formation of these valleys across the summit. 


HYDROLOGY. 137 


3) 


Origin and Geological Relations of the Lakes of Eastern Wis- 
consin. Analogous to the topics which have been under discussion, 
is the consideration of the position and cause of the numerous lakes 
which lend their attractions to the beautiful scenery of this portion 
of the state. 

It has already been said that the great lake on the east lies in a 
basin excavated chiefly from the soft rocks of the Devonian age, and 
that its western edge rests upon the Upper Silurian limestone along 
the trend of which it lies. The fact that its bottom lies three hun- 
dred feet below the level of the ocean, shows that it could not have 
been eroded by running water in its present position; and its width 
and the regular contour of its bottom forbids the supposition, even if 
the proper elevation and slope were givenit. The drift on its margin 
contains material that there is every reason for believing came from 
its bed, and the polishing and grooving of the rocks that form its 
rim show that it has been the theatre of powerful glacial action, and 
to this cause its present regular outline and great depth and breadth 
are undoubtedly due. That it may have been deeply channeled by 
running water before the glacial period, and that such channels may 
have had a directing power over the subsequent and more powerful 
glacial action is not improbable. The fact that it lies within seventy 
miles — less than its own breadth — of a region where the drift action 
was very slight, and the preglacial contour of the surface was not 
more than slightly modified, a region whose present elevation is less 
than three hundred feet above the lake surface, and beyond which the 
drift shortly disappears entirely, lends support to this view. 

Green Bay, Lake Winnebago and the former Lake Horicon oc- 
cupy portions of a similar glacial channel, and owe their origin to 
slight drift obstructions thrown across the valley. The fact that Lake 
Winnebago discharges through a channel having a rocky bottom does 
not militate against this statement, for the real channel of the valley 
is nearer Clifton, on the east side of the lake. The drift blocks this 
up, and the lake pours over a low rock barrier that separates it from 
the parallel valley of Butte des Morts, which occupies a lower geolog- 
ical horizon. 

Were the drift removed, a channel between Menasha and Clifton 
would, without question, drain the lake. 

Lake Horicon was originally confined by drift, which, in time, by 
its own outflow, was cut away. Its place was subsequently supplied 
by an artificial dam, which restored the lake. This, again, was re- 
moved, and the area is now a marsh. 

Lake Poygan seems to have been excavated by glacial action, 


138 GEOLOGY OF EASTERN WISCONSIN. 


chiefly from the yielding Potsdam sandstone, the direction of drift 
movement being here to the westward. It is probable that a river 
channel existed there previously, which enabled the ice to act with 
greater efficiency. 

Green Lake, Puckawa Lake and Rush Lake all lie in one valley 
along which the glacier plowed its way. Rush Lake was eroded from 
the sort St. Peters sandstone, having the harder Lower Magnesian 
limestone for its bed, while the Trenton limestone borders it on the 
east. The rise that separates this from Green Lake is scarcely per- 
ceptible. The east end of the latter lake occupies the same geological 
horizon, but the dip of the strata is such at this point that, in its 
length, the lake cuts across the Lower Magnesian limestone, the Mad- 
ison sandstone, the Mendota limestone, and into a still lower division 
of the Potsdam sandstone. At the west end it is confined by a range 
of drift hills crossing the valley. To these this beautiful lake may be 
said to owe its existence. If they were removed, the lake would dis- 
charge itself into Lake Puckawa, to the west, its elevation being the 
greater. The contour of these hills shows their morainic character 
and indicates that they were heaped up there by the tongue of ice that 
filled and in part eroded the valley. 

Lake Puckawa was eroded in the same way, but from still lower 
strata. On its south side there rises a cluster of hills of Archean 
rocks, which, by their hardness and powers of resistance, may have 
forced the ice mass to more deeply erode the softer sandstone repos- 
ing on their flanks. 

Lake Shawano lies along the northern base of an east and west line 
of bluffs capped by Lower Magnesian limestone resting upon Potsdam 
sandstone, from which the basin of the lake has been excavated. Its 
longer axis harmonizes with the direction of glacial movement, which 
in this region was from the east to the west. We have, then, an 
easily eroded stratum, adjacent to a more resisting one, with a com- 
petent eroding agency acting in a favorable direction, resulting in the 
formation of Lake Shawano. 

Lake Koshkonong likewise lies in the direction of glacial progress 
and is due to the ease with which the St. Peters sandstone was exca- 
vated. An ancient stream had probably cut down to and perhaps 
through it—for such is the fact in reference to the preglacial Rock 
river channel farther south—and the ice plow, taking advantage of 
this, furrowed and filled, leaving a wide, shallow basin. 

The foregoing lakes, it will be noticed, have a definite relationship 
to the geological formations adjacent and subjacent to them, and are 
all to be accounted for on essentially the same principle, viz.: The un- 


HYDROLOGY. 139 


equal hardness of the strata acted upon by a powerful excavating 
agency, that, unlike rivers, did not carry away its rubbish as fast as 
formed, but heaped it up promiscuously in its own track as it melted 
backward, the inevitable result being the formation of lakes along its 
abandoned channels. 

The number originally thus formed was vastly greater than the 
number now in existence, the great majority having cut down their 
own barriers and drained themselves. 

These may then be said to be glacial lakes, for there is no reason 
to suppose that any one of those described, existed before the drift 
period. But as the most of them were probably represented as river 
valleys or gorges, and as their present existence is due also to the un- 
equal powers of resistance of the rock formations, this class of lakes 
is not entitled to be termed glacial lakes in the same sole-dependent 
sense as the following, the most of which show little or no relation- 
ship or dependence on the underlying strata, but are drift lakes in an 
exclusive sense, 

The class now to be described may be subdivided into two subordi- 
nateones. The first are those which lie in valleys, whose greatest length 
is in a line with the glacial grooves, and in this respect are like the 
last class, differing from them only in being independent of the strata 
beneath. These were formed in drift troughs by the retreating 
glacier, very much as the class above described were, only the troughs 
are not excavated rock channels, but valleys, between drift ridges. 

The other kind are those whose greatest length lies at right angles 
instead of parallel to the glacial grooves. 

These lie between the ridges that accumulated at the foot of the 
glacier and which were rudely parallel to each other, yet sometimes 
joining mutaally, and again separating to a considerable interval, they 
left enclosed hollows, which on filling with water, became lakes. 

We would perhaps be justified in being even more specific than we 
are in calling these drift lakes, by designating them morazne lakes. 

From the nature of the case, forms intermediate between all the 
foregoing are to be expected, and are found to occur, and with the gen- 
eral explanations given, it will be needless to designate in the case of 
each of the numerous small lakes, the precise method of formation, 
although it is, in most cases, sufficiently clear. 

More than one hundred of these lakes lie along or adjacent to the 
Kettle Range, and form an important element of its picturesque 
scenery. Among the most noteworthy are Geneva, Delavan, Como, 
Turtle, Bass, Holdens, Otter, Silver, Pleasant, Green and the Troy 
lakes in Walworth county; Mary, Elizabeth, Camp and Silver lakes 


140 GEOLOGY OF EASTERN WISCONSIN. 


in Kenosha county; Wind, Long and Brown’s in Racine county; 
Muskego, Pewaukee and that beautiful cluster known as the Ocono- 
mowoc lakes, about forty in number, in Waukesha county; Cedar, 
Little Cedar and Silver lakes in Washington county; Long and Leound 
lakes in Fond du Lae county; Likhart and Bear lakes in Sheboygan 
county, and Cedar, Pigeon and Wilke lakes in Manitowoc county. 
Lock lake in the town of Lake Mills, Jefferson county, and Clear lake, 
near Milton, Rock county, belong to the same category, though un- 
connected with the main chain of the Kettle Range. 

Of the foregoing, Muskego, Wind and several smaller lakes asso- 
ciated with these, bear evidence of having formerly constituted parts 
of a much more extensive body of water, that leveled by erosion and 
deposition the original uneven surface in their vicinity, so that its 
primitive drift features disappeared and with them the corresponding 
features of those lakes, so that they do not now present those charac- 
teristics which are common to the majority of the others. 

There is also some evidence that the comparatively level area in 
which the Oconomowoc lakes are embosomed was, immediately after 
the glacial period, occupied by an extensive lake that reduced the gen- 
eral surface to its present degree of uniformity by washing down pro- 
jecting points, while it was unable to fill the present lake basins, they 
being below the line of its wave action. 

The value of the lakes of eastern Wisconsin is much greater than 
is sometimes apprehended. Beauty is not an unimportant element of 
value. Attractive scenery adds materially to the worth of both rural 
and urban property. 

The wealth of eastern Wisconsin has been materially increased dur- 
ing the last decade, simply through the charm of its beautiful lakelets. 
Thousands of citizens of other states have visited them, and large ho- 
tels and beautiful summer residences have been erected as substantial 
tokens of the enduring admiration which these gems of nature have 
awakened. 

The salutary influence which they exert over the people of our own 
state by tempting to healthful recreation and by the cultivation of 
esthetic tastes is scarcely to be estimated. 

To those who admire a broad expanse of water, Lake Winnebago, 
with its cliffs on the one hand and its wooded plains on the other; 
Green Bay, with its rocky battlements on the right, its forests on the 
left, its viewless limits on the north, its islands and harbors, and, par 
excellence, the oceanic Lake Michigan present their varied attrac- 
tions. 

Among the smaller lakes that have been accorded the greatest meas- 


HYDROLOGY. 141 


ure of admiration, attention may be called to the deep, clear waters 
and wooded, gravelly shores of the picturesque Geneva, the charming 
variety of the two score lakelets of the Oconomowoc cluster, the em- 
erald waters and picturesque glens and cliffs of Green Lake, the ro- 
mantic little Hikhart,a gem ina rustic framework of wooded drift 
knolls and kettles, and the quiet, restful beauty of Rock, Brown, Clear 
and Delavun lakes. Lakes Koshkonong, Pewaukee, Puckawa and 
others are favorites with sportsmen. 

These lakes abound in a variety of excellent fish, and are the resort 
of large numbers of water-fowl. Through the labors of the state fish 
commissioners, and the enlightened and generous action of private 
citizens, some of them have recently been stocked with choice varie- 
ties of fish from other waters, and it is confidently believed that they 
will, under a continuance of this enlightened policy, render a hand- 
some contribution of excellent food in return. 

Their value as water power reservoirs, though not as yet appreci- 
ated, will, in the unfoldings of the resources of this region in the 
future, perhaps surpass both the considerations above mentioned. 
This point will receive brief consideration under the head of water 
power, a few pages in advance. 

Water Supply. The surface soil possesses, on the average, a fair 
degree of absorptive power, and the underlying strata, both of the 
drift and rock formations, consist of alternating pervious or impervi- 
ous layers, thus presenting suitable conditions for an excellent water 
supply. A less absorptive soil would cause a greater proportion of 
the rainfall to be lost by surface drainage, and a uniformly porous or 
uniformly impervious rock structure beneath would be less favorable 
to frequent springs or veins of water that could be reached by wells. 
As it is, there are few localities at which an abundant supply of water 
cannot be reached at moderate depths. 

Attention will here be chiefly confined, however, to the natural 
sources of supply provided in springs. To casual observation these 
appear to be scattered promiscuously over the region, without any 
definite geological relations, but such is not the fact. There are two 
general systems of springs, those that originate in the drift deposits, 
and those that flow from the rock. The springs of each group occu- 
py several different horizons, which it will be interesting to notice 
briefly, as the subject is one of great importance. It is estimated by 
some authorities that one-third of the diseases which afflict mankind 
are due to the use of impure water. Though this estimate may be 
too high, it is abundantly demonstrated that some of the most terrible 
diseases are directly attributable to this cause. If unaided nature has 


142 GEOLOGY OF EASTERN WISCONSIN. 


provided us any means of escape from this prolific source of danger, 
it is quite certain to be found in our deep seated springs. 

There are several reasons why spring water is more likely to be 
pure than that of wells. On the average it comes from greater depths 
and has passed through a greater extent of the deeper strata which 
are comparatively free from organic impurities, than has the water 
of wells, which is usually drawn from the surface of the water level be- 
neath the location of the wells. Artesian fountains are not here taken 
into account. The water of wells is usually stagnant, while that of 
springs is active, “is living water.” 

There are some exceptions to the first part of this statement. Oc- 
easionally a well is sunk upon an active, flowing, underground stream, 
in which case the superior character of the water will usually be very 
marked. The water of springs is not liable to so many sources of 
contamination, and they more readily discharge impurities that may 
-find their way into them. In view of these facts, the study and utili- 
zation of the numerous springs of the state become of much im- 

portance. So far as possible all cities should be supplied by water 
from springs or Artesian wells. 

The lowest noteworthy horizon from which springs arise is the 
vicinity of the junction of the Potsdam sandstone and the Lower 
Magnesian limestone. The water from this source usually has a 
temperature of 48° to 50°, and is clear and comparatively free from 
organic impurities, but contains a small percentage of the carbonates 
of lime and magnesia, and in some cases a very small percentage of 
iron, with usually some silica, alumina and chloride of sodium. But 
the combined amount of these is small, and the water is “‘soft,”? and 
very pleasant to the taste. A small amount of free carbonic acid is 
usually present, which enhances the grateful effect of the water upon 
the palate and stomach. The springs from this horizon are not nu- 
merous. Jfitchell’s spring near Berlin is a fine example, and deserves 
the attention of the people of that place as a source of pure water for 
domestic purposes, and as furnishing favorable conditions for trout 
raising. Another notable spring of this class lies near the road be- 
tween New London and Hortonville (S. W. } of N. W. 4 See. 28, T. 
32, R. 15 E.), which is very much superior to the water from the 
drift wells of those places. 

Above this horizon springs occur but rarely till we reach the jwne- 
tion of the St. Peters sandstone with the Trenton limestone. Some 
shaly impervious layers mark this division, while the limestone above 
is fissured and the sandstone below is porous. It hence follows that 
the springs may arise either above or below the impervious stratum 


HYDROLOGY. 143 


according to circumstances. (1) Water descending from above may 
be caught and carried out where the strata are cut across to the proper 
depth; and (2) water that gained access to the sandstone at some dis- 
tant and more elevated point may rise from below at places where the 
confining stratum is removed. So that it is proper to include in this 
group some that issue from ledges somewhat above or below the june- 
tion of the formations. These springs are similar in general character 
to the last, but usually contain a more considerable percentage of the 
several mineral ingredients, at least that portion of them that are de- 
rived from the limestone, which still retains traces of many of the 
salts that we have reason to suppose were incorporated with it when 
it was formed beneath the ancient ocean. 

To this class belong most of the springs that issue from the rock in 
the western half of the counties of Rock, Jefferson, Dodge and Fond 
du Lac. Though differing among themselves, they are, as a class, of 
most excellent quality, and should be substituted for the well water 
of those regions, so far as practicable. 

A number of springs in the vicinity of Beaver Dam issue from 
near the junction of the Trenton with the Galena limestone; and at 
other points, streams issue from the latter formation, but they do not 
seem to be confined to any single stratum, and there is nothing in the 
nature of the rock to ead us to expect any well marked system. 

By far the most remarkable water-bearing horizon is found at the 
upper surface of the Cinninati shales, the dividing plane between 
the Upper and Lower Silurian formations. The upper part of the 
shale is little else than a stiff, compact, blue clay, and is the most im- 
pervious stratum in this portion of the state. Above it there lies a 
varying thickness of fissured, cavernous Niagara limestone, through 
which the water descends till its progress is arrested by the clay from 
the surface of which it flows out wherever opportunity offers. Along 
the east side of the Green Bay and Rock river valley, the junction of 
these strata is exposed at frequent intervals for one hundred and fifty 
miles, so that hundreds if not thousands of springs, great and small, 
mark this horizon. When a heavy mass of drift clay lies against the 
line of junction, the water sometimes issues from layers of the lime- 
stone, several feet higher, and where much loose rock has fallen from 
the cliffs above, the stream runs in a concealed channel down the 
slope, and appears to issue scores of feet, sometimes, below its true 
point of exit from the strata. Yet; notwithstanding these facts, with 
proper caution, the point at which the clay and limestone join, even 
when concealed, may be traced approximately by this line of springs. 

Many of these fountains are very large and strong; indeed, some 


144 GEOLOGY OF EASTERN WISCONSIN. 


of them are rather to-be conceived as streams, issuing from the rock 
full fledged, than as the bubbling source of a rivulet, implied by the 
term spring. In some places they furnish, without further augmen- 
tation, sufficient power for efficient flouring mills. In one case two 
mills are supplied by using the water in succession, within one-half 
inile of the source. 

The quality of the water of this class varies more than that of the 
preceding, owing, as it may be conjectured, to the greater or less 
effect of the shales upon it. These contain organic matter, iron py- 
rites, and other ingredients which on exposure indicate their unsta- 
ble chemical nature, by changes of color and otherwise, and, by so 
doing, warrant the belief that they sometimes make unfavorable con- 
tributions to the stream in contact with them. The water of most of 
them, however, is clear, cool and refreshing, and in character very 
similar to those of the preceding classes, though somewhat harder, on 
the average. Several are supercharged with lime salts, which are de- 
posited as travertine about the spring, on the escape into the atmos- 
phere of the carbonic acid which held them in solution. The tem- 
‘perature is also varying, being dependent of course upon the thick- 
ness of the limestone above. 

Above this generous horizon there is no well marked water-bear- 
ing stratum of rock, although there are numerous fine springs issu- 
ing at various points from the Niagara limestone. The widely known 
Waukesha springs are examples. Druecker’s spring, near Ozaukee, 
and several fine ones near Sturgeon Bay, belong to a similar geologi- 
cal position. 

The foregoing are all derived from rocks that were laid down under 
the ancient Silurian ocean, rocks whose ages are to be reckoned by 
myriads of years, and from which there has at least been a liberal al- 
lowance of time for the removal of whatever soluble matter may have 
been originally incorporated in them; and yet we find in all that have 
been analyzed, varying quantities of the oceanic salts. The remain- 
der issue from loose material of much more recent origin, formed by 
the agency of ice and fresh water, so far as the evidence goes; and 
yet, as this material was derived from the preceding oceanic forma- 
tions in great part, the same ingredients may and do occur in the 
water. They are as a class more superficial than the preceding, and 
more liable to contamination from surface impurities, and for a like 
reason their temperature is often less constant and their flow less reg- 
ular. While this is true, some magnificent springs belong to this 
class. It will not be necessary to enter so much into detail here, as 
in many cases the water-bearing stratum is merely local. 


HYDROLOGY. 143 


The Aettle Range is lined through its whole extent with springs. 
Its “pots and kettles” are peculiarly adapted to catch and tempora- 
/rily hold the rainfall, while it is being discharged at the foot of the 
range, and at other convenient points, in limpid springs. From the 
depth of drift which the water penetrates, many of these become 
very constant in flow and uniform in temperature. Dousman’s mag- 
nificent trout spring in the town of Ottawa probably belongs to this 
class, though it lies so near the great water-bearing horizon between 
the Lower and Upper Silurian formations, that it may really originate 
there, though it issues from the drift. Starin’s spring, near Whitewa- 
ter, the “ Big Spring,” near Palmyra, and a large number of others in 
the flats adjacent to the range, without much question, have their res- 
ervoirs among its hills. 

The numerous lakes along the range are largely fed from similar 
sources, which accounts for the clearness and purity, of their waters. 

Near Lake Michigan, where the lowest beach deposit rests upon 
the blue bowlder clay, an almost continuous line of small rivulets is- 
sues from the junction of the two formations, the clay intercepting 
the descending water while the sand and gravel of the beach forma- 
tion furnishes a ready passage for it. They are quite varying in 
chemical character, but are usually inferior in purity and changeable 
in temperature. 

Analagous to this, there is another line along the lake shore at the 
upper surface of the lower red clay, which is overlaid by the second 
beach formation. In cause and character these are altogether similar 
to the last. 

It would be fitting in this connection to give the analyses of such 
of the foregoing springs as have received quantitative examination, 
but a number of these have already been given by Dr. Lapham, in his 
report on mineral waters, to which the reader is referred. It is 
proper to add here, however, several analyses made since the writing 
of that report. 

Wis. Sur. — 10 


146 GEOLOGY OF EASTERN WISCONSIN. 


SUPPLEMENTARY TABLE OF ANALYSES OF SPRING WATER. 


a Gee a MAG rer e. Fo 
ds | ad | dS | Seg | Eas | BE | 
ae, | $32 | cP | Sam | cha | Bs | Se 
Bas | & A-| O45 Fo | oo 1 Pag | & 

ag a -O nas f So ao a 
233 Fi Soc, aod © > mB Aor ng 
faa | y8c | see | Se, | 22. | Sea | see 
S29 | Seo | ms | pad | cag | a3. | 238 
Sem | Cab | Bed | dad ona EB> | Ta 
a a o B q ey iS 
Chloride of Sodium......... 0.3262 0.1792 trace. | 0.470£ 
eee of oon 3 an é wes Aiewanca-en| wartavemelenis|issiewsiy — || Seeeiuare elyeatass 
odide of Sodium.... F arr SOREN EC eG moneor nc 
Bicarbonate of Lime . 14.5196 10.7520 13.778 | 10.2704 
Bicarbonate of Magne 12.2803 6. 8768 9, 7.1450 
Bicarbonate of Soda.. 0.1406 tisteia, tee aa BA iasecsiescie’ 
Bicarbonate of Iron.... 3 0.0396 
Sulphate of Lime... ........ 0.13826 
“Sulphate of Soda.... ....... 542 |... 2 
Sulphate of Potussa......... ‘ 0.3123 
Phosphate of Soda.. ....-. 0.0104 
AlUMINA....i6ee aus ee eas +122 0,0590 
Silica, wicca ssciircitouise é 0.7581 
Organic matter...... ... ... 9 trace. 
Total per U. S. gallon of |” 
231 cubic inches ......... 35.710 | 28.5936 38.211 21.505 | 20.0200 25.367 | 19 9126 


The source of the substances found in these springs is quite clear. 
The salts of lime, magnesia, silica, alumina and iron, are the rock 
substance dissolved, these being the essential constituents of the 
strata from which the waters flow or through which they have per- 
colated. It is to be noted that the relative proportions of these sub- 
stances in the analyses bear a close correspondence to that which they 
sustain in the rock. The compounds of sodium and potassium are 
for the most part those found in sea waters, whence they were de- 
rived at the time of the deposition of the formations beneath the Si- 
lurian ocean. The leaching of ages has not sufficed to completely 
remove them fromthe interior of the strata, and these analyses show 
that they are still being dissolved out and borne back to the ocean. 
The iodine which distinguishes the Beloit springs is doubtless derived 
from the ancient sea weed that is imbedded in abundance in the rock 
from which its flow is derived. It is true, iodine exists in sea water, 
but in a much less proportion than bromine, while here it is greater. 
It is further to be noticed that the ratio of iodide of sodium to chlo- 
ride of sodium, the common salt of the ocean, is greater than in sea 
water. These facts warrant the belief that the trace of bromine was 
entrapped by the forming rocks in the same manner as the more com- 
mon salts, but that the iodine arises from the sea weed that was 
buried by the accumulating sediments. The proportion of iodide of 
sodium to chloride of sodium —common salt—is greater, with ons 
exception, than that found in twenty-two other springs containing 
iodine, with which it was compared. 


HYDROLOGY. 147 


The small amount of organic matter in these springs is doubtless 
derived from the surface by the descending water. 

To enter into a consideration of the medicinal character of those 
springs that have attained a reputation for remedial virtues, would 
transcend our space, if not our province, and so long as medical 
science depends rather upon experimental results than theoretical 
considerations, it might possess little value if attempted. The use of 
these waters has been recommended by many physicians of high 
standing, and the results that have attended such use have been of a 
highly satisfactory character. That there are differences in the com- 
parative merits of the several springs is undoubted, but it is not the 
prerogative of this report to decide between them. It may be said of 
them as a class that they are free from any excessive amount of salts, 
which are objectionable when present in large quantities, though use- 
ful when the amount does not exceed the demands of the human 
system. For example, a certain amount of lime is needed by the 
body for the maintenance of its bony frame-work and the perform- 
ance of other functions, and in the opinion of many authorities this 
may be advantageously supplied through the medium of the water 
ingested; but an excessive amount of lime salts is conceded to be 
conducive to certain ailments. If the amount exceeds that which can 
be held in solution in the various conditions through which the water 
passes in the system, it is certainly to be regarded as excessive, for a 
portion of it must be deposited. The quantity of lime salts of most 
of the noted springs elsewhere exceeds by many fold the average 
quantity found in these. It is to be further noticed that most of these 
ingredients are invariable, if not normal, constituents of the human 
body, and that the hygienic character of the water is beyond question. 

It remains to consider briefly the geological position of those that 
have attained a greater or less reputation for medicinal properties. 
The Bethesda, Hygeia, Mineral Rock, White Rock, and Fountain 
Springs at Wankesha, flaw from the upper portion of the middle 
division of the Niagara limestone which is capped, in the vicinity, 
by the upper beds, known as the Racine limestone. 

The Horeb Spring of this place issues from the drift, which is 
here largely gravel or marly clay derived from the above formations. 
The Beloit Iodo-Magnesian Springs flow from the lower portion of 
the Trenton limestone, a lower horizon than the preceding or fol- 
lowing. 

The Siloam of Milwaukee, the Oakton of Pewaukee, the Palmyra 
springs, the Sheridan of Geneva, the Gihon and Burnes of Delavan, 
the Vemadin of Oconomowoc, Richmond’s, near Whitewater, and 


148 GEOLOGY OF EASTERN WISCONSIN. 


the Cedarburg spring, issue from various portions of the drift. It is 
possible that a concealed connection with the rock may exist in some 
of these; but evidence of the fact is wanting. Zelulah Mineral 
Springs, near Appleton, flow from the drift a few feet from the sur- 
face of rock belonging to the Galena horizon, and from the fact that 
water of similar character flows from a drilling in the rock in the im- 
mediate vicinity, it is claimed that the flow is from that source. 

The following classified list of springs, though far from ie ex- 
haustive, may be serviceable. 


Sulphur Springs. In all these the sulphur exists in the condition 
of sulphuretted hydrogen, which, being volatile, soon escapes into the 
atmosphere, and so unless the chemical determination be made at the 
spring, or special precautions taken, it fails to appear in the analysis. 
This is the case with Richmond’s spring near Whitewater, which is 
very strongly impregnated with this gas, no indication of which ap- 
pears in the analysis. 

The sulphur is derived without doubt in most cases from the de- 
composition of iron pyrites, specimens of which in the state of 
decomposition are occasionally to be found. 


PLACE. OWNER. SOURCE. 
Whitewater, Sec. 1, near center ........... .... A.M. Richmond.......... Drift. 
Whitewater, Sec. 1, N. W. qr. of S. E. qr. «0... EL Jip UAT: <-syatnnceonnusvevers Drift. 
La Grange, Sec. 9, N. W. qr. of 8. W. qr.......5. Pi QlesOniete sagisevercavntingaars Drift. 
ha Grange, Sec.26, Ni Wi Qr sccisieeutenginceeawrsess Di Willaims 3:00:50 sara.ssiere Drift. 
Appleton, helow City s.se.0s-0s oreaneseameanesan J. Es Harrimatiscssonewases Drift. 


Chalybeate Springs. These are characterized by the presence of 
iron compounds, usually derived from the decomposition of iron 
pyrites, and so are closely allied to the preceding. 


LOCATION AND CHARACTER. 
Ahnapee, T. 25, R. 26 E. Sec., N. W. qr. Temperature 45° (August 19), flow 
moderate but brisk; little sulphur, much iron, taste pleasant. 
Byron, Sec. 16, 8. E. qr., large but not very strongly impregnated. 
Empire, Sec 18, N. E. corner, small. 
Herman, Sec. 29, N. E. qr., small, but strongly impregnated. 
Hortonia, on Mr. Briggs’ place, Sec. 18, two small springs strongly charged. 
Lake Mills, Sec. 1, N. hf., contains also a little sulphuretted hydrogen. 
Grand Chute, Sec. 31,8. W. qr., rather small, much iron. 
Whitewater, Sec. 1, 8. E. qr., limited flow, much iron. 
Whitewater Village, small, but strongly impregnated. 


Travertine Springs. These contain an excess of bicarbonate of 
lime and magnesia held in solution by the presence of free carbonic 
acid in the water, which on escaping into the atmosphere causes a 


HYDROLOGY. 149 


deposition of the excess of the lime and magnesia as travertine. It 
frequently coats moss and other vegetation, which are then erroneously 
said to be petrified. Where the base of the moss is coated without 
destroying its form, while the upper portion is still green, as not un- 
frequently occurs, the error is a very pardonable one. The deposit is 
also called calcareous tufa. 

LOCATION. 


Empire, Secs. 6 and 7, several. 

Harttord, Sec. 24, 8. W. qr., several. 
Walworth, Secs. 11, 14 and 15, several. 
Whitewater, Sec. 1, near center. 
Taycheedah, Sec. 21, S. E. qr., large deposit. 
Brooklyn, Sec. 35, Lovers’ Glen. 

Delavan, village, several. 


Trout Springs. The following were noted as possessing sufficient 
volume and apparent purity to justify further attention with a view 
to the raising of trout. In the absence of analyses, their fitness is not 
here asserted and they are named only as being worthy of a more 
careful examination by those who may be interested. Their position 
in general is favorable, having a rapid fall and being unexposed to 
dangerous floods: 

LOCATION. 
Ottawa, Sec. 14, owned by W. James. 
Ottawa, Sec. 11, N. E. qr., volume limited. 
Hubbard, Sec. 12, N. W. qr., volume medium. 
Hubbard, Sec. 5, N. W. qr., several, medium seize. 
Delafield, Sec. 80, S. E. qr., Maxwell’s. 
Herman, Sec. 5, N. E. qr., several, very large. 


Herman, Sec. 6, N. W. qr. 
Theresa, Sec. 28, N. E. qr. of 8. E. qr., large but perhaps not uniform enough in 


temperature. 
Ottawa, Sec. 4, S. E. qr., Dousman’s, already successfully utilized. 
Taycheedah, Sec. 21, 8. E. qr., large. 
Taycheedah, Sec. 16, N. W.-qr. of S. W. qr., very large. 
Taycheedah, Sec. 9, S. E. qr. of S. W. qr., very large, rocks colored, but no iron 
taste distinguishable. 
Ellington, Sec. 27, center, large. 
Hortonia, Sec. 28, N. W. aqr., large. 
Berlin, Sec. 14, Mitchell's. 
Port Washington, J. Druecker’s. 
Cedarburg, now utilized. 
Sturgeon Bay, opposite village. 


Artesian Wells. The term Artesian is sometimes applied to very 
deep wells without regard to whether the water flows at the surface or 
not, but it will here be confined to flowing wells without regard to 


150 GEOLOGY OF EASTERN WISCONSIN. 


depth. It will promote clearness of understanding to call to mind the 
requisite conditions which will be found more amply stated in Vol. I. 
They are as follows: There should be animpervious stratum to pre- 
vent the escape of the water below; a previous water-bearing stratum 
‘upon this to furnish the flow of water; a second impervious layer 
upon this to prevent the escape of the water above, it being under 
pressure from the fountain head. These must dip, and there must be 
no adequate outlet for the water at a lower level than the well. There 
must also be a sufficient collecting area or reservoir in connection 
with the porous stratum and it must have sufficient elevation to act 
as a fountain head. As these wells depend for their essential con- 
ditions upon the character of the strata, it will be necessary to antici- 
pate some things subsequently given in connection with the formations 
involved. To these, the reader, who desires a more perfect under- 
standing than can be obtained from the necessarily brief sketches 
that follow, is referred. It would doubtless best subserve the interest 
and convenience of the general reader, to classify the numerous wells 
according to the formation from which they derive their flow, and to 
treat them as thus grouped. Were this method pursued, the classes 
would be six in number, as follows: 

1. Those that derive their flow entirely from the drift, clay layers 
forming the upper and lower confining strataand sand or gravel the 
the water-bearing seam. The last is usually a beach deposit and at 
least one of the others a lacustrine clay. This group includes the 
fountains of Tuycheedah, Calumet, Poysippi, Rushford, Auroraville, 

Whitewater, Byron, and a part of those of ond du Lac, Oakfield, 
and Oshkosh, with some in the vicinity of Lake Michigan. 

2. Those that derwe their flow from the junction, of the drift 
with the indurated rocks below. In these the drift clays resting on 
the rock constitute the upper confining stratum and the subjacent for- 
mations, the lower, while a layer of sand or gravel or the open nature 
of the rock surface affords passage for the'water. This class includes 
most of the fountains at Mond du Lac, Oshkosh, Oakfield, and Green 
Bay. 

3. Those that originate in the Niagara limestone. This body of 
limestone furnishes in itself, locally, the necessary pervious and i1u- 
pervious strata. The Manitowoc wells belong here. 

4. Those that arise from the Galena and Trenton limestones. 
These formations, like the Niagara, aided by the overlying drift, pre- 
sent all the needed conditions. There are embraced here, most of the 
Watertown fountains and a portion of those at Oshkosh and Fond 
du Lae. 


PLATE,V 


PROFILES ILLUSTRATING ARTESIAN WELLS 
by T. C. Charuberlin, 


Section from 
TAYCHEDAH TO RIPON 
Hor. Seale 2 Miles-/Inch.. Vert.Scale 200 = /Inch.. 


— 
——— 
——— 


= = 
SS FB 


‘ s 
y 
Protile from. ‘ , 
LAKE WINNEBAGO TO SEC. 30 BYRON ao § 
Hor. Scale 4Miles=7Inch.. Vert.Scale 80010 - SInch . yo at § 
at a 

c res 
wi 

a 


1 Profile trom 
SEC.10 BYRON TO SEC. 24 WATIPUN 
Hor, Scale 3 Miles=7Inch.. Vert Scate S001 1 Inch. . 


at 


colt 
ld de gti? 
(iu ee 6 
Laer er we a & 
git! oats Bi 


evel of Leake) Wires 


THE NORTHERN HOSPITAL FOR THE INSANE TO THE TOWN OF CALEDONIA. 


Profile from. g 
wy 

Hor Scale 2Miles-1Inch.. Vort.Scale 20002 = t Inch. 3 
g 


a ARCHAEAN , A 
A An “A “a a a a a A a a 
fa’ A A A A nN “A A A An “A tid A A A A 


Section front 


LAKE POYGAN WESTWARD 


Profile from 
WHITEWATER TO HEART PRAIRIK 


g Hor. Scale 8 Miles=7Inch . Vert.Scale 8002-1 Inch 
Se. & 

é c = § KettleRange 
Bef 5 

=v gs 


Tap Mawar e Latin & | wenCo 


HYRDROLOGY. 151 


5. Those from the St. Peters sandstone. This is by far the most 
widely available, and, except locally, the most important source of Ar- 
tesian wells in eastern Wisconsin. The lower layers of the Trenton 
limestone, resting upon it, form an efficient confining sheet above, 
and the formations below are saturated by water having a higher 
source than that of the St. Peters sandstone, so that there can be no 
loss, but may be gain from beneath. Aside from the porous charac- 
ter of the sandstone, it is much fissured in vertical, oblique and ir- 
regular directions, enabling the water to readily traverse it. From 
this horizon arise the deeper seated fountains at Watertown, Wild’s 
well and several more recently sunk at Yond du Lac, the “ozl well” 
at Palmyra, the exceptionally saline well at Sheboygan, and those at 
Milwaukee, Racine and Western Union Junction. 

6. Those from the primordial zone. The well at the Worthern 
Hospital for the Insane, at. Oshkosh, represents this class. The pub- 
lic well on Algoma street, Oshkosh, the water of which, though it does 
not flow at the surface, rises within a few inches of it, may be also 
classed here. So also the well on the Mair Grounds at Janesville, 
which flows through the aid of hydraulic appliances. A portion of the 
flow of the Racine well is from this horizon. 

These six classes, it may again be remarked, furnish the most sys- 
tematic grouping for study and description, but it will doubtless be 
most convenient and interesting to the people of the state for whose 
benefit the survey was instituted, to describe these wells by the local- 
ities in which we find them situated. 

In number and variety of source, the flowing wells of Yond du Lac 
stand preéminent. They represent four of the six systems above 
mentioned. The accompanying profiles represent much more clearly 
and satisfactorily the conditions under which these fountains are se- 
cured than an elaborate description, and will only need to be sup- 
plemented by some additional and explanatory statements. And I 
desire here to express my special indebtedness for many facts, other- 
wise beyond my reach, to Mr. C. O’Connor, who has sunk many of 
these wells. From his statements it appears that there are three 
classes of comparatively shallow wells that derive their flow from 
within twenty feet of the surface of the rock, either above or below 
it, it being from two to nearly one hundred feet beneath the soi]. In 
the first, flowing water is found in the blue clay which underlies the 
superficial red clay. The water is usually reached in a stratum of 
quicksand, from six inches to six feet in thickness. In the second, 
the flow is obtained between what is locally known as the “eoncrete” 
and the rock. This concrete, which varies from two to twenty feet 


152 GEOLOGY OF EASTERN WISCONSIN. 


in thickness, is the lowest member of the drift at this point, and 
seems to consist of partially cemented sandand gravel. The first flow 
of water is usually accompanied by a green or brown sand. The 
flow of the third class originates in the rock, within from six to 
twenty feet of its surface, and is unaccompanied, in general, by sand 
of any kind. The vast majority of the wells of the city belong to one 
of these three classes. The generous well of Mr. George Hunter, 
known as “Hunter’s Magnetic Saline Fountain,” derives its flow 
from the deeper limestone strata, as is shown from the following sec- 
tion furnished through the kindness of the proprietor: 


Feet. 

edd Clay si2 esas va os ahaha ele ila vata sis pallets ehatee vale ia lehsigtllta rele aie 26 
Blue clay, bowlders and concrete... ......seceecereeeces seeteeeee 30 
HUTA WHEL COULSEL Elbe icieseics ava cuandveccravorseacbosianeieiay seuese-denueaiens hes esate a/oe.e 56 
Brown limestoneesansccacasey sa twaeeieasyaen tae 24 See SOSA, 80% 14 
Second water course at.......0.ceeceeeeeesecceeees eaaecketeen viele are 70 
Brown limMestOnGniacausd neremewan cine ooemveee teewrG.es ovens es 40 
Third water Course abi sani sin ieasisan wea eGR bisa sBinenee dereceuten, em 110 
WV itG: TMS STATION se: doar oia sg cvtrw xine ave ini savese Grd wsdvare tale, Sasetecciejele $4504 A’ PRE 30 
: Hourth: water Course abssicnscisisee sins cio wiiawieis auaiiweieanese sires ep eens ¢ 140 
Crystalline cherty limestone..........0..000 cecreceenee covceeecs 20 
Cherty liniestone..se05 cis sant aware Maikened weckeoenae eae’ 27 
Battle Water COUPse Alb: cenit deieccalecceioiae sche: Vaca: “Sie Sereda eleroiw Sec aes 187 
DO aL: tLe fons cetoce eerie area suosntvacer ste aysieubs abs ver “Qua s Gyoseew auaneastsse alae 187 


The following is an analysis of the rock taken from this well, made 
by Rev. A. C. Barry: 


LAM ©. scars diet dnistadseeteaied aa teae SSeS haa awed vneevcdicteeeies accel 28.90 
Meio T SSL so! adie a cyacontcmup vous wy sier axa lada sieera oyeuaidiore Wap auele Malena ani dieses 20.76 
Protoxide Gf Sron 5 scus wagiavandaiosesige sierdossicdelae, Wereaabeaneloet 2.19 
SOA: w'sisisie' e's Sa a'e sie Sasa sees Gar SRW e SOE Kanu aaeals yaeeewenes 20 
Chlorin@..%3 sse% seexsaue bass s eedear's cise owev see eeehseeuaewics «.. trace. 
Sulphuric aides ssinsak onsets ease wieder eons way ec omdeiraciouge -10 
Carbonic AGIMs 64404 ssdseneia sew woee acess a Uaatereee tere daraieiners 45.51 

97.66 


From which it appears that this rock, in common with nearly all 
so-called limestone of eastern Wisconsin, is really a dolomite. The 
following is the analysis of the water of this well, published by the 
proprietor. As the form is somewhat unusual, the letter communi- 
cating it is published: 

Kroxvk Mepicat Cottecer, February 9, 1874. 
Grorcr Hunter, Esq.: 

Dear Sir: —1 have, to-day, completed the quantitative analysis of your mineral water, 
and with the following results. Out of one gallon of water I obtained 19 grains as 
residuum. 


HYDROLOGY. 153 


The analysis is an approximate, leaving off decimals in calculating the proportions. 
In 100 parts, the following are the proportions of each ingredient: 


1. Carbonate Of limi eis« sara x.stecs steve puttspssspene cia aia tied:Svadve jain invace ein eons 5 
2. Carbonate of potash. ..... cc cece ce eee e seer ecceeeeretetereeees 4 
3. Carbonate of magnesia.........ccecec cece ee cee ners ecenaeene 6 
4, Carbonate ob 8008 sacenesecaeGelaswge igaaateu tauie ita a oa eee eS 4 
oO: Sulphate: Of lniGs savivewnwseseevecd eseceda vide vers sees eee . 12 
6. Sulphate of potash............ sudaoicitusrtcdyeaayes ighas RoGnnE Ra eee LN 10 
7. Sulphate of magnesia..... ccc. see c nese cee nv ee cece ener eceteens 17 
8, Sulphate: of sodaliiijsiisaiceoswieeeteripes see wien aesasee aia ees 13 
9: Chloride of sodititis:siose4oseuesveukwtwaswenweeweluswawes vey s 14 
10. Chloride of potassium .........c cece cece eee e cence een ee eeeeee 3 
DD SiiGaigs 55-0.0 5-58 ye oarsiererna reas eta Ae rewwes Sidsdiale Seu Geille aosateterers 5 
93 

12. Traces Ob tronsisddeecajueatecedaccenae te bout” Seales — 
14, ‘Traces Of bromine: savssassoxsiieaitinnascevediessesdewssaviws's _— 
14. Free carbonic acid.... . sie RNGe SBS Saw iG ee stove fb sto vs eeaaucacaoaincetsr egal a = 
WWE yao: ose cavevasa- susie: bess aol nasqya ella is sasecndasove planes 8 oleae sg eianayerccseseearetese 7 
100 


To my surprise, I found a trace of bromine in it. J did not estimate the free carbonic 
acid. Very respectfully yours, E. J. GILLETT, 


The water has been extensively used for its remedial qualities. 

The magnificent fountain on First street, belonging to Messrs. B. 
Wild & Co., represents a yet more deep seated system. This well is 
326 feet deep, and passes entirely through the Galena and Trenton 
limestones, reaching the St. Peters sandstone below, whence it derives 
a flow of forty-eight gallons per minute. The stream has been carried 
by pipes 53 feet above the surface. It flows with such force that, 
with hose and quarter-inch nozzle attached, it projects a stream from 
30'to 35 feet high, and 48 feet horizontally. An analysis of the water 
of this well will be found in the report of Dr. Lapham, ante, p. 31, of 
this volume. 

The following is the section of the well on the high school grounds, 
kindly furnished by Senator W. H. Hiner: 


Feet 

Drift, red. and ‘bhiie: clay... ss sscsasciwvewnesedaa saw dieewaee weds 95 
Magnesian limestone (Trenton and Galena) .........-+ eseseeeeeee 195 
St. Peters sandstone... .....ececcseeecec ee eeeeseeenseeeeesereeees 185 
Potala. eeu aa vase eaioet sonal usinas detatnan nate slatalale cre 425 


In searching for the fountain head of the first class, or those which 
belong entirely to the drift, we find possible sources on almost every 
side, to the east, south, west and northwest. To the east and south 


154 GEOLOGY OF EASTERN WISCONSIN. 


there lies a ledge of Niagara limestone, underlaid by impervious shale 
from the surface of which issue frequent springs. The clay deposits 
of the basin, in which the city lies, abut against and overlap this shale. 
The junction is in all probablility permeable to water, which would 
thus reach the porous strata of sand and gravel that are found within 
the blne clay. That this is the true explanation of the Artesian wells 
of Taycheedah and Byron is more than probable. To the west, the blue 
clay rises to the surface and lies upon, or graduates into, the more 
gravelly drift hills of that region, and may not improbably derive its 
water supply from thence. 

The fountain heads of the second and third classes, viz.: those that 
rise from the concrete and from the limestone, are doubtless the same, 
or at least their fountain heads are associated, except perhaps those of 
the deep wells, whose reservoir is more distant; in all cases it is 
probably to the westward. Lamartine and adjoining townships furn- 
ish favorable conditions. The surface of the rock, as well as its lay- 
ers, rise in that direction. The slight local exception to this in the 
western portion of the city is not sufficient to afiect the general prob- 
lem. The rock appears at the surface to the southwest, along Seven 
Mile creek, at an elevation of 122 feet above Lake Winnebago. The 
general surface of the town of Lamartine is about 150 feet above Lake 
Winnebago, if a single series of aneroid measurements is to be trusted, 
and consists of low hills and ridges interspersed with marshes. The 
surface drainage is very imperfect. The hills and ridges. are com- 
posed of the varying mixed material of the unassorted drift, and are 
more or less permeable to water. 

Phenomena connected with the boring of wells in this region show 
that certain of the layers of the underlying magnesian limestone are 
practically impervious to water, while others are not. These with the 
clay above furnish the necessary pervious and impervious strata, and 
complete the requisite conditions. 

The fountain head of Mr. Wild’s well is to be found along the line 
of outcrop of the St. Peters sandstone within which its reservoir un- 
doubtedly lies. Near Ripon, the St. Peters sandstone outcrops at an 
elevation of about 325 feet above Lake Michigan, or about 150 feet 
above the surface of the well, thus giving an abundant elevation. 

The flowing wells of Taycheedah are from 60 to 70 feet deep, but 
do not reach the rock. It seems most probable that they derive their 
flow trom veins having their origin at the surface of the shale beneath 
the ledge, as already explained, and as shown in the sections. The 
water in some of the wells is highly impregnated with sulphuretted 


hydrogen. 


HYDROLOGY. 155 


In the town of Byron, adjoining Fond du Lac on the south, on the 
farms of Mr. Henry Bush, Mr. D. D. Jones, and Mr. Scarles, there 
are several wells having a rather scanty and variable flow. They are 
not, however, immediately affected by rains. The wells belonging to 
Mr. Jones are 70 feet in depth. The vein was found in a bed of 
quicksand at least 10 feet thick. Rock was struck at Mr. Searles’ at 
a depth of 170 feet — but did not yield a flow. The fountain head of 
these is probably in the bluffs to the south, as indicated in the profile. 

The Artesian wells of the town of Oakfield are located in sections 
9, 15, 16 and 17, and oceupy an extensive depression stretching north- 
eastward to Fond du Lac. Mr. H. D. Hitt has three wells from 68 to 
T+ feet deep. He gives the following as a typical section: 


1. Surface soil. 

Marl. 

Blue clay. 

. Small vein of sand. 

. Alternating blue clay, sand and gravel. 

. Rock at from 48 to 54 feet from the surface. 


Water flowed in a small stream before the rock was struck. On 
the same authority I learn that Mr. Whittaker secured a fine stream 
ina vein of sand beneath blue clay, at from 20 to 29 feet from the 
surface. Mr. 8. Scovil, residing on section 17, has two flowing wells, 
one 48 feet and the other 75 feet deep. The former, as I was inform- 
by the proprietor, is 37 feet in blue clay and 12 feet in limestone. It 
is situated near the western extremity of the depression before men- 
tioned, where the surface gradually rises toward the drift hills that 
form the “divide”? between the Mississippi and St. Lawrence basins. 
The latter lies somewhat farther eastward, and penetrates 50 feet of 
pure clay without seams of sand or gravel, and extends 25 feet into 
the limestone beneath. This well has a brisk steady flow about one 
inch in cross section, and is not noticeably affected by rains. The 
former one, when visited, had but a slight stream which broke into 
drops in falling six inches, and was said to be much affected by rains, 
the change being noticeable within 24 hours. The wells of Mr. Hatch 
and Mr. Wells are similarly affected. These are said not to penetrate 
the rock. We gather from these facts that there are two systems 
here, the more superficial, whose veins lie near the junction of the 
drift and limestone, being sometimes above and sometimes below, and 
whose reservoir is in the vicinity and is superficial; and the deeper 
one, whose fountain head is more distant. The reservoirs in both 
cases are probably to the westward or northwestward. 


156 GEOLOGY OF EASTERN WISCONSIN. 


The shallower system of Artesian wells at Oshkosh is quite similar 
to that of Fond du Lae, already described. They vary in depth from 
15 to 100 feet, and derive their flow variously from within the drift, 
at the surface of the rock, and at varying depths within it. The 
source of their supply is undoubtedly to the westward and less than 
ten miles distant. 

The deeper wells possess unusual interest from the facts they de- 
velop relating to the strata beneath. Unfortunately no complete 
record of the formations passed through in sinking the well at the 
Northern Hospital for the Insane seems to have been made, and noth- 
ing is now available but the very general statements of the person 
who drilled the lower portion, and an inspection of the mingled drill- 
ings at the well. These showed that variously colored sandstone 
strata had been penetrated to a considerable depth, and that a reddish 
granitic rock had been entered. 

The following items were furnished by Mr. J. H. Johnson, who 
drilled the lower portion: 


Strucle limestone absse vena nherncouabonaude seed bwierdacceasus eneecee 60 feet. 

EBA NASHONG Bbie wncdwaetihee eatins BORA eee ewumT emu Ae Rees © 300“ 
Et) Camaters abasad ssc ec awe aloe een Base eee eee eet ae Secreta goo“ 
fO) - ped garids bOnie ab sede svacsaee spss 5 accede eravenmlacncwinaarteealad ace amabbonnee s 540“ 
et “White RanastOne Bhersscavatncesad Ka voeigwhesewe site eeawe 585 
 -pranitetibadens gover seokeeavantbe a wieroreete 2668 wees. « 714 “ 
white @ranite atiod saad Sosa voce soba seek seiveliewd seek ia sie ys 935 “ 

BRO GEO ei chaps oad seeBoctettye costal cede Arete a sr eew Ais aheeapioeiee main oss vacess 961“ 


Mr. Johnson expressly stated that below 300 feet it was all sand- 
stone till the granite was reached. 

In regular order we should expect in descending, Trenton lime- 
stone, the St. Peters sandstone, the Lower Magnesian limestone, and 
the Potsdam sandstone, including a calcareous stratum, and the gran- 
itic rocks at the bottom as found. The question is naturally sug- 
gested, Is the St. Peters sandstone wanting, bringing the Trenton 
and Lower Magnesian limestones together; or is the Lower Magne- 
sian limestone wanting as such, bringing the St. Peters and Pots- 
dam sandstones together? 

Much light is thrown on this interesting question by the very excel- 
lent record and the drillings of a public well, subsequently sunk within 
the city of Oshkosh, preserved by Mr. K. M. Hutchinson, and sub- 
mitted to me by the kindness of Dr. Lapham. 

The record is incorporated in my notes, on an examination of the 
drillings, which are as follows: 


HYDROLOGY. 157 


1. Drift 92 feet. 

2. From 92 to 300 feet, a hard, bluish-grey, close-textured, semi-crystalline magnesian 
limestone. A few scales of sesqui oxide of iron present. 

3. At 300 feet, reddish, calcareous clay, containmg angular fragments of limestone 
and sesqui oxide of iron. 

4, At 308 feet, chiefly red silicious sand of varying coarseness, mixed with fragments 
of dark shale. , 

5. At 400 feet, light orange, silicious sand, the constituent grains of which are irregu- 
lav in form and surface. White clay-hke fragments, appearing like kaolin, and insolu- 
ble in hydrochloric acid, probably chippings of soft chert, also present. 

6. At 416 feet, dirty red sand, mingled with fragments of magnesian limestone, and 
also lumps of sand and limestone cemented with a reddish or whitish calcareous clay. 

7. At425 feet, white and orange, rather coarse, silicious sand, and a little of the kaolin- 
like material, almost all the fragments of which are marked upon one side by metallic 
iron, evidently from the drill, showing that they were clipped with difficulty from a 
larger mass. 

8. At 435 feet, yellowish-orange, silicious sand; the grains of medium size, and numer- 
ously marked with adherent specks of oxide of iron. Many fragments of chert drillings, 
marked with metallic iron, also present. 

9. At 500 feet, very fine grained silicious sand; a few minute lumps consisting of grains 
of sand cemented by finer material; no effervescence in heated or cold hydrochloric 
acid; color, yellowish white; some chert drillings present. ; 

10. At 557 feet, drillings light pinkish grey, appearing like crystalline powder. Ex- 
amined under microscope, found to be composed of grains of limpid quartz and particles 
of chert associated with the more finely powdered material that gives rise to the color. 
No effervescence when tested with cold or hot hydrochloric acid. : 

11. From 580 feet to 618 feet, the drillings are similar to the above, but the quartz 
grains are larger, more numerous and conspicuous, and the finer material is white. 
A very small amount of oxide of iron is present. No action when treated with acid. 

12. From 685 feet to 695 feet, orthoclase feldspar predominates, attended by consid- 
erable quartz and a less quantity of a dark mineral, probably hornblende. 


Classified, the two sections become: 
. At Hospital. On Algoma St. 


Dri wea sii Grerclouestcan sae e Teo OTS we aaah aie legl sisi 60 feet. 92 feet. 
Testo e doen vou duadswindersweerh arena tees ol 240“ 208 ** 
Sa HONe « 4 vce Asiaclgaieeans ada tueeawiee dvota as Saas ae 414" 330 “* 
Granite Pode ..¢ sss0 04 as aewedee see eie was ts ewes 948 15 “6 
Totals dacs taaseiareee eatanbaseeile heya eee 961 feet. 695 feet. 


The correspondence between the two is quite marked. In the 
southwestern portion of the city the rock of the region is exposed in 
quarries at an elevation very nearly the same as the surface at these 
wells. This rock is clearly shown by its fossils to belong to the Ga- 
lena limestone, in the modified character which that formation bears 
in this region. Itis seemingly the lower portion of the formation, 
and there is good reason for believing it to be entirely wanting at the 
locality of the wells where the drift is deep. The lower strata of the 
Trenton limestone are found at the surface at a distance of less than 


158 GEOLOGY OF EASTERN WISCONSIN. 


six miles to the west. Now between Ripon and Fond du Lae, along 
a parallel and not distant line, the dip of the lower face of the Tren- 
ton limestone is accurately ascertained to be 23 fect per mile to the 
eastward. Calculating upon the basis of this dip, and making allow- 
ance for the drift, there should be less than fifty feet of the Trenton 
limestone at the location of the well on Algoma street. 

This result is confirmed by calculations based on different data, and 
by a general inspection of the problem. Assuming this to be correct, 
the thickness of limestone below is sufficient to occupy the whole 
horizon of the St. Peters sandstone and Lower Magnesian limestone; 
or in other words, the 208 feet of limestone in the one case, and the 
240 feet in the other, just about fill wp the space that we should ex- 
pect would be occupied by the Trenton, St. Peters, and Lower Mag- 
nesian formations. What then has become of the St. Peters sandstone? 
One of the more recent discoveries of the survey makes this perfectly 
clear. The upper surface of the Lower Magnesian limestone in this 
region is very undulating; we might say, billowy. The St. Peters 
sandstone lies in the troughs between these billows, and usually cov- 
ers their crest, but sometimes the Trenton rests directly upon the 
elevated portions of the lower limestone, and the St. Peters sandstone 
is entirely wanting. This has actually been observed in some cases, 
and drilling at other points has left no doubt that this is not an un- 
common fact. If we suppose then that the Trenton limestone here 
rests directly on the Lower Magnesian as it does near Ripon, the 
whole of the difficulty disappears. See Plate VI. 

The calcareous material found in the sandstone below, doubtless 
represents the Mendota limestone, and must be regarded as confirm- 
ing the above conclusions. 

The well at the Hospital discharges about 22,000 gallons per day. 
This, accepting the foregoing views, is derived from the Potsdam 
sandstone, below the calcareous Mendota stratum. Its collecting area 
is probably twenty-five miles to the northwestward, and has but a 
slight elevation. 

At the mill of W. N. Davis, on the shore of lake Winnebago, in 
Calumet, are two fine wells, giving a copious flow of clear, cold, 
sparkling water, impregnated with considerable iron and some sul- 
phuretted hydrogen. The proprietor gave the depth as about 90 feet, 
but was not certainly informed whether rock was reached or not, as 
the well was not sunk by him. These are probably to be classed with 
the Taycheedah wells, having their source to the east, though it is not 
impossible that they belong to the Oshkosh system, as the fountains 
surrounding the lake indicate that its bed is impervious. 


HYDROLOGY. 159 


The Lake Winnebago System. All the drift wells of Oshkosh, Fond 
du Lac, Taycheedah, Calumet, and their vicinity, may be considered as 
constituting one group, owing their origin to the basin-shaped de- 
pression occupied by the lake, the superficial layer of which is imper- 
vious and prevents the water from escaping into the lake until pierced. 

The wells at Green Bay and other points in the valley of the lower 
Fox river derive their flow from, at, or near the surface of the rock, 
and may be classed with the above system. 

The Poygan Lake System. The numerous wells in Rushford, 
Aurora, Poysippi and vicinity, are located in part in the valley of the 
Fox river, but. they all belong to a common depression filled by a con- 
tinuous lacustrine clay deposit, and are essentially alike in nature and 
origin. They all belong to the drift, and owe their existence to the 
alternate porous and-impervious character of the red clay and associ- 
ated beach deposits. The surface of the area is level and considerably 
below that of the surrounding country. The flow is obtained at vari- 
ous depths, but not without some degree of uniformity, giving rise to 
the popular terms “forty foot vein” and “eighty foot vein.” The 
wells rarely exceed 100 feet in depth. 

The material penetrated is usually red clay, with occasional seams 
of sand and gravel, the whole attaining a thickness of from 80 to 100 
feet. There seems good reason for considering the “ forty foot vein” 
as being derived from the beach deposit between the upper and lower 
red clays hereafter to be described, and the “eighty foot vein” as 
corresponding to the beach formation between the lower red clay and 
the blue bowlder clay. These beach deposits are preéminently porous 
and water-bearing elsewhere in the state, and from the nature of the 
1ed clay it would be difficult to account for two veins so persistent as 
these seem to be, on any other supposition. These wells frequently 
interfere with those near them so that it is necessary to adjust the 
penstocks to the same level. This shows that they are derived from 
“common stratum, and lends support to the view given above. The 
flow is usually brisk and abundant, and in some cases is very copious. 
The water is mostly excellent and generally rather soft. Occasionally 
it is impregnated with iron and sulphur. 

The source of the flow of these wells is quite obvious. The clay 
strata terminate on the margin of the basin adjacent to and in asso- 
ciation with sandy drift hills of highly absorbent character. Around 
the rim of the basin thus constituted the water finds access to the 
porous layers and through them supplies the fountains. The num- 
ber of these wells is large and constantly increasing, as the clay may be 
bored with the greatest facility and at: trifling cost. 


160 GEOLOGY OF EASTERN WISCONSIN. 


The Artesian wells of Watertown belong to two classes, the one, 
including the greater number, arising from the Trenton limestone, 
the other embracing the deeper wells from the St. Peters sandstone. 
The first class vary in depth from 18 feet to 100 feet; the second 
from the latter depth to 215 feet. 

One of the most interesting of the latter class is located near the 
shops of the Milwaukee & St. Paul Railway Company, to whom it 
belongs. The following record was furnished Dr. Lapham through 
the kindness of Mr. G. W. Waring, who superintended the work of 


sinking it: 
Depth of soil... ...e sce cee cece eee c cent eee sentences eeen eee eerness 50 feet. 
Depth of limestone......+. ese cere doce e ees eeneeenn rece sete en erees on 
Depth of sandstone... ....csccce cece ese e eect eeee cnn nent eee scees 108“ 
TOtilecis seed eda sep e bert ceveeescwed obaeGb vee SH ee ae teem. ws 215 * 


Water began to flow when a depth of 107 feet was reached, and 
could be raised 10 feet above the surface. 

The two following brief records will sufficiently illustrate this class. 
They were furnished through the courtesy of Mr. 6. S. Woodward, 
who has taken a deep interest in the subject: 


Drift os:aiphecaslawieies aire conse pare ears pasar aia sean ened etaene 10 feet. 15 feet. 

Weititestone’s se sce os Se vee ee ees Ge tees Sacha ssdcgaea als 93 «OS 103“ 

SandstOneauke ee ererea waar hndadana teks oy sure OB 
TGfalt- pa awincierateuwanedeeeuon pec agea wecnan se 103‘ 41 “ 


If we assume that the flow of the former was from the surface of 
the St. Peters sandstone, the upper face of the sandstone will be 107 
feet, 103 feet, and 118 feet, respectively, below the surface, at the 
three wells, facts which may be of service in sinking others. 

The first one, that of the Railway Co., is 243 feet above Lake Mich- 
igan, and hence its bottom is 28 feet above the lake level. 

The source of supply for both classes seems to lie to the west of 
north, where, both near and distant, occur many depressions entrapped 
between limestone and drift ridges, giving abundant superficial reser- 
voirs, while in this direction also may be found the outcropping edge 
of the sandstone. This sandstone likewise comes to the surface to the 
west of Watertown, but the low elevation in that region seems to in- 
dicate that the flow is not from that quarter. The western edge of 
the sandstone, where it comes to the surface, follows the east bank of 
the Crawfish river, from Lowell to Aztalan, and at no point between 
those places has it an elevation much greater than the railroad junc- 
tion at Watertown. It is not to be expected then that fountains can 
be obtained from the St. Peters sandstone, which will flow at a mnch 


PLATE VI 


mR 207 TTT 


( 


ST 
ST 


HE 


Racine 


| & EET 
4 ie i ae 
Hi: Aa ee (ie. gi 
. } B : 1 7 c 
g TEATS S en : 4 
H| THI Mel oS If ache 3 & s ws 
é AHH S Ries : 
: B S Me = =, g & 
- ‘I | Nice ii Wes S$ ge OE 
z SERS ibis S S ve 
su tf 8 Hs = = nq gy 
4 MALT aN ~ oe) hee SE 
a HN a He Le Ws: 
a MEH a HHS s Hes 
te Hi a THE HIS : 3: 
< ! eS Weis Ss 25 
e y tg) © iH My lePs s oe 
CHINE: HIBATINES : 
g qui i F y ws 3 
Ry " Wy 8 
i > EU HH <a 
x Sst MET? His it NEE mys 
& a i I b:} Bl = | 4 a g J g 2 
il 3 Si I: " 2 | Hi Me = Ra Ss 
& = } RCH SRS GS sé 
z F § eG ane ne 
Ei tH ll: i S MEERA He N 
= Ry A WT 8 
4% | g | pe, H ME 8 S 
m CH | FCA ites & g 
x CA Nas SAREE & $ 
é HAE SSRI eS . 
I if oo 3 ie 3 
mz } SAAT! Sallie Ze 
ee SEN ike a* 
eT) ey cea ¢ 
& 2 5 ‘ A iI Q i f g 
4 2 i 3 i 5 ifs Lik g 
Pe hy aa 83 
: a en ms 
2 3 Sorry) Mf el me g5 
5 5 a ce ea R s* 
Bi st Gull 1 ete & We st 5 
7) Ny Wi ets i : : Ss 
. BOM: a Fa BIBS 2 
4 I ff nf! &, iF =| S Ss 
o Mi AS e s Pa 
0) me a oe he 
5 ran 72 8 ich ihe ae 
& i ie Hel WRIA 3 
Ht HAN Hine Ay ai Z 
} Mad a Phu, 
Pa fi : HH ii f an IS & 5 re 
|: 1) ai : 
z cH SCE Ei: ie 
& Mh ‘ai g8 
: Wi i We ie 
5 nad TN a : 
al i iG j co Se 
i] hi i > ao 
: i} TO NG & R 
; a 
ay VEC SENG H 
=) H)} qn ath t i x 
& i SAR me 
Cy) eA er e3 
VY Ad Ht f: a x & 
x () JM t eas = 8 ; 
SM Ran g é 


= || W 


fun Mawernir bo rte Naser 


HYDROLOGY. 161 


greater elevation than that already attained, viz.: 253 feet above Lake 
Michigan. By penetrating the Potsdam sandstone there is a reason- 
able probability that a flow competent to rise to a higher elevation 
could be obtained. 

The following is an analysis of the water of Mr. Buckhert’s fountain, 


by Dr. L. Brandecke: 
Grains in 1 gal. 


Bicarbonate of 80d « «+ o:24x054 cy 94 vera as buses so ea eee coe eee aee RS 1.898 
Bicarbonate of magnesia... ....e esse cece cee en cece cence cree eeaee 5.818 
Bicarbonate of lime,... 2.60... eee e eee cece ee ee ee ee eres sg bidipasaateugene 12.094 
BiGarbOnateORirONcseravdeadgececwaneds nee. Aces wdlesmalegsaneds 0.100 
Sulphate-of potassaijcwiecinw cies taie's usd dae tiss'sle ved eds deere ees seve 0.054 
Silica si ses nekaeeid weeelunwe wae cea e eee e Eee KY ONES KENES teeedeet ee 0.305 
Orparic Matter swassis sees cass Saws Fede toe cde en dd ceeded eee eae 0.346 

Total .cocanitssttccee tie aves pokGica de weancusernie eins 20.615 


While the above mentioned facts are still in mind, it will be con- 
venient to speak of the Palmyra “ oil well.” A failure as a source of 
oil, it yet has proved of some value in demonstrating the possibility of 
Artesian wells in that and similar situations. The following is the rec- 
ord kindly furnished me by Dr. Lapham: 

Palmyra Artesian Well (1865). Begun about 250 feet above Lake 


Michigan (828 feet above the sea). 


46 feet. Drift — struck limestone. 
176 ‘‘ Limestone; supposed to be “‘ Blue Limestone.”’ 
229 ‘* Water. 
235 ‘“* Slate and sand. 
255 ‘+ ‘Good show of oil.”’ (!) 
257 ‘* ‘Big show of oil.”” (!!) Struck sand rock. 
263 ‘* Great flow of water. 
983 ‘* Metal 2 inches. (Iron ore ?). 
350 ‘ Supposed Lower Magnesian limestone; Calciferous sand rock. 
412 ‘* White sandstone. 
421 “* Gray sandstone. 
455 ‘* Red sandstone. 
461 ‘“‘ Black sandstone. 
ie Hard sandstone, 3 feet. 
480 “ Gray sandstone. 
482 ‘“ Soft sandstone. 
489 ‘* Hard sandstone. 
507 ‘‘ Soft sandstone. 
587 “* Red sandstone. 
600 ‘* Gray sandstone. 
615 ‘* Red sandstone. 
660 “* Drab or cream colored sandstene. 
683 ‘* Soapstone or shale. 
687 “Gray sandstone to bottom of well. 
750 ** Bottom of well, being 500 feet below Lake Michigan; 78 above the sea. 


Wis. Sur. —11 


162 GEOLOGY OF EASTERN WISCONSIN. 


These may be distributed as follows: 


46 feet. Drift. 

130 ‘* Galena limestone, 

81 ‘© Trenton limestone. 

93 “ St. Peters sandstone. 

62 “ Lower Magnesian limestone. 
338 ‘* Potsdam sandstone. 


The flow is derived from the St. Peters sandstone. It cannot have 
its source in that formation directly to the west, since the outcrop is 
lower than the surface of the well. The fountain head is probably 
in the same region as that of the Watertown wells of its class. Iwas 
told that originally the stream was very large, and could be raised 30 
feet above the surface, but at the time of my visit it was meager, and 
would rise less than four feet. Whether this was due to defective 
tubing, as was claimed, could not be ascertained. 

The flowing wells at Whitewater are confined to the drift, and owe 
their origin to the fact that a bed of lacustrine clay rests upon the 
flank of drift hills to the southeast, that are admirably adapted to 
serve as collecting areas. The well of Mr. P. Dorr is 52 feet deep in 
a stiff blue clay. Its flow is copious and is charged with iron and 
sulphuretted hydrogen. 

The number of these wells may be somewhat increased in all prob 
ability, but the limited extent of the clay deposit will confine them 
to the localities occupied by it. 

The surface of the Niagara limestone at Manitowoc is thickly 
covered by impervious drift, and the strata beneath rise to the west- 
ward, and are partially permeable to water, so that the requisite 
conditions for a flowing well are found at no great distance within 
the limestone, if the boring is fortunate in striking a suitable vein. 
At the well of Mr. William Rahn, the drift is sixty feet deep and the 
rock was penetrated ninety feet. The wells at Washington Park and 
at Woodman’s Tannery are given as about the same. An analysis of 
the water of Mr. Rahn’s well is given in the report of Dr. Lapham, 
in this volume, gnte, p, 31. 

The following section of the well at Western Union Junction 
is prepared from data furnished my predecessor by John C. Gault, 
from the general manager’s office of the Milwaukee & St. Paul Rail- 
way Company, to whom the well belongs. This and the following 
are of especial interest as giving, at a point so near the southeast cor- 
ner of the state, the thickness of several of the formations, and as 
frrnishing data for the reliable estimate of dip, and for other cal- 
culations: 


HYDROLOGY. 163 


} : Feet. 
Dithty essen cee ean easecanecse seinen Apo | Bead oases Ledaiae basa 147 
Niagara Hm eston’ acces casero wriaaiinaatnie ese dtnle wer coe edad Seue beds 233 
Cincinnatishale:ssisqaaciieraeiversce vecieuanae eseeubausies cnentacs a 200 
Trenton and Galena limestones ......... 0. cece eee ce cent ence cee eeteee 285 
St. Peters sandstone (small flow) 00.0... ccc cee e rece eee ee te ee ee aeeen 100 
Lower Magnesian limestone .......... eee cece eer ee eee e eee eet eeeee 141 
Potsdam sandstone........... eee eeee (ise Vs be MERA ee eee 157 

Totals iors aka see ey ar paar eee aaa eRaRnine at 1263 


The record says that fifteen feet of limestone were passed through 
in this lower sandstone; but at what depth is not stated. It also 
adds that red rock mingled with the sand from below. These facts 
leave no doubt that this is the Mendota limestone, which, at the 
typical locality near Madison, has its upper surface 35 feet below the 
superior face of the sandstone. 

The surface of this well is 144 feet above Lake Michigan, and hence 
its bottom is 541 feet beneath the ocean level. The water rose at.the 
time of drilling to the height of 40 feet above the surface, or 184 feet 
above Lake Michigan, As only a few points in the eastern part of Ra- 
cine and Kenosha counties exceed that elevation, this well has demon- 
strated the possibility of obtaining fountains over a considerable area. 

At Racine a fine flowing well has recently been secured, of which 
Dr. P. R. Hoy has kindly furnished me the data which show the 
following section: 


Feet. 

Diiths4 eatescakane rae ie tenses. tees s pi Dae Sat eRe wE tae 115 

Niagara limestone....--.-sseee sees cee eee e eee eee ee ete ee tener e ee 305 

Cincinnati shale... ....-. 60sec cere teen eee n etre eran ence ereaneneres ,- 185 

Calena and Trenton limestones.... 065.66 cece ee ee cece e tence een eeeee 283 

St Paters gandstone: wan ca cesacci ovens s us daiecin oaabedmeeen eee. 48 

Lower Magnesian limestone... ....+..seee eee eter eect ener ener te enees 100 

Potsdam group — 

Madison sandstone.....--..--- aes ate Gas Steere eastern sleace 47 
"Mendota limestone... ...-- eee cece cece cece cere cteneeeeees 31 
Red sandstone.....-c.seccce cece crete ee eretenneeeeeenees 110 
Hard sandstone..... 2... eceeceeeeeseeten ere r ener ceesneere 10 

Leb idee Re AGR4 RE ENOREI HERERO E RENEE eX Te Sepia 

Soft sandstone. ... abe 

Total depth ......scececeeee cree cece tees en ene e anaes 1240 


When the St. Peter’s sandstone was reached, a flow was secured, 
which was increased on reaching the Madison, and still further 
augmented when the soft sandstone was struck. The water rose in a 
tube 65 feet above the surface. This record is valuable in that, it 
demonstrates the existence of three water-bearing strata above the 


middle Potsdam. 


164 GEOLOGY OF EASTERN WISCONSIN. 


The following is the section of the well at Milwaukee: 


Diittins such och ve ede antes Oho ad eae e eee es eee es Seas dese eee ee 170 feet. 
Niagara Tme@StOne ecse.niowecain scart wisvesdia macenacd acne acbicte aecdie nde Hala ale a 267 “¢ 
Cincinnati shale) ccc: cswiew tetas een enene cr ears «he Var Gene acne es 165 ‘ 
Trenton and Galena limestones..........ce ee ceee eee ee ee eeeeeneee 253“ 
Sb... Peters sandstone. «0. c.ccccaecesa steven seas as tes pa ba pee <dianwiens 193“ 
1048 “ 


The surface of the well is about ten feet above Lake Michigan. Its 
flow is strong enough to fill a four-inch pipe at sixty feet above the 
surface. From the pressure at the surface, it was estimated by the 
engineer of the company that the water would rise 100 feet above the 
surface, or 110 feet above the lake, which makes it probable that a 
similar flow might be obtained at other localities in this region whose 
altitude does not exceed that. By consulting the table of elevations, 
it will be seen what territory is included in this limit. 

It will be observed that this flow is from the St. Peters sandstone. 
By sinking deeper to the Potsdam, a vein capable of rising higher, as 
at Western Union Junction, would probably be reached. 

The well of Sen. W. H. Jacobs, in the suburbs of Milwaukee, is 1,200 
feet deep, and delivers 300 gallons of water per minute. The flow may 
be carried over 50 feet above the surface. An analysis of the water 
by Gustavus Bode shows it to have the following composition: 

Grains in 1 gal. U.S. measure. 


Chloride Of potassin 2% 65 cous dereceeeeeeeneteesevesdedayvewatay 0.2745 
Chloride: of isaditii, s<ecs% ee esses ee tenedssencsscre cbexiareeseas ree 0.6405 
Sulphitite Of 80d. is vere desiereie. sccge Biase dss pioesn tonics wale sewedie pisldis gaeee 8 6 ee 8.8572 
Sulpliatevotlime: sc.10 s2co ce. 09-243 25d ome eeaheanteatieeweaheesas 14.5485 
Bicarbonate Of Me: sc. sa ci4 cicsa ve dand ccc taae casi se eied aegle ene iia 8.6925 
Bicarbonate of magnesia .........ce cee cece cece ene eteneenees tees 6.6307 
Bicarbonate Of Otis sss esses ete vegas isae wees Se wehbe bes he bees 0.1842 
AV GMa 0 sae Rae chee a AES eae hee oho aos dud bean b44 daw abuse 0.1891 
Gili Gale de. eh. de tea ee san See eee OA RE AOS nee tinea Lh alent a ee eadatae 2.3790 

ENN bed: ansstaatstjake easacnsuc ntact ee eto le aioe asec Raed ueda aie atm tees 42.3462 


The city of Sheboygan has recently sunk a public well that pos- 
sesses unusual interest, both in reference to the strata passed through, 
and the character of the water obtained. The data for the following 
section were furnished through the courtesy of Mayor George End: 


Dire ep tesisare seed hase a eveiese enecead iis tondsatcvoad synces HWE ADE ues LOvR Geena een 92 feet. 
Niagara; limestone: sierines saturated nein aeraporiogn dgadaamemres 719 ‘“ 
Cincinnati shale...........-..000,- prize a hse bablasevava racavd paheceoy Bauectatorareiees 240 “ 
Trenton and Galena limestones.,.... 0 sess eee ee cece cess eceeceeee 919 * 
St. Peters sandstone ......... ni gpnees S64. aadudan ede ets aisl nore ale O19), 


HYDROLOGY. 165 


The exact depth of the well is 1,475 feet and 4 inches. At the 
bottom, a very hard rock is said to have been struck, which was be- 
lieved to be granite, and which may have been one of the Archean 
rocks, as they rise into that horizon occasionally. The surface of the 
well is 42 feet above Lake Michigan; its bottom 855 feet below the 
ocean level. 

Flowing water was obtained at 1,340 feet, being in the upper por- 
tion of the St. Peters sandstone. The pressure at the surface is suf- 
ficient to raise a column of water 104 feet above the surface, or 146 
feet above the lake, which differs only two feet from that obtained 
from the same formation at Western Union Junction. The discharge 
of water is 225 gallons per minute. Temperature, 59.1° Fahr. 
Our deep seated springs range from 47° to 48° Fahr., as taken in 
connection with field work, during the summer season, when they 
would be warmest, if they vary at all. This seems to show that the 
water of the well is influenced by the depths from which it comes. 

The following is an analysis of the water by Dr. C. F. Chandler: 


Grains per U.S. Gallon. 


Chloride of sodium .... 6. ese cececeee cree ec ee tenet eee eceeeenees 806.9436 
Chloride of potassiMe .. cp ien ase s wee eed tae ee cbse eb eda ween ss 14.4822 
Ghiovide: Gf Tithiutitecedscaeucuse. Giese veaesiea cee Ges sae Haw ee 0.1062 
Chloride of magnesium....-..... ce cece cece cree eeeeeeees feeaveas 54.9139 
Chloride of calcium ..... ce sec ce cece ee teers enees pscelgncelaeaGvaPeie 27.8225 
Bromide OF BOdMIM ie oii oe se ed cee eae ceersbennnaomecsiemees a 0.1873 
TOdide@ OF BOCLUTM vs deadciece's cece ee w caw we: ce eres Seabee Senngminte ein gevigrnnevors trace. 
Sulphate of lime...... Baits ha. dace Wie days wise iin cx ala neers erie 169.8277 
Sulphate of baryta ......ceec cece ee eee cece ete e eee eenenes scorers trace. 
Bicarbonate of lime ......e cece cece sree nee ee eee e nc eeeeneenerees 18.6585 
Bicarbonate of iron ......- cee ce cece eee ee ceeneesetcssceeesenees 0.5044 
Bicarbonate of manganese.....+-+.-+++-- eeaniete aches sad estegs 0.1742 
Phosphate of lime.....-- ++ sees eeeeeeees Seiiwe ye hedak ae SENS awe 0.0883 
Biborate of soda........--eencccccvence seetentestenneernetenees trace. 
Alumina. 662s 3 ee a sar sineemine Clivctaiate RON AWA AM GR Aw aNE NOME EO 0.1283 
Sie suigess: Sede Sota ona ROAM SNROE NORE OEE te dee R eee ess ores 0.4665 
Organic matter ....seeeeee ce cece eect ee et eeee erent eesenees trace 

Total ..... ato acuigeter nave doayomacaeelsiar sia wh ate eis an bins Ra te oe Pas 589.2536 
Tienatliy jaadacago-cs sua veka soepantenaawians wiveeiererssewenG 1.0093 


The large variety and quantity of salts contained in this water 
have naturally attracted much attention, and experience will doubt- 
less soon demonstrate the specific medicinal effect of the combination 
here presented. 

At first thought it would seem not a little remarkable that so saline 
a water should be obtained from the St. Peters sandstone, a formation 


166 GEOLOGY OF EASTERN WISCONSIN. 


composed alinost exclusively of quartzose sand, and one whose waters 
elsewhere contain rather less than the usual quantity and variety of 
salts found in our native waters. But we must consider that there is 
here a depression of the strata, the sandstone being here lower by sev- 
eral hundred feet than it is either north, south or west, and it is not 
known to outerop anywhere to the eastward, though the strata above 
and below again come to the surface in Canada. 

The facts of the case warrant us in believing that there is no escape 
for the waters in that direction. We have then here a basin reaching 
hundreds of feet below the ocean level. Its waters have no outlet 
and no escape except by the slow process of diffusion and percolation 
through almost impervious strata. 

That the water should, under these circumstances, become highly 
charged with saline ingredients is not at all remarkable, though the 
facts are of an exceedingly interesting nature. 

The well at Janesville is located upon the Fair Grounds, at an ele- 
vation of about 295 feet above Lake Michigan. The following is tho 
section developed by an examination of a series of drillings preserved 
by Mr. Cyrus Miner, to whose kindness also I am much indebted for 
other information relating to the well: 


DRIFT. 


From 1 to 100 feet, open well through gravel. 

From 100 to 240 feet, ‘‘ running gravel.” 

At 240 feet, sand and gravel of drift origin; several kinds of rock represented. 

At 259 feet, sand, gravel and calcareous clay. 

From 215 to 240 feet, calcareous arenaceous clay. 

From 260 to 350 feet, sand and gravel, largely quartz and chert, a little granite, dio- 
rite and some limestone. 

POTSDAM. 


From 350 to 360 feet, a red ocherous material mixed with a nearly equal quantity of 
green particles much resembling the green sand of the Upper Potsdam. Drft gravel, 
probably from above, also present. The red and green mixture effervesces tardily in 
cold acid (hydrochloric), but very briskly in hot, showing a calcareous and magnesian 
element present. 

At 390 feet, ght colored quartzose and cherty sand, with a few granitic and calcarc- 
ous grains. 

At 400 feet, fine-grained white, chiefly quartzose sand, but indicating the presence of 
calcareous material by a slight effervescence with cold, and strong action with hot acid. 

At 450 feet, essentially the same as above. 

At 515 feet, quartzose sand, red ocherous material, and particles of a purplish shaly 
rock partially soluble in hydrochloric acid. 

At 530 feet, reddish ocherous material, dark calcareous shale and small drift pebbles, 

At 565 feet, greenish blue calcareous shale containing minute glistening scales re- 
sembling mica. 

From 560 to 570 feet, similar to the last. 

At 615 feet, fine grained light yellow quartzose sand; slight effervescence. 


a 


HYDROLOGY. 167 


At 630 feet, fine grained white quartzose sand ; slight effervescence. 

At 640 feet, fine grained quartzose sand, with slightly reddish clay-like calcareous 
material. 

At 710 feet, fine grained, light colored, quartzose sand; slight effervescence. 

At 758 feet, rather coarse, white and slightly greenish quartzose sand, with a, little 
clayey material; no effervescence. 

At 940 feet, coarse white quartzose sand. 

At 975 feet, similar to above, but coarser. 
At 1022 feet, very coarse, transparent quartz sand, some of the grains one-sixth of an 
meh in diameter. 

Bottom, 1033 feet. 


SUMMARY, 

DFU Goats ahem Heal tadtvh re Mik cemeuieacwe yey oes wey nee’ 350 feet. 
Red and green rock, probably Mendota horizon ..........+esseeeees 1o *“ 
Fine grained, slightly calcareous sandstone..........-eseeeseececes 155“ 
Calcarcous: shales ssssie.siss saves cerensits sedherscerbesarciaes’ecacl iacatasatdie aaialas 80 “ 
Fine grained, very slightly calcareous sandstone............00e00005 163“ 
Coarse non-caleareous sandstone ......0.s.cececesecceseccseucecee 275 
Dobel a titeiaragnars emaunon sa talnnons Gira Bes Suse Sousa eg ae san eee 1033“ 


Drift, 350 feet. Postdam, 683 feet. 


Probably 40 to 50 feet of the upper portion of the Potsdam has 
been removed, making the thickness about 725 feet, with the bottom 
not reached. 

In the upper portion of the Potsdam horizon, a vein was struck 
which gave a permanent rise in the tube of 48 feet above the water 
level in the open well, without the aid of a seed-bag or other appara- 
tus for preventing lateral leakage. This corresponds, according to 
aneroid measurement, to 147 feet above Lake Michigan, or 7 feet 
above the depot at Janesville. 

The unusual thickness of the drift is probably due to an old pre- 
glacial cafion of Rock river, now filled, as the full series of formations, 
up to the Trenton limestone, occurs on the opposite side of the river, 
and also at a short distance to the east. The circumstances that ne- 
cessitated the selection of the fair grounds for this test well are to be 
regretted, since at the locality for which my estimate was given, the 
exceptional difficulties with the drift would not have been encoun- 
tered, and a satisfactory flow would undoubtedly have been obtained. 
Nevertheless, through the enterprise and ingenuity of the parties hav- 
ing the matter in hand, a success scarcely less satisfactory has been 
attained. Advantage has been taken of the rise of 48 feet in the tube 
above that in the well, to raise a portion of the generous flow to the 
surface by hydraulic appliances. 

Possibilities of obtaining wells at other points. Reference has 
been had to this important practical question in the foregoing des- 


168 GEOLOGY OF EASTERN WISCONSIN. 


criptions, and in the subsequent treatment of the geological series, 
large, and it is hoped ample contributions will be made to it, though 
it will not be always specifically designated, as that would burden the 
report to the exclusion of other valuable matter. Special estimate 
should be made for every locality before commencing to sink an ex- 
pensive well, as there are often local elements that enter into the prob- 
lem and determine success or failure. It needs also to be borne in 
mind that even ina favorable locality, failure may result, as the strata 
are not uniformly porous, and it is possible to bore through a forma- 
tion that is in most parts highly water-bearing, without striking a 
vein or seam. Only a single marked instance of this, however, has 
come to my notice. Failure, also, often results from not properly 
controlling the water, by the intelligent use of tube and seed-bag, or 
equivalent apparatus, and by failure to recognize a suitable vein when 
reached. These and other matters will be found more fully discussed 
in the general article on the subject in Volume I. 

Bearing these points in mind, and leaving out of consideration the 
drift system of wells which, from their superficial character and the 
nature of the formation, have only a local importance, there are three 
extensive areas over which there is a reasonable presumption that 
fountains may be obtained. 

The first is @ belt adjoining Lake Michigin. Where the elevation 
is but afew feet above the lake surface, streams will be found, in some 
cases, in the Niagara limestone, which, if intelligently controlled, will 
furnish a flow at the surface. This source will be, however, uncer- 
tain. But by penetrating to the St. Peters sandstone, the probabili- 
ties of success will be large, and they will be reinforced by the chances 
lying in the Potsdam sandstone below, though the depth of this 
will be considerable. Near the lake level, the chances from these 
sources will be good for the whole of the lake border. From Mani- 
towoc county southward, they may be said to hold good for elevations 
not exceeding 100 feet above the lake, and to be fair up to 140 feet, 
but slight above 150 feet, though perhaps possible in some locations 
at 200 feet or more. 

The elevations previously given in this report, and the topographi- 
cal map will show what localities fall within the limits of these con- 
ditions. The facts connected with the wells already described, and 
the data given in relation to the several formations, will permit an ap- 
proximate calculation of the depth, nature of the drilling, and conse- 
quent cost. 

The second area consists of the Green Bay valley, from Fond du 
Lac northward. In the vicinity of Lake Winnebago, a flow from 


HYDROLOGY. 169 


either the St. Peters or Potsdam sandstones can not be relied upon at 
an elevation exceeding 15 feet above the lake surface, though Mr. 
Wild’s well has demonstrated that it is possible at 50 feet. On the 
other hand, however, the wells at Oshkosh show that the limit given 
is the extreme one that is reasonably trustworthy. 

To the north of Lake Winnebago the limit in altitude descends at 
about the same ratio as the general surface of the valley. It must 
be remembered, however, that the St. Peters sandstone is not so relia- 
ble in this region as farther south, where its thickness is more uni- 
form. The Potsdam sandstone should, however, present reasonable 
probabilities for the region along the Bay, at elevations not exceeding 
25 or 30 feet above its surface, with slight chances for greater alti- 
tudes. 

The third district lies in the valley of Rock river. An elevation 
of 250 feet must be taken as the upper limit of favorable chances. 
That a flow at this altitude is attainable is shown by the wells at 
Watertown, Palmyra and Janesville. The St. Peters sandstone is 
available for only a portion of the area that falls below that altitude, 
since in some parts of it, this formation is deeply eroded by the 
streams, and its fountain-forming possibilities destroyed. Success in 
these portions will be chiefly dependent on the Potsdam sandstone. 

The list of elevations and the maps will be found indispensable to 
an intelligent calculation of probabilities in this region, and something 
more than wonted caution may here be recommended, because of the 
nature of the formations, their nearness to the central anticlinal axis 
of the state, and the presence of deep ancient river gorges now filled 
and concealed by drift. 

As the majority of the deep seated wells of eastern Wisconsin de- 
rive their flow from the St. Peters sandstone, it is important to know 
at what elevation the upper face of that formation outcrops. The fol- 
lowing list will supply the requisite data: 


ELEVATIONS OF THE JUNCTION OF THE ST. PETERS SANDSTONE AND TRENTON 


LIMESTONE. 
Hook County. ae Rock County — (con.) 
von — ; eet. | Magnolia — Feet: 
Sec. 5, N. E.ar., . 272 Sec. 6,8. W. ae mary 
Beloit = , : at 7, Sy E. gr, - - a 
Ge, OO Gc ce... 90), age Og OO 
8, 8S. W. qr.ofS. W. qr., 196 P : 

10, N. E. qr., - - 180| Porter sn 

10, §. E. qr., a ote 200 Sec. 9, N. W. ar., - - 25 

Fulton — Rock — 

Sec. 10, 8. W. qr., - - 219 Sec. 32, - - - 189 
Newville bridge, Rock river, - 208 Afton, - - - - 206 


170 GEOLOGY OF EASTERN WISCONSIN. 


ELEvATIons, etc. — continued. 


Rock County — (con.) Dane County — (con.) 
Spring Valley — Feet.| Rutland — Feet. 
Sec. 3, 8. OW. ae of S. W. qr, 314 Sec. 34,8. E. qr, - - 348 
4, 338 | Dodge County. 
9, eae - 821)" Fiba — 
13, mid. N. line, - 300 Sec. 25, (very near),  - - 254 
b,S.E.qr, - 321] Fox Lake — 
28, N. E. ar., : - 296 Sec. 17, 8. E. ar., 294 
_ 88,8. Ei gr, - = 268 31, N cme a. of N. W. a. 
Union — (est.) 368 
Sec. 12, near center, - - 298 31, mid. Ww. oe N. We. qr., 329 
veferson © County. Lowell ‘ci 10, R. 14)— 
ake M sec. 19 (est.), - - 195 
Sec. 3 N. W. ar., - - 319 RS a ) 
4, N. W. ar., 330}. Sec. 6,N.W.gr, = - - 296 
Milford —’ 31, a 948 
Sec. 7,8. W. qi - 251) Shields — 
38). Er (est),—- 257 Sec. 32 (near), - a Bhd 
Oakland — Westford (T. 12, R. 13)— 
Sec. 18, S. E. qr., 246 See, 25 266 
16, N. W. corner, - 264 da lk Count 
28, mid. B. line (est), 933 no ounty. 
Tee ee 258) "geo. 31, 8. W. comer, 412 
Sec. 18, (est.), - - 202} Ripon— 
Waterloo — a 80 rods. W. of P.O. (near) 381 
Sec. ee county line (est), 823 city, falls under tressel bridge, 333 
3, 8. E. qr. (est.), - - 277 W. of city, - 414 
Dane County — Sec. 20, N. W. qr. of N. W. qr., 328 
Christiana — 20, little W. of center, - 297 
Sec. 24, N. hf (est.), - 261 21, 8. E. gr. of 8. W. ars 364 
Medina — 29, N. E. ar., 350 
Sec. 25, E. hf (ear), - 331 29, i. hf, valley, - - 341 


Those marked estimated, or near, are cases in which the actual junction was not seen, 
but was calulated from the thickness of the Trenton limestone above. 


Water Power. The great interior and the west are. laboring un- 
der a serious error which intelligent action may remove. They pro- 
duce vast quantities of erude material neediug manufacture. This 
bulky and heavy matter they transport athousand miles to be worked 
up. They likewise produce immense quantities of food. This they 
carry the same thousand miles to feed those who manufacture the 
other material. They then bring back the manufactured article mur- 
muring at its expense and praying for cheap transportation. More 
simply and truly stated, the situation is this: Atone end of a thous- 
and miles is a man and his tools; at the other end is the heap of the 
crude material he is to manufacture, the bulky food he is to eat, and 
the market for his products; and the problem is, Shall the mountain 
go to Mohammed or will Mohammed come to the mountain?! An 
intelligent practical answer to this will go some way toward solving 
the problem of cheap transportation. Agriculture, mining, and man- 
ufacture form a triangle of industries that are mutually dependent, and 
the nearer they can be brought together the more successful will 
eaclr be. 


HYDROLOGY. 171 


The question then, What facilities for manufacturing does our state 
present? becomes one of the highest importance, especially so to our 
preponderating agricultural interests. Chief among these is water 
power. 

In the district under consideration there is a vast amount of water 
power situated in the heart of an exceedingly rich farming country, 
with abundant facilities for transportation, and, not by any means a 
subordinate consideration, in the midst of an intelligent, cultured so- 
ciety. The object of this chapter will be to give trustworthy facts for 
the guidance of capitalists, who may have the prescience to foresee 
that the natural facilities for manufacturing in the interior must in 
the immediate future be utilized to their utmost capacity and must 
become correspondingly valuable. 

Water Power of Rock river. For a portion of the facts here 
given, credit is due the report of Brevet Maj. Gen. James H. Wilson, 
on the survey of Rock river, under the direction of the U. 8. Engi- 
neer Department, and for another portion to a very careful survey of the 
lower portion of the river by Edward Ruger, C. E., made to deter- 
mine the availability of Lake Koshkonong as a storage reservoir. I. 
am indebted for the use of the latter to the kindness of J. M. Cobb, 
Esq., through whose efforts the enterprise has been brought to a suc- 
cessful issue. The remaining data have been gathered during the 
progress of the present survey. 

The entire area drained by Rock river and its tributaries in Wis- 
consin is 8,635 square miles. From the Table of Rainfall at Milwau- 
kee, given in Dr. Lapham’s report, this volume, it appears that the 
average rainfall for the past thirty years is 30.27 in., which may be 
assumed as at least approximately correct for the. Rock river valley. 
The average fall for some portions of Wisconsin is given in Gen. 
Humphrey’s work on the hydraulics of the Mississippi at 35 inches. 
But reckoning at 30 inches, the rainfall upon the drainage area under 
consideration would be 253,344,960,000 cubic feet. Now itis asserted 
by various authorities, based on experience, that one-half the rainfall 
can be utilized. This would give 126,672,480,000 cubic feet per an- 
num. Mr. Ruger says: “ From personal observations, and after con- 
sulting many authorities as to rainfall, springs, evaporation, filtration, 
ete., I estimate that the total annual quantity of water passing in 
Rock river at the state line, including Turtle Creek, is 98,437,536,000 
cubic feet,” which may be regarded as a safe estimate. The daily 
supply, by this estimate, would be 269,691,879 cubic feet. We need 
next to ascertain what is the average descent of this volume. Some 
of it falls over 600 feet, while other portions practically no distance. 


172 GEOLOGY OF EASTERN WISCONSIN. 


The average elevation of the rim of the basin above the point where 
the river leaves the state is about 250 feet, its average distance about 
50 miles, showing an average fall of about five feet per mile. But 
this is less to the point than the following. 

The average elevation of fifteen powers, the first of importance on 
their respective branches is about 155 feet above the surface of the 
river where it leaves the state at Beloit. The average fall from these 
powers to the state line is a little less than three feet per mile. 

With these general statements, we will set aside the tributaries, 
several of which are important, and consider more accurately the 
main stream between Horicon and Beloit. The collecting area above 
Horicon is 436 square miles, upon which the annual rainfall, reckoned 
at thirty inches, would be 30,387,456,000 cubic feet. Allowing one- 
half for evaporation, filtration, and other sources of loss, the theoretical 
discharge at the outlet of Horicon marsh would be 15,193,728,000 
cubic feet. Jteckoned at the lowest rainfall in the last thirty years, 
the amount would be 10,114,749,120 cubic feet. Col. Worrall gives 
in the report previously referred to, as the result of a careful meas- 
urement of the flow at a time when the volume was estimated to be 
only three-fourths of the average, a supply of 27,651 cubic feet per 
minute, or 14,533,365,600 cubic feet per annum, from which it “would 
seem that the calculated amount is not far from the truth. From 
the foregoing data, estimating the accession from tributaries, it is 
thought to be safe to consider the average flow between Horicon and 
Beloit as in round numbers 50,000,000,000 cubic feet per annum. 
The fall from Horicon to the state line is 127 feet. An estimate of 
the theoretical power generated by the main river shows it to be up- 
wards of 20,000 horse power. Of the 127 feet fall, less than 60 feet 
are utilized. Of the unused portion there is more than 30 feet fall 
between Horicon and Watertown, corresponding to above 1,600 horse 
power, and about 23 feet fall between Janesville and Beloit, equal to 
upwards of 7,000 horse power. A portion of this latter may readily 
be made available at Beloit by means of a race leading from a dam 
situated above the slack water of the present one. Another power 
near the state line can also be utilized to the profit of this place. 
Upon the river and its tributaries are a large number of lakes that 
may be utilized as storage reservoirs, thus affecting a much greater 
economy in the use of the water. 

Water power of the Fox river.!. The upper Fox river from its 


1 For the leading facts here given, I am indebted to an article prepared for the Cen- 
tennial Commission by Pres. G. M. Steele, of Lawrence University. I am also indebted 
to Prof. J. C. Foye of the same institution for similar favors. 


HYDROLOGY. 173 


slight descent furnishes no water power, a fact which is compensated 
for by the facilities it offers for navigation. But the lower Fox river 
presents an almost continuous series of rapids from Lake Winnebago 
to Green Bay. In this distance of about thirty-five miles it has a 
fall of 170 feet, so distributed as to be completely and economically 
utilized. The powers upon this river possess an immense advantage 
in the grand natural reservoir furnished by lake Winnebago, which 
embraces an area of about 350 square miles. Neither floods nor 
drouth cause any considerable or inconvenient fluctations in its level, 
and the steady reliable flow thus secured at all seasons is a vast ad- 
vantage. The channel of the river consists of a gorge between clay 
banks, with a floor of heavy bedded limestone, so-that it may be 
dammed with material taken from its own bed, and without overflow- 
ing adjacent lowlands. The great reservoir makes it unnecessary to 
have more than a limited local one, sufficient to guard against inter- 
ference from other powers. 

The minimum flowage is estimated at 150,000 feet per second, this 
amount being available at all seasons of the year. The height and 
power of the several falls estimated on this basis are as follows: 


Names of places. Height of fall. Horse power, 
Neenah and Menasha ..... 0. . cece e cee eee teen eee beeen 10 3,000 
Appleton... ... cece cece eect n eee ee ne eter renee meee ene es 38 11,500 
Cedars saaccdsuinnuaenncdemath ea Riaeteaas ee arated ae 10 3,000 
TittleChute nieacveos hendinae an ar acotates Saaes®. axawear 88 11,500 
Raakaina, io gavsonteecncatace ae deeias dep Saseiestee 40 14,500 
Rapid Crosche ..0.-. cece e cece cree cree e eee ee ener eeereee 8 2,300 
Tittle Kawkatna:-sosise cscs esta ney cesses eset ners’ ences 8 2,300 
De Peres oe sac oot mars avn deeds ca oieselnnarniam eevee ae TS 8 2,300 


STD Lela ctccasass-& sian ental athe aie re CE 150 50,400 


At Neenah, Menasha, Appleton and De Pere, a considerable per- 
centage of the power is now utilized, though a large amount is still 
unimproved, particularly at Appleton. But at the other points only 
the merest fraction is now used, and a wealth of power remains unoc- 
eupied. Attention has already been called to the facilities for trans- 
portation available to manufacturers in this valley, and by consulting 
subsequent portions of this report it will be seen that the agricultural 
and other industrial capabilities of the adjacent and tributary regions 
are very great. 

On the upper portions of the Wolf, Oconto, Peshtigo and Menom- 
onee rivers are numerous falls and rapids furnishing immense power, 
but these lie chiefly beyond the limits of the district under descrip- 
tion. The falls of the Oconto, however, where, by including the rapids. 


174 GEOLOGY OF EASTERN WISCONSIN. 


above and below, a descent of about 60 feet may be made available, 
and the lower rapids on the Peshtigo and Menomonee lie within our 
province and also within the limits of settlement, and must, in the not 
distant future, be improved. 

On the Lake Michigan slope all the available power must soon be 
called into use by the rapid development of that region. 

The average height of the watershed is over 300 feet, and its aver- 
age distance from the lake less than 30 miles, giving a fall, if a direct 
course to the lake were pursued, of more than 10 feet per mile. Or 
to put it in a more utilitarian form, a dam might be constructed at 
the end of every mile, having a fall of eight feet, and still leave de- 
scent enough to cause a rapid flow. The crooked course of the rivers 
however very much reduces the rapidity of descent. 

The Milwaukee river is first utilized as a water power at a height 
of about 475 feet above Lake Michigan. At Barton it has become a 
very considerable stream, and is still 311 feet above the lake level. 
Between West Bend and its mouth, it has a fall of 295 feet. If it 
pursued a direct course to the lake, it would have a fall of 163 feet to 
the mile. If it pursued a direct course to its mouth, it would have a 
fall of 9% feet to the mile. As it is, notwithstanding its tortuous 
course, it has an average fall, as nearly as I can estimate it, of five 
feet per mile. A portion of the power thus given is not yet im- 
proved. 

The Sheboygan river is utilized at a height of about 320 feet, and 
is capable of affording an extensive reservoir at that elevation. 

The Manitowoc is a very considerable stream at an elevation of 275 
feet, and has a very rapid descent in the lower half of its course. 

Many of the smaller streams also furnish efficient water power. 

Changes in Drainage. A comparison of the streams and smaller 
marshes, as laid down on the government plats and earlier maps, with 
the present facts show important changes in the drainage of the re- 
gion. Large areas that are represented as marsh on the plats of the 
government survey are now comparatively dry and arable. Many of 
the smaller streams have disappeared or become mere periodical runs. 
On the accompanying maps the areas Jaid down as marsh by the 
original govenment survey have been indicated with such correc- 
tions as could be made. They are, however, designated as wet lands, 
since a large part are not-now really marsh, and indeed a portion is 
cultivated in all but very wet seasons. They are as a class among 
the most valuable lands in the state. The mapping of these areas, 
besides being valuable as topographical and geological data, has a his- 
torical significance; since it shows what was regarded as marshy at 


HYDROLOGY. 173 


the time of the government survey, and thereby indicates the changes 
that have since ensued. These changes have been much more marked in 
the forest regions than in the more open country, and are so intimately 
connected with the clearing away of the timber that it is a fair infer- 
ence that this is the main cause. 

The timber is often very heavy, and consequently permits but a 
very feeble undergrowth. The removal of the original forest thus 
leaves the surface almost entirely bare, and it is usually at once put 
under cultivation. The effect of so great a change would naturally 
make itself felt upon the drainage of the region. To the extent to 
which this has gone thus far, it has doubtless on the whole been a 
benefit to the region, as it has induced a drier, lighter, warmer soil, 
and more healthful atmosphere. But the limit of benefit in this di- 
rection may be assumed to have been reached except in certain locali- 
ties, and the danger now to be apprehended is that it will proceed to 
an injurious extent. This, however, can easily be avoided, if clearly 
foreseen and justly appreciated. 


176 GEOLOGY OF EASTERN WISCONSIN. 


GHAPT HR. CEH, 
NATIVE VEGETATION. 


The most reliable natural indications of the agricultural capabilities 
of a district are to be found in its native vegetation. The natural 
flora may be regarded as the result of nature’s experiments in crop 
raising through the thousands of years that have elapsed since the re- 
gion became covered with vegetation. If we set aside the inherent 
nature of the several plants, the native vegetation may be regarded as 
the natural correlation of the combined agricultural influences of soil, 
climate, topography, drainage and underlying formations and their 
effect upon it. To determine the exact character of each of these 
agencies independently is a work of no little difficulty; and then to 
compare and combine their respective influences upon vegetation pre- 
sents very great additional difficulty. But the experiments of nature 
furnish us in the native flora a practical correlation of them. The 
native vegetation therefore merits careful consideration, none the less 
so because it is rapidly disappearing, and a record of it will be valua- 
ble historically. 

It is rare in nature that a single plant occupies exclusively any con- 
siderable territory, and in this respect there is an important difference 
between nature’s methods and those of man. The former raises mixed 
crops, the latter chiefly simple ones. But in nature, the mingling of 
plants is not miscellaneous or fortuitous, They are not indiscrimi- 
nately intermixed with each other without regard to their fitness to be 
companions, but occur in groups or communities, the members of which 
are adapted to each other and to their common surroundings. It be- 
comes then a question of much interest and of high practical import- 
“ance to ascertain, within the region under consideration, what are the 
natural groupings of plants, and then what areas are occupied by the 
several groups, after which a comparison with the soils, geological 
formations, surface configuration, drainage and climatic influences 
cannot fail to be productive of valuable results. 

The following natural groups are usually well marked, though of 
course they merge into each other where there is a gradual transition 
from the conditions favorable for one group, to those advantageous to 
another. In some instances it is unquestionably true that other cir- 


NATIVE VEGETATION. 177 


cumstances than natural adaptabilities control the association of these 
plants, and an effort has been made in the study of the region, to dis- 
cern these cases and eliminate them from the results, so that the 
groups which are here given are believed to be natural associations of 
plants. Their distribution is held to show in what localities condi- 
tions peculiarly advantageous to them occur, and hence advantageous 
to those cultivated plants that require similar conditions. 


A. UPLAND VEGETATION. 
(1) Herbaceous. 


Crass I. Prairie Group. One of the most natural and sharply 
defined groups is constituted by our prairie vegetation. It differs 
from all other groups that grow upon the uplands, in being almost 
exclusively herbaceous, and in the fact that the species composing it, 
more rarely intermingle with the other groups. It is more distinct 
from them than they are from each other, and justifies the division 
of the upland flora into prairie and forest vegetation. Its characteris- 
tics are too well known to need further definition here. 


(2) Arboreous. 


Crass II. Zhe Oak Group. This is most nearly related to and 
most closely associated with the prairie group. The prairies are rarely 
contiguous to any other form of arboreous vegetation. . 

The Burr Oak (Quercus macrocarpa), the White Oak (Quercus alba), 
the Red Oak (Quercus rubra), the Pin Oak (Quercus palustris), are 
the most prominent species, and give name to the whole. The Chest- 
nut Oak (Quercus prinus) is associated with these just north of Janes- 
ville, but I have observed it at no other point within the state. The 
common Poplar or Aspen (Populus tremuloides) is the most con- 
spicuous associate of these oaks, but it is not confined to this associa- 
tion. The Large-toothed Poplar (Populus grandidentata) is some- 
times found with this group, but much prefers association with the 
maples. This and the preceding species are in a sense the comple- 
ments of each other. Those associations that are avoided by the one 
are sought by the other, though they not unfrequently mingle. The 
Populus balsamifera and P. candicans have not been observed min- 
gling with this group. The Shell-bark Hickory (Carya alba) is an- 
other prominent member of this cluster. The Pignut Hickory (Carya 
glabra) is occasionally, but not frequently found in this group. It 
sustains the same relation to the Shell-bark Hickory tl at the Great- 
toothed Poplar does to the Trembling Aspen. The Crab Apple (Py- 


Wis. Sur. —12 


178 GEOLOGY OF EASTERN WISCONSIN. 


rus coronaria), the Wild Black Cherry (Prunus serotina), the Choke 
Cherry (Prunus Virginiana), and the Wild Plum (Prunus Ameri- 
cana), represent the Rosacee. The Sumac (Rhus typhina) is com- 
mon, but not significant, as it is a member of other groups. 

The attendant underbrush is equally characteristic. The Hazel- 
nut (Corylus Americana) is almost everywhere present with this 
group, though rare or wanting in connection with the others. The 
Panicled Cornel (Cornus paniculata) is very common, and with the 
Hazel constitutes the chief underbrush. The Wild Red and Black 
Raspberries (eubus strigosus and occidentalis) and the High-bush 
Blackberry (Rubus villosus) are all present, but seem to prefer asso- 
ciation with the other groups. 

If we descend to the herbaceous vegetation beneath, similar facts 
will be found, but it would transcend the brevity desirable in this 
report to enter fully into the details. And there is this further rea- 
son for not doing so in this connection, that many of these plants are 
more dependent upon the conditions furnished by the overshadowing 
vegetation, than upon the nature of the soil, and are therefore less 
instructive as to agricultural questions. 

This group as here constituted includes both the “ Oak openings” 
or “Oak orchards,’ and the denser oak forests. There are sufficient 
reasons, however, for separating them into two classes, as they indi- 
cate different, though allied, agricultural capabilities. The oak open- 
ings are most nearly related to the prairies, while the oak forests 
graduate towards the following classes. Those plants which have been 
mentioned as preferring association with the subsequent groups, as the 
Pignut Hickory, Great-toothed Poplar, ete., are found chiefly in the 
forests, and much more rarely in the openings, while of the species 
common to the prairie and oak groups, the majority are only found 
in the openings, and but few in tke denser oak forests. 

Crass IIT. The Oak and Maple Group. It is difficult to draw 
sharp lines of demarkation between the several classes of heavy forests, 
and tu circumscribe the areas occupied by each. The fact is, that no 
abrupt line of separation exists. But perhaps the distinctions here 
attempted are as clear and as legitimate as in many other departments 
of science, where such distinctions are sanctioned, and for the practi- 
cal ends for which this investigation is made, it is essential that such 
divisions should be attempted, and besides the tout ensemble is dis- 
tinct, though the constituents may be linked into the groups on either 
hand. These observations seem especially demanded as an introdue- 
tion to the definition of this class. The oaks which have been made 
the most conspicuous characteristic of the preceding group are made 


NATIVE VEGETATION. 179 


joint partners in naming this division, and will be found to mingle 
with those that follow. The maples which are here introduced to 
our attention will also play a conspicuous part in subsequent classifi- 
cations. This group is not then characterized by the exclusive pres- 
ence of any prominent plant, but by a distinctive association of plants 
common to several classes. 

The White Oak is the most prominent of its genus, and attains a 
large size. The Red Oak and Burr Oak are usually present. Their 
proportionate number is very much the same as in the denser oak 
groves of the preceding group. But to these oaks there is added the 
Hard or Sugar Maple (Acer saccharinum), and the Red Maple (Acer 
rubrum). The latter seems to have its best development in this asso- 
ciation. The. Elms (Wlmus Americana and U. fulva) are more or 
less present, but not prominent, as also the Linden or Basswood (Tilia 
Americana). The Ironwood (Ostrye Virginica), and the Beech 
(Fagus ferruginea) are excluded from this group. The White Ash 
(Fraxinus Americana) is rarely seen in this connection, but the 
Black Ash (F’ravinus sambucifolia) is common in contiguous low- 
lands. The Hazel (Corylus Americana) is not prominent though 
present, and the Cornus paniculata of the last group is largely replaced 
by Cornus circinata. 

Crass IV. Maple Group. The leading member of this group is 
the Sugar Maple (Acer saccharinum), not that at every point it is 
more numerous than any and all others, but that on the average it 
surpasses the other species. This is, however, in a high sense, a 
mixed group, and embraces some of the densest forests of the state. 
The Oaks of the last group are present here also, but in less numbers 
and in subordination to other species. The Linden (Zilia Ameri- 
cana) is very numerous. The White Elm (Ulmus Americana) which 
in the areas occupied by the foregoing classes was chiefly confined to 
the low lands and river bottoms, here extends itself more upon the 
highlands, and is intimately intermingled with a large assemblage of 
species. The Ulmus fulva is also present. Both the White and 
Black Ash are found, the latter in the lower lands. The Ironwood 
(Ostrya Virginica) is abundant and highly characteristic. The Black 
Walnut (Juglans nigra), and the Butternut, (Juglans cineret) are com- 
mon. The Carya alba (Hickory) is chiefly replaced by Carya glubra 
(Pignut), and similarly the Populus tremuloides gives place to the 
Populus grandidentata. The White Thorn (Crataegus coccinea) is 
common, while the Crab Apple (Pyrus coronaria) is correspond- 
ingly rare. The Wild Plum (Prunus Americana) is less abundant 
than in the Oak group, while its congener, the Black Cherry (Pru- 


180 GEOLOGY OF EASTERN WISCONSIN. 


nus seroting) grows to ampler proportions. The Paper or Canoe 
Birch (Betula papyracea) is occasionally found in favorable local- 
ities, but is uot strictly a member of the class. The Beech (Wagus 
Jerruginea) is excluded and made characteristic of the following 
group. 

Of shrubs, the Round-leaved Cornel (Cornus circinata) exceeds all 
others, and almost entirely excludes the Hazel and Panicled Cornel, 
the dominant forms in the Oak group. 

The herbaceous vegetation is similarly well characterized, but for 
the reasons previously assigned, will not be dwelt upon here. This is 
a well marked group, and its distribution is highly significant. 

Crass V. Maple and Beech Group. This group is essentially 
the same as the preceding, with the addition of the Beech (/’agus 
ferruginea). This separate class for a single tree and a few subordi- 
nate associates is thought to be justified by the fact that the Beech is 
confined to the lake region,' and appears to be especially indicative of 
lake influence, as it occupies different classes of soils and covers dif- 
ferent geological formations. There is less oak in this than in the 
preceding class. 

Crass VI. Zhe Hardwood and Conifer Group. This class con- 
sists of a modification of the last, and the important addition of the 
Conifers. One of the more conspicuous modifications is the more or 
less complete disappearance of those representatives of the Oak group 
that have lingered through the foregoing classes. The Ironwood is 
far less abundant; the Black Walnut and Butternut are rare; the 
Witch Hazel (Zamamelis Virginica), and the Mountain Maple 
(Acer spicutum) appear more prominently among the underbrush. 
The berry-bearing plants are multiplied, as if to compensate for the 
disappearance of the larger fruit-bearers. These changes are pro- 
gressive as we penetrate the area occupied by this class. 

Of the Conifers, the first to be introduced is the White Pine (Pi- 
nus strobus),if we except the Arbor Vite (Zhaja occidentalis), which 
from its proneness to swampy land and other selected localities can 
scarcely be considered a member of this, as an upland group. Far- 
ther to the north, the Red Pine, commonly called Norway Pine (P- 
nus resinosa), becomes somewhat common. The Hemlock (Abies 
Canadensis) is one of the most prominent and abundant members of 
the group. The Balsam Fir (Adbzes balsamea), although preferring 
the immediate vicinity of water, mingles somewhat with the group, 
especially in its northern extension. It is especially abundant on the 
shores of the Green Bay peninsula. An occasional Spruce (Abies 


'See article of I. A. Lapham, Trans. Wis. State Agri. Soc., 1854-5-6-7, p. 236. 


NATIVE VEGETATION. 181 


nigra) wanders away from its marshy habitat, and the Arbor Vite 
extends itself quite freely upon the uplands. 

Crass VIL. Pine Group. This includes the well known vegeta- 
tion of the “ Pine Lands.” It is here made to include those regions 
over which the pine is predominant in distinction from those in 
which it is simply scattered through prevailing hardwood timber, as 
in the preceding group. The leading tree is the Pinus strobus. 

Crass VIII. Limestone Ledge Group. This is a small but inter- 
esting vegetal cluster, covering limited areas in which there is the 
most meager soil, resting upon limestone. In this heavy drift region, 
such areas are few and small, but the distinctness of the flora is so 
marked, and so well illustrates the fundamental principle upon which 
the value of all these observations rests, that it merits a name and 
place as a separate class. The Poplars (Populus tremuloides, grandi- 
dentata, and balsamifera), the Canoe Birch (Betula papyracea), the 
Snowberry (Symphoricarpus racemosus), the Smooth Sumac (Lehus 
glabra), with the Conifers, constitute the major vegetation, and rather 
from the combination than from the constituents, cause it to stand 
out in marked contrast to the heavy timber by which it is fre- 
quently encompassed. It forms a thicket rather than a forest. 
The most characteristic feature is the abundance of the Poplars and 
the Birch. 

The Populus tremuloides is not common in the forests by which 
the typical areas of this class are surrounded, which makes its abund- 
ance here the more conspicuous. 

The Rubus strigosus, Cornus circinata and Lonicera parviflora 
are attendant shrubby plants. The herbaceous vegetation is also 
peculiar. 

Crass IX. .The Comprehensive Group. This class consists of a 
commingling of nearly all the arboreal species of the foregoing groups. 
Clusters may be selected that are representatives of nearly all the 
other classes, but in general the species are curiously mingled, and do 
not array themselves in the definite associations that characterize the 
preceding groups. It is most nearly allied to the Maple, Beech and 
Conifer group, and lies contiguous to it, and near the limit of marked 


lake influence. " 
B. MARSH VEGETATION. 


Crass X. The Grass and Sedge Group. This includes the well 
known occupants of our open meadow marshes. It corresponds to 
the prairie group among upland vegetation, and in many cases gradu- 
ates imperceptibly into it. It embraces several subordinate groups 


‘183 GEOLOGY OF EASTERN WISCONSIN. 


which are very indicative of the nature of the marsh bottom on 
which they grow, but which can scarcely be described in a manner 
intelligible tu the general reader, although they are readily distin- 
guished by observing farmers. It may be remarked in general, how- 
ever, that the better class consist of the grasses proper (Graminea), 
not only because they are in themselves valuable, but also because 
they indicate a bottom susceptible of easy improvement by the sub- 
stitution of more valuable grasses. The Sedges (Cyperacea) in gen- 
eral oceupy marshes that are of inferior value now, and are less 
promising of immediate returns to labor spent in improvement. 
Fortunately the former class largely predominate. 

Crass XI. The Heath Group. This association of swamp vege- 
tation is characterized by the predominance of the members of the 
Heath family (Z’ricacew). Among these the most characteristic 
plant is the Leather Leaf (Cassandra calyculata), and the most im- 
portant one is the Cranberry (Vaccinium macrocarpon). The Wil- 
low, Larch and Sphagnum mosses and a variety of other plants are 
very frequent associates. This class is worthy of attention, not so 
much in view of its prominence as a botanical group, as on account 
of its present and prospective economic importance. The actual ex- 
istence of ‘the cranberry plant in its native state assures us of condi- 
tions favorable to its growth and indicates where cultivation will be 
raost likely to prove remunerative. Where the cranberry itself is 
not present, it is eminently desirable to know what plants are its ha- 
bitual associates and demand similar conditions of soil and moisture, 
since these may be almost equally good guides in the selection of a 
suitable marsh for improvement. Of plants which serve this purpose 
the Cassandra calyculata is regarded as the most reliable. On this 
point an excellent work on the subject says: “In selecting a loca- 
tion it is very important to observe the varieties of plants or trees 
existing upon the ground. Although no cranberry vines may be 
growing there, yet the presence of other plants requiring similar 
conditions of soil and moisture indicate a soil congenial to the growth 
of the cranberry. For instance, the Feather-leaf, also called Gander- 
bush and Leather-leaf (Cassandra calyculata), so abundant in heath 
ponds, is considered a sure indication of a proper locality.’’! 

The distribution and additional facts relative to this group will be 
given a few pages in advance. 

Crass XII. Zhe Tamarac Group. The name is perhaps a sufli- 
cient definition even to the commonest observer. The Tamarac or 
American Larch (Larix Americana) constitutes the entire arboreal 


1 Cranberry Culture, by J. J. White. 


NATIVE VEGETATION. 183 


growth; the Hricacee form the chief undergrowth, and the Sphag- 
noid mosses carpet the peaty bottom, forming a well-marked flora. 

Crass XIII. The Arbor Vite Group. This is similar to the last 

‘save that the Arbor Vite, or White Cedar, as it is frequently called 
(Thuja occidentalis), takes the place in whole or in part of the Tama- 
rac. Usually the Tamarac is present in greater or less numbers. A 
not unfrequent arrangement consists of a predominance of the Arbor 
Vitee around the borders of the swamp, and of the Tamarac toward the 
center. The latter is a more thoroughly swamp species (although oc- 
casionally seen on the hillsides) than the former. 

Crass XIV. Lhe Spruce Group. This is similar to the two pre- 
ceding groups, except that the Black Spruce (Abies nigra) is the chief 
arboreal form. The Larch and Arbor Vite are frequently present. As 
the Spruce is confined to the northern regions, more of the northern 
forms of minor vegetation are associated with this group, although 
the same tendency is shown in the other classes in the same latitude. 

From the habit of these three paludal conifers of mingling, it is 
sometimes difficult to classify a given swamp, and it has not been 
thought important to distinguish them on the accompanying map of 
vegetation, although they were so distinguished on the original map. 


C. GROUPS INTERMEDIATE BETWEEN THE UPLAND AND MARSH 
GROUPS. 


Crass XV. The Black Ash Group. In this, as the name implies, 
the Black Ash (Fraxinus sambucifolia) is the predominating plant. 

The Black Alder (Alnus incana) is a subordinate and quite constant 
associate, and the two characterize the group. The Arbor Vite is fre- 
quently present, and sometimes the Witch Hazel. Otherwise, as far as 
observed, the association is not constant. 

Crass XVI. The Yellow Birch Group. This is not altogether a 
well defined group. The abundance of Yellow Birch (Betula lutea, 
excelsa) is the most marked feature of the vegetation. The Hemlock 
is very common, and the Maples and Beech are present. Under the 
dense shadow of these, several species of Lycopodium, the Dwartf 
Yew (Taxus Canadensis), the large Purple-flowered Raspberry (Rubus 
odoratus), the Ericacese (Pyrola rotundifolia and secunda), the Co- 
hosh (Actea spicata, var. alba) abound among others, though the 
most of these are present in other groups. This group occupies only 
some limited areas in the peninsula east of Green Bay, and in the 
press of other duties, sufficient opportunity was not afforded for satis- 


factory study. 


184 GEOLOGY OF EASTERN WISCONSIN. 


Distribution. On the accompanying map of vegetation, the dis- 
trict covered by each of these classes is delineated, with as much of 
detail and accuracy as was compatible with the demand of other de- 
partments of the survey, and with the rapidity necessitated by the 
large area examined. As that presents their distribution far more 
vividly and accurately than any verbal description, I need only add 
here a few supplementary remarks. 

It will be seen by consulting the map, that ¢he pracries are almost 
exclusively confined to the southwestern portion of the district, or 
chiefly to the Mississippi drainage system, though this fact perhaps 
has no special significance. The surface of a portion of these prairies 
is level, and bears evidence of having formerly been a lake bottom, 
while that of others is elevated and undulating, and bears no evidence 
of having been submerged since the retreat of the glacier. The areas 
of prairie and forest are so intermingled as to forbid any topogra- 
phical distinction between them, and to negative any explanation of 
their origin that is dependent on surface features. It is not proposed 
to enter here upon the much discussed question of the origin of prat- 
ries, but simply to remark that the tenor of the facts in this region, 
bearing upon the question, supports the general views so ably pres- 
ented by Profs. Dana, Newberry, Guyot and others, and at the same 
time harmonizes with the observations of Prof. Whitney, to the ex- 
tent that the nature of the soil is the most essential primary agency. 
It is not however because the soil is incapable of supporting trees, for 
when planted upon the prairies they flourish luxuriantly, and when 
the soil is cultivated or shaded so that a proper degree and constant 
supply of moisture is secured, trees are propagated from the seed with 
facility. In the first case, in planting the trees, the superficial com- 
pact soil, which is believed to be the real barrier to the extension of 
the forests in ties region, is penetrated, and the roots of the treo 
placed below it, and it is at the same time loosened, and mingled with 
the subsoil; and in the second case, artificial stirring of the soil or 
special conditions supply the moisture essential to the growth of ar- 
boreous vegetation. But in its native, undisturbed condition, the fine 
superficial soil becomes exceedingly dry at intervals during the sea- 
son, and renders it impossible or exceedingly difficult for the young 
seedling to maintain its existence until it can gain a foot-hold upon 
the deeper and uniformly moist subsoil. This difficulty is increased 
by the antagonism of the grasses that can successfully withstand these 
variations of moisture, and by annual fires. The latter have doubt- 
less modified the form and extent of the prairies in some degree, but 
it is generally conceded by those who have studied the subject com- 


NATIVE VEGETATION. ‘185 


prehensively, that it is entirely inadequate as an explanation of prai- 
ries in general. 

Lhe Oak group is likewise chiefly confined to the southwestern part 
of the district. It occupies all classes of topography and all eleva- 
tions from the lake level to 500 feet above it. It shows a tendency to 
invade the districts of the heavier forests, along the liue of the Kettle 
Range. This is due to the nature of the soil that accompanies the 
Range, as will be seen hereafter. 

The Oak and Maple group usually lies contiguous to the last or 
along the Kettle Range. It was in the latter relationship that its pe- 
culiarities were first and chiefly noticed. This seems to be due to the 
fact: that the soil is adapted to the Oak group, while the surroundings 
are favorable to the propagation of the Maple and its assoviates. A 
conflict of conditions is the result, in which neither has a decided ad- 
vantage. 

The Maple group occupies an irregular belt that has a northwest 
and southeast trend, bordered chiefly by Oaks on the south and Beech 
and its associates on the north. It is quite distinctly limited in the 
direction of the Oaks, but much less so toward the Oak and Maple, and 
the Maple and Beech groups, into which it merges almost impercepti- 
bly. It reaches from the lake shore to about 500 feet in elevation. 

The Maple and Beech group covers a large surface stretching from 
the lake shore northwestward, a direction which neither corresponds 
to geological nor topographical lines, but is none the less instructive 
on that account. It does, however, correspond very closely with tne 
isothermals for the summer months;' which, with the other elements 
of the lake influence, as already intimated, are undoubtedly the con- 
trolling agencies. 

To the north of this the Hardwood and Conifer group extends to Port 
de Morts, being more extensive than either of the others. The great- 
est elevation within its area is less than 400 feet above Lake Michigan. 

The Convprehensive group occupies a portion of the crest and west- 
ern slope of the outcropping rocky ridge of our district. It is limit- 
ed chiefly to the Green Bay region. It seems to be the result of the 
conflicting demands of lake and boreal influences, on the one hand, 
and of soil and warm, dry southwest winds, sweeping up the Green 
Bay valley, on the other. 


!See Map of Wisconsin with lines showing the Remarkable Effect of Lake Michigan 
in Elevating the Temperature for January and Depressing that of July, by I. A. Lap- 
ham, 1865. Also Transactions Chicago Academy of Sciences, Vol. I, Plate X, 1865. See 
also, The Isothermal Lines of Wisconsin, by J. G. Knapp, Transactions Wisconsin Hor- 
ticultural Society, Madison, 1871. 


186 GEOLOGY OF EASTERN WISCONSIN. 


In the lowlands, the Grass and Sedge marshes which correspond to, 
and in many cases are, unquestionably the forerunners of the prairies, 
are like them, chiefly confined to the southwestern region. 

As we enter the dense forests to the north, the Zamarac swamps 
almost entirely replace them, and these in turn, in the still higher 
latitudes, are in part replaced by the Vedar and Spruce swamps. The 
Ash swamps are more abundant and extensive at the north, and the 
Yellow Birch flats are entirely northern. 

The distribution of the Heath, or Cranberry group, is not less in- 
teresting than important. The marshes occupied by this class readily 
arrange themselves, on inspection, into four clusters, having a definite 
relationship to the geological formations. Those in the northwestern 
part of the district are to be grouped with the great marshes near 
Berlin and to the westward, and rest upon the Potsdam sandstone. 
Those in the western part of Jefferson county lie upon, or near, the 
St. Peters sandstone. Those in Oconomowoc, Concord, Hebron, Sum- 
mit, Delafield, Ottawa, Eagle, Richmond and Sugar Creek, form a 
numerous group of small marshes, and rest wpon a sandy district that 
seems to have had its origin in drift from the arenaceous layers of the 
Cincinnati shale, subsequently modified by lake action, of which the 
swamps are the lingering representatives. The fourth group com- 
prises those that lie along the line of the ancient sand beaches of Lake 
Michigan, of which the marshes near Sturgeon Bay and Peshtigo are 
examples. Zhe demand for silica is thus shown in the natural dis- 
tribution of the plant, and we have in this a beautiful illustration of 
the fundamental principle insisted upon in this report. Native cran- 
berries occur at the following locations: 


Sugar Creek, T. 3, R. 16 E. Sec. 18. 

Richmond, T. 3, R. 15 E. Sec. 18. 

Eagle, T. 5, R.17 E. See. 31, N. W. qr. 

Ottawa, T. 6, R.17 E. Secs. 32 and 28. 

Hebron, T. 6, R. 15 E. 

Lake Mills, T, 7, R. 13 E. 

Concord, T. 7, R. 16 E. See. 26. P 

Summit, T. 7, R, 17 E. Secs. 9 and 12, N. W. qr. © 

Delafield, T. 7, R. 18 HE. Sec. 34, N. E. qr., and sec, 27, 8. E. qr. 

Oconomowoc, T. 8, R. 17 E. Sec. 4. 

Oakland, T. 6, R. 18 E. Sec. 8,8. W. qr., and sec. 17. 

Sturgeon Bay, T. 27, R. 26 E. Sec. 12, W. hf. 

Caledonia, T. 21, R.14 E. Sec. 29. 

Peshtigo and Marinette, T. 30, R. 23 E. Sec. 21 and adjoining. 

Aurora, T. 18, R. 18 W., where the marshes occupy several sections east and 
southeast of the village of Auroraville, and are among the most extensive and 
productive in the state. 


NATIVE VEGETATION, 187 


Doubtless they occur also at other points that escaped my knowl- 
edge. When it is considered that the size of the district required 
the inspection of from 3,000 to’4,000 square miles each season, some 
omissions in matters not specifically geological will doubtless be par- 
doned by a generous public. 

The elements of success in cranberry culture, so far as they are rel- 
evant here, seem to be the following, as I glean from several author- 
ities: 

I. A Suitable Bottom. A good bed of peat is the best, that being 
the principal food of the plant. At the east, cedar swamp bottoms 
are preferred by many. Our tamarac swamps will doubtless be 
equally satisfactory; indeed, native cranberries are sometimes found 
growing on them. 

Il. Facilities for drainage, and complete control of it, so that the 
marsh may be drained or flooded, as may be demanded. 

III. A Sufficient Supply of Silica. This is sometimes already 
present, but is usually to be supplied by covering the surface with 
sand. ‘Silica plants”? differ from “peat plauts” in appearance and 
mode of growth, and in yielding at least three times the amount of 
fruit produced by the latter. The successful culture of the cranberry 
is also limited to certain latitudes. If too far north, the early frosts 
prevent their maturing and render them a precarious crop. If too far 
south, the heat interferes with their proper development. Actual ex- 
perience is the best guide in respect to this, as well as the other con- 
ditions, and hence the value of observations on the experiments that 
Nature has herself made. 


188 GEOLOGY OF EASTERN WISCONSIN. 


CHAPTER IV. 
SOILS. 


There are few subjects upon which it is more difficult to make an 
accurate, and at the same time an intelligible report, than upon soils. 
This difficulty arises partly from the nature of the subject, and partly 
from the vagueness of the terms used in speaking of soils. Aside 
from the vagueness, these terms have a different signification as used 
by different persons, which adds to the difficulty. We speak of “light 
soils” and “heavy soils,” and perhaps, without thinking, we suppose 
that these terms refer to actual weight, or, in the terms of science, 
to specific gravity. But such is not usually the fact. Thus, we say, 
“a heavy clay soil” and “a light sandy soil,’’ but in fact the weight 
of the clay soil is only about three-quarters of that of the sandy soil, 
measure for measure. These terms, as commonly used, really refer 
to adhesiveness, degree of comminution, or power of holding water, 
or, more properly, perhaps, to the way in which the soil “works.” 
Again, the term “sandy soils” is supposed, even by persons some- 
what versed in the sciences, to mean those that are made up of grains 
of quartz; or, in other words, are silicious, and hence are more or less 
barren. But this is not always true. Some sandy soils are composed 
of grains of limestone, and are very fertile, an instance of which will 
be described presently. So, a clay soil is supposed by many some- 
what intelligent in chemistry, to be composed of aluminous material, 
but this is far from always being the case, as the term is commonly 
used. 

This obscurity will, however, in a measure, disappear as we procecd 
to consider the orzgin of the soils of Eastern Wisconsin, which appro- 
priately claims our attention here. 

The organic constituents of the soil have manifestly been derived 
from the plants that the soil has itself produced, and are only the re- 
sult of accumulated self-enrichment. Local exceptions to this are to 
be found in those cases where soils have received organic material 
washed from adjacent areas. This vegetable matter takes various 
forms, but all may be spoken of under the comprehensive term, 
humus. In marshy locations, the moisture prevents the decay of 


SOILS. 189 


vegetable accumulations to such an extent that the resulting humus 
forms the main constituent of the soil, and the mineral ingredients 
are entirely subordinate in amount and function, thus forming a soil 
of vegetable origin. 

With this exception, the leading elements of our soils are derived 
directly or indirectly from the rocks, either through their powdering 
by mechanical means, or disintegration by chemical agencies. The 
chief mechanical agent in pulverizing the rocks has been water in its 
various states, especially in the form of glacial ice. When the great 
glacier plowed over this region, it broke fragments from every forma- 
tion over which it passed, ground them to various stages of commin- 
ution, and left the commingled mass spread over the face of the coun- 
try, forming a most excellent foundation for our soils. Subsequently, 
water in the form of lakes and rivers washed out and redeposited a 
portion of this material, giving rise to sandy beach lines and lacus- 
trine and fluviatile deposits of clay. 

But this material was still too crude to constitute a fertile soil, and 
besides, over many small areas, these agencies left the rock entirely 
bare. Then followed a process of disintegration, of a chemical or 
chemico-physical nature, popularly spoken of as the action of the ele- 
ments, by which the surface of this material, and the rock surface, 
where exposed, was reduced to the condition of soil, which in the pro- 
gress of ages enriched itself by its own vegetation. It appears, then, 
that (1) a portion of our soils were derived directly from the glacial 
accumulations, and are properly called drift soils; that (2) a portion 
were derived from the same kind of material, but after it had been 
washed and redeposited by lake and river action, forming soils of 
lacustrine and fluviatile origin; and (3) that another portion had their 
origin in the direct decomposition of the undisturbed rock formations. 
It will now be clear that the character of a soil will depend upon (1) 
the nature of the rock from which it was derived; (2) the manner and 
degree of its reduction; (3) the amount lost by leaching and other- 
wise; and (4) the amount gained by vegetation from above or capil- 
lary action from beneath. Or, to put the matter much more simply, 
a soil depends chiefly upon (1) the chemical nature of the material, 
and (2) its physical state or the degree of fineness to which it is ro- 
duced. These elements will receive prominent attention in the de- 
scriptions of soil that follow. . 

To fully understand the nature of the material, all the rock forma- 
tions of the region and those that lie to the north and east, whence 
the glacier came, should be studied, since they have all made contri- 
butions to our highly composite soils, and herein the strictly geologi- 


190 GEOLOGY OF EASTERN WISCONSIN. 


cal relations of the subject are apparent. It will be sufficient. here, 
however, to call attention to the four general classes of rocks that 
have chiefly entered into the formation of the soils of the part of the 
state under consideration, and for fuller knowledge, refer the reader 
to the general report. These are (1) the Archean rocks, whose min- 
eral nature is very complex, but which give rise chiefly to silicious 
and aluminous material; (2) the sandstones that contribute silica; (3) 
the shales, that are chiefly aluminous; and (4), most abundant and 
important of all, the dolomites or magnesian limestones, that contrib- 
ute lime and magnesia. Soda, potash, phosphorus, and other ingre- 
dients, exist in small quantities in the several formations. The lime 
and magnesia occur chiefly in the form of carbonates, and their pres- 
ence is manifested by effervescence on the application of acid, with 
which the soils were extensively tested in the field. 

The following descriptions of the soils of the district under con- 
sideration relate rather to the subsoil than the soil proper; at least 
there has been an effort to set aside purely surface characters, first, 
because the surface soil is subject to so many local and changeable 
influences, and has been so much modified by cultivation and other 
artificial causes, that a series of observations upon typical or “virgin” 
soils was scarcely possible, and secondly, because the future of our 
agriculture depends not so much upon the present soil as upon the 
subsoil, since winds, waters and cropping are rapidly sweeping the 
surface away, and but comparatively few years will pass before our 
present subsoil will be at the surface, and for the further reason that 
the power of the surface soil to retain the strength it has, and to draw 
mineral resources from below, is most evidently dependent on the 
subsoil. 

If, in reading the descriptions that follow, the reader will be kind 
enough to place before him Plate III of the accompanying atlas, the 
areas occupied by each class will be seen more definitely than they 
could be presented by description, which will then be for the greater 
part omitted. It will be readily understood by every one, that soils 
vary much in every section, and even on the same farm, and that the 
varieties graduate into each other in the most intricate and impercep- 
tible manner, and yet at the same time cvery region has a prevailing 
character that can be classed, described and mapped. The accom- 
panying map is only intended to indicate such prevailing kinds, and 
of course each color covers patches of greater or less size, of different 
kinds. 

Notwithstanding the impracticability of mapping these local varia- 
tions and intermediate varieties, it is believed that the map given will 


SOILS. 191 


prove of some essential service to the increasingly large number of 
our agriculturists who desire to study the interests of their professiou 
in a comprehensive and philosophic manner. The following descrip- 
tions will, however, be found quite closely applicable in detailed study. 

Crass. I. Prairie Loam. This class is too well known to need 
much description. It sometimes arises from the decomposition of 
the underlying limestone, sometimes from the disintegration of lime- 
stone gravel, and sometimes it arises from the deposit of an ancient 
lake. There are several varieties, but all have at least a moderate 
degree of fineness of texture while some manifest this quality in a 
very high degree. This is more particularly true of those that are 
derived directly from the decomposition of the limestone, the type of 
which is a black “light” soil, that works like an ash bed when dry, 
and rolls into little pill-like pellets when wet, and refuses to scour ex- 
cept with the very best of plows. It is a warm soil, but not so rich 
as its blackness might lead one to suppose, yet very responsive to 
proper fertilizers. This particular variety occupies but limited areas. 
The other kinds are slightly more arenaceous and work with the 
greatest ease. 

In chemical composition, silica is the chief ingredient, with which 
is associated ‘variety of mineral substances that constitute plant food, 
as shown by the analysis at the close of these descriptions. 

The small quantity of the carbonates of lime and magnesia may 
seem at first strange, since the soil is chiefly derived from magnesian 
limestone, but it becomes clear enough when we consider that the 
disintegration by which it was formed consisted of the dissolving ont 
of the lime and magnesia, leaving the residue. But as these sub- 
stances exist in abundance in the stratum immediately beneath, and 
impregnate the water, they are brought to the surface in dry weather 
by capillary action so that these soils rarely suffer for the want of 
mineral substances. In judging of the strength of our soils from 
analysis it should be borne in mind that there exists in the immediate 
substratum an inexhaustible supply of the soluble mineral substances 
needed for plant food. Our soils are new gevlogically as well as new 
in the history of cultivation. 

Vegetable matter in the form of humus penetrates this soil to 
greater depths than in most of the following classes, and imparts to 
it a darker color. 

The areas occupied by it will be found on the map above referred 
to. It will be observed that they are mainly confined to the south- 
western third of the district under consideration, or, as it happens, 
perhaps casually, to the Mississippi basin. 


192 GEOLOGY OF EASTERN WISCONSIN. 


Crass Il. The Lighter Marly Clay Soils, or Clayey Loams. 
These are drift soils, having been derived chiefly from a calcareous 
bowlder clay, which in turn was formed by the powdering of various 
kinds of rocks, but chiefly magnesian limestones, by glacial agencies. 
It therefore contained originally a large proportion of calcareous and 
magnesian material, and a less amount of silicious and aluminous; 
but the leaching action of water and the growth of vegetation has re- 
moved a much larger amount proportionally of the lime and magne- 
sia than of the other ingredients, so as to leave these the chief con- 
stituents at the surface. But the deeper subsoil is highly marly in 
its nature. There is just enough of sandy material in it to make it 
loamy. The dark vegetable matter does not penetrate as deeply as in 
the prairie loam, so that the plow frequently turns up the reddish or 
yellowish subsoil containing very little humus. This soil works with 
the utmost facility, indeed is unsurpassed in this respect. It stands 
both wet and drought well, and is a very durable and fertile soil. 

This class graduates into the sandy loams on the one hand, and 
heavier clayey loams on the other. It prevails in the same general 
region as the prairie loams, its areas being irregularly interwoven 
with them. 

Oxass III. The Heavier Marly Clay Soils, or Heavier Clayey 
Loams. This class is similar to the preceding, both in origin and 
character. But the drift from which it was derived contained more 
Archsan bowlders, especially those containing feldspar, hornblende, 
and similar minerals in large proportion. From the powdering and 
disintegration of these, a large amount of clay proper was derived, 
mingled, however, with the quartzose material of the same rocks and 
with much caleareous and magnesian clay, derived in a similar way 
from the dolomites which usually form a prominent part of the drift. 
This is not then a true clay soil, for there is a notable proportion of 
lime, magnesia and free silica present, but it is, as named above, a 
marly clay, of the heavier class, when compared with the foregoing. 
The term -:loam is not properly applicable to the subsoil, but at the 
surface, drainage has exercised an assorting influence over it, separat- 
ing and carrying away the finer material, and leaving the sand, which 
gives to the surface a lighter loamy character. This surface soil 
rarely gives any effervescence when submitted to the action of hydre- 
chloric acid, while that from greater depths usually responds with 
vigorous action. We find here again what I have found to be true 
everywhere, that the surface soil is almost entirely exhausted of the 
carbonates of lime and magnesia, even where they exist in g'eat 
abundance in the deeper subsoil. And it is for this reason that the 


SOILS. 193 


origin and nature of the comparatively unmodified subsoil must be 
studied if we are to arrive at any reliable conclusions as to the per- 
manent resources of our soils. A considerable proportion of iron 
exists, as might be expected, from the decomposition of the horn- 
blende and allied minerals, and gives to the soil a yellowish orange or 
reddish color. The high color indicates the presence of the sesquiox- 
ides; and the more or less chalybeate character of the waters demon- 
strates the existence of the more soluble compounds; while a magnet 
drawn through the pulverized soil frequently brings forth a bristling 
edge of magnetite, showing the presence of iron in that form. The 
surface is frequently strewn with bowlders, chiefly ‘‘hard-heads,”’ 
while cobble stones and pebbles mingle more or less with the soil, 
though not to an extent that would often justify the term gravelly. 
The vegetable mold is confined mainly to a few inches at the surface. 

This soil works with more difficulty than the last, but is strong and 
enduring, and will improve rather than otherwise with use. It be- 
comes lighter and warmer as it is stirred, and is gradually becoming 
fitted for crops that did not at first flourish upon it. This is the pre- 
vailing soil in the heavily timbered regions in the central portions of 
our district. 

Cuass IV. The Red Marly Clay Soils. The term “red clay” is 
popularly applied to a very extensive deposit in the northeastern 
part of the state, and to the soil derived from it. It is very properly 
denominated a clay, if we use the term in asimply physicalsense. It 
is finely comminuted, close, compact, adhesive and almost impervious. 
It washes, cracks and otherwise deports itself asa clay. These qual- 
ities, however, do not reach an excessive development. It never pos- 
sesses that extreme tenacity when wet, or that obdurate hardness 
when dry, that characterizes the typical aluminous clay. It contains, 
moreover, in most localities, fragments of limestone, and occasionally 
other rock, which modify these qualities. In chemical composition, 
however, it is not a true clay. Beside the aluminous element, there 
is a varying proportion of silicious matter, a notable ingredient of 
carbonate of lime and magnesia, and a very constant intermixture of 
hematite and magnetite. It is rarely that a magnet drawn through 
a handful of dust fails to bring forth grains of the latter. In like 
manner the application of acid to the unleached subsoil seldom fails 
to give a prompt and vigorous effervescence. The opposite is true, 
however, of the surface soil. The difference between the two is also 
usually indicated by physical characteristics. One of the most no- 
ticeable of these is the intimate fissuring of the upper subsoil when 
dry, by innumerable little cracks that divide the mass into small rude- 

Wis. Sur. —13 


194 GEOLOGY OF EASTERN WISCONSIN. 


ly cubical blocks, so that when dug up it is neither pulverulent nor 
aggregated in rounded clods, as is the case with arenaceous and loamy 
soils, but is simply a heap of little blocks. From this portion the 
carbonates have been pretty thoroughly removed. Hydrochloric acid 
seldom produces effervescence, never any vigorous action. The fissur- 
ing is to be regarded as the cause rather than as the result of this re- 
moval of the soluble carbonates. The color of this portion is also 
somewhat duller and more inclined to a mottled and brownish hue 
than the lower unmodified portion, which is usually a pinkish or pur- 
plish red. This lower portion is the true subsoil, and is the part 
previously described. The immediate surface has an ash color. 

This soil needs thorough working, which is not so easily accom- 
plished as with the loamy arenaceous soils, but it yields excellent re- 
turns. It is an exceedingly strong, durable, fertile soil. Its strength 
lies in its native constitution and not in a superficial layer of vegeta- 
ble mold, soon to be exhausted. Cultivation improves rather than 
exhausts it, and it will still continue to yield bountiful harvests when 
many other soils will need the constant stimulus of fertilizers. The 
stirring, the washing out of the finer materials, and the exposure to 
the air incident to cultivation, give it a lighter and warmer character, 
so that after a few years cultivation, crops may profitably be intro- 
duced that at first were unsuccessful. 

The map shows it to occupy a belt along Lake Michigan, from Mil- 
waukee to Sturgeon Bay, widening to the northward until it passes 
the summit between the lake and the great valley, and occupies the 
basin of the Fox river and Lake Winnebago. 

Crass V. The Limestone Loam. This is not a very sharply de- 
fined class. It appears to have its origin in the decomposition of the 
magnesian limestone upon which it rests. It thus differs from either 
of the marly clays, to which it is most nearly allied, in not being a 
drift soil. It is usually yellowish or reddish in color, rather plastic 
and adhesive, moderately comminuted, of only medium porosity, and 
in chemical nature it is chiefly silicious and aluminous, or in the lan- 
guage of its origin, the insoluble residue of the limestone. The car- 
bonates of lime and magnesia, though, forming the chief constituents 
of the original rock, are present in the soil in very limited quantities. 
This makes the use of the name here given objectionable, if it is 
thought to indicate the composition of the soil. It was selected for 
want of a better one to indicate its origin. 

The depth of the soil, except in the valleys, is not considerable, and 
the rock itself is really to be regarded as the permanent subsoil. It is 
reached even by the roots of cereals over much of the area occupied 


SOILS. 195 


by this class. It is a fertile soil, is easily worked, and supports a 
dense growth of timber. 

Crass VI. Silictous Sandy Soils. This class needs little atten- 
tion here, because, in the first place, it is too well known to require 
elaborate definition, and, in the second place, it fortunately occupies 
so little area that it posseses no great importance in considering the 
district asa whole. As found in this region, it had its origin in beach 
deposits made by the lake in former times, and in drift from silicious 
rocks. As it occurs chiefly in narrow strips surrounded or bordered 
by clay soils, it may not on the whole prove a great disadvantage, 
although of itself it is a sterile soil, for when it mingles with the 
adjoining clay it produces a rich, fertile loam, better adapted to some 
crops than the clays themselves. 

Crass VII. Zhe Caleareous Sandy Soils. My attention was first 
called to this class by observing a heavy growth of maple and associ- 
ated trees upon a sandy soil. This was so contrary to previous obser- 
vations that it led to an examination of the sand. This showed it to 
be composed of small crystals of dolomite mingled with a-varying 
quantity of silicious grains. From the immediate surface the more 
soluble dolomite has been removed, leaving the silicions sand at the 
top in such a way as to disguise the true nature of the subsoil. This 
surface soil is light, warm and arenaceous, but, to casual observation, 
would give no promise of permanent fertility. The fact that the sub- 
soil is so largely dolomitic, instead of silicious, adds not less than 
one hundred per cent. to the value of the land. A general knowledge 
of this fact on the part of the proprietors ought not only to add to the 
appreciation in which their land is held, but enhance their returns by 
guiding them in selecting those crops for which their soil is peculiarly 
adapted. This also presents a rich field for the study of agricultural 
problems relating to sandy and calcareous soils. This is not, however, 
the sole occupant of any considerable area, but is freely intermingled 
with marly clay and gravelly soils and various intermediate grades, as 
well as the silicious variety. It is a drift soil. The calcareous sand 
had its origin in the granular dolomites of the Niagara Group. 

Crass VIII. Zhe Humus Soils. Under this head is grouped 
those soils in which humus in some of its varieties, chiefly peat and 
swamp muck, is the predominant element, and in which the mineral 
ingredients are largely concealed by it. The peaty soils are the type 
of the class. In these, not only the surface but the subsoil is chiefly 
of organic origin. Soils simply covered with a layer of vegetable mold 
arenot hereincluded. Almostall the swampy, anda large portion of the 
bottom lands, are covered by this soil. But it is not so easy to define 


196 GEOLOGY OF EASTERN WISCONSIN. 


the adaptabilities of this class, or measure its fertility. Some por- 
tions, with simple drainage, will produce the most luxuriant growth 
of grass or grain. Others are impregnated with organic acids derived 
from the humus, and are known as “sour soils,” and are unfit for the 
growth of the cereals and the better class of grasses. Others still are 
so largely composed of organic matter that they do not contain the 
requisite amount of mineral ingredients. The character of the vege- 
tation naturally growing upon it is the best indication of the nature 
of any given example of this class. 

Alluvial Soils. Closely associated with this last class, and inter- 
mediate between it and the prairie loam, we find a soil formed by the 
aceumulation of sediment washed from the uplands and deposited on 
the bottom lands adjacent to streams, and in other favorable localities. 
It is better marked in its origin than in its character, for when min- 
eral ingredients predominate, it very closely resembles the prairie 
loam, both in the fineness of the material and in its chemical nature, 
and when vegetable matter becomes predominant it does not differ 
essentially from the humus soils. For this reason, and because its 
distribution has no special significance in studying agricultural prob- 
lems, it has not been mapped as a separate class, although it occupies 
in the aggregate a large area, and is an exceedingly fertile and valu- 
able soil. The following analyses are by Mr. Bode: 


100 PARTS OF THE DRIED SOIL 
CONTAIN 
ANALYSES OF SOILS. 5.4.4 eg 

ase | B84 (PES 

2d 2O¢ a8 8 
27 & |AU ae 
‘3 Eb a ad lg BES 
aS | GAS [Boss 

Soluble in hydrochloric acid — 

Organic matter... 1+. ssse eee ee ee eee ee ees 4.94 91.40 5.84 
Oxide of WON .. +... eee e eee ee eee eee teen eens 2.88 3.59 3.03 
Alumina = At evans OMS aay eeH oeGna ee PR MAL Nes 2.84 2.52 2.82 
Silica... eee eee eee eee e teen ener es 0.60 0.07 0.50 
Oxide of manganese. ...... 6... + ee eeee ee eee ees 0.18 0.18 0.12 
Lime cece eee cece eee eee eee eee eee 0.18 0.28 4.02 
MA GneBifiscamsddnasamcnecer men neaeadenwames 0.04 0.03 8.48 
Oda ancien ae wvesiain ae ewes cneteh a iene wate nionies 0.49 0.51 0.15 
Potassai:s craves vor ernee awe eeers wo-wews cewies 0.19 OTE: lene teas 
Phosphoric aCid.... sss seceeceeeeeeneeeeeeneee 0:06 0.12 0.19 
Caen’ ear i oli Tae tte Ancora Seaeel aaa tanta 0.52 0.25 7.08 

UlpHUTIG ACilecessewensemers toes sans Looe ceeds 0.03 i ’ 
Insoluble in hydrochloric acid — oo ne 
SHCA eee eee eee ee eee eee ee ee cee eee ees 78.99 64.42 59.76 
Oxide OL ILOM @ hs eee esi ces ted eaeeeeee agers gees 5.28 9.15 1.36 
Lime .- essere ee PTUs LMT SE ea HER SR TT AEE eS 1.12 1.34 1.01 
Magnesia... sce cree eee e cree eee e cece cere eens 1.08 0.60 |iacsesvd 
AMWMING «. cece eee eS Save w ees tenaced Zasuedss 1.88 2.28 10.62 
100.00 100.00 100.00 


SOILS. 197 


Magnesian Character of these Soils. It is worthy of notice here 
that these soils are magnesian. This, I believe, in the future unfold- 
ings of agricultural science, will befound to be a very important fact. 
Magnesia has been a much abused substance. It was formerly sup- 
posed that magnesian limestone made an inferior quick lime, and it 
long lay under disfavor. But experience has finally shown that pre- 
cisely the opposite is true. It is far superior to pure limestone for this 
purpose. It was long, indeed almost even now, thought to be unsuited 
for flux with iron ores, but this opinion has recently been modified. 
Magnesian limestone, burned to quicklime, was formerly prohibited 
as a fertilizer, and the ban has been only recently removed. That 
some such revolution of opinion must take place in reference to its 
utility as an ingredient of the soil seems to be forcibly suggested by 
the following extracts from analyses taken from Prof. Johnson’s ex- 
cellent treatise “ Ilow Crops Grow,” “being the average of all trust- 


worthy analyses published up to August, 1865”: ; 
Magenesta. LIME. 
Per cent. Per cent. 


Woh Giititend oJcdsscvegacteleevintniaerdetia a ena aiclukeaniedtabaamta del 12.2 3.1 
Rive varateaiertieiger ab ine ds och vs Gee eee eee esas eyes Sees 10.9 2.7 
Barley’ ssncken comeseyoedes cee 40 $49 654 Fe sdaG a oes wees 8.3 2.5 
Oats: na0 sees eis BRAGA tie Re eee eee haa teaeeeae neat 7:8 3.8 
Maize} chse Sar oalarneacblhiaclen Gabe Shiwea Seen bes en swe enone 14.6 oF, 
Buck wheatincicsuissiuuss sca ci aw sec wa. Geaey sea yaee ei as 13.4 3.3 
TAS hes AS enotedinar urate nels s ae ee ees aula O's alone ealog eles 13.2 8.4 
Bebb iviaue cd aesnedees ope o ee eie we hae esa Sees eedee es 18.9 15.6 
TT RUTAP 5 eisidipinecsaicnswrewdis Sunes Aka ea acetal BEd Sate deeitis HAS 8.7 17.4 
Gairob) 1 else Sueenawat kama aecotnad Nextarieas 6.7 38.8 
DP Gais) c e2.4 ods aeRO SeG WHO Hes ee by ee ne ee ede eae eee 8.0 4.2 
Wield H6anS:suiseciokedieas oar eeeaseied ees 2425 6 ee eawa a 6.7 5.2 
Garden beans s2-cnarscsssawnad ened saree ca vend iene seiees 7.5 7.7 
(ower Sed atnn 5 Whikes ceed he Re aaies aamieaaine meee eee 14.2 6.2 
POtALOES scat a dow See se eE Es oe aa ae SEEN FE Wee ete ale 4.5 2.3 


From which we see that in the grains, the magnesia predominates 
decidedly. In the fibrous part of the plant the opposite is true; as 


follows: 
Maanesia. Lime. 


Per cent. Per cent. 


Winter wheat straw. ..--2ecececereeeeecereeeneeteseerane 2.6 6.2 
RYy@ cece cece ce cect ener ere n eee n een eee n enn nenens 3.1 7.7 
Barley... .cseceeec cee c cree eee teen eeeen een cece ces eraees 2.4 7.6 
(0) (= 4.0 8.2 
Maize cc ccc cece cece cece eee erence ne ene ne nee eee e ten eee 5.5 10.5 
So 7.7 87.9 
Field beans. ... cc cecceeceeeer cece nc ee et eeeeteeennenceees 7.8 23.1 
Garden beans .... eee ce cree reece eee eect ersten cnet ee ce ees 5.2 27.4 


Buckwheat....cceceec cee ce eee ene eenseeeee eer earenceees 8.6 18.4 


198 GEOLOGY OF EASTERN WISCONSIN. 


Maenesta. Lime. 
Per cent Per cent. 


Oaks Ody WOO wien nitew teen esse taaeaecenes panels 4.8 73.5 
Oak, small branches with bark..........0020 ceeeeee cree 7.5 54.0 
Poplar, young twigs ..........cscec cece eect ence ee eeenene 7.5 58.4 
Elm; Young: GWIeS os. sekecawksoeae wan ssa taaiiew tinea 10.0 87.9 
Elin, body w00dss.« ss crsaues eee eae ce eee eee new sees vee 47.8 
Linden (Bass: WO0d). «cic cca cise a earseesedanaeersuen wee 4.2 29.9 
JAS pL er tHEE: on ea, caenean Moree nai ndee ton deaths day sa ROMER RRS 5.7 81.0 
Apple tree, entire fruit... 2.0... cece cee e ener cere ceeneeeee 8.8 4.1 
Beech) secvavvates ealsctauns aiene sume, Shea a aaed penance 45.8 16.8 
White piney; <soraaueecumse ies samwaueldliceined aaa esas 5.9 50.1 
Darth: sinc ciedsaeaeaees sedan Aaa sees eee eee 24.5 27.1 


The percentages relate to the ash of the plant. 


For other facts of similar import, see the work cited above. These 
facts go to show that magnesia is more concerned in fruit produe- 
tion, and lime in the formation of fiber. In view of this it may be asked 
whether the well known superiority of Wisconsin wheat is not due to 
the magnesian element in her soils. 

If we compare the map of soils with the map of vegetation we 
shall find some interesting and important relations. The Prairie 
Loam is of course covered by prairie vegetation. The Lighter 
Marly Clays are chiefly occupied by the oak group, the Heavier Mar- 
ly Clays by the vegetal groups in which the maples are prominent, 
The Red Marly Clay by very much the same; the Limestone Loam 
by the maple, beach and conifers in the peninsula and chiefly by the 
oaks elsewhere, this difference being due probably to climatal influ- 
ences; the Silicious Sandy soils by the conifers chiefly; the Calcareous 
Sandy soils by the maple and oak and the maple and beech groups. 
The Humus soils are occupied by the several classes of swamp vege- 
tation. Where a patch of heavy clay occurs in an area of the lighter 
class it usually sustains heavy oak timber, especially white oak, 
rather than the “openings,” and where the reverse is true, the oak 
and maple group usually displaces the other maple groups. The 
pine is frequently found on soils that are quite decidedly clayey in 
nature, but in many of these cases a substratum of sand is to be found 
within a few feet of the surface. 

These correspondences, which are susceptible of being carried out 
to much greater detail, illustrate the mutual relations of soil and na- 
tive vegetation, and open to the agriculturist a wide field for profit- 


able study. 


QUATERNARY FORMATIONS — THE DRIFT. 199 


CHAPTER V. 
QUATERNARY FORMATIONS—THE DRIFT. 


The formations of this region consist of two great classes, the one 
made up ot indurated rock, the other of loose material in the form of 
clay, sand, gravel and bowlders. The former had their origin in de- 
posits made by the ancient ocean, which have become hardened to the 
state in which we now find them. The others had their primary ori- 
gin, as is now generally believed, in the action of ice in the form of a 
glacier. Subsequently a large portion of this material was washed 
out and redeposited or otherwise modified by the action of lakes and 
rivers. That portion which remains in the condition in which it was 
originally left by the glacier is known as unmodified drift, while that 
which has been rearranged and redeposited by the subsequent action 
of water is termed modified drift. Taken together, they constitute 
the chief Quaternary formations. Since they occur at the surface and 
are diverse from the bedded rocks below, in their nature and origin, 
it will be most convenient to consider them independently. 

The primary drift, or that portion of the material which exists in 
the condition in which it was left on the retreat of the glacier, will 
be considered under the head of (1) moraine ridges, and (2) bowlder 
clay or till. The secondary or modified drift consists of a series of 
beach deposits of sand and gravel, and of lacustrine deposits of clay. 
In addition to these there are many local deposits made by running 
streams and small lakes that will not receive special consideration. 

Glacial Movements. To clearly understand these drift formations, 
it will be desirable to first study the character of the glacial move- 
ments which gave rise to them. At the commencement of the great 
cold period which led to the vast accumulations of ice which over- 
spread this portion of: the continent, this part of Wisconsin had 
already been long elevated above the surface of the ocean, and had 
been subjected to very great erosion, by which extensive and deep val- 
leys had been formed. There can be no doubt that the Green Bay and 
Rock River valleys were already in existence, though doubtless pre- 
senting many features very different from those exhibited at the: res- 


ent time. There is abundant evidence that some of the streams had 


200 GEVLOGY OF EASTERN WISCONSIN. 


cut channels from one to three hundred feet deeper than those which 
they now occupy. These preéxisting features of the surface, exerted 
a very marked and peculiar influence upon the direction of glacial 


movement. 


A striated half-cone of rock on a glaciated surface of limestone, scen at Pelton’s quarry, Pewan- 
kee. The parallel lines represent the strie. The base of the cone is not striated and the adjacent 
surface is at first rough, but becomes gradually smoothed, and at length merges into the polished 
plane sirface, demonstrating the direction of glacial movement. 


In its progress the ice mass abraded the surface of the rock, carry- 
ing away and grinding up the material detached, and by means of it, 
embedded in its base, polishing and scoring the ledges below, there- 
by indicating the direction of its movement, and leaving us its own 
history engraven on the surface of the rock. By careful observation 
of these scratches or striae, it has been found possible in all except a 
few cases to tell the point of compass towards which the movement 
took place. Bysuch observatious it appears that the movements of the 
ice in this region were of an exceedingly interesting character. On 
the east side of the Kettle Range, with some unimportant exceptions, 
the direction of movement was in a westerly or southwesterly direc- 
tion, or towards the Idange. The exceptions are cases in which two 
sets of strive are present, the one set corresponding to the general di- 
rection just indicated, the other to the general trend of Lake Michi- 
gan. On the other side of the Kettle Range, between it and the erest 
of the ledge that borders the Green Bay valley, heretofore described, 
the direction is to the southeasterly toward the Kettle Range. With- 
in the great Green Bay valley the direction is uniformly parallel to 
its trend, and the cutting and planing indicates a long continued and 
powerful action. To the west of this valley, the strie have a west- 
ward and southwestward direction, the tendency being in general] 
more to the westward as the slope is ascended. It appears then that 
the movement on the east side of the Kettle Range was up the slope 
obliquely towards it; that on the west side of the Range, between it 
and the margin of the Green Bay valley, the movement was obliquely 
down the slope toward the Range; that within the Green Bay valley 
the ice moved up it until it reached the dividing ridge between it and 
the Rock River valley, when it descended the latter, the lines gradu- 


QUATERNARY FORMATIONS —THE DRIFT. 901 


ally diverging as it did so; and that on the west side of the valley, the 
movement was again up the slope, and gradually divergent. Over tha 
Green Bay peninsula, striations dre very rare, on account of the ab- 
sence of conditions favorable to their preservation, but there is un- 
questioned evidence that the movement was obliquely across the penin- 
sula from the Green Bay valley to the trough of Lake Michigan. In 
the following table. the striz have been alasatfied with reference to 
these general movements: ee 


I.—Brrween THE Kerrie Rana anp Lake MIcHIcan. 


Horlick’s quarry, Racine (doubtful),...... is oS RAEN el CR tn 8. 26° W. 
Schwickhart’s quarry, Sec. 26, .N. W. qr., Wauwatosa.........eceeeee eee 8. 49° W. 
Sheboygan Falls, ‘villages. «/...tawsie saves vena teacea matcanicaxhean ance’ 8. 64° W. 
Sheboygan Light-house — : 
Dies biseb ys scupion dando nec Deets onaalea tier dudedeGanea sana Suaaaes 8. 56° W. 
Second! Setiviwweniacewoe anaes eenene cuax ged vuvue ds etactue aves’ 8. £W. 
Howard’s quarry, Sec. 16, Sheboygan Falls......... 0.0.0 sees eee e creas 8. 78° W. 
Kuntz’ quarry, on Manitowoc river, Sec. 15, Manitowoc Rapids..'........- 8. 81° W. 
One half mile below the above, Sec. 15, Manitowoc Rapids..............- 8. 79° W. 
Moody’s quarry, 4th Ward, Milwaukee ........... ccc cece eee cece eee ees S. 86° W. 
Pelton’s quarry, Pewaukee ........ cece e cece cece ence ee ee tence neeees 8. 82° W. 
Delafield, ‘Sée:,20, 8. By Gta csewniaccecapewsemedetedenseeesexe tive de 8. 116° W. 
Pewaukee, Sec. 18, N. W. qr... cc. cece ence tcc e nese ener eas cerns yekedes 8. 92° W. 
Tashens SegvB)s ide. Have! canidemecdardied stew audveeade Segue coed cee Hike S. 96° W. 
Il.—Berween tHe Kerrne Rane axnp THe Green Bay anp Rock River 
VALLEY. 
Casco, Sec. 14, 8. W. qr., T. 24, R. 23, on summit of ridge... ..........6 8S. 4 E. 
“* on east. brow of the ridge, on top and edge of layer....-...-..--4-- 8. 21° W 
Marshfield, J. Steffer’s quarry, Sec. 30, 5. W.gqr...... cee ceer eee ee eneee 5. 28° E. 
Taycheedah, T. 16, R. 18, Sec, 29, 8. W. gr. of 8. HE. qr... . cee ee ee ener 8. 10° E. 
Hinpive, Sée.-6, No Widths svaise ssccxevevesasecavenerendeeuseuueaaes 8. 18° BE. 
Ashford, ‘Ra kieut, Seg 11 ce oiec seve cancannagiinsvdetaem nunc ated teas ws yen 8, 59? E, 
Elmore, Ashford, Sec. 26, N. E. qr........ se Sea eean hype nities Macca ssi saree 8. 44° E. 
Whitewater: near Kinney's: . <0. -savicetdnssune cava vgeadaeapewtinlewtna 8. 7 E. 
Whitewater, 8. Ei. of Cravath lake... ... sess ccseeeereeeese eens er eenene 8. 12° W. 
Il.—Iy tur Troven or Tne Green Bay anp Rock Riven VALuey. 
Ft. Howard, Sec. 10, Bennett’s quarry, Duck creek........2.++ esse seers Ss. 29° W. 
ft es North quarry......-...45 Payptas deeb navausgrepas aise sla ene 8, 20° W. 
Peshtigo, T. 30, R. 22, Sec. 4, near center........ 5... bso es aults Ginptiig ein lecest ys 8. 41° W. 
Peshtigo, T. 30, R. 22 E., Sec. 21, E. hf. 8. W. qr..-...---- ere ae 8, 27° W 
Oneida Reserve, mill on Duck creek «2... 00. e eee e eee e eee ect t ence eres 8. 20° W. 
Menasha, Sec. 11, E. hf. of S. W. gre. se. e eee cere eee eee tere een e eens 8. 214°W 
Neenah, Sec. 34, N. EB. qr cece eee ece cece eee cree cect eee eter cnet eeeees 8. 27° W. 
Fond du Lac, Moore’s quarry....-+.ceeee cece cece cree eens eee eneneneee §. 15° W. 
‘Taycheedah......-- e+e eereceeee ees Be eatecee ig ooh Ene SAAR sB EWS aE he se ois 8S. 15° W. 
Byron, Sec. 10.00.00. sce e cece cece cree cree eee e eet e een e anne rene ere r ess Ss. 8° W. 
Beaver Dam, Sec. 20, S. BH. qr... eee ecee cece cert eee ee eee ee teenies due south 
Koshkonong Prairie......sececeeeece esse ee eeenne seen eter en ercnre sense 8. 7 EB. 


Fuilton, Sec. 12, N. B. qt. se cscs ceeeer eens eens sees en eee r ener ene e eens : 


202 GEOLOGY OF EASTERN WISCONSIN. 


IIIl.—On tue West Store oF THE GREEN Bay AND Rock RIVER VALLEY. 


Portland; 806.35; So Eeodites cs0sc-s pose sca nties eben aesns cases wea als au 8. 30° W. 
Milford, S60: 83)Si- WiiGtcrsvesese.ataiagicsduensiwsteasrdd eset oreun 4s 8. 380° W 
Calamus, Sec. 18, near center...... 6.006 cece cece cee ene eens cece eee eees S. 36° W. 
Westford, Sec. 19, middle 8. E. gr. — 
First betiv ss ccak devs aeesacgseeeeeenseees ads seeegarseasosmagiorees 8. 24° W. 
Crossed. by SecOiid SOtiici.:ccceece di ees cher sec acess eee NE SL ORS DOae 8. 46° W. 
Trenton, McFarland’s quarry......sseccesecveenessuweseesevanaeee sacs 8. 50° W. 
Green Lake, Sec. 36...... eccalewier grater i tate Mee Macdedonaenewe es. 8. 45° W. 
Green Bake, See: iis vv skeis theese Weegecuenslcateledgs Ho Bea seeteaesas due west. 
Ripon, Sec. U9. csig. cuvas see seveycy eevee eas Sera ven ye nee ey ceayewees 8. 82° W. 
Metomien;:Sée.1; N-oB. Gri .cctadian ached hasticienicu tage, amangadenaceie anes 8. 45° W. 
Nepeuskin, Sec. 4, near middle south line...........eeeeeceaeeeeeveeens 8. 94° W. 
Nepeuskin, Séé."15, Ns. Ws iG iiss-so sana dagunddar Gra tieoeoueldnaoneke aes 8. 87° W. 
Nepeuskin, Sec. 15, near center......-- sc eccccccsecscceccenseeeceeenes 8S. 84° W 
Black Creek, watering station G. B. &M. R. Ru... eee cece eee eee 8. 72° W. 
Peshtigo, T. 33, R. 20, Sec. 21, E. hf, of S. W. qr....---.ee ee ee eee ce eee 8. 82° W 
Fie. 3. IV.—GreEeEn Bay Pentysuna, Frorp Rucron. 
Liberty Grove, T. 31, R. 28 E., Sec. 25, near North Bay. 
Wirgtisebinacenscuadeees sueonmadecccs 8. 9° E. 
Crossed by second set .......---.05 8. 4 E 


Besides the striae, there is abundance of 
evidence from other sources, testifying to 
these movements. Where Archeean mass- 
es protrude through the Paleozoic torma- 
tions, as in the towns of Berlin, Marquette, 
Green Lake, Portland and Waterloo, trains 
of bowlders stretch away from them in the 
direction of glacial motion. In the latter 
case these trains have been traced to the 
southern line of the state, 50 miles distant, 
as illustrated in the accompanying map. 

a Evidence of a similar nature, though less 
a2, BE Ea ie conspicuous, is furnished by drift from 
peculiar beds of Paleozoic formations. 

In addition to this, the contour of the rock surface furnishes cor- 
roborative testimony. Elongated domes of rock having a linear ar- 
rangement, with their longer axes parallel to each other, indicate the 
direction of the moving ice. In the same way elongated drift hills 
and ridges, often of a very great length, indicate the direction of 
movement, either because they lie in it, in which case they have a 
rounded, flowing contour, or because they lie transverse to it, in 
which case they usually have a sharp or irregular outline. On the 
east side of the Kettle Range, in the region of southwestward-point- 


7? Te rs 76 


LZ? 


QUATERNARY FORMATIONS —THE DRIFT. 203 


ing strize, the rock ridges and drift ridges of flowing outline have a 
westerly or southwesterly trend. On the west side of the Range and 
adjacent to it, they have a southerly or southeasterly inclination. In 
‘the upper portion of the Rock River valley, they are often exceedingly 
conspicuous in their southerly, southeasterly or southwesterly trend 
according to their position within, on the east, or on the west of the 
main line of glacial movement. The persistency and uniformity of 
this arrangement in Dodge and Jefferson counties is something re- 
markable. As will be observed, in all these cases, the arrangement 
of this class of drift hills corresponds to the direction of the glacial 
grooves, 

In this connection we need to consider some peculiar phenomena 
that occur at Mr. Smith’s quarry, near Burlington, and at Mr. Cas- 
tleman’s, in East Troy. The position of these quarries is such as to 
make the following facts of much interest in relation to the Kettle 
Range, aside from that 
which attaches to them in- 
dependently. The accom. 
panying sketch represents 


a vertical section along the 
east side of Smith’s quarry. «oid nee ottinestone, 2 Shaly bale Uhl ayes 
The upper four or five feet tilted blocks of limestone. : 
consist of soil and debris resting upon the regularly bedded argilla- 
ceous limestone. The upper portion of the loose material is a marly 
clay of dark reddish brown color, and partly stratified. The lower 
portion is made up of fragments of the limestone that forms the body 
of the quarry, imbedded in sand, clay, and gravel. The blocks of 
limestone are angular and unworn, and sometimes not even separated 
from the layers with which they were contiguous before disturbance. 
They are almost uniformly tilted, so as to dip at high angles toward 
the south or southwest, as represented in the figure. The number of 
the titled blocks is so great, and their position so constant, that the 
phenomena cannot be regarded as a mere chance occurrence. 

The surface of the undisturbed rock is frequently smoothed, but 
no distinct strive could be found. On the opposite side of White 
river, five or six rods distant, the surface is thoroughly smoothed, but 
presents no striz, and although planed to a general level, undulat- 
ing portions are smoothed in a way not readily attributable to ice. 
Taken altogether, the phenomena seem to point to original polishing 
by glacial agencies, and subsequent modification by water. 

In the northern part of the quarry, the strata are removed to a 
lower level. The upper layer represented in the sketch is firm and 


204 GEOLOGY OF EASTERN WISCONSIN. 


compact, but fractured, as shown. Just below this hes a softer and 
more yielding shaly layer. At the left, where unprotected by the 
layer above, it is sharply arched. Unfortunately, debris obscured the 
section beyond this point. Enough, however, was removed to show 
all the essential features. 

At Castleman’s quarry the loose pieces were tilted more irregularly, 
but the surface of the rock is smoothed, and some obscure striz are 
to be found whose direction is 8. 45° to 50° W. 

The combined import of these facts is, that the force producing the 
phenomena acted from the northeast. This demonstration is the 
more important since we have little other evidence of a decisive na- 
ture relating to the direction of glacial movement in this region. ‘But 
such evidence as can be derived from the drift and topography cor- 
roborates this conclusion. 

The combined testimony of these several witnesses establishes, be- 
yond question, the remarkable character of the glacial movements 
above indicated. The accompanying diagram (Plate VII) exhibits 
these movements to the eye. The outlines of the main rivers, and 
the principal bodies of water, are indicated by dotted lines. The rock 
ledge that forms the eastern margin of the Green Bay valley is indi- 
cated by a line of small crosses. 

fiords. In addition to what has been said, the peninsula lying 
east of Green Bay, merits special consideration, by virtue of its pe- 
culiar features. The Green Bay side of the peninsula is high, bold 
and precipitous, while the Lake Michigan shore is low and incon- 
spicuous. But while the two sides are in striking contrast in this re- 
spect, they are conspicuously similar in the deep indentations that 
characterize either side. And that which gives especial interest to 
this is the correspondence that exists between them —they are in 
paws. At the extreme north is Hedge-hog Harbor, opposite which, 
to the southeast, lies Big Sandy Bay, with a lake between them. A 
little south lies Ellison’s Bay, and over against it Rowley’s Bay. A 
few miles further south we find Sister Bay mated with North Bay. 
At an equal distance farther south Eagle Harbor stretches far in 
toward Douglas’ and Bailey’s Ilarbors. Again, Fish Creek and Kan- 
garoo Lake form a pair, and Egg Harbor is linked across to White 
Fish Bay by lakes and streams, while Sturgeon Bay well nigh severs 
the peninsula, and Little Sturgeon Bay is wedded to the estuary-like 
Ahnapee river. Nor is this a mere arbitrary or fanciful linking. By 
consulting the topographical map accompanying this report, it will be 
seen that deep valleys connect these indentations, and that a depres- 
sion of less than 100 feet would reduce the peninsula to a linear 


PLAIL, VI 


= 
a MICHIGAN 
Se 
DIAGRAM BS EEE te 
showing BSeaicem 
Glacial Movements 
in 


EASTERN WISCONSIN 
by cesen 
T. C. Chamberlin Ne 


1876 
Scale, 35 miles to the tnch 


LAKE MI CHIGAN 


QUATERNARY FORMATIONS —THE DRIFT. 905 


group of islands, whose counterpart we now have in the chain that 
stretches onward to the north. 

Near North Bay the surface of the rock is peantifally striated 
in a direction varying from 8. 1° W. to S. 13° E. These stric are 
near the summit of a slightly elevated but nearly level area, and 
present no indications of local modification. An inspection of 
the more accurate maps shows many features in the outline of 
the inlets and coast that harmonize with these south and south- 
easterly groovings. The conclusion is forced upon the mind that 
the inlets are glacial troughs, fords, perhaps, we should call them, 
though they were not formed by the descent of a glacier from 
the interior of the peninsula toward the coast on either side, but by 
the passage of the ice mass across the peninsula, forming the inden- 
tations on the Green Bay side, in its ascent of the ridge, and those 
on the Lake Michigan side in its descent. The charts of the U. 8. 
Lake Surveys show that, with this explanation, the term fiord is en- 
tirely applicable. These troughs are continued far ont under the 
surface of the water. On the Lake Michigan side they reach from 
twelve to fourteen miles at least from the heads of their respective 
bays. At from eight to ten miles out they show a tendency to curve 
to the southward, i. e., to take a direction more nearly parallel to the 
axis of the great depression in which the lake lies. Prof. N. H. 
Winchell has called attention to some of these features, and has asso- 
ciated them in a very interesting way with the general glacial phe- 
nomena of the region.’ I was not aware, however, at the time the 
fiord-like characters first forced themselves upon my attention that he 
had used the same term to characterize them. 


GLACIAL DRIFT. 


I. Morarnezs. 


1. Kettle Range. The term “Potash Kettle Range”’ has been 
popularly used to designate an extensive series of drift hills and 
ridges in eastern Wisconsin, whose full extent and relationship were 
unknown previous to the investigations of the present survey, and 
concerning the true nature and origin of which, diverse opinions 
have been held. As the term “ Potash” has no special significance 
in this connection, it will be discarded. The northern terminus of 
the range lies in the town of Casco, Kewaunee county. From this 


1The Glacial Features of Green Bay of Lake Michigan, with some observations on a 
probable former outlet of Lake Superior. Am. Jour. of Science and Arts, Vol. Il, July, 


1871, 


206 GEOLOGY OF EASTERN WISCONSIN. 


point it stretches away to the southwestward, through the counties of 
Manitowoc, Sheboygan, Fond du Lac, Washington, Waukesha, and 
into the northern portion of Walworth. At this point it divides, one 
portion extending southward, through the towns of Richmond and 
Darien, thence eastward, though not at this point conspicuous, to 
Lake Geneva, whence the main portion extends northeastward to the 
vicinity of Burlington, and then southward into Illinois. The other 
-portion, branching from the main range in the town of Whitewater, 
about twenty miles north from the state line, extends westward to 
‘Rock River, after crossing which, it curves gradually to the north- 
ward, and enters the district examined by Professor Irving, and will 
be found described and mapped in his report in this volume. A por- 
tion of this part is outlined upon the accompanying diagram for the 
convenience of the reader. 

The peculiar feature of this range that gives rise to its descriptive 
name, consists of numerous depressions in the drift variously known 
as “ Potash Kettles,” “ Kettles,’ “ Potholes,’ “ Pots and Kettles,” 
“ Sinks,” ete... Those which have most arrested popular attention 
-are circular in outline, and symmetrical in form, not unlike the 
homely utensils that have given them a name. 

Occasionally they approach the form of a funnel, or of an inverted 
bell, while the shallow ones are mere saucer-like hollows. But it is 
important to observe that large numbers of these depressions are not 
perfectly circular, but rudely oval, oblong or elliptical, or are ex- 
tended into trough-like, or even winding hollows, with irregular de- 
partures from all these forms. 

In depth, these depressions vary from the merest indentation of the 
surface, to bowls sixty feet or more deep, while in the irregular forms 
the descent is not unfrequently more than one hundred feet. In most 
of these cases, however, the rim is irregular. Symmetrical cavities 
seldom exceed sixty or sixty-five feet in depth. The slope of the sides 
varies greatly, but in the deeper ones it very often reaches an angle 
of 30° or 35° with the horizon; or in other words, is about as steep as 
the material will lie. In horizontal dimensions, those that are pop- 
ularly recognized as kettles seldom exceed 500 feet in diameter; but 
considered with reference to their origin and structural nature, they 
cannot be limited to this dimension, and it may be difficult to assign 
definite limits for them. One of the peculiarities of the range is the 
large number of small lakes without inlet or outlet that dot its course. 
So true is this, that in field work I soon learned to anticipate the 


1Compare, On the Fresh Water Glacial Drift of the Northwestern States, by Charles 
Whittlesey, Smithsonian Contributions to Knowledge. 1866. 


QUATERNARY FORMATIONS -- THE DRIFT. 207 


position of the Range from the distrfbution of these lakes on the map. 
Some of these are merely ponds of water at the bottom of typical 
kettles, and from this they graduate by imperceptible degrees into 
lakes of two or three miles in diameter. These are simply kettles on 
a large scale. 

Next to the kettles themselves, the most striking feature of this 
peculiar formation is their counterpart in the form of rounded hills 
and hillocks, which may not inaptly be called inverted kettles. These 
give to the surface an irregularity sometimes designated, not inap- 
propriately, as knobby drift. The trough-like, winding depressions 
have their counterpart in sharp, serpentine ridges. The combined 
effect of these elevations and depressions is to give to the surface an 
entirely distinctive character. 

These features, however, may be regarded as subordinate elements 
of the main range, since these hillocks and depressions are variously 
distributed over its surface. They are usually most abundant upon 
the more abrupt face of the range, but occur in greater or less degree 
on all sides of it, and in various situations. Not infrequently they 
occur extensively distributed over comparatively level areas adjacent 
to the range. Sometimes they prevail in the valleys, the adjacent hills 
being free from them; and again they are present upon the hills, 
but are wanting in the adjacent valleys. These facts have an import- 
ant bearing in considering the question of their origin, which may 
best be deferred until all the facts are presented. The range itself is 
of composite character, being made up of a series of essentially par- 
allel drift ridges that unite, interlock, separate, appear and disappear 
in an irregular and intricate manner. At least four of these subordi- 
nate ridges are often clearly discernible, and at points the number is 
considerably increased. Associated with the main range, there are 
occasionally sharp gravel ridges, known as “hog’s-backs,” rising as 
abruptly as the nature of the material will admit, to the height of 20 
or 30 feet, and occasionally to 60 feet, or even more. These usually 
lie upon the flanks of the more massive ridges, and are distinguished 
from the serpentine ridges spoken of before in no essential way except 
in their greater size, extent and distinctness. It is usually between 
the parallel ridges, and occupying depressions evidently caused by 
their divergence, that most of the larger lakes associated with the 
range are found. Ridges running across the general trend of the 
range, as well as transverse spurs extending out from it, are not un- 
common features. The component ridges are themselves exceedingly 
irreguiar in height and breath, being often much broken and inter- 
rupted. The combined effect of all the foregoing features is to give 


208 GEOLOGY OF EASTERN WISCONSIN. 


to the formation an exceedingly irregular and complicated aspect. 
It is apparently the equivalent of the Kames of Scotland, and Prof. 
Geikie’s graphic description is specifically applicable to our Kettle 
Tange: 


‘““The sands and gravels have, as I have just said, a tendency to shape themselves 
into mounds and winding ridges, which give a hummocky and rapidly undulating out- 
line to the ground. Indeed, so characteristic is this appearance, that by it alone we are 
often able to mark out the boundaries of the deposit with as much precision as we could 
were all the vegetation and soil stripped away and the various subsoils laid bare. Oc- 
casionally, ridges may be tracked continuously for several mules, running like great 
artificial ramparts across the country. These vary in breadth and height, some of the 
more conspicuous ones being upwards of four or five hundred feet broad at the base, and 
sloping upwards at an angle of 25° or even 35° to a height of 60 feet and more, above 
the general surface of the ground. It is most common, however, to find mounds and 
ridges confusedly intermingled, crossing and recrossing each other at all angles, so as 
to enclose deep hollows and pits between. Seen from some dominant point, such an 
assemblage of kames, as they are called, looks like a tumbled sea—the ground now 
swelling into long undulations, now rising suddenly into beautiful peaks and cones, and 
anon curving up in sharp ridges that often wheel suddenly round so as to enclose a lake- 
let of bright, clear water.” 


The width of the Range is from one to ten miles, and its peaks oc- 
casionally rise 300 feet above its base. 

Gravel, sand, bowlders and clay constitute the material of the Range, 
and are variously intermingled in its composition. On the whole, 
gravel is the most prominent element exposed to observation. It is 
usually coarse but very irregular, and frequently full of rounded 
bowlders. It is to be noticed that the cobble stones are spherically 
rounded and not flat, as is common in the beach gravel along Lake 
Michigan. They are chiefly composed of the magnesian limestone of 
the region. Zhe sand is usually associated with the gravel, and it is 
only occasionally that a deposit of pure sand, free from gravel or 
bowlders, is found. The clay is usually of a light color, moderately 
tough, calcareous in composition, and contains imbedded in it erratics 
of all sizes from those more than ten feet in maximum diameter down 
to pebbles. Bowlders of Archzean rock are subordinate in numbers 
to those of the Paleozoic formations, except where clustered in partic- 
ular localities, as occasionally happens. But from the fact that no 
Archean formation is known to exist near the Range, the special dis- 
tribution of this class of bowlders is of little importance. Quite the 
contrary, however, with the limestone erratics, which are especially 
demonstrative of its origin and formation. 

Near Burlington there is an exposure of a thin-bedded, rather 
argillaceous dolomite, different from any seen elsewhere, and contain- 
ing the Trilobite, Jllenus emperator, in considerable numbers, with 


QUATERNARY FORMATIONS — THE DRIFT. 909 


but few other fossils. Nothing that could be mistaken for it by a 
careful observer has yet been found elsewhere in the state. In the 
Kettle Range, southwest of Burlington, large quantities of this rock 
are found, and at heights very considerably above the present surface 
of the rock. The blocks are usually somewhat worn, but still sub- 
angular. Their identity is put beyond question by the presence of 
Lllanus imperator. 

Passing northward along the Range, in the town of Whitewater, 
there appear large masses of the subjacent Galena limestone, distrib- 
uted upon and through the drift, being found at from 150 to 175 feet 
above the bed rock in the vicinity. These erratics are frequently 
very little worn, and in one case a stratified mass that seemed to have 
been bodily transported was found at least 100 feet above the bed 
rock. Metamorphic and igneous erraties occur in great abundance 
and variety here. . 


Fig. 5. 4A59F 


Section cf the Kettle Range on the line of the C., P. & L. 8, R. R., southeast of Whitewater. The 
figures show the elevation above Lake Michigau. The north ridge is cumposed of exceedingly 
coarse, mixed material. 


In the towns of Palmyra and Eagle where the Range crosses the 
Cincinnati group, large quantities of the peculiar areno-argillaceous 
and calcareous shales, belonging to the lower portion of that forma- 
tion, and which on the east side of Lake Winnebago lie at from 175 
to 200 feet below the upper face of the group, are found in the ridges 
of the Range. It is a soft rock that could not resist much abrasive 
action, and yet it predominates in some of the ridges over all other 
forms. It contains an abundance of small linguloid fossils, rendering 
its identification beyond question. Although so abundant here, these 
bowlders are found but very rarely except for six or eight miles along 
the Range where it crosses the formation from which they were evi- 
dently derived. They are most abundant in the ridges on the west 


side of the Range. 


Fig. 6. 


Profile across the Kettle Range from Eagle westward. 


Ws Sur.—14 


210 GEOLOGY OF EASTERN WISCONSIN. 


In the same region, bowlders of clay, which probably originated’ 
in the argillaceous layers of the Cincinnati. group, occur, imbedded 
in the common drift mass. 

Immediately beyond this, in the northern part of Eagle, and on- 
ward, where the range passes over the thick, heavy heds of the Niag- 
ara Group, the drift is characterized by great blocks of that. forma- 
tion, often but little eroded. Here, as well as southward, there is 
present a very considerable portion of well-worn, white, compact, 
fine-grained, often cherty, dolomite, that probably came from the 
Waukesha beds of the Niagara Group, on the east side of the Range. 

When we reach the central and northern parts of Washington 
county, large quantities of dolomitic sand enter into the composition 
of the drift. This is especially true of the eastern flank, The sand 
arises unquestionably from the crushing of the granular dolomites of 
the Racine limestone, which is the prevailing rock. to the east and 
which underlies the Range in part in this region. The northern and 
southern limits of this sand are very nearly coincident with the 
northern and southern limits of the granular rock in the vicinity of 
the Range. 

Large bowlders of brecciated limestone, containing Pentamerus ob- 
longus, ave found in this region, and on the west side of the Range in 
the towns of Kewaskum, Ashford and Auburn, beds crowded with 
this fossil are found in situ. 

In the northern part of Sheboygan and the southern part of Mani- 
towoce counties, blocks from the Upper Coral and Racine beds, along 
which the ridge runs, form the most marked constituent of the drift, 
and similar facts are true to the extremity of the Range. 

It appears then that throughout its extent, the neighboring or un- 
derlying rock has contributed.a noticeable element to the composition 
of the Range. To this extent its local origin is clearly demonstrated. 
At the same time it is an equally conspicuous fact that there is pres- 
ent at all points a large percentage of material which had a more re- 
mote origin. It is not difficult at a single point to find specimens 
representing several of the formations of this state besides those of 
Michigan. ative Copper is found quite frequently at all points 
along the Range, and must have traveled from one to three hundred 
miles. It is evident then that the agency which produced the Range, 
gathered its material all along its course for at least three hundred 
miles to the northward, and that its largest accumulations were in 
the immediate vicinity of the deposit. 

Structure. — The formation presents both the stratified and un- 
stratified condition. If we could trust to such exposures as w: se 


QUATERNARY FORMATIONS — THE DRIFT. O11 


along highways and streams, the stratified condition would unques- 
tionably be considered the prevailing t-rm of structure, but these are 
very often deceptive. The flanks of all drift ridges become stratified 
by wash, winds and gravitation, whether originally so or not, and the 
excavation of a road or stream is much more apt to expose this por- 
tion than the real nucleus of the hill. The deeper excavations that 
have been made, however, demonstrate that to a large extent, at least, 
the core of the Range is unstratified. 

A few additional features deserve consideration, among which is 
the comparative abruptness of the opposite slopes of the Range. In 
treating of this and the following topics, reference will be had chiefly 
to the eastern and main portion of the Range, since the recurving 
western branch is not sufficiently conspicuous to render observations 
of this kind of special value. 

In the town of Randall, Kenosha county, the eastern face is quite 
abrupt. Between Burlington and Lake Geneva, the more abrupt face is 
toward the northwest. The same is true in the towns of Richmond, 
Whitewater, La Grange, Palmyra, Eagle, Ottawa, and Delafield. In 
Washington county the difference in the abruptness of the two sides 
is less marked, but the general truth is the same. Likewise in She- 
boygan county, in general. In the towns of Plymouth and Rhine, the 
eastern face is well defined, but the fine development of kettles, men- 
tioned and figured by Col. Whittlesey, occurring near Greenbush, lie 
upon the northwestern flank, and the western face in the town of 
Rhine is also sharply limited, and the peculiar features of the Range 
are more strongly marked on this than upon the opposite side. In 
Manitowoc and Kewaunee counties both flanks as well as the whole 
Range are much subdued and neither presents sharp outlines. 

It is a general and, indeed, a pretty well sustained fact that the 
westward face of the Range is the more abrupt, and that the more 
conspicuous peculiarities of the formation lie upon that side. Long, 
sharp ridges, termed hog’s backs, occur in Walworth and Waukesha 
counties, flanking the main ridge, but have no counterpart upon the 


east side of the Range. 


Fie. 7. 


Profile acrogs the west branch of the Kettle Range south of Whitewater, showing the position of 
the ‘‘kettles’’ on the northern slope. 


212 GEOLOGY OF EASTERN WISCONSIN. 


The general relationship of this Range to the rock terrane that un- 
derlies it has already been stated under the head of Topography, viz.: 
that the southern portion rests wpon its crest, and the northern upon 
its eastern slope. Instead of lying along the ridgepole of this rocky, 
one-sided roof, the northern end has slid half way down to the eaves. 
But something more of detail as to its topographical relations is 
needed. 

Beginning again in the town of Randall, its abrupt face looks out 
eastward upon a comparatively level surface with no intervening land 
of equal height between it and the lake. The opposite side in the 
town of Walworth is also higher than the surface west of it. The 
Range between Burlington and Geneva faces higher land on the oppo- 
site side of the White river. In the northwestern part of Walworth 
county there isa broad area of much lower land to the northwest, 
while on the opposite side of the Range the surface rises toward Elk- 
horn, which is the highest portion of the county. The surface in 
Mukwonago rises higher than that of the Range in Eagle, and in Wau- 
kesha county generally, the surface is higher to the east than the base 
of the Range, although its peaks are the highest points in the county. 
Throughout Washington county, except along the northern line, the 
ridge is conspicuously higher than the surface on either hand. In 
Sheboygan and Fond du Lac counties, it is much higher than the sur- 
face east, but barely equals the highlands of Taycheedah, Empire and 
Eden on the west. Beyond this it is higher than the surface east, 
but lower or barely equal to that west. 

It should be borne in mind that these comparisons have reference 
to the summit of the Range, and that the base may be reckoned 200 
feet lower on the average. This fact is the more important, since in 
considering the question of its origin, the elevation of the base and 
not of the summit is the important consideration. 

Taking this into account, it becomes a conspicuous fact that, 
setting aside the irregularities near the state line, the Kettle Ringo 
in the southern portion is flanked on the east by higher lands, that 
near the center it attains the supremacy, and that in fhe northern por- 
tion it is overtopped by highlands on the west. 

This is not to be considered as at variance with the statement 
already made in reference to the rock ridge that underlies it, for the 
highlands to the east of it in the southern portion are great drift 
hills, but of regular, rounded contour as previously described. 

And I may here again call attention to the fact that the hills and 
ridges on the east of the range have an east-west trend, and those on the 
opposite side, a north-south trend, or unessential variations from these. 


QUATERNARY FORMATIONS — THE DRIFT. 213 


All these facts, which have been matters of careful attention, are 
of supreme importance in considering the origin of this remarkable 
formation. 

The summit altitudes of a few of the more prominent points will 
be of interest in this connection. Others, if desired, may be found in 
the list of elevations previously given, or, in a general way, by refer- 
ence to the topographical map. 


Tn Sec. 36, S. hf., S. E. qr., Randall, near the state line .............. 340 feet. 
Near the state line in the towns of Linn and Walworth, above........ 400 *“ 
The observations not being sufficiently reliable to warrant a more 
exact statement. 


Tree Bluff, Sec. 24, near center, Whitewater ..........0..ce cess eeeee 457“ 
Bald Bluff, Sec. 83, S. E. qr., Palmyra... 02... .. esses eee eee eee eee 463“ 
Government Hill, town of Delafield........-... secs eeee cece eee eereee 6l1 * 
Lapham’s Peak, Sec. 14, Erin. .... 0... cece eee cece ener cece ener neces 824 “ 
Sugar Loaf in Sec. 24, near middle S. line, Hartford ................. 740“ 
Hill near iniddle §. line, Sec. 2, Mitchell.............2-..0. 02. eee eee 580‘ 
Top of Range, N. W. qr., Sec. 5, Memee..........- es ee ee eee eee eee 348“ 
Last prominent hill in the Range at the north, middle W. hf., Sec. 18, 

CSCO ia cere eaten sees uae Baie ASG Y aus dev doa eee eeu wees 235 “ 


The Range then reaches its culmination in Lapham’s Peak, 824 
feet above Lake Michigan. Several of these hills rise from 150 feet 
to 250 feet above their immediate bases. The depth of the drift can- 
not be less than 300 feet at many points along the ridge, from which 
we see that the accumulation is vast, and that the force that heaped it 
up must have been powerful. 

The foregoing facts gather themselves into a mass of evidence 
whose force is altogether irresistible. Zhe Kettle Range is evidently 
a gigantic moraine. The main Range from Kewaunee county to 
Walworth county marks the westward limit of the glacier that oc- 
cupied the basin of Lake Michigan, and the eastern limit of the one 
that plowed through the Green Bay valley. The branch that extends 
southward into Illinois, is the continuation of the terminal moraine 
of the Lake Michigan glacier. The branch that recurves through the 
northern part of Rock county and thence northward, is the terminal 
moraine of the Green Bay glacier, upon that side. 

Neither of these indicates the extreme limits of the glacial move- 
ment, for in the eastern part of Rock county, although strie are 
absent, the contour of the hills, together with the composition of the 
drift, show that the movement was from the eastward. In the vicinity 
of Beloit, fossils of the Racine limestone are common. On the other 
hand, the train of bowlders extending southwestward from the 


214 GEOLOGY OF EASTERN WISCONSIN. 


quartzite in the towns of Portland and Waterloo, stretches directly 
across the Range and onward into Illinois. It seems evident, then, 
that before the formation of the Kettle Range, the glacial movements 
were essentially the same as they were subsequent to its formation, 
and that its accumulation was due to unusual conditions affecting the 
rate of the recession of the glaciers. The structure of the Range 
seems to indicate an alternating retreat and advance of the ice-mass. 
During the former, debris was thrust out at the foot of the melting 
mass, which, when the glacier advanced, was plowed up into im- 
mense ridges. 

If this process be supposed to be repeated several times, parallel 
ranges will be accounted for, and the irregularities incident to such 
retreat and advance will explain the complexity of the Range. Where 
the later advances were equal to the earlier ones, the whole accumula- 
tion of drift material would be forced into a single massive ridge. 
Where any advance failed to equal a former one, an interval between 
the accumulations of the two would result, giving rise to a depression 
whose form would depend upon the relations of the two accumula- 
tions, but would, in general, be more or less trongh-like in character. 
Where tongues of ice were thrust into the accumulated material, a 
serrated edge or projecting spurs and corresponding indentures would 
result. If masses of the ice became incorporated within the drift, as 
has been suggested, their subsequent melting would give rise to a de- 
pression constituting one form of the kettles which characterize the 
range. The suggestion just made, with reference to the irregular ad- 
vance of the ice mass, accounts for other forms, and at the same time 
for the irregular hills, mounds and ridges that are so conspicuous a 
feature of the Range. 

Certain of the “kettles” may have an origin diverse from either of 
the causes above suggested. A portion of the material of the forma- 
tion is a loose quicksand, easily removed by the action of water. The 
irregular surface of the Range, and its porous character, facilitate the 
collection of water, which issues from its base in numerous perennial 
springs; indeed, in some cases, brooks of no inconsiderable size flow 
full-fledged from its base. These are entirely competent to carry 
away, through their underground channels, quicksand and similar 
material, thus undermining the surface and causing a depression. It 
may be prudent to remark in this connection, that depressions alto- 
gether similar to many of those under consideration occur within 
eastern Wisconsin, which are manifestly due to very different causes. 
One of these is the well known formation of sink-holes in limestone 
districts, by the dissolving out and removal of the rocks by under- 


QUATERNARY FORMATIONS — THE DRIFT. 915 


giound drainage. Of similar nature to these are those cases in which 
the drift, by its open nature, furnishes underground channels of 
drainage. A marked instance of this kind occurs in the vicinity of 
Beloit. During the spring of 1876 and 1877, a very considerable 
stream flowed for several weeks into a shallow basin, and was entirely 
lost. Another class, but of insignificant importance, is due to the ac- 
tion of lakes, in throwing up ridges across small bays or indentures 
along their shores. These, however, are rarely so symmetrical as to be 
misleading, and their situation is such as to readily indicate their origin. 

In the vicinity of the Kettle Range proper, and at several localities 
more or less distant from it, there are areas presenting a similar un- 
dulating surface, marked by the peculiar hills and basins that charac- 
terize that formation. These unquestionably owe their origin to a 
similar cause, save that it was local and circumscribed in character. 
Owing to their limited extent and general inconspicuous character, 
they do not require extended or special description in this connection. 
One of the best examples of this class is to be found in the vicinity 
of Rock Lake, in Jefferson county. 

2. Minor Moraines. It will be most convenient to consider in 
this connection certain minor morainic features of no very great ex- 
tent or importance in themselves, except from their interesting char- 
acter. The most noteworthy of these occurs in sections 4, 5 and 6 of 
the town of Herman, and in sections 33 and 34in the town of Theresa, 
Dodge county. It consists of a narrow, well defined ridge, rising not 
usually more than twenty feet in height, extending in a general east- 
erly and westerly direction for a distance of about three miles, with 
occasional interruptions where it is crossed by streams and dry runs. 
The accompanying rude map shows its topographical character and 
relations. At its western extremity it is terminated by a remarkable 
transverse ridge, oblique to the main range, as is imperfectly repre- 


sented on the map. 
Fie. 8. 


7/1 WN. BAIT E 
Map of Moraine in the towns of Herman and Theresa. 


216 GEOLOGY OF EASTERN WISCONSIN. 


Near the western extremity, there is a conspicuous north and south 
drift range, over which the minor ridge under consideration passes; 
and in doing so, ¢¢ curves to the northward in a very peculiar manner. 
Throughout sections 5 and 6, the ridge lies upon an elevated table- 
land or plateau formed of drift material. To the east of this it grad- 
ually curves to the northeastward and descends to a considerably 
lower level, the eastern extremity being very much lower than the 
western. The two peculiarities worthy of special notice are the fact 
that it is a drift ridge, superposed upon an evidently earlier drift for- 
mation, to whose surface configuration it conforms in a measure, and 
the fact that its elevation is markedly different in different portions. 
These facts are sufficient to show of themselves that it could not be 
formed by the action of water, since no supposable warping of the 
earth could bring it into such a position as to constitute the margin of 
a lake or other body of water supposed to be capable of forming such 
a ridge, and for the same reason its origin cannot be attributed to 
floating ice. In addition to these facts, its structure and the material 
of which it is composed, forbid such a supposition. It is composed 
of confusedly intermingled coarse and fine unstratified material. A 
large number of bowlders of various classes of rocks — Paleozoic and 
Archean —are imbedded in sand, gravel, and clay, in most promiscu 
ous confusion, and in some cases in such a position as would forbid 
the supposition that they were deposited upon the surface of a grad- 
ually accumulating mass. In one 
instance a mass of finely laminated 
clay, apparently a clay bowlder, 
was found surrounded by the com- 
mingled unstratified material. The 
accompanying figure illustrates the 
Section oF Moraine in Town oF HERMAN. gener al nature of the structure of 
the ridge. It is apparently due to a local advance of the thinned 
edge of the glacier upon the surface of drift already deposited, roll- 
ing up the ridge in front of it. It will be evident that such an ad- 
vance would be retarded by the north and south ridge in section 6, if 
the thickness of ice were inconsiderable, and at the same time its 
melting hastened, which accounts for the peculiar flexure of the mo- 
raine in crossing it. 

A similar chain of hills and ridges occurs in sections 16, 21 and 27 
in the townof Beloit. The base of the chain at its eastern extremity 
has an elevation of about 200 feet above Lake Michigan. As it ex- 
tends northwestward, the surface upon which it rests rises until the 
moraine rests upon the crest of a rock ridge, at least 250 feet in 


Fie. 9. 


QUATERNARY FORMATIONS — THE DRIFT, O17 


elevation, over which it passes obliquely and descends into a pre- 
glacial valley. The material of this chain is chiefly composed of 
rounded, well-worn limestone gravel, mingled with a large propor- 

Fra. 10. tion of sand, and more or less clay, 

Beloit. with occcasional small bowlders, as 
in the preceding case. No flexure 
of the crust can be supposed to 
Seelé “ SeclS have taken place, capable of bring- 
y ing the bases of these hills and 
ridges to the same level, which 
eS would be necessary in accounting 
for them by the action of water or 

floating ice. Besides, the general 
Ee seal configuration of the adjacent coun- 


Pe try and the nature of its superficial 
S4 deposits preclude the idea of sub- 
ae 


valley GOL, 


mergence of either side of the range. 
Another case occurs in the valley 
* yan See PT of Grand river, between the vil- 
: lage of Markesan and Manchester, 
in Green Lake county. The chain 
TH | RIZE. of drift hills stretches across the 
Moraine in the tuwn of Beloit. main valley, which is occupied by 
the Grand river, and was doubtless originally the cause of the detour 
which that stream makes through the site of the village of Markesan. 
In all of the three cases above mentioned, the general direction of the 
ridges is transverse to that of glacial movement, which harmonizes 
with the view here entertained, that they are terminal moraines. 


ROOF ¢. 


II. Bowtprer Cray, or TI. 


Reference has already been made to the fact, that, previous to the 
formation of the great moraine, the Kettle Range, the glacier pushed 
southward in the Rock river valley, abrading the surface, modifying 
its contour, and finally, on its retiring, left the material strewn upon 
the surface. This constitutes the earliest drift formation within the 
limits of the dis‘-"ct under consideration. It consists of a commingled 
mass of clay, sand, gravel, and bowlders variously arranged with ref- 
erence to each other, and spread out irregularly over the surface of 
the rock below. As would naturally occur under the circumstances, 
a portion of this is sorted and stratified, forming beds of brick clay 
or of sand or of gravel, and leaving in certain localities accumulations 


218 GEOLOGY OF EASTERN WISCONSIN. 


of coarser material. This action took place in part simultaneously with 
the formation of the deposit, and so these rearranged and stratified 
beds, mingle irregularly with the unsorted material. Taken as a class, 
this constitutes the original glacial deposit or ground moraine, and 
in this report it is known by its most characteristic feature, Bowlder 
Clay, or by the term Till? That portion of the bowlder clay which 
antedates the formation of the Kettle Range merges into that forma- 
tion, and on the opposite side, a precisely similar deposit of bowlder 
clay takes its origin from the great moraine and spreads over the re- 
maining area of the district, although overlaid in part by subsequent 
formations. So it appears that the Kettle moraine is simply a pecu- 
liar and irregular aggregation of this wide-spread ground moraine: 
In relative age then, a portion of the Bowlder Clay is older than the 
Kettle Range, and a portion, more recent, there being no essential dis- 
tinction in character between the two parts. 

If we descend to a more special and critical examination of the 
material of this formation, the clay, the chief element, will be found 
to be of the most heterogeneous character. The prevailing color is 
blue, but it is not unfrequently reddish, greenish, earthy brown, or 
ashy. In texture, it varies from that which is highly plastic and ad- 
hesive to varieties so arenaceous and friable as scarcely to cohere in 
lumps. In general, however, it is intermediate between these ex- 
tremes, being marly in character. The imbeded bowlders are of all 
sizes from those that weigh many tons downwards, and are as various 
in character. A large proportion of those at any given point are 
usually from the subjacent rock, or from some formation in the im- 
mediate vicinity, but there is usually present, a large proportion of 
Archeean erratics. Along the lake shore there are many bowlders that 
represent various formations newer than any known to exist in Wis- 
consin, having doubtless been derived from the basin of the lake, or 
from Michigan. 

These bowlders show every degree of erosion. Some have not only 
been thoroughly rounded but have suffered much reduction in size, 
as is shown by the projection of the harder and more unyielding por- 
tions, giving the specimen often a unique and fanciful form. Some 
specimens are polished and striated on one side, but rough and an- 
gular on the others, due doubtless to their having been firmly im- 
bedded in the under surface of the glacier, and so polished as they were 
forced along over the rocky surface below. Other fragments are al- 
most wholly unmodified, though often of soft and fragile material. 


18ee The Great Ice Age, by James Geikie, 1874. 


PLATE, VII 


2238 


= 230 feet. 


fee} 
Terraces 


ers 
+ Modified Red Clay 


—| 
{ pper Red Cay 


Lewer Red ¢lan- 


R 
= 
os 
= 
= 
5 
4 
> 
& 
= 
3 


a 
= 
al 
L 
o 
= 
A 
, 
a 
a 
po 
m 
ca 
Lae 
os 
Z a 
we 
Og 
oe ome 
BOLE 
= v4 
Wl 4 2a 2 ‘ 
gv! at iol ‘Ss 
fAes = 
aos e = ry 
i Tos ae Il 
SiS ‘i 
0: pe agra il = ; 
- : ma ( 
a le id cael 
vd é ty = 5 2 iS ny 
ot eles 5) %Q ee 
= : i 
ae : of i 
Tons & 2 a 
os q 
= 28 : 
wa g 
wet S 
Aa 2 a 
Ons Ss 
ze g 
=e § 
aa y 
5 § 
of = 
a = 
15 
s a8 
ad he 
i 
= 
= 
a 
ps 
e 
3 
2 
= 
rE 
h 
yal Ba 
3 % 
i es 
x a: 
2 
& i 
oe fa 
y i 
= KB 
= & 
x s 
aq $ 
= 
2 
ggees 2a: 
y. Miavarker hee 51S ay 


QUATERNARY FORMATIONS — THE DRIFT. 919 


Usually such specimens have been derived from the immediate vicin- 
ity, but such does not seem to be always the case. 

An interesting peculiarity, 
sometimes observed, consists of 
cavities filled with tine uniform 
gravel, which presents the appear- 
ance of having been deposited in 
the form of gravel bowlders, either 
cemented, or, as suggested by Dr. 
E. Andrews, in the frozen state. 
These have been observed of va- 
rious sizes, from six inches to two 
or three feet in diameter, and of 
irregular, though usually some- 
what rounded, forms, as shown in 
the accompanying figure. 

This figure also imperfectly il- 
lustrates the irregular stratifica- 
tion and lamination which fre- 
quently characterize portions of 

A, Bowlder Clay. B, Stratified Red Clay. this deposit. Contorted lamina- 
Wied powlder clay. “by Clayey sand. e Sand, tions, unsurpassed by anything pre- 
Sy Seals Eee aera _ sented in the metamorphic rocks, 
are sometimes to be seen, closely associated with bowlders, stratified 
clays, pockets of gravel, stratified sand deposits, gravel beds and un- 
stratified hard pan, constituting a most changeable and irregular struc- 
ture. The surface area of this formation is shown on Atlas Plate IV. 

In harmony with the irregular nature of this formation, the rock 
here and there was left uncovered by it, and at some points it was 
swept away by subsequent agencies, but with these exceptions, it is to 
be regarded as covering the immediate surface of the rock over the 
entire district. 


MODIFIED DRIFT—CHAMPLAIN, 
I. Bracu Formation A. 


During the deposit of Bowlder Clay, there is abundant reason for 
believing that the general surface was more elevated to the northward 
than at present. Subsequently, however, perhaps cotemporaneously 
with the retreat of the glacier, and possibly also the cause of its re- 
cession, there occurred a relative depression to the northward. This 
depression was accompanied by a vast accumulation of water in the 


220 GEOLOGY OF EASTERN WISCONSIN. 


form of fresh water lakes, which are to be regarded simply as the 
expanded predecessors of our present great lakes. As this water grad- 
ually accumulated and advanced upon the land, it washed out the 
finer material of the Bowlder Clay, carrying it backward into the still 
water, where it was redeposited, while it left along the beach the 
coarser sand, gravel and other material, forming a beach deposit. 
This deposit, to distinguish it from those which subsequently fol- 
lowed, is here designated Beach Formation A. It is abundantly 
exposed along the shore of Lake Michigan, above and below Milwau- 
kee, where it overlies the Bowlder Clay and underlies a subsequent 
deposit of red clay. The accompanying figure illustrates its relations 
and relative thickness. 


Fie. 12. 
WHITE 
FISH Vara 
BAY 4% 
# 
MILWAUKEE CITY. ay’ . 
“ i ‘ is G 


Sections showing the relations and magnitude of the Bowlder Clay, Beach Formation A, and 
Lower Red Clay, at and near Milwaukee. 


The deposit consists chiefly of sand, gravel and bowlders, with in- 
cluded layers of clay. The material is thoroughly stratified, and ex- 
hibits most beautiful and abundant examples of cross and oblique 
laminee, which indicate the nature of its origin. The sand is usually 
white or yellow, but sometimes ferruginous or dark colored. The 
constituent grains are of all sizes, from afineness that renders the mass 
compact and almost plastic, and quite indistinguishable at the dis- 
tance of a few feet from the clay bands, to a coarseness that is only 
arbitrarily distinguished from gravel. It is banded and laminated in 
the greatest variety of forms. Horizontal, oblique, undulating, and 
even contorted laminations, are present in variety. 

The gravel exhibits every gradation, from sand to that which is so 
coarse that it is scarcely less than a bed of bowlders. It is chiefly 


QUATERNARY FORMATIONS—THE DRIFT. 231 


composed of limestone, and is thoroughly water-worn, and frequently 
shows an oblique arrangement. 

Interstratified with these beds of sand and gravel are bands of clay, 
sometimes quite pure, but more frequently arenaceous. These are 
usually finely laminated, most frequently in a horizontal direction. 
Occasionally the clay develops to a stratum of several feet in thick- 
ness, but more often it only forms narrow bands alternating with the 
finer grades of sand, which are also more frequently laminated in a 
horizontal direction than in the coarser kinds, showing that both were 
deposited in comparatively quiet waters. 

An occasional large bowlder oceurs in the sand and clay as well as 
in the gravel. Small fragments of rock, usually subangular, are 
sometimes seen in the clay. 

The formation is subject to rapid changes as it is traced laterally. 
At one point the section may be composed almost wholly of fine sand 
and clay, and within forty rods, these may be entirely replaced by 
coarse sand and broad bands of gravel. Large lenticular masses of 
sand, gravel, or mixed material, are not unfrequent. This formation 
reaches a thickness of about sixty feet. 

From its nature this deposit has a very limited extent as a surface 
formation. In the abrupt banks of Lake Michigan, it displays itself 
abundantly, as represented in plate VIII, which likewise shows its 
relation to the overlying and inferior deposits. Where it comes to the 
surface, it displays itself very feebly, and is scarcely distinguishable, if 
at all, at many points. It forms, where present, a narrow, irregular 
belt between the surface occupied by the Bowlder Clay and that of the 


ower Red Clay. 


II. Tue Lower Rep Cray. 


Lying upon the formation just described, we find a massive clay de- 
posit. It differs most obviously from the Bowlder Clay, in possessing 
4 deep reddish or purple color, which weathers at the surface to an 
ashy drab, while the Bowlder Clay, although not infrequently reddish 
or even purple, is usually blue or drab, and differs also in the great ir- 
regularity of its coloration. Hence the formation in question is ev- 
erywhere known as the “ved clay.” It likewise differs from the Bowl- 
der Clay in respect to the rock fragments contained in it. In the 
Bowlder Clay these are extremely abundant, and of all sizes, from 
mere pebbles to those of many tons weight. In the Red Clay, where 
they are not entirely absent, they are, with rare exceptions, small, sel- 
dom exceeding six inches in diameter, and more frequently they are 
mere hand specimens. The great majority of these fragments are of 


222 GEOLOGY OF EASTERN WISCONSIN. 


magnesian limestone, and were apparently derived from the Silurian 
formations prevalent in the region. In some instances this is put be- 
yond question by the occurrence of Niagara fossils in them. The sur- 
faces and angles of these fragments are worn, but not to such an ex- 
tent, usually, as to give them a symmetrical rounded form, and it is 
especially to be noted that the surface is scratched and subtranslucent 
instead of having an opaque, somewhat granular surface, such as arises 
from the wearing and solvent action of water. Occasionally a bowl- 
der of considerable dimensions occurs within the formation, but there 
is a very marked difference between this formation and the Bowlder 
Clay in that respect. This fact becomes a very conspicuous one in 
examining adjacent areas, occupied by the two formations. The sur- 
face of the Red Clay is comparatively free from bowlders, while they 
oceur in the very greatest abundance on the surface of the Bowlder 
Clay. It may be here remarked that there is no such abundance of 
bowlders on the surface of the Red Clay district as to suggest any 
other origin than that of wash from the formation itself’. The clay 
which constitutes the chief element is highly calcareous in character. 
It contains, also, a considerable portion of finely comminuted quartz- 
ose material, in addition to true aluminous clay, so that while the 
whole is quite compact and impervious, it yet has not that extreme 
toughness and adhesiveness that is possessed by the typical aluminous 
clays. 

A considerable ingredient of magnetite, in the form of minute 
grains, is present. A magnet drawn through a handful of the pulver- 
ized clay usually brings forth more or less of this mineral, Along 
the lake shore, where the clay is washed away by wave action, the 
magnetite is left as a deposit of black sand, mingled with the quartz 
sand of the beach, whence it may be collected in large quantities. 
The lower part of the deposit is usually very highly laminate, and pas- 
ses, by alternations and gradations, into the subjacent beach deposit. 
The main mass of the formation presents little indication of the lines 
of deposit, but upon close inspection, minute lamination may be ob- 
served. The relation of this to the imbedded rock is interesting. As 
the lamins approach the fragments, the greater portion curve down- 
ward and pass beneath it, while a portion curve over it. It would 
appear from this fact that the fragments were dropped upon the sur- 
face of a yielding clay mass, and covered by subsequent deposit. Near 
the sonthern extremity of this formation, it has, along the lake shore, 
a thickness of from 15 to 20 feet. At Whitefish Bay, above Milwau- 
kee, it is from 20 to 30 feet thick, near Ulao, 40 feet, and in the vicin- 


1 Compare Geological Survey of Ohio, Vol. II, Part 1, page 4. 


PLATE, IX 


QUATERNARY FORMATIONS — THE DRIFT. 2293 


ity of Port Washington it reaches its maximum observed thickness of 
75 feet, although it doubtless somewhat exceeds this at some points. 
At many places along the lake shore, owing to slides and washing, 
it appears to have a thickness considerably exceeding this. 

It has a wide surface distribution, as will be seen by consulting the 
accompanying map. Commencing near Milwaukee, it widens to the 
north until the Kettle Range is reached, by which its western boun- 
dary is deflected to the eastward until it passes that barrier and swings 
around upon the western side, and, passing the watershed, occupies 
the Green Bay valley. It ascends this valley to a few miles south 
of Fond du Lac, and reaches up the Upper Fox river beyond Berlin, 
while in the Wolf river valley it extends beyond Shawano. West of 
the bay it appears in much less amplitude than to the southward. 

From what has already been said concerning this and the underly- 
ing formations, no doubt remains that it was a subaqueous deposit. 
Its extent should, therefore, indicate approximately the amount of the 
encroachment of the lake at the time of its formation, and the alti- 
tudes to which it rises are significant of the amount of relative de- 
pression that attended its formation, and hence, an especial interest at- 
taches to its vertical distribution. At its southern extremity, it reach- 
es an altitude of a little more than 100 feet above Lake Michigan. 
Where its western limit crosses the north line of Ozaukee county it is 
about 200 feet. A few miles east of this it rises upwards of 300 feet. 
At the northwest corner of section 36, town of Lynden, Sheboygan 
county, it is 315 feet. In the town of Rhine, of the same county, the 
limit is found at 322 feet; at the middle of the north line of section 
21, town of Memee, Manitowoc county, at 248 feet, and on the oppo- 
site side of the Kettle Range, at St. Nazian, at the same height. 
North of this its limitation is less well defined. There are some in- 
dications that it passed entirely over the Kettle Range, in the central 
portion of Manitowoc county, or at least that the waters of the period 
did. Nowhere north of this was it observed at a height exceeding 330 
feet above Lake Michigan. Near Chilton it reaches an elevation of 
372 feet; north of Stockbridge, 358 feet; south, 390; in se tion 6, 
Marshfield, 401 feet; in section 5, Taycheedah (T. 15, R. 23), 315 feet. 
These have been selected from a large number of observations, either 
because more reliable, or because more significant, on account of their 
positions. A more general and comprehensive appreciation of the 
facts may be gained by a comparison of the map of Quaternary For- 
mations with the Topographical map, both of which will be found 
upon plate IV, conveniently arranged for such comparison. It will 
be observed that the formation rises gradually from its southern ex- 


224 GEOLOGY OF EASTERN WISCONSIN. 


tremity to the region of Lake Winnebago, beyond which it declines. 
On Lake Superior an analogous clay rises at least one or two hundred 
feet higher. * 

Aside from the general northward depression indicated by these 
facts, a special flexure seems to have taken place in the region of Lake 
Winnebago, either of the nature of a greater depression during the 
time of deposit, or of a greater elevation subsequently. This fact is 
entirely in harmony with the concurrent indications of several pecu- 
liar features in the underlying formations and general structure of the 
region. It is on the basis of this general northward depression, and 
on the sequence of the formations, that this and the associated de- 
posits are referred to. the Champlain period. 


JII, Beacu Formation B. 


Reposing upon the Lower Red Clay, there lies a deposit of sand 
and gravel, with included layers of clay, reaching a thickness of 66 
feet or more, and constituting a well defined formation. It differs in 
no essential respect, so far as its character is concerned, from Beach 
Formation A, which has already been described, and hence it will not 
receive special description here. At some points however, where the 
depositing waters found a rocky shore, instead of the accumulations of 
clay, sand and gravel, large blocks of the neighboring limestone, more 
or less eaten by the waters, are strewn on the shore in a manner sim- 
jlar to that which is now being enacted on the rocky beach of the 
Green Bay peninsula further north. The formation best exhibits itself 
along the lake shore from Manitowoc northward, where fine vertical 
sections may be seen, one of which is illustrated in the accompanying 


figure. 
8 Fie. 13. 


PROFILE SECTION ON LAKE SHORE, NEAR MANITOWOC. 


1. Lower Red Clay. 2. Sand Deposit. 3. Alternating Belts of Sand and Clay. 


It becomes a surface formation between the Upper and Lower Red 
Clays. Appearing upon the lake shore in the vicinity of Manitowoc, 
its surface exposure stretches northward in the valley of the East 
Twin river into Kewaunee county, whence it curves slightly to the 
eastward into the basin of the Ahnapee river, from the valley of which 
it passes over the watershed into the Green Bay valley, which it skirts 
on the east as far south as Lake Winnebago, whence it returns on the 


” QUATERNARY FORMATIONS — THE DRIFT. 225 


westward slope of the valley, and runs north, parallel to its axis, until 
it crosses the Menomonee into Michigan. Its highest observed ele- 
vation is about 200 feet, in the vicinity of Lake Winnebago. Its sec- 
tion, as shown on Lake Michigan, may be seen on Plate VIII of this 
volume, and its surface distribution on Plate [V of the accompanying 
atlas. 


IV. Urrer Rep Cray. 


The description that has been given of the Lower Red Clay applies 
almost completely to this deposit, the only grounds for separating 
them being the intervention of the beach deposit which has just been 
described. The similar character of the clay, the angularity of the 
imbedded fragments of limestone, and their unweathered nature, the 
high color of the clay, the large content of magnetite, are likewise 
characteristic of this formation. It covers the northeastern corner of 
Manitowoc county, the eastern portion of Kewaunee county and the 
adjoining portion of Door county. It doubtless originally covered 
the entire Green Bay peninsula and was apparantly swept away by the 
action of the lake as it gradually retired. 

Its thickness is nowhere considerable. Along the lake shore where 
it is best exposed, and possibly thickest, it rarely exceeds 20 fect. 

In Racine and Kenosha counties, there is a yellowish clay deposit 
quite similar in most of its characteristics to the Red Clays, except 
in its color and the more frequent presence of bowlders. In addition to 
the evidence drawn from the nature of the deposit itself, the configur- 
ation of the country indicates the modifying action of water. It 
seems probable that this was more immediately connected with the 
melting and retreat of the glacier than the formations above con- 
sidered. 


V. Bzacu Formations C anp D, anp tae Mopiriep Rep Cray. 


Along the eastern border of Racine and Kenosha counties, extend- 
ing on the average about one mile back from the lake shore, we find 
at the surface a deposit of sand and gravel, with a varying but subor- 
dinate admixture of clayey and marly material. The gravel is usually 
fine and thoroughly waterworn, and is interstratified with the sand 
and occasionally with clay, and almost everywhere presents beautiful 
examples of oblique lamination. It rarely exceeds twenty feet in 
thickness, and on the average is about half that amount. At its base, 
along the lake shore, numerous springs issue, the water being pre- 
vented from descending farther by the impervious clay that lies below. 

‘Wis. Sur. —15 


226 GEOLOGY OF EASTERN WISCONSIN. 


These springs are frequently ferruginous, as are also certain bands of 
the deposit. 

The western limit of this formation is marked by a low flat ridge, 
usually only six or eight rods in width, and less than three feet in 
height. At most points, this is composed of fine gravel, except near 
the state line, where it becomes sandy. The surface between this 
beach ridge and the lake is level and free from bowlders, but imme- 
diately to the west of the ridge, small bowlders occur, except over 
certain areas that are covered with lacustrine and fluviatile deposits. 
Here and there a stream has cut a deep, sharply-defined gorge for it- 
self, but broad, sloping valleys are wanting. 

Immediately beneath the above beach formation lies a finely lam- 
inated compact clay. It has a prevailing reddish hue, which is at 
some points pronounced, but at others is bluish or dark grayish. It 
contains but few pebbles and very rarely anything that could be de- 
nominated a bowlder. The laminations are horizontal and often ex- 
ceedingly fine. Some arenaceous layers are usually present, especial- 
ly toward the top. 

In the vicinity of “The Point,” near Racine, this clay rests di- 
rectly upon the Bowlder Clay. The line of junction is most sharply 
and distinctly marked. The surface of the obdurate hard-pan, which 
here constitutes the lower formation is sometimes planed almost like 
a glaciated surface, and the resemblance is enhanced at some points 
by parallel lines of white material, the significance of which was not 
ascertained. .In other cases it presents an undulatory ripple-like sur- 
face, and in still others is more irregular. These observations are 
made possible by the distinctness of this hard-pan from the fine put- 
ty-like red clay that rests upon it. In digging it away, the red clay 
peels off from the surface of the lower clay, leaving it perfectly clean 
and distinct. 

But as we trace these clays northward a stratum of yellow sand 
develops between the two and rapidly increases in thickness, while 
the red clay correspondingly, but somewhat less rapidly, thins out. 
Four drift formations are well shown at this point; a beach forma- 
tion (D), at the top, being here a stratum of yellow sand only a few 
feet in thickness, the red clay (modified) next, and beneath this 
another beach formation (C), resting upon the Bowlder Clay, as shown 
in the accompanying figure. 

As we advance northward, or more strictly northwestward, the three 
upper formations rise and disappear at the surface in succession, each 
seeming to have been cut off above by erosion. This is not accom- 
plished, however, until the thinning out of the red clay, and the ap- 


QUATERNARY FORMATIONS — THE DRIFT. 927 


proach of the sand deposits above and below, toward each other, have 
forced the conviction that these latter really jom at points where the 
erosion has not taken place, and that the beach ridge that I have 
already described marks their junction, and that they enclose the red 
clay deposit as an equitant leaf does its fellow. 


Fia. 14. 


SEcTION Nortu oF “ THE Pornt,”’ NEAR Racine. 


1. Bowlder Clay. 2. Beach Formation C. 8. Modified Red Clay. 4. Beach Formation D. 5. Sup- 
posed Original Surface. 


It seems clear that these formations were produced by an advance 
and subsequent retreat of the great lake. The advance was attended 
by a deposit of sand and gravel along the beach, where the material 
was acted upon by the breakers, and by a deposit of fine, clayey ma- 
terial on the undisturbed bottom off shore. This progressive move- 
ment continued until the position of the beach ridge already men- 
tioned was reached, where a halt was made for a time, during which 
the ridge was thrown up by the waves, after which the water retired, 
but at a higher level than the line along which it advanced, as would 
be necessitated by the filling up caused by the deposits made in the 
interval. As the lake retired, the upper beach deposit (D) was formed, 
and the deposit of clay off shore continued. This explains com- 
pletely the cuneate form of the clay deposit. Taken as a whole, the 
clay was synchronous with the beach deposits, though in any given 
vertical section, it was later than that below, and older than that above. 

This will be made more clear by an examination of the following 
partially ideal figure, illustrating these formations. 


Fie. 15. 


1. Racine limestone. 2. Bowlder Clay. 3. Beach formation C. 4. Modifled Red Clay. 5. Beach 
formation D. 6. Beach formation in progress. 7%. Offshore clay deposit in progress. 


These formations are isolated from the red clays and beach deposits 
previously described, and their relations to them are not certainly 
established, and therefore the provisional names originally assigned 
them are retained; and in the absence of demonstrative evidence, and 


225 GEOLOGY OF EASTERN WISCONSIN. 


= 


of sufficient space for the wide discussion of the Champlain deposits 
of the great lake region, to which a proper treatment of the subject 
would lead, it is deemed best to leave the question for future consid- 
eration. 

The elevation of the beach ridge which marks the western limit of 
these deposits above Lake Michigan is as follows: 


Wear the Wives Tine: +s tes ceca aeearsteceie siete a stew ew Gieuiae Ghiacrn acres 55 feet. 

A Tittle facther north. .ccocxsccesery ames Ravence deeddee cameo ed sows 5B: 

In Sec. 18, S. E. qr. T. 1, BR. 23 Boece eee eee eee cece ence ene 40 ‘ 

In See. 1, middle S. line S. E. qr. T. 2, R. 22 H.... wee eee eee eee eee 44“ 

In Sec. 19, S. E. corner T. 3, R. 23 Hee. c ee eee cece ee ence cere eens 80 “ 

In Sec. 29, S. E. qr. 8. line T. 4, R. 23 H...... scavtave suarsespreanereR nae 68 “¢ 
TERRACES. 


Just north of the lighthouse north of Milwaukee, the bank facing 
the lake is low, but a few rods back there is a well defined terrace 
running nearly parallel to the lake shore, and rising from 50 to 100 
feet above it. This continues northward, with interruptions, for sev- 
eral miles. A similar terrace accompanies the greater portion of the 
shore line between Port Washington and Sheboygan, and near Cen- 
terville there is a feeble development of the same phenomenon, beyond 
which it is absent for a considerable interval. Just north of Abhna- 
pee the terrace reappears in sharp and rigid outline, and extends with- 
out essential interruption to the vicinity of Sturgeon Bay. It attains 
in this portion a height of 75 feet. Between the terrace and the lake 
a mature growth of forest vegetation, of a highly mixed character, is 
to be found. 

Beach Ridge of Sand. In the vicinity of Sturgeon Bay, the ter- 
race is replaced by a beach ridge of rather fine yellow sand. With lim- 
ited interruptions this ridge extends to Port de Morts. 

Beach Ridge of Lock-fragments. As we round the point and re- 
turn on the Green Bay side, much more frequent interruptions occur 
from the rocky promontories that characterize this shore; and instead 
of being sandy, the ridge is here chiefly formed of chip-stone with par- 
tially rounded angles, and of the flat pebbles that mark a rocky beach, 
where the fragments are worn rather by sliding than by rolling. 
These form sharp ridges, sometimes rising 20 to 30 feet above their 
bases, on either side, and become a very conspicuous feature at 
Ephraim, Fish Creek, Egg Harbor, and elsewhere. 

Terraces of Ieock. Along this shore also, notably between Egg 
Harbor and the mouth of Sturgeon Bay, terraces of rock sustain a re- 
lation to the present shore altogether similar to that held by the clay 


QUATERNARY FORMATIONS — THE DRIFT. 929 


terraces further south. ‘These rise in some cases almost vertically, to 
a height of more than 100 feet. The distance between them and the 
bay varies from a few rods to half a mile or more, and the interval is 
strewn with water-worn fragments of rock and occasional slight beach 
ridges. 

The three forms united. Near Green Bay (Sec. 24, T. 24, R. 21 E.) 
there is an.inconspicuous beach ridge, formed of worn chip-stone, 
first appearing on the bay shore and extending a few rods, when it is 
replaced by a well defined terrace of red clay, which extends south- 
ward nearly parallel to the shore for about two miles, when it is in 
turn replaced by a low, flat, sandy ridge, which may be traced around 
the extremity of the bay and northward along the western side to the 
Menomonee and beyond. 

The intimate association of the ridges and terraces here exhibited, 
and found less conspicuously elsewhere, leaves no doubt that they are 
only different phases of the same formative process. 

Between the lake shore and the terrace of red clay and of rock, the 
surface does not usually exceed fifteen feet above the lake level. The 
sandy ridge that succeeds the terraces rises to the northward, reach- 
ing 44 feet in Sec. 9, T. 33, R. 29 E., being the most northern point 
at which the elevation was taken. The rocky or gravel ridge attains 
a greater height. 


At Hedge Hog Harbor itis... 0... cece cece e cece eect eee teen eee 40 feet. 
At: Bie Sister Bayscscexcan Ge vests wea aid pea made ieee weno 65“ 
At Magle: Harbors: os 2034 oeusenayen age Sai eead ae make Pagn Hee Ge 33 
At Bee Harbors scccs cesses ccss osan es meres ter aanks caehaainr cent ene 50 
At WishOreek.sscia cece pecs eases Soe e cae Ges o48 ba need epee teed Res OS 55 


The elevation becomes less again toward the southern extremity of 
Green Bay. These elevations were all taken upon the crest of the 
ridge. 

Secondary Beach Lines. Between this ancient beach and the pres- 
ent one, there is frequently a second well defined ridge of lower ele- 
vation, and occasionally a third. These are sometimes sandy and 
sometimes composed of rock fragments, like the primary ridges. 


GENERAL MOVEMENTS. 


The movements made by the agencies which produced the foregoing 
Quaternary formations are of an exceedingly interesting character. 
There was first the advance of the great glacier through the deep 
basin now occupied by Lake Michigan, and through the Green Bay 
valley. The diagram of glacial movements, given on a previous page 


230 GEOLOGY OF EASTERN WISCONSIN. 


cannot be supposed to accurately represent the details of the original 
advance of the glacier, but rather the movements at the time of its 
retreat; but there is sufficient evidence to warrant the general state- 
ment that the original advance was along the two great valleys men- 
tioned. Then came the melting away and the consequent retreat of 
the ice mass, leaving strewn over the surface the Bowlder Clay, and 
by a great halt and advance in the midst of its retreat, forming the 
great morainic Kettle Range. Following the retreat of the ice sheet, 
there was an advance of the lake, giving rise to Beach Deposit A, and 
the off-shore lacustrine formation, the Lower Red Clay. When this 
advance had reached its maximum extent, the waters were withdrawn, 
apparently with much rapidity, since we find little or no evidence of 
beach action on the surface of the red clay. As to how far the lake 
retreated there is no evidence, but returning, it again advanced upon 
the land, but to a less extent than before, and in that advance, pro- 
duced Beach Formation B, and the Upper Red Clay, as the coérdin- 
ate off shore deposit, after which it again retired, leaving little or no 
evidence of its retreat upon the surface. A third time it advanced, 
but at a lower elevation. It cut deeply into the previous deposits, 
whether of drift or rock, forming the extensive terraces that charac- 
terize the shores of Lake Michigan and Green Bay. After this, for a 
third time the lake retired, and is now advancing at a still lower level. 
These movements will perhaps be more vividly apprehended by con- 
sulting the accompanying diagram. 


DisGRam ILLUSTRATING THE ADVANCE AND RutTREAT OF THE LAKE SHORE, AND THE OSCILLATIONS 
oF TUE LAKE LEVEL, SINCE THE GLACIAL Epocn. 


The Moraine and the Bowlder Clay were formed by the Retreating Glacier. The white bands through 
teh ie eons pass represent Beach Deposits A and 3B, and the lined bands, the Upper and 
ower Re ays. 


It has already been stated that some of these advances of the lake 
were due to relative depression of the land. It becomes evidently a 
question of the most vital importance to ascertain whether the pres- 
sent advance is due to simple erosion, or to a subsidence of the land, 
and we are thus led to the subject of Lake Encroachment. 

Encroachment of Lake Michigan. A considerable portion of the 
shore of Lake Michigan is formed by high, steep banks of clay, sand 
and gravel. These are being continually undermined, thrown down, 
and borne away by the restless activity of the waves. The rate at 


QUATERNARY FORMATIONS—THE DRIFT. 231 


which the land is thus being swept into the lake becomes a question 
of importance. 

It should be understood that the lake is not advancing at all points, 
and that the rate of its advance at different points is uot uniform. 
The encroachment seems to be most rapid in the neighborhood of Ra- 
cine. The land at this point projects into the lake, and is thus more 
exposed to the action of the waves. To Dr. P. R. Hoy, of that place, 
I am indebted for data and personal assistance in investigating this 
subject. He had previously estimated the average erosion in that 
vicinity at four feet per year. The measurements given on a subse- 
quent page show that for the entire shore line of the county the ave- 
rage advance is 3.33 feet, which shows that the estimate of Dr. Hoy 
for the more immediate vicinity of Racine, where it is greater, cannot 
be far from the truth. 

As an example of rapid erosion, careful measurements of the cem- 
etery lot at Racine were made and compared with previous surveys, 
with the following results: 


Length on the lake shore... ..... sc esseceee cree creer ee en teenies 921 feet. 
Width. at the: south Gndissaccssccce ceases sbeeasdansverstenetias 404“ 
Width. atthe north 6nd. sa cos. cas eeserv eset scsisaeees tage eras 466‘ 
Average Width. ..ccuce tense csens ees eeteseaneteeeeententeasene 435 “ 


Amount of land at present date, 9.18 acres. To this is to be added 
9 acres sold from the west side, making 18.18 acres. In 1840, there 
were 25 acres, making a loss of 6.82 acres in 24 years, or more than a 
quarter of an acre yearly, or, stated in an another form, the lake has 
been advancing at that point the last 24 years at the rate of 9.73 feet 
per year. The data for this calculation were furnished by Dr. Hoy, 
and the measurements were made with his assistance. It is not prob- 
able that the erosion at any point exceeds this, and it has recently 
been checked by break-waters. 

The following carefully prepared data were furnished me by Dr. 
Lapham, and I am glad to substitute them for the less complete meas- 
urements made by myself. 

“Mr. §. G. Knight, of Racine, has carefully measured for the Geo- 
logical Survey, from the nearest section corner or quarter post, to the 
bank of Lake Michigan, along all the section lines in Racine county, 
the results of which, compared with the government survey made in 
1836, are given in the following table. Had these measurements been 
made at right angles to the shore line, the result would have been a 
trifle Jess; but as some portions of the bank have been artificially pro- 
tected, we may assume the result as a close approximation to the 


239 GEOLOGY OF EASTERN WISCONSIN. 


actual amount of loss, during the past thirty-eight years, in Racine 
county. These measurements will have their value many years hence. 


LAKE SHORE IN RACINE COUNTY. 


Section Lines. 1836. 1874. Loss. 
North line of Sec. 6, T. 4, R. 23 ....00-+ 9090 wcuswess 30.80 ...... 2.40 
North ‘“ He T, Ded, Ri 2B soe awas « BAGS ese ease Boao wee ers 1.23 
West ‘ a 8, LD. 4y Ri 23 eee esiees SOB acacousenete BOAO eee es 0.48 
North “ “ 197,7.4, BR. 98 «0.200 162988 scceeccne 14.60 ...... 1.78 
West * © 16,94, 7B. OF vesccexs WE casos Oia cased 1.1 
North “ « 91,7. 4, B. 28 ......-- T55S aces ace 14:50) we eces 1.08 
West ‘ 90 TA, Ry 28: sacncee es 19:39 ves ccees VAR seaiacens 0.96 
North ‘ SDR Td Re OB eecetesrecy QWGIBD ces. aadirs 96.39! wie eee 0.00 
North ‘ te Ba Lod, Ry 28 aveceeen 16.04 ciececcs LBi4T vice 0.57 
West ‘¢ eC 84 AR 23) ee gains S150" 5 se seated 30.00 ...... 1.50 
South ‘ BB MB. A, RDB as sscsiicerses QBBT evscee x 27.84 ; sali 1.53 
North ‘“ Ce i es 3 D808) eves noe 26.50 
North ‘ 0.78, Ris 28 wasgwnas 1Bi82) fiesta 18.00 ...... 0.82 
North ‘“ © 916, 'T..3, Ry 23) sen aees DBO! eae vetacens 20.60 ...-.. 6.20 
North ‘ 01 EO, Re 28 adisaewe OL OD cieexeen 18.00 ...... 3.25 
North ‘“ CO 208 BIB OR Dor ieee BO08 os a iosal ays B16 exeee% 1.06 
West ‘ MS 298 TB; Ry 28 aces ees 3020: ws eons ws D3 OU: ane ete 6.33 
North ‘“ CO BO INO Ris Qo: alasenn oigpers BABS eseathnsis 82,40. aaleens 2.45 
South ‘ fF 330, EB, Ri 28? sis inlies 46.60 ......-. WANES aceite 1.87 
Mean of 18 places, chains ......... 0 esc e eee c cece cence ee eneeeeeees 1.92 
Saiie ii FES si wisiaie eo lhe vie dig Siese ie are lesecn gas a egw pease a eee cen eeeeerts 126.72 
LLoas per anion in feet) v2 sacs sd bx sovies pee as do ene naseraleecdebuces 3.33 


The following measurements were made to ascertain the amount of 
the abrasion of the west shore of Lake Michigan, in Milwaukee 
county, since the government survey made in 1835 and 1836. 


1835. 1874, Anwuat Loss. 
PLACE. Chains. Chains. Feet. 
On the South line of Sec. 1, T. 5, R. 22 ...... 45.61 ...... 44.50 ...... 1.90 
a ne 6; D6). Re 22 sss es 15.90) va. essere 14.40 ...... 2.60 
“ ee D4.-T:. 8; Ry 22: wa0es 19.29 ...... 18.70 sess 1.00 
a ae OT. 7, Rs 22 waves BD aes BAD a secers 0.50 
ss as 15 De hy Ri ODF aie sectiece BBP neeeas D382" scwetts 4.31 
se es 10; Bs Tye 22! iniccaieses 43.35 ceeees 41.64 ...... 2.90 
a fs 8. Di cRis 22 eacgee, 1934 ess TUBB sghasnce 3.33 
ee fe 84, 'T: 8; Ri 22 s-caciers 22:00 .scess 18169 wecwns 5.61 
Meaiisciicd: evleaiionspceia's pepehokrasleMmaten aricentaminn Giraewa nee ees diese 2.77 


The loss in the other counties bordering the lake is less on the aver- 
age. 
These facts are sufficient to show the importance of taking imme- 


QUATERNARY FORMATIONS —THE DRIFT. 933 


diate steps to save our territory from the voracity of Lake Michigan. 
The question naturally arises, Is this advance of the lake due toa 
subsidence of the land? This question very materially affects the value 
of all the property along the shore, for if this advance is due to a sub- 
sidence, it is largely beyond our control, and where and when it will 
end could only be conjectured, and it would be practically useless to 
attempt to permanently stay its progress. But fortunately there no- 
where appears to be any evidence of such subsidence. If any consid- 
erable movement were in progress it would doubtless have been no- 
ticed in some of the harbors, but none has been detected. 

It has been shown above that the entire Wisconsin shore of the lake 
has in recent geological times stood from 10 to 50 feet lower than at 
present, reckoning the water level as constant, or that the lake 
is now at a lower level than at that period. It is also known from 
the same facts that in a period of years that must be reckoned by 
hundreds, if not thousands, the lake has on the whole made no ad- 
vance. Along 120 out of 200 miles of lake shore the present line is 
farther east than the ancient one, and the territory of Wisconsin 
seems to be somewhat greater now than then. The encroachment. is 
hence not a cause of grave apprehension, although it demands ener- 
getic attention. 

The material washed out from the shore is borne southward and 
accumulates rapidly on the north side of all the solid piers, that ex- 
tend out from the shore, forming triangular areas of “ made land,” as 
it is termed with questionable propriety. 


DUNES. 


A few miles south of Sheboygan, and at several other points along 
the shore, the narrow area between the ancient beach line just men- 
tioned and the present one, is covered with beach sand which the 
winds are still engaged in heaping up into dunes, which are being cut 
and shifted after the manner of that formation. From their nature 
and surroundings they have not and probably never will become large 
or conspicuous, and are mentioned here rather as a matter of interest 


than of importance. 


EROSION AND DEPOSIT IN PROGRESS. 


Aside from the special case of lake encroachment already mentioned, 
there is a general work of erosion and deposit in progress, as is patent 
to the commonest observation. This work in the soft drift deposits 
progresses easily and rapidly. The hills are being swept down and 


234 GEOLOGY OF EASTERN WISCONSIN. 


the depressions filled wp or excavated deeper, according to their na- 
ture. The irregularities of the Kettle Range in particular are grad- 
ually losing their conspicuous peculiarities under the gnawings of the 
“tooth of time.’ The erosion of the later lacustrine and beach de- 
posits under favorable circumstances is very rapid. We were fortun- 
ate enough to secure reliable data in a striking instance of this kind 
near Racine. The eroding agency is a small rivulet that is usually 
dry a portion of the year. Twenty-eight years ago, according to Dr. 
Hoy and others, it was the merest ditch across which two logs and a 
few puncheons formeda rude bridge. A resident informed me that 
two years earlier he was accustomed to drive across it without diffi- 
culty, no bridge having been constructed at that time. At the point 
where the bridge is now located, farther up the stream, the lake hav- 
ing cut away the lower portion, the ditch which has been excavated is 
120 feet across the top, 40 feet deep, and 23 feet across the bottom. 

Farther up the stream, a distance of 1,350 feet, the channel is 40 
feet across the top, 16 feet deep and 15 feet across the bottom. It 
is still a considerable trench at 2,750 feet from its mouth. Through- 
out it is remarkably uniform in character and direct in course. A 
very cautious and safe calculation shows the material removed to have 
exceeded 2,600,000 cubic feet, or more than 3,400 cubic yards per 
year. It is situated in a level country and does not seem to have 
been much assisted by freshets. 

The upper portion of the material excavated is sand and gravel, an 
ancient beach deposit, the lower portion chiefly clay. From the sur- 
face of this clay numerous little springs seep forth and moisten the 
sides which slide down to the bottom as soon as they are in the least 
undermined, and the stream is thus constantly fed with silt. These 
peculiar conditions might seem to be exceptional, but they are really 
quite cormmon in the lake border region. The loss from lake erosion 
is vastly increased by the action of springs similarly situated in the 
banks facing it. In general it may be said that the erosion of these 
later deposits, especially of the red clays and the beach deposits, is 
unusually rapid. 


INDUSTRIAL VALUE OF THE DRIFT FORMATIONS. 


By far the most important resource springing from the drift of 
this region has already received consideration. I refer to our fertile 
and enduring sozls. The powdering and commingling of such a vast 
variety of minerals by the glacial forces was a process than which 
none could be better suited to produce a secure and permanent foun- 


QUATERNARY FORMATIONS — THE DRIFT. 935 


dation for agricultural industries; a resource for the many, not the 
few —a wealth for the people. 

Brick. Second only to this in importance are the building mate- 
rials furnished by this formation, prominent among which are the de- 
posits of brick clay. These belong to two classes, the light colored and 
red clays. The former are lacustrine, or fluviatile deposits, derived from 
the wash and redeposit of the bowlder clay, and occur within the area 
covered by that formation. They are local accumulations, and are of 
various bluish drab and yellowish hues. A portion of these clays 
burn to a beautiful cream color, while other portions become red. 
The superiority of the former in texture as well as color has almost 
entirely excluded the products of the latter from the market. The 
second class, the red clays, are simply those portions-of the red clay 
deposits already described as are sufficiently free from pebbles for the 
purpose. Such portions are almost invariably found at the junction 
of the beach formations with the main clay deposit. At that horizon 
are beds of clay and sand, and of the two variously mingled, thus fur- 
nishing the two essential ingredients of brick manufacture in the 
most convenient proximity and association. Very frequently a stra- 
tum mingled in the proper proportion by nature may be found. This 
is a definite and wide spread formation, and affords the most unlim- 
ited quantities of excellent material. 

Notwithstanding its native red color, it burns to a very desirable 
white or cream hue. This fact has very justly excited not a little 
surprise, none the less so because a portion of our light colored clays 
burn red. 

That the light color of the brick is not due to the absence of iron 
is evident from the manifest presence of that substance as the color- 
ing matter of the clay, and this has been confirmed by analysis. It 
has been observed that the brick frequently contain small black, 
glassy points, and it has been thought that, in the progress of burning 
a process of segregation took place, whereby the iron was concentrated 
in these concretions, and this view was apparently confirmed by the 
fact that the brick are red up to a certain stage in the burning. The 
recent investigations’ of Mr. E. T. Sweet upon the Milwaukee brick 
have thrown much additional light upon the subject, though not 
specifically applicable to the red clays, since the brick of the “ Cream 
City” are made from a light colored clay. For the purpose of com- 
parison, Mr. Sweet analyzed a specimen of the Madison clay, which 


1 Paper read before the Wisconsin Academy of Sciences, Arts and Letters, February 
15, 1877. 


236 GEOLOGY OF EASTERN WISCONSIN. 


burns red, and a specimen of clay and of pressed brick from Milwan- 
kee, with the following result: 
Milwaukee Madison Milwaukee 


Clay. Clay. Brick, 
DiiGAcareO rman vane Agee nwes sees Deewana 88.22 75.80 53.78 
AMUN A iets Seaie eae ieee ieee adeked ee 9.75 11.07 13.21 
Peroxide: Of 1WOnesos aiaz saree vines capes owe 2.84 3.53 4.92 
Protoxide Of i0nis ccnesececs  dataasere sda 1.16 381 -26 
Carbonate of lime... 1.6... sce eee e eee eeeee 28.20 DAG og baat 
Carbonate of magnesia........e.es seer cerns 15.83 17 7.41} 
Time (CaO): ssadesccdte wesne nein aveinns eigen acocnanays 8.24 39 17.71 
Potushicsiedssesidadcoug thie nncargees wages 2.16 1.74 1.54 
Soda. gavewaror nae saie0uldaues au werent 65 1.40 92 
Water in composition...........ceeee scenes 1.85 BelG eee 
Moisture accaaasncs sedi sGaclgnoinsa nium 95 1.54 19? 


1 Magnesia. * Loss on ignition. 


From these analyses it appears that there is even a larger quantity 
of iron oxides in the Milwaukee clay, that burns white, than in the 
Madison clay, that burns red. and that in the white brick there are 
over five per cent. of iron oxides. It is also to be observed that the 
Milwaukee clay contains a very large ingredient of lime and magne- 
sia, of which the Madison clay contains but little. In view of these 
facts Mr. Sweet suggests that the ingredients of the clay enter into a 
combination somewhat analogous to some members of the amphibole 
group in which the iron does not manifest itself as a coloring material. 

This view is confirmed by the hard and often semi-vitreous charac- 
ter of the brick, and by the fact that the light color is developed at 
the point of incipient vitrification. It is at least certain that the 
light color is not due to the absence of iron, but to the manner of its 
combination. 

The red clays, as has been already repeatedly remarked, are highly 
calcareous, and from the close similarity of the brick formed from 
them to the Milwaukee product it is evident that both undergo essen- 
tially the same reactions. 

It is thought to be entirely safe to say that in quantity, quality, 
convenience of situation and facilities for shipment, these clays are 
unsurpassed on this continent. The superiority of the brick is uni- 
versally acknowledged, and their beauty is a matter of general com- 
mendation. The entire number annually manufactured is estimated 
at 50,000,000, and the value of the product approaches half a million 
dollars. The test and verdict of the recent great fires has been highly 
favorable to brick as a building material, and there can be no doubt 


QUATERNARY FORMATIONS — THE DRIFT. 937 


that in the near future their use, already large, will be vastly in- 
‘creased. 

The following statistics, though incomplete, will indicate the meth- 
ods, extent and local details of the industry (1873 and 1874): 

At Milwaukee there are six yards, at which about 24,000,000 brick 
are made annually, which are nearly all needed for the local demand. 
The common brick are sold at $12 per thousand, and the pressed. at 
$25, the value of the entire annual product being about $300,000. A 
large proportion of the brick are made by machine, steam power be- 
ing used. The capacity of each machine is about 30,000 brick per 
day. The kilns consist of from ten to twenty or more arches, each 
arch numbering 20,000 brick. The product has the light cream 
color, so well known in the market as the characteristic of “ Milwau- 
kee brick.” They are made from a light colored clay, a modified 
form of the glacial deposit. 

At “The Point,’ near Racine, two firms— Messrs. Erskine & 
Morris, and the Burdick Bros. — mannfacture about 3,500,000 cream 
colored brick per year from red clay and a layer of sand from the 
overlying beach deposit. Their kilns usually number from 250,000 
to 500,000, which require from five to seven days in burning. One 
cord of mixed wood, at a cost of about $5, burns about 5,000 brick. 
The molding is done by hand, with water instead of molding sand. 
About forty hands are employed. 

At Ozaukee there are two yards where fine cream colored brick 
are manufactured from red clay derived from the transition beds be- 
tween Beach Formation A and the Lower Red Clay. The brick are 
sold at $8 per thousand. 

At-Sheboygan Falls 300,000 excellent cream colored brick are 
burned annually. The kilns contain about 150,000 and require from 
seven to nine days in burning, consuming one-half a cord of beech 
and maple wood per thousand brick, the cost of the wood being $3 
per cord. Red clay, to which twenty to thirty per cent. of sand is 
added, is used. The brick are molded by hand, and sell at from $7 
to $10 per thousand. 

At Manitowoc large quantities of cream colored brick of good 
quality are made from sandy red clay associated with Beach Forma- 
tion B. No additional sand is required. The brick are molded dry 
and by hand. Full statisties were not obtainable. 

At Kewaunee from 75,000 to 100,000 brick are annually made 
from clay, of essentially the same geological horizon as the above. 
The product is light colored, and is sold at from $8 to $10 per thou- 


sand. 


‘288 GEOLOGY OF EASTERN WISCONSIN. 


Near Appleton Mr. J. H. Carver burns about 1,800,000 excellent 
cream colored brick per year. A variegated red clay furnishes 
the crude material which is wrought by horse power. About three. 
tenths of a cord of soft wood, worth $2 per cord, burns 1,000 brick, 
which sell at $8. 

At Neenah two parties —J. Bailey and E. M. Hulse — manufac 
ture about 1,600,000 per year from red clay, using horse and hand 
power. The former gentleman makes about 25,000 pressed brick. 
He uses six grinders and employs from nine to twenty men. Mr. 
Hulse has three grinders and employs eleven men. About two-fifths 
of acord of soft wood, or one-half a cord of mixed wood, is con- 
sumed per thousand brick, at a cost of from $2 to $2.50 per cord. 
The brick are cream colored, and sell at $8 per thousand. 

At Menasha there are two firms, Messrs. Holke & Schelke, and P. 
McFadden. Both parties use steam power, and Guard’s mixing and 
molding machine, and make 1,800,000 per year. The clay is red, but 
burns in six days to a light cream color, consuming one-half cord of 
mixed wood, which costs $2.50 per cord. About thirty hands are 
employed. 

At Clifton a yard producing 1,000,000 per year is owned by B. F. 
Carter, and one making 700,000, by H. Day & Co., of Oshkosh, the 
latter under the superintendence of H. W. Carter. Mr. B. F. Carter 
employs sixteen hands and uses steam power, with a Burnham ma- 
chine. Nine men are employed at the yard of Day & Co. The crude 
material is in the form of beautiful laminated red clay andsand. The 
brick are light colored, and are sold at $7 per M. 

At Watertown, from 3,500,000 to 4,000,000 excellent cream colored 
brick are burned yearly by D. 8. Chadwick, and about 1,000,000 by 
F. Black. The crude material is a light colored, sandy, fluviatile clay, 
about 16 feet in depth. Williams’ tempering machine is used, and 
the molding is done by hand in water. Three tenths of a cord of 
wood, with one and a half bushels of coal dust ground into the clay, 
is sufficient to burn 1,000 brick. The coal dust effects a large reduc- 
tion in expense, and is also used in some of the above mentioned 
kilns. Mr. Chadwick has ten pits for tempering, and employs forty- 
five men. Mr. Black has six pits and employs eighteen hands. The 
brick bring from $7 to $10 per M. 

At Waterloo, M. J. Rood burns about 600,000, and John Helms 
from 800,000 to 1,000,000 per year, which are sold at from $7 to $10 
per M. A light colored, fluviatile clay is used. 

Large quantities are also manufactured at J eferson, It. Atkinson, 
Edgerton, Whitewater, and greater or less quantities at Johnson's 


QUATERNARY FORMATIONS —THE DRIFT. 939 


Creck, Geneva, Kewaskum, Mutheim, Two Rivers, Northeim, Center- 
ville, and doubtless at other points that escaped our notice. 

Teles, for draining, are manufactured at Whitewater, from a light 
grayish blue clay, by Mr. A. Y. Chamberlin. Pottery is also made 
at the same place from a clay obtained in the vicinity. 

The drift formations likewise furnish abundant beds of sand of ex- 
cellent quality for building purposes, and of gravel suitable for roads 
and other purposes. 

Magnetic Iron Sands. It has already been stated that the red 
clay contains a notable amount of magnetite. As itis eaten away. by 
the lake, the grains of magnetite accumulate on the shore, and form 
what is popularly known as “Black Sand.”? Occasionally a layer of 
three or four inches of this may be found almost free from silicious 
sand, but usually it is in thinner lamin, or mixed in varying pro-. 
portions with common sand. It exists in greater or less abundance 
along the whole shore line, and the aggregate amount of it is large. 
It has never been used for economic purposes, so far as I can learn, 
except as “drying sand,” before the era of blotting paper. Similar 
accumulations are successfully utilized in the manufacture of steel in 
other regions, and the value of this deposit may be worthy of consid- 


eration. 
SHELL MARI. 


It will be most convenient to consider in this connection a fine de- 
posit of shell marl that occurs in sections 17, 18, 19 and 20, town of 
Pierce, T. 24, R. 25, Kewaunee county, around the margin of a small 
lake, and upon a shoal within it, which, by recent drainage has become 
an island. At some points it -is mixed with peat and at others 
with alluvium, but on this island it is almost perfectly pure shell 
debris. It is soft, light, porous and pulverulent on the surface. 
When brought up from beneath the water level, it is a soft, somewhat 
granular and clay-like mass. A pole was thrust down nine feet with- 
out giving any evidence of change in material. A specimen of this 
narl gave on analysis by Mr. Bode, 


Carbonate of lime......-- cece cece cert e eect ere e ere t eee enneeaesane 86.09 
Carbonate of MAQnesia....eececcereece rer eceeree ene eaeeeenereeets 7.18 
Silica co.cc ce cee ee eee r eee cee r cece tenes ee en en nese tana eree areas 1.48 
Oxide of iron and alumina....-..- see ee secre eee n ere e eee eeneeerene 0.19 
Sulphuric acid... . secs ese e cece erect e eee e eee eene nese tetee recente 0.44 
W atei sc vii nceosing eee PP SE ERE ehoee eee ee AEE eee Re Run 1.67 
Organic matter .....seeeee oe cere eee eee enter nese nen ter ene es 2.95 

100.00 


For lands deficient in lime this will furnish the needed fertilizer. 


240 GEOLOGY OF EASTERN WISCONSIN. 


In the valley of the Mink river in Door county, at White Clay lake 
in Shawano county, and, in lesser quantities, at other points, similar 
accumulations occur, usually associated with peat. . 


PEAT. 


When the glacier retired from our state, it left its debris in the 
form of drift heaped up in an irregular way over the surface, giving 
rise to numerous depressions which soon filled with water, resulting 
in lakes of various forms and sizes. It is perhaps not too much to 
say that within our district, these numbered thousands. In most cases 
they soon filled to the brim and then began to overflow their margin 
at some point, thus forming a channel, which was rapidly cut deeper 
and deeper, at the same time draining the lake. As the water became 
shallower, vegetation sprang up in the form of reeds, flags, rushes and 
the so-called water mosses, which, on dying, fell to the bottom of the 
lake, and being prevented by the water from complete decomposition, 
accumulated as a peat deposit. As the draining continued ,these lakes 
became marshes, and a new class of vegetation sprang up, varying ac- 
cording to the character of the marsh formed. 

In the region now occupied by prairies and by oak openings, the 
marshes were occupied generally by members of the grass or sedge 
group, accompanied with those mosses that are usually found associ- 
ated in this group. As the vegetation thus produced died with the 
succession of seasons, it was added to the accumulating peat deposit. 
In the more heavily timbered regions of the state, the marshes usually 
came to be occupied by the swamp-frequenting conifers, the most 
abundant of which is the tamarac. In association with these there 
is everywhere to be observed a luxuriant growth of minor vegetation, 
among which the Sphagnum mosses are most efficient in peat produc- 
tion. These have the property of dying below while growing densely 
above, and thus they contribute to the rapid accumulation of vegeta- 
ble debris, and for this reason they take foremost rank as agents of 
peat formation. They are not confined in their association to the ar- 
boreus vegetation named, but in the region under description are most 
abundant in that connection. 

In regard to the amount of peat formed in these several ways, the 
order will be the reverse of that in which they are named. The ac- 
cumulation appears to have been much more rapid in the tamarac and 
similar swamps, than in the open marshes, and as a result the deposits 
of these marshes are almost universally found to be deeper than those 
of the other class. The amount of accumulation that took place in 
the open marshes, after they became such, was undoubtedly much 


QUATERNARY FORMATIONS — THE DRIFT. 941 


greater than the accumulation during the period that they existed as 
lakes. 

Aside from the accumulation of peat in these extinct lakes, deposits, 
oe in similar ways, took place in wet localities in connection with 
running streams, or in wet valleys, that bear no evidence of having 
once been lakes. 

Bearing in mind the method of formation, it will readily be antici- 
pated that great variety in the character of the peat will be the result. 
Its degree of decomposition ranges from merely dead vegetation to 
that which has become thoroughly disintegrated, and the value of any 
given deposit will depend in part upon its character in this respect, 
since the fibrous condition of peat is one of the serious obstacles to its 
profitable utilization. It will also be readily understood from its 
mode of origin, how impurities may become incorporated with it. On 
the margin of the marsh, the wash from the adjacent uplands will nat- 
urally introduce more or less of earth or sand. Near the bottom of 
the bog, earth will naturally become incorporated with the peat, and 
in those cases where the surrounding regions have in recent times 
been cultivated, the unusual amount of earth carried down by tho 
waters will render the entire surface of the peat more or less impure. 
That portion of the peat which accumulated while the lake was grad- 
ually becoming drained to a marsh is more or less tilled with the 
shells of snails, and the remains of other animals that inhabited the 
lake. In many cases the amount of accumulation of this kind is very 
considerable, sometimes equaling and occasionally surpassing the ac- 
cumulation of the peat itself, forming a mixture of marl and peat 
that will prove very serviceable as a fertilizer. Where the peat accu- 
mulated in the vicinity of running streams, their periodical overflow 
has contaminated the deposit in a greater or less degree. A fourth 
source of impurity arises from travertine, or calcareous tuta, deposited 
from springs. This, while it is detrimental to peat as fuel, enhances 
its value as a fertilizer. Hence, in the selection of peat marshes, 
those which have been, from their situation and nature, sheltered from 
these sources of impurity, will, to that extent, be favorable to a pure 
deposit. The situation and the nature of the marsh will also furnish 
some indication as to the abundant presence or comparative absence , 
of the acids which interfere with the direct use of peat as a fertilizer. 
The character of the vegetation growing upon the bog will, however, 
be a more reliable indication of this. The presence of shells or marl 
may be taken as satisfactory evidence of the absence of any harmful 
quantity of these acids. The number of deposits of peat within this 
portion of the state is very great, and their purity ranges through all 

Wis. Sur. — 16 


242 GEOLOGY OF EASTERN WISCONSIN. 


degrees, from a very slight impurity, to that which is more properly 
denominated muck. The depth of these deposits is also exceedingly 
varying. In the investigations of the survey, an auger capable of 
penetrating 12} feet was used. In most of the peat deposits oceupy- 
ing open marshes, this was found sufficient to penetrate to the bottom. 
In most of those arising from the sphagnum mosses in the forest 
region, the depth was found to exceed that amount. In some cases 
marshes were said to have a depth of two or even three times that 
amount. The quantity of peat in eastern Wisconsin is to be reckoned 


by millions of tons. 


Details of Borings. The first marsh tested occupies portions of sections 28, 29, 30 
and 32, town of Whitewater (T. 4, R. 15 E). Ten bormgs were made along two lines, 
one across the marsh and one longitudinally. 

1. The first boring was on a springy elevation, near the center of section 32, from 
which the line stretched northward across the marsh. The peat at this point was very 
much mixed with shells, travertine, and apparently some argillaceous material. Sandy 
clay way reached at a depth of 11 feet 4 inches. A ditch near by exposed a washed sur- 
face of the upper portion from which were taken fresh water shells of the genera Spher- 
ium Planorbis, Limnea, and Pupa, the smaller species of these genera being very 
abundant, the larger, rare. This shows that the peat is of lacustrine origin, and that at 
no distant day this has been a lake. 

2. At 50 rods from the first boring, we find about equal proportions of shell-marl and 
peat. The following is the section: 


Soft, watery, dark reddish, marly peat............. ce sees eee ee 4 ft. 6 in. 
Thin layer of whitish Wat «+. a cceiece. cists nsaveisiereiai ape nareaie sailed epee 2 in. 
Gab aa AD OV Orcs cs.: tetewss-tngic otnavlasc andi iene aecags aeigias dae Sa mediate 1 ft. 
Hard, well decomposed peat.....-...-cesce cece eee ce cece eet one 4 ft. 
Bluish clay, fillud with pebbles at....... cc cece eee e eee eee eee 9 ft. 8 in. 
3. The third boring gave the following section: 
Marly peatie cnx ccsnc er stan seen renee wee reese eeee anes ee 4 ft. 
Hard, Compact Peat «c<sewssasvorssenetae sian S4aeewed Hanne noe } ft. 6 in 
CBRE scons arte ese eR tos ie seus iets O14 aLeladgenadh meee Guna acaaanlele 9 tt. 4 in 


The bottom of a ditch near by contains calcareous sand, evidently washed from the peat. 

4, The fourth boring gave 8 ft. 8 in. of reddish, partially decomposed marly peat, con- 
taining shells. Bottom blue clay as before. 

A section exposed by a ditch between borings 4 and 5 gave 2 ft. of peat, succeeded 
by 4 in. of shell-marl mingled with peat. 

5. The fifth boring showed 2 ft. of moderately decomposed marly peat as before, 3 ft. 
somewhat more compact, with hard blue clay at 5 ft. 

The remaining borings were on a line trom the S. E. qr. of the 8. W. qr. of sec. 29, to 
the N. W. corner of the 8. W. qr. of sec. 29. 

6. The first two borings were male to ascertain the structure of a mound 6 feet high 
and about 50 feet in diameter. The boring at the base gave 3 feet of muck-like peat, 
with clay below; that in the top of the mound gave 7 feet 8 inches of peat, mingled with 
much travertine, with clay and sand mingled at the bottom, which is about 11 feet 
above the bottom of the boring at the base, showing an accumulation of sand and clay 
beneath the mound, which undoubtedly owes its origin to a spring. 


QUATERNARY FORMATIONS —THE DRIFT. 243 


7. Thirty rods farther west, the chief boring showed 8 feet 4 inches of watery, partially 
decomposed peat, free from noticeable travertine or marl. Bottom, blue clay. 

8. The fourth boring, 60 rods from the last, showed 5 feet 6 inches of watery, partially 
decomposed peat, 3 feet 6 inches of a compact, close textured, reddish, well decomposed 
peat, with blue clay at 9 feet. ; 

9. The fifth boring showed a similar section, blue clay with shells being reached at 
8 feet 4 inches. 

The lower compact peat of the last two sections presented all the physical appearances 
of superior quality, being apparently free from the calcareous material found so abun- 
dant in the first series. The marly peat will undoubtedly prove a good fertilizer, and 
is well adapted to the sandy soil of the neighboring farms. 

At the head of Lake Geneva there is a small area of similar marly peat, 8 feet deep. 
__ In section 20, town of Sugar Creek (T. 3, R. 16 E.), there is a peat marsh about one- 
fourth of a mile wide, which extends eastward for several miles, but is narrow. To the 
westward it widens and connects with an extensive mazsh in the town of Richmond. 
The following is a typical section from the center of section 20: 


1. Surface black and somewhat earthy. 


2. Well decomposed, dark peat of moderate compactness...........- 5 ft. 
3. Firm, well-decomposed peat... . 1-2 :ee cece cece cece eee eee e es 4 ft. 
4. Drab clay, mingled with peat, ab.........0. ce ees eee ee ee eee eee 9 ft. 


The narrowness of the marsh at this point, and its evident exposure to wash from the 
neighboring land, render it probable that a portion of the firmness of this peat is due to 
very fine silt, that could not be detected by sight or touch. At other points the surround- 
ings were more favorable. 

Horicon marsh was tested near its south end, with the following meager results: 


First Boring — 

1. Surface, loamy peat. 

2. Coarse undecomposed peat ...... 0. cece cece eee cere ene 2 ft. 6 in. 

8. Black peaty clay......... ee eeee eens ius acute lanepiana tro 1 ft. 6 in. 

4s BUG Cla ysne: ss ociesen teas ae tee aedoamnoannssinas wee ens 1 ft. 

Fv CERAVEL Abi ene coxa ve cw wh 4 ange mene enrgnedten and nate steer ate Ss 5 ft. 
Second Boring — 

T, Peaty soil. cisci ced Gsenckades vere ated eee er Vex sees 1 ft. 

2. Yellow Clay... ..cscc cere cece ere teen eee ence een ee ees 3 ft. 

3. Blue clay, lower part sandy...-...-.-+ceee cece eee eeeee eee 2 ft. 6 in. 

AL. Chraveliabijien cect o08 } ae aee SAGES Rea) etlomneeeude alos sews s +e 6 ft. 6 in. 
Third boring essentially the same. Probably other portions of the marsh would show 

more peat. 


A marsh near Berlin, the peat of which, I was informed, had received a favorable opin- 
ion from judges at the east, was tested. It lies along the Fox river, whose inundation 
must be supposed to affect its quality. Three out of several borings will represent its 


nature : 


First Boring — 
1. At 1ft. 6 in., fibrous, not well decomposed. 
9. At 3 ft. 6. in., fibrous, not well decomposed, yellowish brown. 
3. At 5 ft. 6 in., better decomposed, reddish. 
4, At 6 ft., dark greenish blue clay. 
5, At 6 ft. 6 in., clayey sand. 


244 GEOLOGY OF EASTERN WISCONSIN. 


Second Boring — near river — 
1. At 1 ft., fibrous, loose, dark. 
2. At 3 ft., layer of decomposed wood. 
3. At 3 ft. 6 in., clay as above. 


Third Boring — near center of marsh — 
1. At 1 ft., dark, fine fibrous, soft, not well decomposed. 
2. At 3 ft. 6 in., less fibrous, reddish. 
3. At 5 ft. 9 in., clay as above. 


One of the more interesting of the smaller marshes is found in the W. hf. of sec. 30. 
Beaver Dam (JT. 11 N., R. 14 E.). There are perhaps 80 acres of available peat. It is 
surrounded by timber and has no stream flowing through it, and was formerly a lake, a3 
shown by the shells of Spherium, Paludina, and Helix, found in the underlying clay. At 
8 rods frora the edge, there were 4 feet of firm, dry, reddish, well decomposed peat, un- 
derlaid by clay. Thirty rods from the edge, the following section was obtained: 


1. At 3 feet, firm peat struck; that above, soft. 

2. At 5 feet 6 inches, reddish, well decomposed peat. 
3. At 7 feet, firm, color of brown paper. 

4, At 12 feet, clay and peat mixed. 


At the centre of marsh: 
1. Upper portion as above. 
2. At 6 feet, firm, red, fairly decomposed, apparently derived from wood. 
3. At 12 feet (length of auger), bottom not reached; material much resembling 
brown paper pulp; contained the shells mentioned above. 


In the town of Calamus (T. 11, R. 13 E.), N. W. qr. of sec. 25, and 8. W. qr. of sec. 
24, es a marsh of 200 acres. A small stream flows through it. The following may 
represent five borings of similar import: 

1. At 2 feet, well decomposed, firm, black. 

2. At 3 feet, well decomposed, firm, black. 

3. At 5 feet, well decomposed, firm, yellow. 

4, At 5 feet 9 inches, well decomposed, firm, color brown paper. 
5. At 7 feet, well decomposed, firm, color brown paper. 

6. Blue marly clay, containing shells, 


The peculiar brown material was found to be sandy in two of the borings. 
In the town of Lake Mills, secs. 1 and 2, a large marsh, partially covered with tama- 
rac, gave the following sections: 


First. — Nine rods from the edge: 
1. At 4 feet, dark, well decomposed. 
2. At 7 feet 6 inches, dark, well decomposed. 
3. At 10 feet, reddish, woody, sandy. 
4. At 11 feet, sandy, blue clay. 


Second. — Forty rods from the edge: 
12 feet of soft, wet, not well decomposed, dark, reddish, woody peat. 
No evidence of sand; bottom not reached. 


Third. — Nearer the edge: 
1. At 6 feet, firm, half decomposed, dark reddish, woody fiber. 
2. At 10 feet, dark, well decomposed, firm, apparently excellent. 
3. At 12 feet, sandy; bottom not reached. 


As an example of the greater depth in tamarac marshes, I may give the section ob- 


QUATERNARY FORMATIONS — THE DRIFT. 945 


tained in the smallest marsh tested during the summer, consisting of only a few acres, 
in W. hf. of S. E. qr. of see. 11, Summit (T. 7, R. 17 E.). It was tested within six or 
eight rods of the edge, with the following result: 


1. At 6 feet 6 inches, began to be wet. 
2. At 10 feet 8 inches, spongy, undecomposed mosses. 
3. At 11 feet 8 inches, still in peat; bottom not reached. 


Tested in a dry ditch, nearer the edge, to a depth of over 13 feet, without finding 
bottom. 


The foregoing may be taken as representing the average character 
of the open peat bogs of the region. There are deeper and more ex- 
tensive deposits than the ones given — the selection of those to be 
tested having been controlled by the necessities of other departments 
of the survey. 

Peat has been used in this region to some extent as a fertilizer, 
and always with good results. Its value is much increased when 
mingled with other kinds of fertilizers, and it is especially efficient 
in absorbing the liquid manures that are usually wasted. The good 
results of the few trials that have been made, corroborated as they are 
by experience elsewhere, and justified by reasoning from the nature 
of the peat, commend this subject to the earnest attention of our agri- 
culturists. In reference to the last point, 1 may be allowed to pre- 
sent succinctly those properties of peat that render it valuable as a 
manure, chiefly on the high authority of Prof. 8. W. Johnson: 

1. It absorbs moisture both as a liquid and a vapor, and so coun- 
teracts the effects of droughts, and makes it invaiuable to the more 
arid soils. This hygroscopic property indicates a natural adaptation 
to use as a fertilizer rather than as a fuel, it being detrimental in the 
latter respect. 

2. It improves the texture of the soil. 

3. By its decay it furnishes ammonia and carbonic acid, and some 
mineral substances. 

4, It assists in the disintegration of other substances in the soil. 

5. It absorbs ammonia from the air, and thus furnishes it to the 


plants. 
6. By its dark color it absorbs heat from the sun, and thus in- 


creases the temperature of the soil. 

Attempts have been made to utilize it asa fuel at several points 
with varying success. In almost all cases it seems to have furnished 
a very fair fuel, and in some cases it is claimed to be equal to the 
best hard wood. The general tenor of the results, where machinery 
has been used, is unfavorable; where the simpler methods have been 
employed, the prospect is more encouraging. In reference to the 


246 GEOLOGY OF EASTERN WISCONSIN. 


want of entire success in the former case, I gather the following 
causes: 

1. Too much is expected, and consequently too great expense is 
incurred and too great risks taken. Theoretical calculation readily 
shows immense profits, and leads to manufacturing on a false basis, 
unless large deductions are made for practical difficulties, and larger 
margins left for unforseen contingencies. The manufacture of peat 
in this state should only be undertaken on the basis of reasonable, not 
immense, profits, as the result of judicious and careful management. 

2. The price of other kinds of fuel in some places leaves too small 
a margin for profit. 

3. Errors in the selection of the marsh. The simple existence of 
peat of a suitable depth does not ensure a suitable quality. The eye 
and the fingers often reveal fatal impurities, and of those that pass 
the examination of the senses, chemical analysis will show that some 
are unsuitable. The proximity of a stream that habitually inundates 
the bog is a prima fucie cause for suspecting the peat to be impure. 

4, Errors arising from using that which is too near the edge, top, 
or bottom of the bed. The edge and bottom are impure for obvious 
reasons. . Before the surrounding country was cultivated, the top was 
as pure as other portions; but cultivation has immensely increased 
the amount of earthy material carried into our marshes by the water, 
and thus rendered the surface peat more impure. 

5. Errors in the manufacture. Prominent among these is the 
failure to suitably dry the peat. Much of it contains, when taken 
from the bed, ninety per cent. of water. This must be reduced to 
about twenty before it becomes suitable fuel. The peculiar hygro- 
scopic property of peat, which is one of its valuable qualities as a 
fertilizer, is a source of difficulty here. Our dry and windy climate 
is however favorable, and if this difficulty has been overcome else- 
where, it may most assuredly be here. 

6. Want of the best conveniences for burning it. Our stoves and 
furnaces are especially adapted to coal or wood, and although peat 
may be used in either, it is placed at a disadvantage. It must com- 
pete with them on their owu ground. 

7. Want of knowledge on the subject, and a natural indisposition 
to change habits. 

These and other errors will readily be corrected by experience, and 
if the laudable efforts that are being made to develop this new source 
of fuel are sustained and encouraged by an enterprising public spirit, 
we may confidently anticipate a final success. 


GEOLOGICAL STRUCTURE OF EASTERN WISCONSIN. OAR 


GEOLOGICAL STRUCTURE OF EASTERN WISCONSIN. 


The rocks of the district under consideration consist of two great 
classes, widely distinguished in age and character. The more ancient 
one consisted originally of sedimentary materials which were subse- 
quently metamorphosed into quartzites, granites, porphyries and sim- 
ilar rocks, and were folded and tilted at various angles. These (for- 
merly known as Azoic or Eozoic) constitute the Archean formations. 
Upon these were afterwards deposited a series of sandstones, shales 
and limestones that have remained essentially unaltered and undis- 
turbed to the present day, which constitute the Paleozoic formations. 

The following table exhibits in their natural order the formations 
that will claim our attention: 


HamILton, Devonian, -_ - 
Lowrr HetpErBere, - 


\ Upper Silurian, - 
NIAGARA, ) 


CINCINNATI, ) 
GALENA, 3 
TRENTON, = 
Sr. Permrs, 

Lower Maenesian,— - : 
Porspam, 


TRONIAN,, = : : Archean. 
LAURENTIAN, - - 


“‘OIOZOATVd 


| Lower Silurian, 


248 GEOLOGY OF EASTERN WISCONSIN. 


CHAPTER VI 


ARCHAAN FORMATIONS. 


The district under consideration is occupied almost exclusively by 
Paleozoic formations. The Archean rocks form the great sloping 
floor upon which these later deposits rest, and rise to the surface along 
their northern border. But the Archean surface is very irregular, 
and here and there knobs rise through the superincumbent formations, 
giving rise to isolated hills of quartzite, porphyry and granite in the 

-midst of the areas of later rocks. It is to these protruding, but not 
intrusive, masses that our attention will be chiefly confined. 

Along their northern border, the Paleozoic formations lap upon an 
immense series of granitic and allied rocks, that will receive due con- 
sideration in the several reports upon the Archean regions. They are 
here referred to as a convenient point of departure in describing the 
isolated areas above referred to, whose main importance depends upon 
their position with reference to this Archean region, and their rela- 
tions to subsequent formations. 


Tur Mouxwa Granite. 


The isolated outlier found in the S. E. qr. of the N. E. qr. of See. 
26, and the N. W qr. of the 8. W. qr. of Sec. 25, town of Mukwa, 
Waupaca county, lies nearest the main Archean area. This outcrop 
seems to have been unknown to the geologists heretofore, and came 
to my attention through information derived from Mr. Carr, of New 
London. 

It consists of three large, and as many small, rounded, elongated, 
dome-like outliers, arranged nearly in a line trending W. 35° to 40)” 
N., and rising near the center to a height of nearly 70 feet. 

The rock consists chiefly of red feldspar, with which is associated a 
less quantity of quartz and a small and varying amount of a dark 
mineral, which was not seen in the distinct crystalline form, bnt 
which seemed to be an aggregation of minute blended blades of bio- 
tite. The crystals of feldspar are never large, seldom exceeding a 
quarter of an inch in length, and are usually quite minute, so that 
some portions, from which the dark mineral is absent, closely resemble 


ARCHAAN FORMATIONS. 249 


red quartzite in appearance. The rock is intersected in various direc- 
tions by veins of quartz. It is also cut into pyramidal masses by 
smooth, straight fissures, which are usually inclined at an angle of 
from 60° to 85° to the horizon. In trend these fissures constitute three 
groups: the first nearly north and south; the second nearly east and 
west; and the third northwest and southeast. There are also large 
irregular fissures, and occasionally points are to be observed from 
which an unusual number, both of the smooth and the irregular ones 
seem to radiate. 

The rock is very little affected by weathering, and affords an excel- 
lent building material, though the form of the blocks is unfavorable, 
and it is somewhat hard to dress. 

No rock was found in contact with it, but, about half a mile to the 
southeast, in the line of its trend, the Lower Magnesian limestone ap- 
pears, into whose horizon the outcrop rises, though it lies chiefly in 
that of the Potsdam sandstone, as shown in the accompanying profile. 


Fie. 17. 


PROFILE SECTION SHOWING THE RELATIONS OF THE MUKWA GRANITE. 
1. Outlier of Granite. 2. Potsdam Sandstone. 3. Lower Magnesian Limestone. 


Tsar Bertin Porruyry. 


At Berlin, thirty miles south of the above, we next find an out- 
standing Archzan mass,! consisting of three large elongated domes 
arranged en échelon, bearing northeast. The rock is composed essen- 
tially of small crystals of orthoclase feldspar dissiminated through 
a peculiar cryptocrystalline base of felsite and quartz, forming a 
quartz-porphyry. The erystals of feldspar are usually grayish before 
weathering, becoming reddish afterward. The base in its unweath- 
ered state very much resembles quartzite, and is of dark grayish cast 
with a very slight reddish tinge, so modified by its translucency as to 
give to the whole what may be called a water hue. Very thin splint. 
ers may be fused before the blow-pipe with difficulty, forming a 
transparent glass-like bead. The effect of weathering is marked and 
peculiar. The color changes to a light reddish, pinkish, or grayish 
white, and occasionally to a bright red, while the mass becomes opaque 
and finely granular, and so soft as to be easily cut. There are oe 
sionally spots, streaks, or leaves of dark material in the base, which 


_ 1 Comp. Dr. Percival’s Report of 1856, p. 106. 


250 GEOLOGY OF EASTERN WISCONSIN. 


are doubtless the portions referred to by Dr. Percival as “interlami- 
nated hornblende and mica.” 

The rock is very uniform in character at all points exposed. It 
presents an obscure parallel structure giving rise to a somewhat defi- 
nite system of cleavage, but traces of distinct bedding were not ob- 
served. The mass is traversed by extensive fissures which are readily 
arranged into three groups, the predominant one of which bears N. 
W., and the smaller ones E. of N. and N. of E., respectively, thus 
dividing the horizon into nearly equal ares; but none seem to be de- 
pendent on the cleavage structure of the rock. 


Fie. 18. 


East anp WE=sT SECTION THROUGH THE BERLIN PorPHYRY. 


1. Porphyry. 2. Potsdam Sandstone. 3. Lower Magnesian Limestone. 


On the south slope of the hill, and within a few rods of the expo- 
sure of porphyry, occurs a sandstone in which are imbedded masses 
of the porphyry of various sizes. The sandstone also contains several 
species of Potsdam fossils, demonstrating the presence of the por- 
phyry as an island or reef during the deposition of the sandstone. 
These facts entirely negative the view that these hills were either 
ejected as an igneous mass, or thrust up as such by upheaval. They 
are simply projecting points of an eroded formation. 


Tue Quartz-Porpuyry or Pine Buvrr. 


Seventeen miles south of Berlin there rises out of the flood plain 
of the Grand river a conspicuous mass of quartz-porphyry known 
as Pine Bluff. It ascends by steep, and even precipitous acclivities 
to a height of one hundred feet, and being entirely isolated from 
surrounding elevations, and largely bare of soil and vegetation, be- 
comes a striking object. The rock consists of white, gray and flesh 
colored crystals of orthoclase, and of glassy feldspar, set in a very 
hard, gray or black quartz-felsite base. The crystals of feldspar vary 
in size from three-tenths of an inch in length, downwards, but are 
rendered conspicuous by contrast of color. The rock is susceptible of 
very high and beautiful polish, but is wrought with difficulty on ac- 
count of its hardness. The dip is about 20° to the E. of S. Obscure 
glacial strie, still preserved, testify to its endurance. Their direction 
is S.45° W. The accompanying profile exhibits its relations to the 


ARCHAAN FORMATIONS. 251 


Silurian formations, from which it will be seen that it rises to about. 
the base of the Galena limestone. 


Fire. 19. 


NortH AND SoutTs Sx¥cTIoN THROUGH Ping BLUFF. 


1. Quartz-Porphyry, Pine Blu®. 2. Lower Magnesian limestone. 3. St. Peters sandstone. 4, 
Trenton limestone. 5. Galena limestone. 


Tur Quartz-Porpuyry or Marquerte. 


Near Marquette, a little more than twelve miles west of Pine Bluff, 
very similar quartz-porphyries display themselves in moré considera- 
ble force, constituting a group of prominent hills. A portion of the 
rock is precisely identical in character with that of Pine Bluff, and 
the greater mass is but an unimportant variation from it, but cer- 
tain portions depart from the porphyritic character, and become al- 
most, or entirely, crypto-crystalline. One variety of this kind very 
closely resembles the more homogeneous of the red Huronian quartz- 
ites, and another is a compact close-textured rock, usually of dark 
color, but sometimes greenish. Neither of these varieties occupies 
exclusively any one horizon, but the quartzite-like variety is found in 
the more southern outcrops, the last mentioned kind immediately 
north of that, the darker porphyries next, and the coarser, lighter 
colored ones in the most northerly exposures. 

The bedding is very obscure, but the laminations of certain portions 
and belts of particular varieties of rock show the strike to be north. 
eastward. The dip is made out with much less certainty, but ap- 
pears to be to the northward, and to vary from 15° to 45°. 

Though the Berlin porphyry differs from that of Pine Bluff and of 
Marquette in the absence of glassy feldspar, yet the close lithologi- 
cal alliance of the three is very evident, and they doubtless all belong 
to the same group of the Archzan series. The general strike of 
these formations, projected westward, encounters several similar out- 
liers, that are described in Prof. Irving’s report, and still further 
southwest he has found similar quartz-porphyry overlying the Bara- 
boo quartzite. There seems to be sufficient reason for regarding the 
latter as Huronian, so that the porphyries must be regarded as a 
newer portion of that formation. 

All of these masses present the rounded contour of glaciated sur- 
faces, and still bear the glacial groovings, and, in some cases even 


252 GEOLOGY OF EASTERN WISCONSIN. 


remnant polished spots, and from all these, trains of porphyry bowl- 
ders stretch away in the direction of the striz. 


Tur QuarrziTes oF PoRTLAND AND WATERLOO. 


Thirty-five miles south of Pine Bluff, over an area entirely covered 
by Paleozoic rocks, some as recent as the Galena, we again encounter 
the Archean rocks in the form of the quartzites of Portland and 
Waterloo. 

The outcrops in the town of Portland! are several in number. The 
most southwesterly is an oval island, lying mostly in the S. E. qr. of See. 
33, and is entirely surrounded by lowland or marsh. The outcrop at- 
tains but a slight elevation, and its rounded contour shows abundant 
evidence of the glacial agencies that have swept over it. Not only 
striee, but deep, broad furrows, show the direction of movement to 
have been 8. 15° to 20° W. Bowlders appear in great force upon the 
protected side of the island, and doubtless thickly underlie the deep 
morass in that direction, as they appear again upon the hills be- 
yond. Directly to the east, in sec. 34, there is a slight exposure near 
the base of a somewhat elevated north and south ridge, of which it 
doubtless forms the nucleus, if not the chief portion. 

Less than one mile north of these outcrops, the quartzite again dis- 
covers itself on the brow and west flank of the ridge facing Waterloo 
Creek. There is no evidence that any later formation overlies the 
quartzite between this and the two preceding outcrops, and so the 
three will be found mapped as constituting a single Archzean area. 
A short distance further to the north (N. W. qr., ses. 27), the quartz- 
ite rises in the midst of a marsh-like lake, constituting Rocky Island. 
It may be characterized as a low dome covered with unsymmetrical 
roches moutonées. 

About two miles southeast, at the foot of a hill, and on the edge of 
a marsh, occurs a low and limited outerop (sec. 35, 8. E. 4, and sec. 30, 
S.W.4). One-half mile to the northeast, across a marsh, there occurs 
another exposure, similarly situated in the southern extremity of a 
north and south ridge, and about the same distance to the southwest, 
still another one may be seen; the three lying nearly in a straight 
line, and separated by marshes. They are regarded as being project- 
ing knobs of a common area, and are so mapped. Between these and 
the three outcrops first mentioned, as also between both these and 


1 See note on the Age of the Metamorphic Rocks of Portland, Dodge Co., Wis., by 
R. D. Irving, Am. Jour. Sci., Third Series, Vol. V, p. 282. 


ARCHAAN FORMATIONS. 253 


Rocky Island, later formations intervene, so that they must be regard- 
ed as forming three distinct, though closely associated, surface areas. 

The first mentioned outlier of the last group still preserves on its 
exposed surface the scorings of the drift forces, there being two sets, 
the one pointing 8. 33° W., and the other S. 55° W. 

From the several outliers there stretch away to the southwestward 
trains of bowlders of quartzite, which gradually spread out into a fan- 
like form, the fragments meanwhile becoming more rounded, smaller, 
and scattered. I have traced them fifty miles distant into Illinois. 
A figure illustrating these facts has already been given. Their special 
significance here relates to the question whether other masses of 
quartzite protrude through the Paleozoic formations in this region. 
If so, they should indicate their presence by erratics in the drift. 
Bowlders, in limited numbers, reach about three miles east, and a 
somewhat greater distance north of the outcrops, but as traced in 
those directions, no concentration toward a point of origin was ob- 
served with sufficient definiteness to locate their source. 

The discovery of a train in the town of Waterloo led to more sat- 
isfactory results. The abundance of angular blocks in the drift led 
to the conviction that their source was in the immediate neighbor- 
hood, and, under the guidance of the Rev. G. S. Hubbs, the actual 
outcrop was found. Like the others, it lies at the foot of a ridge on 
the border of a marsh. The exposure is small, but interesting. 

At one point there is a very fine exhibition of ripple marks running 
parallel to the dip, thus demonstrating the true 
tilting with certainty. This was found to be 

==- 464° N. E., the strike being N. 45° W. 
- The rock of all these outcrops is a hard, 
Rirriz-markep Ooruisx. thoroughly metamorphosed red, or gray quartz- 

Powe at Walter, ite. Metamorphic conglomerates occur in cer- 
tain portions. In others there is a foliated material of talcose appear- 
ance, yet seldom sufficient to give the rock a schistose structure. The 
gray variety of quartzite predominates, especially in the more westerly 
outliers, while the red is more abundant in the eastern. 

The relations of these quartzites to the surrounding formations are 
exceedingly interesting. About eighty rods south of the outlier in 
Waterloo, the lower layers of the Trenton limestone, reposing upon 
the St. Peters sandstone, occur at the same level as the quartzite, with 
no indication of disturbance. The accompanying figure will render 
the situation clear. 

In the intermediate space are bowlders of conglomerate, the peb- 
bles of which are of quartzite, precisely similar to that of the out- 


254 GEOLOGY OF EASTERN WISCONSIN. 


liers, while the matrix is of white sand similar to that of the St. 
Peters sandstone. There are also fragments of sandstone contain- 
ing the cylindrical cavities known as Scolithus. A single bowlder 
was also found uniting the two. Ihave found Scholithus tubes in 
the upper transition layers of the St. Peters sandstone, and as there is 
no known Potsdam sandstone along the line of drift for more than 
one hundred miles, and rarely then, in contact with quartzite, it seems 
altogether most rational to conclude that the St. Peters sandstone 
was laid down around the island of quartzite from which the pebbles 


Fia. 21. 


PROFILE SECTION SHOWING THE RELATIONS OF THE WATERLOO QUARTZITR. 
1. Quartzite. 2, St. Peters Sandstone. 3, Trenton Limestone. 


of the conglomerate were derived by beach action, and that the 
bowlders in question were derived from the deposit thus formed. The 
greater fineness of the rock, which is a matter of observation, may 
account for the preservation of the Scolithus tubes, which are very 
rare in the more friable portions. This view is both corroborated and 
complicated by the still more interesting facts observed in the town of 
Portland. Opposite Rock Island and near the water’s edge, we find a 
white sandstone bearing abundant well preserved Scolithus tubes. 
This graduates above into a fine conglomerate, which becomes coarser 
and coarser until at a height of 48 feet, where it adjoins the quartzite, 
it consists of bowlders three or four feet in diameter, imbedded in 
finer grades of conglomerate. There is here no question as to the ori- 
gin of the conglomerate, or of the relations of the Scolithus to it. 
The quartzite rose as a rocky island in the depositing seas, and yield- 
ed its material to the beating of the waves, by which the eonglomerate 
was formed. 

But on the opposite side of the ridge, somewhat more than a mile 
distant, a peculiar shaly, arenaceous rock is found at the same eleva- 
tion. One variety of this rock is exposed in the railroad cut in See. 
3 of the town of Waterloo. It is of variegated, reddish aspect and 
irregular texture, and closely resembles the variegated shales of the 
Mendota beds of the Potsdam, and also some of the modified forms of 
the St. Peters sandstone, where it lies contiguous to the domes of 
Lower Magnesian limestone, subsequently to be described. It has 
been penetrated at several points in the vicinity by wells which in 
some cases reach the quartzite underneath it. The owners of the 
wells usually describe it as a red, sandy rock. At one point (middle 


ARCHEHAN FORMATIONS. 255 


N. line of N. E. qr. of 8S. W. qr., See. 35, Portland), a rock of similar 
uature, but of light buff color, was penetrated to a depth of 18 feet, 
below 36 feet of drift, when quartzite was reached. In the S. E. qr. 
of Sec. 3, town of Waterloo, after 18 feet of drift, 41 feet of what 
was described as a rather soft, sandy red rock, was penetrated, below 
which a hard rock, probably quartzite, was found. The accompany- 
ing cut shows the relations of this rock with the quartzite and con- 
glomerate. 
Fig. 22, 


Nortu anp Sovru SECTION THROUGH PoRTLAND QUARTZITE, 


1. Quartzite. 2. Conglomerate. 38. Shaly Sandrock. 


Figure 23 shows the horizon which the quartzite and the accompa- 
nying formations occupy. The nearest approach of the Trenton and 
St. Peters, in their normal character, is about two miles. 


Fia. 23. 


PROFILE SECTION, SHOWING THE RELATIONS OF THE PORTLAND QUARTZITE. 


1. Quartzite. 2. Shaly Sandrock. 3. Lower Magnesien Limestone. 4. St. Peters Sandstone. 5, 
Trenton Limestone. 


Without assuming demonstration, it seems most in harmony with 
all the facts, and freest from gratuitous assumptions to refer the 
conglomerates, sandstones and shaly sandrock to the period of the 
St. Peters, and they will be found so mapped It is to be remarked 
(1) That these quartzites were originally sandstones and conglomer- 
ates. (2) That they were metamorphosed before the deposit of the 
neighboring horizontal rocks, since the pebbles included in the latter 
are metamorphic. (8) That they were tilted before the deposit of 
horizontal rocks, as shown by their unconformability. (4) That their 
upheaval and metamorphism were probably synchronous and congen- 
ite. (5) That extensive erosion took place before they were com- 
pletely covered and protected, as shown by the fact that they expose 


1(Qn the accompanying map the area of quartzite in Sec. 34 is placed one-third mile 
too far north. 


256 GEOLOGY OF EASTERN WISCONSIN. 


in great thickness their truncated edges and dip at a high angle in a 
common direction — northeast. (6) That there was a vast lapse of 
time in which the erosion might take place. These rocks are un- 
doubtedly a portion of the Baraboo quartzite series which has been 
proven to be pre-Potsdam, and since the Portland and Waterloo 
quartzites rise at their highest points into the Trenton horizon, there 
must at least have elapsed time enough for the deposit of 1,200 feet 
of sandstone and limestone before they were finally covered in the 


Trenton period. 


POTSDAM SANDSTONE. Q57 


CHAPTER VII. 


LOWER SILURIAN. 


POTSDAM SANDSTONE. 


There rests upon the very irregular surface of the metamorphic 
rocks above described, filling up its depressions and for the most 
part surmounting its hills (over the area so occupied), a deep and ex- 
tensive deposit of sandstone, known under the above name. That it 
is the exact equivalent of the Potsdam sandstone of New York, as 
would seem to be implied by the name, is not absolutely certain, but 
as the term has been used to designate this formation in previous re- 
ports upon the geology of the state, and as the weight of evidence 
and authority favors this view, the name Potsdam sandstone will be 
used without further qualification in this report. 

The upper surface of this formation is essentially uniform and 
nearly horizontal, and is overlaid by the Lower Magnesian limestone. 
These two formations, then, the limestone above and the Archeean 
rocks below, furnish one of the means by which the sandstone may 
be identified and its position and thickness determined. Since its 
upper surface is nearly uniform, and its bed very irregular, it 
necessarily varies greatly in thickness, the known range within 
the state being from zero to about 1,000 feet. Within our district 
its variation in thickness is known to be but little short of this, and 
from the nature of the case, it is evident that the extreme thickness 
of this rock may much exceed that which has been observed. This 
irregularity in thickness should be kept in mind in making any cal- 
culations dependent upon the depth of this formation. 

General Character. The rock is chiefly composed of cemented 
grains of silicious sand. To the unassisted eye, these grains appear 
spherical, but upon examination under the microscope, they are seen 
to be more or less angular and irregular, and show that they have 
been formed from small fragments, and in some cases, perhaps, 
minute crystals of quartz, which have been worn by friction to their 
present form. These grains vary much in size in different localities, 
and in the various strata of the formation. 

Wis. Sur. —17 


258 GEOLOGY OF EASTERN WISCONSIN. 


In general, as seen in outcrops in eastern Wisconsin, they ire 
neither very coarse nor very fine, but range through the medium 
varieties. Near the base of the formation a very coarse grained 
sandstone occurs, but it is not known to outcrop in the district. In 
some cases these grains are embedded in more finely comminuted 
silicious powder, doubtless worn from the grains themselves, so that 
the rock possesses considerable compactness, but only a small degree 
of cohesive power. In other cases, the filling between the grains is a 
clayey material, or a green earth, forming an argillaceous sandstone, 
or one of the varieties of greensand. 

Still again, and very commonly, the grains of sand are firmly ce- 
mented by calcareous or ferruginous matter. In many cases this is 
not so much a filling of the spaces between the grains as it is a coat- 
ing of the grains themselves, by which they are firmly bound to- 
gether. It is this variety that furnishes the most serviceable building 
material. 

Asa result of these facts, the formation presents several varieties 
of sandstone, which may be known respectively as the calcareous, the 
non-caleareous, the argillaceous, the ferruginous, and the green sand. 
Sandstone entirely free from calcareous matter is rare in this forma- 
tion in eastern Wisconsin. 

Whether we examine outcropping ledges, artificial exposures, or the 
drillings of Artesian wells, the presence of more or less of lime is 
usually indicated, except in the lowest stratum of the formation. As 
has been before remarked, the waters issuing from this formation 
usually contain a small percentage of lime salts. Whether they de- 
rive their calcareous burden from the sandstone, or, on the contrary, 
are the sources in part of the lime in it, having obtained it originally 
from the limestone above and yielded it to the sandstone in passing 
through it, may be a matter of doubt, in some cases, but a portion of 
the lime was undoubtedly deposited at the same time with the sand. 

All of the non-calcareous sandstones, observed in the district 
under consideration, crumble so easily as to be of little industrial 
importance except as a source of sand, and as they form a sterile soil, 
their rarity may be considered a matter of good fortune. 

In the argillaceous class, the clayey material sometimes becomes 
so abundant as to render the rock shaly, and in some cases it go far 
predominates that the rock is known as a shale, rather than a sand- 
stone. These argillaceous layers are usually’ impervious to water, 
and demonstrate their utility by giving origin to valuable springs. 

There are two classes of green sand, one, which consists of grains 
of quartz colored by some substance —iron in those cases which I 


POTSDAM SANDSTONE. 259 


have examined — the other and much more prevalent, which consists 
of a mixture of ordinary white quartz grains, and deep-green grains 
of glauconite, or a closely allied mineral. 

The ferruginous varieties embrace at one extreine, those in which 
the amount of iron oxide is barely sufficient to color or cement the 
mass, and at the other, those in which it becomes so great as to justi- 
fy calling the mass an iron ore. Neither of these classes is abun- 
dant in this portion of the state, though important features in other 
parts. The sandstone of this regiqn is usually very light colored, and 
nodules, seams, or layers of iron, though present, attain to no signifi- 
cant development. 

As has been already remarked, the great mass of this sandstone is 
more or less calcareous. The limy portions become so great in some 
layers that they are more properly limestones than sandstones. The 
lime in this case, as is usual in this state, is associated with mag- 
nesia, so that these layers become really arenaceous dolomites. In 
some portions, the calcareous matter, instead of being dissemina- 
ted through the rock, forms concretions, by binding lumps of sand 
into hard spherical masses, giving the beds a nodular structure. 

The foregoing general statements may perhaps suflice to indicate 
the prevailing chemical and molecular nature, and the minute struc- 
ture of this formation. More specific facts will be found in connec- 
tion with the local sections and descriptions. We may now consider 
its more massive characters. Where bedding is distinctly marked 
the layers are not usually more than three or four feet in thickness. 
From this thickness they are to be found of all lower dimensions down 
to layers of slate-like thinness. The beds show oblique lamination, 
ripple marks, and other evidences of shallow water deposit. 

Owing to the prevalence of heavy deposits of drift, exposures of 
this formation in eastern Wisconsin are quite unfrequent, and very 
limited in extent; a very fortunate circumstance for the agriculturist, 
though quite the reverse for the geologist. However, by diligent 
search and careful collating of data, it appears that the formation 
consists of six subdivisions, as follows, beginning at the top: 


Sandstone (Madison)... .. 0. ese cee cece c eee ee eter ence eee e eee e es 
Limestone, shale and sandstone (Mendota).......--..--+++++-++22+ 60 


Sandstone, calcarcous.......e.eeeece eee r cnet ene eee tees nent ne ees 


Bluish shale, calcareous,...... 00s ee eee eee e eect cece seen eee e anaes 80 “* 
Sandstone, slightly calcareous,..- +++... essere eee e eee e eee eres 160“ 
Reda. deine Se eee a pen asoame me 280“ 


Very coarse sandstone, non-calcareous, 


The thicknesses given are subject to considerable variation. Asa 
general rule they grow less toward the northeast. Where the total 


260 GEOLOGY OF EASTERN WISCONSIN. 


thickness of the formation is reduced by the inequalities of its Arch- 
ean bottom, it is by the loss of the lower members of the group and 
not by the thinning of all. 

z. Madison Sandstone. This name has been assigned, by Prof. 
Irving, to the uppermost subdivision, from its occurrence in the vi- 
cinity of the capital, where it is extensively used, under that name, as 
a building stone. He regards this as a member of the Calciferous 
group above, rather than of the Potsdam, in respect to which, howev- 
er, I feel compelled to differ from him, for reasons given below. 

At its more typical localities, this sandstone is a rather coarse 
grained, thick bedded, compact, but soft, slightly calcareous, light 
colored sandstone. It is best shown at Lucas Point, on the southern 
shore of Green Lake, a few miles west of Ripon, where, however it is 
more than usually fine-grained. 

At this point it is horizontally laminated, and marked by wavy 
lines of reddish yellow iron stains, though these are probably not con- 
stant characters. In its upper portion, immediately beneath the low- 
er magnesian limestone, it is at most locations coarse, and the topmost 
layer is often broken up and mixed with calcareous material, giving it 
a coarsely brecciated structure. This layer, or its equivalent, usually 
marks the upper limit of the formation with distinctness, though more 
or less of sand mingles with the lower ledges of the limestone above. 

2. Mendota Limestone. This name has been given to this group of 
strata, by Prof. Irving, from its occurrence on Lake Mendota, near 
Madison. The term limestone is applicable, however, to this division 
in eastern Wisconsin, only in a qualified sense. It consists really of a 
group of alternating strata of arenaceous magnesian limestone, sandy 
caleareous shales, and shaly and calcareous sandstones. The lime- 
stones are soft, granular, porous, friable, rather thin bedded, buff 
colored, and frequently contain seams of greensand. 

They resist erosion to a greater degree than the sandstones above 
and below, and so sometimes form the protecting cap of terraces. 

The shales are variegated with yellow, redand purple. Those of the 
latter class are quite characteristic, though something very similar 
occurs at a few exceptional localities in the St. Peters sandstone. 
The purple portion, which only makes up a part of the mass of the 
rock, consists of irregular layers, lumps and patches mixed with red- 
dish and yellowish portions, giving the whole a peculiar mottled ap- 
pearance. The lighter colored shales occur intimately associated with 
these. Both classes are more or less arenaceous and calcareous, are 
soft and brittle, easily crushed, and readily decomposed under the ac- 
tion of atmospheric agencies. 


POTSDAM SANDSTONE. 261 


The sandstones are of two kinds, those consisting of the common 
white, buff, yellow or orange quartzose sand, with more or less of cal- 
careous and aluminous admixture, and those formed by a mingling of 
the common quartzose sand with green particles of glauconite, and 
altered forms of it, producing as a result various shades of gray, yel- 
low, green and mottled sandstones. The component grains frequently 
have but a slight cohesion, so that the mass is fittingly termed green 
sand. 

The upper and lower limits of the Mendota group are scarcely de- 
finable. It graduates above into the Madison sandstone, so as to make 
it difficult to draw a line between the two, and below, the alternation 
of calcareous and arenaceous rock make it equally diffieult to say 
where the series ends. 

A thickness of fifteen or twenty feet would include the greater por- 
tion of the lime rock, while about sixty feet would be required to 
cover the entire alternating series. This will be clearly seen by in- 
specting the local sections subsequently given. 

This constitutes one of the objections to separating this from the 
Potsdam sandstone series, and grouping it with the Lower Magnesian 
series. The lower limit of the Magnesian limestone is in this region 
and elsewhere so far as I have personally observed, well defined, al- 
though sandstone mingles with the formation above and calcareous 
strata extend scores, if not hundreds, of feet below into the Potsdam 
sandstone. Aside from other objections, there seems to me no good 
reason for placing the dividing horizon at any other point than that 
which has very generally been recognized by geologists, viz.: at the 
top of the Madison beds. 

It is to be remarked, however, that in central Wisconsin where the 
Mendota beds develop a greater thickness and purity of dolomitic 
character as well as greater lithological similarity to the Lower Mag- 
nesian limestone, they have heretofore been mistaken for that forma- 
tion, and something of confusion introduced into the geology of this 
horizon, which the distinct recognition of the Mendota beds by Prof. 
Irving has removed. 

The paleontological evidence very strongly corroborates the view 
here taken. Without attempting an exhaustive discussion, it may be 
remarked that the Mendota beds are undoubtedly the eastern equiv- 
alents of Dr. Owen’s Fifth Trilobite bed, the common horizon being 
characterized by the presence of Dicellocephalus Minnesotensis, D. 
Pepinensis, Lingula aurora, L. mosia, and a few other species of lim- 
ited horizontal distribution. The primordial aspect of this fauna is 


unquestionable. The collections of this season have shown Lingula 


262 GEOLOGY OF EASTERN WISCONSIN. 


sosia to be associated with Lingulepis pinniformés, which is con- 
sidered by Owen and Hall as characterizing the lower beds of the Pots- 
dam, and Dicellocephalus Pepinensis was found with LT llenurus 
quadreatus, which Prof. Hall refers to the middle Potsdam, thus show- 
ing specific paleontological bonds with the lower strata. 

On the other hand there is not, so far as I am aware, any case of 
the occurrence of any of these species in the Lower Magnesian lime- 
stone, as limited in this report, there being ample reasons for believ- 
ing that in all cases where Dicellocephalus Minnesotensis has been 
doubtfully referred to this horizon, the specimens really belonged to 
the Mendota or other intercalated beds. 

The lower divisions, constituting the main body of the Potsdam 
sandstone, present but very few exposures in this region, and these of 
very limited extent, so that we are’ dependent chiefly on the evidence 
derived from Artesian wells for positive knowledge of their nature. 
So far as thus indicated, there are four subdivisions. 

3. Lhat which lies next below the Mendota beds is a light colored, 
fine to medium grained sandstone. The constituent grains are chiefly 
quartz, with a less quantity of chert and a few limestone and granitic 
particles in some portions. It is slightly calcareous, even where the 
limestone particles are not observable. 

4. The next division consists of a bluish green shale of highly cal- 
careous nature, containing minute, glistening, mica-like scales. It 
was not seen in outcrop, and may be quite local, though it appears 
to be represented in the northwestern part of the state, 

5. The fifth division is very similar in nature to that above the last, 
being a rather fine grained, light colored quartzose sandstone, contain- 
ing occasionally some clay-like calcareous matter. 

6. The lowest subdivision is a very coarse, non-caleareous sand. 
stone, composed of large grains of transparent, light colored quartz of 
irregular but rounded form. 

Organic Remains. The following is a list of the fossils found in 
the Potsdam in this portion of the state. These, and all subsequent 
identifications in this report were made by Prof. R. P. Whitfield, 
whose eminent qualifications are a guaranty of their correctness: 


Puants. 


Paleophycus. Sp. und. 


Mo.iuscoa. — Bracutopopa. 
Orthis Pepina. 


ARTICULATA. — ANNELIDA. 
Tubes of scolithus?2 


POTSDAM SANDSTONE, 263 


TRILOBITES. 


Conocephalites diadematus, H. 
Conocephalites minor, Shum. 
Conocephalites Gibbsi, n. sp.1 
Dicellocephalus Misa, H. 


This is probably very far from being a fair representation of the 
actual fauna, but the meagerness of the outcrops in this region, and 
the fact that the rock is very rarely quarried, make it practically 
impossible to secure a full collection. 

Method of Deposit. That this sandstone was deposited beneath 
the ocean is shown by the remains of marine life found in it. That 
the water was comparatively shallow is indicated by the ripple marks 
and beach structure that abound in the formation. The rounded and 
yet irregular character of the grains of sand that constitute the chief 
element of the rock leaves no doubt that they were originally small, 
angular grains of quartz that have been worn by friction to their 
present form. The fact that this formation lies upon the surface of 
the Archeean rocks, which abound in quartz in the form of irregular 
grains and crystals, and in mica, feldspar and other minerals found 
in the sandstone, that these rocks have been decomposed and eroded 
to an enormous extent, and that they were, at the time this deposi- 
tion was in progress, exposed to the action of the waves and atmo- 
spheric influences, make it certain that the sandstone was derived 
from these older rocks, and that this was accomplished by the same 
process of wear, decay, and redeposit that is in action at the present 
time, producing similar accumulations of sand, that may in time be- 
come hardened to rock. The clayey material was doubtless derived 
in the same way from the feldspar and other aluminous ingredients 
of the same granitic rocks, but the calcareous portion was doubtless 
chiefly formed through the agency of marine life. 

A microscopic examination of the grains of sand is entirely fatal 
to the view still occasionally advanced, that they were produced by 
erystalization from solution, as they neither have in general the crys- 
talline nor coneretionary form, nor one that would naturally be de- 
rived from either of these by friction, if indeed friction were suppos- 


able under that theory. 
Extent. It has heretofore been remarked that the Potsdam sand- 


1The names of new species given in this volume are from the manuscript of Prof. 
Whitfield, which will be published at an early day. They are here introduced for the 
obvious value they will give the report when the descriptions shall be published, and 
with no reference to any claim to priority of publication. 


264 GEOLOGY OF EASTERN WISCONSIN. 


stone in Wisconsin has the general form of a crescent. We have the 
right or eastern horn of this crescent under consideration. It enters 
the district obliquely from the southwest, and occupies the western 
margin of Green Lake, Winnebago and Outagamie counties, from 
whence it extends to the northeastward, passing into Michigan across 
the upper great bend in the Menomonee river. It is much narrower 
in this than in the central portion of the state, averaging only from 
ten to fifteen miles in width. The formations in this part of the 
state have a rudely zigzag or stair-like outline, in which this sand- 
stone participates. This is more especially true of its upper limit or 
eastern boundary, where it is overlaid by the Lower Magnesian lime- 
stone. Its lower limit cannot be mapped with equal precision, owing 
to the unevenness of the underlying formation and the ever present 
obscuring drift accumulations. Beyond the limits marked on the 
maps, where detailed investigations have not yet been made, isolated 
patches will doubtless be found resting upon the Archeean rocks. 

A more clear and accurate view of the surface extent and location 
of this rock than it is possible to convey by verbal description, may 
be obtained by consulting the accompanying maps, to which the at- 
tention of the reader is respectfully invited. 

The formation dips to the east, and passes under all the formations 
lying in that direction, as shown in the sections on the accompanying 
maps, and in this volume under the head of Artesian Wells, so that 
it underlies at varying but ascertainable depths the whole of the east- 
ern part of the state. 


SECTIONS AND LOCAL DESCRIPTIONS. 


The township of Kingston in the southwest corer of Green Lake county, being the 
most southerly town in the district under consideration that is occupied to any extent 
by this formation may serve us as a suitable point whence to proceed northward in sketch- 
ing such local developments of this formation as may seem to demand notice, the more 
fittingly so because it presents several prominent elevations that expose the formation. 
The most satisfactory of these is Bartholomew’s Bluff, in sec. 15, 8. hf of N. E. qr., T. 
14, R.11 EH. This hill is conspicuously terraced, the lower shelf being capped by the 
Mendota beds and the upper by the more enduring Lower Magnesian limestone. The 
sandstones that form the rest of the hill, being soft, have been more affected by erod- 
ing agencies, leaving limestone-capped benches as seen in the accompanying figure. 

The following is the section exposed at this point, in descending order: 

1. Bluish-gray, thick bedded, sub-crystalline, slightly silicious dolomite, uneven tex- 
ture, granular in part, compact in part, and approaching a brecciated structure in por- 
tions, weathering to a rough ragged aspect; fossils absent or very rare; the bottom lay- 
ers of the Lower Magnesian limestone, not completely exposed but probably about 20 
feet in thickness. 

2. Slope of the terrace, concealed by debris; known to be occupied in part at least by 
a yellowish quartzose sandstone, with slight calcareous cement. It is probable, from ob- 


POTSDAM SANDSTONE. 265 


servations elsewhere, that the whole slope is underlaid by the Madison sandstone. Thick- 
ness 380 feet. 

3 Rotten calcareous chipstone, occupying the surface of the lower terrace, derived by 

. disintegration from a rock similar in char- 
Fig. 24, acter to the stratum below. Thickness 3 
feet. 

4. Light butt, thin bedded, impure, gran- 
ular, porous, soft, easily fractured magne- 
sian hmestone, marked with fucoidal impres- 
sions and interlaid with thin seams of green 
sand. Mxamined under the microscope, the 
component grains appear very angular and 
in the dry state mostly opaque. On the addi- 
tion of acid, part are dissolved with efterves- 
cence, leaving many transparent angular 
particles insoluble in warm acid. Used for 
building purposes. Thickness 8 feet. 

5. Unexposed, 4 feet. 

6. Greenish and grayish, scarcely cohe- 
rent sandstone, composed of white or light 
colored grains of quartzose sand and green 
grains of glauconite. Thickness 6 feet. 

7. Calcareous, banded and mottled white 
and orange, coarse granular, sandrock, part- 
ly formed of quartz grains and partly of 
small crystals of dolomite. Thickness, 514 
inches. 

8. Soft, white, very friable, quartzose sandstone. Thickness, 2 feet and 5 inches. 

9. Calcareous layer of mottled, greenish and orange color, coarse granular, uneven 
texture -and medium hardness, graduating into the green sand below. Thickness, 9 
inches. 

10. Green sand of deep color, speckled with reddish iron stains, very friable, gradu- 
ating into the layer above. Thickness, 21 inches. 

11. Porous, granular, crystalline dolomitic layers, marked by nodules of hematite. 
One layer is 71g inches thick, and firm and excellent for building purposes. The layers 
are separated by thin seams of green sand. Thickness, 3 feet and 6 inches. 

12. Greenish white sandstone containing spherical concretions and Scolithus tubes. 
The walls of the tubes are usually cemented with iron oxide and the fossil stands out 
beautifully on the weathered surfaces. Thickness, 6 feet. 

18. Orange yellow, calcareous sand rock, containing crystals of calcite. Thickness, 
13 inches. 

14. Sandstone, containing spherical concretions. Thickness, 4 feet. 

15. Orange yellow, calcareous rock, as above. Thickness, 1 foot. 

16. Dirty greenish white sandstone, full of the spherical concretions and blotched 
with iron stains. Thickness, 3 feet. 

17. Orange yellow, calcareous rock, with calcite crystals imbedded. Thickness 15 
inches. 

18. White friable sandstone, the upper foot filled with concretions, the lower three 
and one-half with Scolithus. Thickness, 4 feet and 6 inches. 

19. A layer consisting of quartzose sand cemented by calcareous material, containing 
calcite crystals, and marked with limonite. Thickness, 8 inches. 

20. Sandstone filled with concretions. Thickness, 8 inches. 


PROFILE SECTION oF BARTHOLOMEW'S 
BLurFF. 


266 GEOLOGY OF EASTERN WISCONSIN. 


21. Soft, friable, dirty yellowish sandstone of very uniform medium grain. Thick- 
ness, 6 feet. 

The concretions above referred to are globular aggregations of quartz sand cemented 
by calcareous material, in size and form, resembling a boy’s marbles. They are fre- 
quently attached to each other, producing odd and fantastic forms. 

On Mt. Maria, two and a half miles southwest, the main exposure is the Lower Mag- 
nesian limestone, but at the base of it, at some points, sandstone is exposed and con- 
tains Scolithus tubes within two and a half feet of the limestone above. On the eastern 
slope of the hill the calcareous shales of the Mendota horizon may be seen. 

Near the center of section 24 of the same town the gulley of the road exposes imper- 
fectly a considerable portion of the Mendota formation, which is here more shaly than 
at Bartholomew’s Bluff and does not expose any firm thick layers of limestone, the sec- 
tion being composed chiefly of shales and sandstones, as follows: 

1. Coarse yellow crystalline limestone, graduating into sandstone. 1 foot. 

2. Green and orange sandstone with calcareous matter in seams and aggregations. 
2 feet. 

. Green calcareous sandstone. 6 inches. 

. Orange sandstone, 1 foot. 

. Slope, covered, about 3 feet. 

. Whitish sandstone containing Scolithus, 3 feet, 3 inches. 

. Orange calcareous sandstsone, 8 inches. 

. Yellow sandstone containing spherical concretions, 1 foot. 
. Calcareous sandstone, 1 foot. 

Farther south the section is extended upward about 36 feet, by aneroid measurement, 
and consists of arenaceous and calcareous shales, interstratified with and graduating into 
green sandstone, and, more rarely, into gray sandstone. Some of the shales appear 
highly argillaceous, and some near the middle pass into an impure limestone. An ad- 
jacent hill is capped with Lower Magnesian limestone, to whose enduring character it 
owes its existence. 

Less than a mile west of this, Bow’s Hill, likewise indebted to a protecting cap of 
Lower Magnesian limestone for its origin, presents along its slopes partial exposures of 
the formation under discussion. At this point, red and purple shales are found, associ- 
ated with the various varieties of rock described at the previous localities, These red 
and purple shales have already been described as a characteristic of the Mendota group, 
but as shown by the previous sections, they are not always present. These shales are 
well shown in the town of Dayton, Sec. 27, N. W. qr. of S. W. qr., in a little quarry 
along the brook not far from the road. 


co CO SI & Ot Pe CO 


Fig. 25. 


GREEN LAKE 


Profile section from N. W. to S. E., across Green Lake, showing (1,2 and 3) Potsdam group, (2) 
Mendota beds, (3) Madison sandstone, (4) Lower Magnesian limestone, (5) St. Peters sandstone, 
and (6) Trenton limestone. 


They are again seen on the shores of Green Lake, toward its western extremity. On 
the south side of the lake they occur as a low exposure at the water's edge, covered by 
drift. On the opposite side, north of Norwegian Bay, there is a more considerable dis- 
play of Mendota strata. The cliff has a protecting cap of Lower Magnesian limestone, 


POTSDAM SANDSTONE. 267 


from which descends a steep slope covered with debnis that doubtless conceals the Mad- 
ison sandstone, helow which there comes in a series of impure limestone layers. These 
are thin bedded, inclined to be shelly, of earthy fracture, soft and quite argillaceous, the 
aluminous material forming shaly partings. Below this follow a group of arenaceous 
shales and shaly sandstones, chiefly of greenish and purple casts, whose structure is 
somewhat changeable as traced horizontally. Oblique lamination is most beautifully 
shown in some portions. Underlying these are heavy beds of calcareous sandstone, of 
yellowish color, and rather uniform, firm texture, below which lie purple, iron-stained 
‘arenaceous shales, succeeded by calcareous sandstone similar to that above. The expos- 
ure reveals a low axis, the strata dipping both east and west from its center. 

Sugar Loaf, on the opposite side of the Bay, discovers essentially similar strata. Sur- 
mounted by like Lower Magnesian ledges, its talus-covered slope of 60 feet is succeeded 
by alternating layers of the Mendota group. 

Limited outcrops of the Potsdam strata occur at several points in Green Lake county, 
which cannot here be specially described for want of space, but which the accompany- 
ing maps will enable any one to identify, who may desire to do so. 

At Berlin, adjacent to the porphyritic ledges, a coarse silicious sandstone occurs, con- 
taining, imbedded in it, fragments of the porphyrite, often of large size. These frag- 
ments are sometimes well worn and rounded, but oftener angular. Fortunately these 
beds are also fossiliferous, and the following species have been identified from the col- 
lection made by Mr. F. H. King: Paleophycus, Sp. und., Orthis Pepina, Scolithus, Con- 
ocephalites diadematus, C., minor, C., Gibbsi, n. sp., Dicellocephalus Misa. These show 
that this sandstone, conglomerate and breccia, is of the Potsdam age. The position at 
which these occur in the western part of the state would indicate that these beds belong 
to the middle portion of the formation, though the elevation as compared with that of 
the Lower Magnesian limestone, which occurs a little to the east, is such as to lead to 
the belief that it belongs to a higher horizon. 

The conglomerate and breceia were undoubtedly formed by the beating of the waves 
against the adjoining porphyrite cliffs, which formed a rocky island in the ancient ocean. 

From this point northward the Potsdam beds are almost wholly concealed by duit, 
except as a few feet are exposed here and there at the base of the Lower Magnesian 
ledges, that mark the western limit of that formation. Such exposures occur in the 
towns of Winchester, Caledonia, Mukwa, Hortonia, Ellington, Cicero, Shawano and 
Gillette, but nowhere is more than a few feet of the upper part of the formation shown. 

Near the “ Big Bend” of the Oconto river, the bluffs on the south side are crowned 
with impure limestone very meagerly exposed, below which the Potsdam sandstone oc- 
casionally shows itself. About two miles below the bridge, the ‘‘ Flat Rock ”’ is formed 
by beds of quartzose sandstone, stretching across the river and forming gentle rapids. 
The rock is grayish white, mottled with yellow, and composed of well rounded grains of 
transparent quartz of varying size, cemented with a little calcareous matter. The beds 
dip gently to the southeast. The face of the layers, as they cross the river, is pitted with 
“pot holes ’’ not often exceeding the size of the homely utensil that gives them a name, 
in some of which the gravel is still eddying about, continuing the process of formation. 

At Little Falls on the Peshtigo river, a lower portion of the formation is presented, 
consisting of white friable sandstone, composed of nearly uniform, well rounded grains 
of quartz, with very little cementing material. The upper beds are thick and massive; 
below these, the layers are thinner and softer, beneath which again are thicker beds. 
The falls owe their origin to this irregularity. 

Several miles down the river in Sec. 12, T. 31, R. 20 E., there is a low exposure con- 
taining Scolithus tubes, and representing a higher horizon. 

The formation barely demonstrates its presence where it crosses the Menomonee yiver 


into Michigan. 


268 GEOLOGY OF EASTERN WISCONSIN. 


LOWER MAGNESIAN LIMESTONE. 


Reposing upon the upper face of the Potsdam sandstone lies a 
group of silicious dolomitie beds, to which the term Lower Magne- 
sian limestone was applied by Dr. Owen, to distinguish them from 
the Galena and Niagara dolomites, which constituted his Upper Mag- 
nesian limestone. The former name has very properly been retained, 
while the latter, for good reasons, has been discarded. The term Cal- 
ciferous sandrock, applied to the near equivalent of the Lower Magne- 
sian limestone at the east, is not admissible in this state, from the 
lithological nature of the rock. 

General Character. It is, as the name implies, a magnesian lime- 
stone or dolomite, sufficiently pure to burn to a serviceable quicklime 
in its lower, middle and upper portions, though not in each layer of 
these subdivisions. The chief impurities are quartz, clay, iron and 
greensand, ; 

The dolomite occurs in the earthy, the granular crystalline, and the 
eryptocrystalline forms. The second is the more prevalent form. 
Even when the rock has a decided earthy aspect and fracture, exami- 
nation with a lens often shows a large element of crystalline grains, 
and on the other hand, in most of the cases where the crystals seem 
to have completely blended with each other, concealing themselves in 
the common mass, the crystalline facets are apt, upon close examina- 
tion, to be more or less discernible, so that, except where the rock is 
silicious, the cryptocrystalline form is not common. In some por- 
tions the mass of the rock is formed almost exclusively of small crys- 
tals of dolomite, rather loosely aggregated, leaving minute, angular 
spaces between the crystalline grains, forming a very pronounced 
granular rock. There are occasional evidences of what is probably 
the common fact, that this crystalline structure was assumed after 
the deposition of the beds, and it may have been synchronous with 
their dolomization. The silicious material is present in four princi- 
pal forms: that of dissemination through the mass of the limestone, 
of concentration in nodules of chert or flint, of aggregations of quartz 
crystals, and of scattered grains of quartzose sand. 

The amount of silica disseminated through the rock is less than, I 
think, is commonly supposed, which is likewise true of the quartzose 
sand. The granular character of the rock causes it to weather to a 
harsh sand-like surface, which appears more silicious than it really is. 
Judging from the analyses made, the silicious ingredient rarely ex- 
ceeds ten per cent., and occasionally falls below two. 

The chert, of which the quantity, on the whole, is large, is not con 


LOWER MAGNESIAN LIMESTONE. 269 


fined to any one horizon, though most abundant in the middle por- 
tion. Its distribution is irregular, though the nodules are frequently 
arranged in layers along the bedding planes of the limestone. 

The more distinctly crystulline quartz forms, in some portions of 
the deposit, multitudes of little clusters, completely filling small cav- 
ities in the rock mass, and in other portions, where the cavities are 
larger, the crystals only form a lining, producing drusy little grottoes, 
some of which are very beautiful. The quartz is most frequently 
transparent or opalescent, but it is sometimes red, brown, or rose 
colored. The crystals are sometimes grounded on a chalcedonic base, 
forming a beautiful combination. 

The quartzose sand is confined chiefly to the vicinity of the june- 
tion with the sandstone below and above, and to a subcentral band of 
shale, subsequently described. A portion of the odlitic grains Lave a 
silicious core. 

Argillaceous material is not abundant in the formation, except in 
shaly bands, where it sometimes constitutes as much as 20 per cent. 
of the whole. In the upper part of the formation it sometimes 
amounts to six per cent., but itis seldom that the rock is notably ar- 
gillaceous. Neither is the amount of iron conspicuous, though its 
compounds sometimes reach four or five per cent. The rock seldom 
appears ferruginous. : 

In addition to these chemical and crystalline characters, the oélitic 
structure distinguishes some portions. In most cases, the spherules 
differ but little in size from those of the roe of our common fish, 
which they so much resemble, but some, as those at Oconto Falls, 
reach a much larger size. It isa significant fact that the odlitic struc- 
ture is confined to essentially the same horizon with the sand above 
mentioned. A portion of the spherules are simply grains of sand, 
coated with concentric layers of carbonate of lime and magnesia. 

Passing from these to the more massive features, the rock presents 
a very irregular structure, owing to unevenness of hardness and com- 
position, and inequality of deposition. The effect of weathering is to 
exaggerate this, and hence outliers of this formation present a very 
rough and often grotesque exterior. A portion of the rock is brecci- 
ated, having been apparently once broken up by the waves, and in 
gome cases somewhat rounded by rolling, and afterwards recemented 
by material similar to the fragments themselves. These layers add 
to the coarse aspect of the rock. In addition to this, the bedding is 
often very irregular, and sometimes obscure, and the beds not unfre- 
quently undergo change when traced horizontally. The color of the 
weathered and leached portions is a dirty white, gray, or very light 


270 GEOLOGY OF EASTERN WISCONSIN. 


buff On the interior, the rock often has a greenish blue or gray 
cast. Some of the thinner beds and shaly layers are variegated with 
red and purple. From the ease with which the sandstone below is 
eroded, the lower portion of the formation is often left projecting in 
mural cliffs, or forming a protecting crown for some isolated hill, 
which owes its existence to such defensive covering. The strata dip 
to the eastward, and are soon lost beneath the later formations, by 
penetrating which the formation may be reached at continually in- 
creasing depths, as we go eastward. 

The floor of the formation, so far as has been ascertained, is essen- 
tially plane, but the upper surfuce is highly undulating or billowy, 
for the latter term very accurately pictures to the mind its remarka- 
ble nature. The billows of this petrous sea vary in height, from a 
gentle swell to elliptical domes rising one hundred feet above their 
bases, while their length ranges from a few rods to a quarter of a mile 
or more, and their width, from one-third to one-half the length. The 
regularity of outline here indicated is a frequent and typical, but not uni- 
versal, fact. The slope of the sides varies from 30° downwards. The 
axes of these domes lie in an easterly and westerly direction, much 
more commonly than otherwise. 


Fia. 26. 


Ja 


East AND WeEsT SECTION NEAR Ripon. 


1. Lower Magnesian limestone. 2. St. Peters sandstone. 3%. Trenton limestono. 


The superficial strata of these rock-hillows dip in every direction 
from the center, most rapidly at the sides, and less so at the extremi- 
ties; or, in other words, they are essentially concentric with the sur 
face. 

These statements are made with reference to the original condition 
of the mounds before erosion. There are satisfactory evidences that 
during the deposit of the St. Peters sandstone upon this unequal sur- 
face, the exterior of these prominences was somewhat eroded, and in 
the removal of the latter formation by the elements and the drift 
forces, resulting in their present exposure, they were still further acted 
upon. 

The eastern and northeastern extremities suffered considerable abra- 
sion from the latter cause. But neither of these agencies modified, 
except superficially, the form of these prominences, while they served 
to demonstrate more satisfactorily the quaquaversal character of the 
dip. 


LOWER MAGNESIAN LIMESTONE. O71 


Unfortunately, little is positively known to me concerning their in- 
terior. The deeper strata observed were of very irregular character, 
being either brecciated or showing a tendency to a rude concretionary 
grouping of material into irregular lump-like enlargements of the lay- 
ers. Ina very few instances, supposed to belong to this class, nota- 
bly an outlier one mile south of the village of Markesan, the whole 
of the rock exposed is a thoroughly brecciated mass, with obscure or 
absent bedding lines. This may, perhaps, be the remnant of a larger 
iass that formed the nucleus over which the sloping strata were de- 
posited, for the weight of evidence goes to show that this is a phenom- 
enon of deposition and not of upheaval. 


Fia. 27. 


SEOTION (north of Stiles) SHowmne THE RELATIONS OF THE ST. PETERS SANDSTONE AND LOWER 
Maongsian Limestone. 


Organic Remains. These are very meager. Fucoidal remains, 
Salterella (%), an undetermined species of Stromatopora; Ophileta uni- 
angulata, two undetermined species of Trilobites, doubtfully referred 
to the genus Barthyurus, embrace those found in this region. 

Area. It has been remarked that the Potsdam sandstone area 
forms a rude crescent, the eastern limb of which enters the district 
under consideration in Green Lake county, and extends thence to the 
Menomonee river. The Lower Magnesian limestone forms a serrated 
band or a fringe on the convex edge of this crescent, averaging about 
seven miles in breadth. It barely enters the district on the western 
margin of the counties of Jefferson and Dodge, but invades Green 
Lake county with its full width, and thence passes diagonally on- 
ward to the northeast, through Winnebago, Outagamie, Shawano, 
and Oconto counties, as exhibited on the accompanying maps. 

Thickness. Owing to the uneven surface, the thivkness varies 
greatly. The observed extremes in this region are 62 feet and 141 
feet. Calculations based on dip give very similar results, but it is 
highly probable that the thickness sometimes exceeds these limits. 

Local Descriptions. The most southerly point at which the Lower Magnesian lime- 
stone appears within the eastern district, is at Waterloo, in Jefferson county. Along 
the stream below the lower bridge, at the village, a low ledge presents its rough, weath- 


ered face to view. It consists of a coarse, cherty, buff, silicious dolomite, in medium 
beds of rough, uneven texture, owing in part to irregular cavities and granular porous 


272 GEOLOGY OF EASTERN WISCONSIN. 


spots, and in part to the presence of nodules of chert. This inequality of structure is 
exaggerated by the effects of long weathering, giving the surface a very ragged aspect. 
The exterior of the chert is usually white and rather soft, while the interior is dark or 
reddish, hard, translucent and flint-like. The outcrop represents the upper portion of 
the formation. 

This limestone next appears to the north, within our district, on the Crawfish river, two 
miles below Columbus, in alow exposure in the banks of the stream, similar to the 
above. Three-quarters of a mile northeast from this, near the center of the 8. E. 4 
sec. 19, town of Elba, a quarry exposes the following section of impure magnesian lime- 
stone: ; 

1. A brecciated stratum, composed of small, compact, dark gray fragments between 
which are numerous invegular spaces filled with white pulverulent material. Thickness, 
2 feet. 

2. Beds more homogeneous than the above, yet porous in parts and compact in oth- 
ers, containing nodules of chert. Thickness, 4.6 feet. 

3. A very highly brecciated layer, formed of compact. dark colored dolomitic frag- 
ments, covered with black dendritic crystals, and full of small, irregular crystal lined cav- 
ities. Thickness, 1.45 feet. 

4, A stratum of very uneven texture and composition, containing silicious nodules. 
Thickness, 5.7 feet. 

5, A single thick-bedded, porous, moderately soft dolomitic layer of uneven texture. 
Thickness, 2.3 feet. 

6. A band of rather thin sheets of irregular arrangement, inclosing large, coarse, nod- 
ular masses of breccia-like rock, hard, compact, cherty, red stained, some portions ap- 
parently silicious, some nearly pure dolomite. Thickness, 4.35 fect. 

7. Thick, uniform bed of moderately hard, compact texture, the upper portion 
marked with greenish silicious sand, iron stained. Thickness, 2.75 feet. Total, 21.15 feet. 

North of this, in Dodge county, this formation shows an occasional limited exposure, 
similar to the preceding. 

In Green Lake County it has already'been remarked that the Lower Magnesian 
strata crown several of the prominent hills. These are the lower layers of the forma- 
tion, and constitute the small patches lymg west of the serrated edge of the main body 
of the formation, as represented on the accompanying maps. 

The extensive prairies of Manchester and Dayton townships are underlaid by this 
rock, while those to the eastward repose on the Trenton and Galena limestones. It is 
in this county that we first find a clear demonstration of what constitutes the most re- 
markable feature of the Lower Magnesian limestone, viz.: the undulatory nature of the 
upper face of the formation already mentioned. North of Lake Maria, in the town of 
Mackford, are several conical mounds, partially covered with earth, which rise nearly 
to the level of the base of the Trenton limestone, which occurs a few rods to the east, 
while in the town south, at least 23 feet of sandstone intervene, and in the town north, 
at least 82 feet, and near Ripon, over 100 feet. So far as exposed, the strata forming the 
mounds dip away from the center. But we need not linger upon so poor an exposure. 

In the 8. E. qr. of Sec. 7 of the same town is a conical hill surmounted by a turret 
of massive breccia, which needs to be noted in this connection, though there is nothing 
except its elevated position to show that it indicates any irregularity in the surface of 
the formation. Butin the N. E. qr. of Sec. 15 of the same town, at the point where 
the road crosses a small stream, there is a most satisfactory demonstration of this in the 
vise of an arch of Lower Magnesian strata into actual contact with the Trenton lime- 
stone, causing the thinning out of the St. Peters sandstone to absolute zero. This is il- 
lustrated by the accompanying figure. 

The layers of the Lower Magnesian at this point, especially as seen down the stream 


i LOWER MAGNESIAN LIMESTONE, 273. 
a few rods, consist of two classes, thin undulating beds and thick brecciated ones; the 
two alternating, in a measure, with each other. Thelatter are very hard and crystalline 
in texture. Some of the angular cavities that constitute the interspaces between the 
fragments of the breccia are filled with calcite and pyrites, but most of them are empty, 
giving the impression that the rock had been crushed. But this, with one or two other 
similar cases, is exceptional. The breccias that are so common a feature in this lime- 


Fig. 28. 


1. Lower Magnesian Limestone. 2. St. Peters Sandstone. 3. Trenton Limestone. 


stone cannot, in my judgment, be satisfactorily explained by any form of crushing after 
deposition. In this instance the undulatory nature of the thin beds, and the hardness 
and crystalline character of the brecciated rock lend some plausibility to the idea of com- 
pression, or forable upheaval, as the cause of this apparent flexure of the Lower Magne- 
sian strata. But we shall have occasion to consider a large mass of facts not in 2onso- 
nance with such a view. 

The figure, which exhibits an east and west section, shows that the strata dip in both 
those directions, and by following down the stream to the northward, they are seen to 
slope rapidly in that direction also. To the south they are concealed, but judging from 
analogy, they descend also in that direction within a short distance, thus forming a 
dome supporting the Trenton strata above. 

The character of the sandstone, which will be considered more fully under its appro- 
priate head, makes it evident that the sides of this dome were subject to the action of 
the waves while the St. Peters sandstone was being deposited, demonstrating that 
whatever cause produced the arch, acted before the sandstone was formed. 

In sections one of this town and thirty-six of the town north, the Lower Magnesian 
and Trenton strata are found at the same level and very near each other, leaving no 
doubt that here is another instance of the lower formation rising into the horizon of the 
upper. This is shown by Fig. 19, ante p. 251. 

Six miles to the west of this, on the shores of the Little Green Lake, the same 
peculiarity is again manifested. At the southeast angle of the lake, a low arch is par- 
tially exposed, while on the north shore a more decisive instance occurs. A precipitous 
bluff, crowned with Trenton strata, skirts the lake on that side. At the west end of this 
bluff, there are fifty-four feet of St. Peters sandstone between the Trenton layers and the 
water’s edge, and how much is concealed beneath is unknown. But within eighty rods. 
to the east, the Lower Magnesian strata rise above the water's edge, and approach 
within eighteen feet of the Trenton above, if, indeed, they do not come into actual con- 
tact, as the nature of the slope seemed to indicate, but which could not be observed on 
account of the talus covering the side of the bluff. In the opposite direction, within a 
half mile, the Lower Magnesian strata may be found arching upwards to elevations of 
thirty and forty feet, or more, above the lake level. 

About half a mile to the northwest, a valley reveals the arcuate nature of the strata 
most clearly. On entering the gorge below, the layers are found to dip southward at 
an angle of 20° and upwards, but as the crest is mounted, the inclination becomes less 
and less until they are lost beneath the soil, within twenty feet of the Trenton horizon. 


Wis. Sur. —18 


274 GEOLUGY OF EASTERN WISCONSIN. 


Toward the top, there are to be found some very sandy layers that appear to rest, in a 
measure, unconformably upon a worn surface beneath, and probably represent the St. 
Peters sandstone, which would naturally be calcareous in such a situation. 

A portion of the rock of this dome is a coarsely brecciated, very hard crystalline dolo- 
mite, but the greater part belongs to the more common class of coarse, impure magne- 
sian limestone that characterizes this formation. 

Passing by a number of minor exhibitions of the same phenomena, we find, in the 
vicinity of Ripon, this peculiarity developed to a wonderful extent. Just west of the 
Ceresco Mills, in the lower part of the city, there rises a rock hill, having an elongated 
oval contour, somewhat enlarged and curved at the eastern extremity. Its base is 
skirted on the east and north by streams above which its crest rises to an average height 
of about one hundred feet. Its axis lies east and west, and does not much exceed one- 
fourth of a mile in length. It is terminated at the west by a deep ravine, beyond which 
rises a second ridge of similar form and height, and somewhat greater length, but which 
is less conspicuous because of its connection with the plateau on the south. The ridge 
first mentioned is nearly isolated by a deep ravine on the south, which reveals its form, 
though the rock exposures are chiefly confined to the eastern end. On the northeast 
slope, thick, heavy, rough beds of Lower Magnesian limestone show a dip of 15° to 18° 
to north of east. On the easternmost point, the dip is 18° to the eastward, while on the 
southeast curve a slant of 25° to 30° to the southeast is observed, and farther along the 
south side of the hill, a more southward and southwestward dip seems to be indicated, 
though the exposures are very unsatisfactory. A small quarry above the limekiln, and 
near the top of the hill, shows within itself dips of 3° E., 121° N. E., and 7° N. W., 
with all intermediate inclinations. This irregularity is not caused by the folding or con- 
tortion of even bedded layers, so much as by the thickening and thinning of irregular 
ones. Great lumps, as it were, occur at certain points, swelling two or three fold the 
thickness of the layer, or causing it to disappear entirely in a structureless mass. The 
rock is greenish blue, somewhat argillaceous, aud contains a few fossils. 

Down the slope from this quarry, and within six rods of it, a bed of St. Peters sand- 
stone les immediately against the flank of the Lower Magnesian arch, the top of the 
sandstone being 30 feet below the crest of the ridge. The actual junction of the sand- 
stone with the limestone was not visible at the time of either of my visits, but I was 
credibly informed that in a filled portion of the sand pit it had been previously exposed. 

Wells in the vicinity show that the surface of the limestone descends to at least 100 
feet below the top of the hill. There is here then within a horizontal distance of less 
than one quarter of a mile, a rise and fall of the upper limits of the Lower Magnesian 
limestone of not less than 100 feet. 


S. SIN : 
ENTINA ™ 
ZEN 


Nort anp Soutm Section, NEAR Ripon. 
1. Lower Magnesian limestone. 2. St. Peters sandstone. 3. Trenton limestone. 


Within less than a half mile south of this arch, the Lower Magnesian strata again 
mount into the Trenton horizon, more than 100 feet above the intervening depression, 
and again to the south, less than half a mile, another arch appears, but passes 
under the bluff to the west before attaining so great an altitude as the two preceding 
ones. The rock forming this one is unusually ivegular in hardness, and weathers out 
into the most fantastic shapes, so that the loose wom masses are much admired as lawn 
ornaments. 

The accompanying figure will assist in illustrating the foregoing facts. The irregu- 


LOWER MAGNESIAN LIMESTONE. OI5 
larity is unquestionably due chiefly to the undulation of the upper strata of the forma- 
tion; but there is evidence that the sides of these prominences were somewhat worn by 
wave action during the deposit of the St. Peters sandstone and a portion of the rock 
incorporated in that formation. Near the west line of the township of Ripon, on the 
lowlands, near the ledge that marks the limit of the Trenton plateau, the upper por- 
tion of one of these swells is finely shown. It is only a few rods in extent, and attains 
but a meager elevation compared with those just described. It is oval and symmetrical 
in outline, and has its greater axis, which is about twice its transverse diameter, east 
and west, in harmony with the general rule. The surface rock, which alone is exposed, 
is rather even bedded and homogeneous for this formation, in which irregular structure 
is the prevalent form. 

West of Rush Lake, at several points, the billowy character of this face of the for- 
mation is shown by variously dipping strata and half exposed domes of rock. 

In the railroad cut adjacent to the lake shore, near the center of section 15, Nepeuskin, 
something of the nature of the interior of these mounds is revealed, though the cut does 
not exceed six feet in depth. The surface of the rock is irregularly undulating, consist- 
ing of hummocks and hollows; notwithstanding which, it is interesting to note that it 
is polished and covered with glacial strie, bearing westward. It might be supposed 
that the present surface is due to erosion, were it not for a sandy layer, covering a por- 
tion of the surface, that seems to belong to the sandstone subsequently deposited. The 
rock is very irregular in bedding and stratification. The layers thicken and thin, enter 
and disappear, in a very remarkable way, and that within the space of a few feet. At 
the same time they curve and dip in various degrees and directions. The accompany- 
ing cuts, from sketches made on the spot, will serve to show this imypertectly. 


Fig. 30. 


SKETCHES FROM SECTION 15, NEPEUSKIN. 


Showing irregular structure of Lower Magnesian limestone. 


The irregularity is such that it seems necessary to attribute it to the conditions of de- 
position and not to subsequent disturbance. During the process of deposition there ap- 
pears to have been more or less of loosening, breaking up, rounding and rearranging of 
the somewhat indurated sediment and its redeposit, intermixed with finer material, but 
after the final deposition there is no evidence of subsequent disturbance beyond that 
common to all formations. Northwest of Winneconne these mounds become so pre- 
valent that the surface of the formation may very fittingly be termed billowy. They 
seldom exhibit a greater length than forty rods, nor an elevation of more than thirty or 
forty feet, and are usually much less than this. Of course mention is here made only of 
that portion which protrudes above the drift, and not of the actual dimensions. Their 
greatest length here, as elsewhere, is east-and west. The dip in all cases, so far ag 


276 GEOLOGY OF EASTERN WISCONSIN. 


could be determined, was quaquaversal, being greatest on the sides and perceptibly less 
at the extremities. The greatest dip observed in this vicinity was 20°. 1n most cases 
apparently only the crest of the arch was exposed and the dips were low. 

One of these hills, situated near the center of the east line of section 15 of the town of 
Winneconne, presents some special features deserving mention. The upperniost layer, 
where still preserved, contains a large ingredient of quartzose sand, or is incrusted with 
sand, or in other cases, consists of a conglomerate or breccia whose matrix is quartzose 
sand. This layer is also sometimes odlitic. As similar facts were observed at several 
other widely separated localities, this sandy portion is believed to be the transition layer 
to the St. Peters sandstone, and if so, it indicates, where preserved, the original form 
of these mounds, and that in these instances the drift forces have only removed the in- 
coherent sandstone above. This is rendered the more probable by the fact that usually 
this sandy layer was found on the southwestward side of the prominence, where it would 
be protected trom the more forcible action of the glacier, while the northeastern corner, 
which sustained the full force of the ice mass coming from that direction, was often con- 
spicuously abraded. 

Another interesting fact observed at this point was the presence of distinct mud- 
cracks and ripple marks. The latter are far less common on limestone than on sand- 
stone, and the tormer are more abundant in shales. Both occur here together on the 
gentle slope of one of these peculiar mounds. The dip, here, varies from 0 to 8°, con- 
forming as usual to the shape of the hill, which in this case departs somewhat from the 
usual symmetrical contour. The rock structure is very irregular. Some portions are a 
well marked conglomerate, both matrix and pebbles being, however, dolomitic. A layer 
near the surface is very fossiliferous, over the small space exposed, but the casts are so 
obscure as to preclude satisfactory specific determinations. They consist of the internal 
casts of an Ophileta and two undetermined species of Raphistoma. 

While our attention has thus been fastened upon the peculiarities of the superior face 
of the Lower Magnesian formation, we have been led northward along the eastern mar- 
gin of the outcrop, where alone the upper portion has escaped erosion, and have passed 
by some noteworthy outcrops belonging to the middle and lower parts of the formation. 
If we now return to the vicinity of the village of Eureka we shall be introduced to a 
feature that characterizes the submedian portion of the formation. The ledge south- 
west of that place presents the following section in descending order: 

1. Heavy irregular beds of impure dolomite, containing many cavities, more or less 
filled with quartz crystals of the transparent and milky varieties; texture varying; bed- 
ding uneven and somewhat undulatory; rock weathers to a very rude ragged aspect. 
Thickness, 10 feet. 

2. Reddish shale, variegated with gray and green, the lower portion mostly soft, break- 
ing and crumbling easily; some parts quite arenaceous; the upper portion more caleare- 
ous or dolomitic, and containing many aggregations of quartz crystals, usually of the 
opalescent variety. The layers are irregular and somewhat undulating. Thickness, 15 
feet. 

3. Very heavy beds, nearly uniform in thickness, and horizontal in bedding. The 
rock contains many almond-sized but irregular cavities, only a small proportion of which 
are filled with crystals. It is uneven but distinctly granular crystalline in texture, me- 
dium in hardness, and dirty gray or buff on the exterior, but mottled bluish on the in- 
terior. It is well adapted to heavy masonry, as foundations, piers and locks. It 
is used for the latter purpose in the construction of the adjacent locks on the Fox river. 
Thickness exposed, 6 feet. 

Attention is here called to the shale which constitutes the middle member of the sec- 
tion. What appears to be the stratigraphical equivalent of this, occurs at several points 
to the northward, the most remote being over one hundred miles distant. From this 


LOWER MAGNESIAN LIMESTONE. OTT 


fact it has a value as a guide in fixing the position of the subordinate divisions of the 
formation. 

In speaking of the sandstone below, mention has already been made of several locali- 
ties in Green Lake county, where the lower strata of this formation are visible chiefly in 
the position of protecting caps covering sandstone hills. 

Mt. Tom, in the township St. Marie, while affording another example of this, exposes 
a considerable group of the bottom layers of the Lower Magnesian limestone as follows, 
in descending order: 

1. Rough, silicious, conglomeritic dolomite, of dirty gray aspect, weathering to a very 
ragged surface, which develops prominently its conglomeritic character, and also the 
many aggregations of white quartz crystals that abound in it; rather thick bedded. 
Entire thickness of original stratum not known, as it forms the apex of the hill. 28 feet. 

2. Light bluish gray, thin bedded dolomite of even, fine grained texture, and easy, 
regular, earthy fracture, which would render it very excellent for buildig purposes if 
the courses were thicker, as they probably would be found to be where less affected by 
surface agencies. 4 feet. 

3. A thick, rough, brecciated bed similar to No. 1 above. 2 feet. 

4, Shelly, magnesian limestone and calcareous shale. The layers are thickest and 
most calcareous at the top, becoming thinner and graduating into the more shaly por- 
tion below, which is grayish buff and purple, and appears to be quite arenaceous, thoug!: 
not so in fact. 8 feet. ; 

5. Coarse, rough, thick bedded, dirty gray, hard, granular, silicious dolomite, contain- 
ing small inconspicuous geodes; irregularly cracked and fissured, and frequently form- 
ing over-hanging ledges from the removal of the softer sandstone below. 15 feet. 

On the slope below the limestone occasional slight exposures of red and yellow Pots- 
dam sandstone are visible. 

In sections 11 and 14 of Brooklyn, in this county, the beds exposed are unusually 
geodiferous. Nearly or quite half the volume of the rock in some cases 1s formed ot 
cavities lined with quartz crystals. These are chiefly red, brown and pink, sometimes 
forming very handsome, though small and irregular geodes. At numerous other points 
in Green Lake county, there are slight outcrops of this formation, which do not merit 
special description, but which may be readily identified by the characteristics already 
given, or by reference to the accompanying maps. 

In the town of Poygan, Winnebago county, the western limit of this formation is 
marked by a line of bluffs, along the face of which occasional outbreaks of the strata 
occur, but no conspicuous escarpments. 

In the N. W. qr. of Sec. 26, a quarry has been opened and a kiln constructed for the 
purpose of manufacturing hydraulic and quicklime. At the top of the quarry, three feet 
of thin-bedded undulatory layers of magnesian limestone are burned for the latter pur- 
pose. Below this is a layer exhibiting very unequal deposition, whose irregularities seer 
to give rise to the wave-like natnre of the beds above. This is underlaid by sixteen feut 
of a rather soft, granular, argillaceons, magnesian liniestone of a slightly olivaceous 
gray color, which disintegrates readily when acted on by the elements. The beds are 
below medium thickness, and, in some cases, furnish good flagging, and the material 
from which the waterlime is prepared, At the base is one foot of a yellowish-gray rock, 
eight inches of decomposed rotten stone, reposing on the common hard dolomite of the 
formation, which is very slightly uncovered. 

In the erosion of the Wolf river valley, in Caledonia, Mukwa and Hortonia, the 
sandstone below was readily removed and the more resisting ledges of dolomite left pro- 
jecting in vertical cliffs of moderate height. By combining the facts exhibited at several 
points along this line of ledges, chiefly those in Hortonia, the following section, rep- 
resenting about 60 feet of the base of the formation, was obtained. 


GEOLOGY OF EASTERN WISCONSIN. 


Earth. 
. Curved strata of hard, compact, flint-like, bluish dolomite. 18 inch ~. 
. Compact bluish white dolomite. Purest layer. 13 inches. 


. White compact dolomite, with quartz in layers, at the bedding j.a'4. 26 
inches, — 
. Compact whitish dolomite, similar to the above, but less silicious. 72 ir snes. 
Unexposed. 4 to 7 feet. 


. Blue compact hard dolomite, somewhat silicious. 9 inches. 
. Yellow, fine-grained dolomite, softer than the above. 3 feet. 


. Thin sandy, argillaceous Jayer. 1 inch. 
Thin bedded dolomite, suitable for lime. 12 inches. 


. Fine grained, but rough bedded dolomite. 3 feet. 


. Thinner bedded, compact dolomite. 3 feet. 


. Thin, shelly, sandy layer. 10 inches. 
. Unexposed. 3 feet. 


. Mottled brecciated dolomite. 18 inches. 
. Very rotten, chippy layer. 18 inches. 
. Brecciated mo:tled layer, as above. 18 inches. 


. Thick bedded, rough, uneven-textured dolomite. 6 feet. 


. Shelly rotten layer. 3 feet. 


. Not exposed. 3 feet, 


. Rough, uneven-textured dolomite. 1 foot. 


10, Flinty layer. 4 inches. 
21. Somewhat sandy, dolomitic limestone. 4 inches. 


Rough, irregular dolomite. 3 feet. 

. Sandy layer. 1 foot. 

. Light colored, slightly sillcious and moderately hard dolomite. 2 feet. 
. Broken rotten layer. 14 inches. 


j. Silicious, dolomitic limestone, very hard and flint-like. 2 feet and 9 inches. 


. White sandstone, marked with green, 4 inches. 
. Sandy layer. 3 inches. 
. Similar to No. 26. 3 feet and 3 inches. 


. Oolitic layer. 4 inches. 


. Coarsely brecciated layer, chiefly sandstone, but with some quartz and quart- 
zite-like rounded and angular masses. 4 feet and 2 inches. 


. Coarse friable sandstone of uniform grain, and containing nodules of iron 
ore. Quartzite-like layer near the top. 3 feet and 3 inches. 


Unexposed. 


LOWER MAGNESIAN LIMESTONE. 279 


In tracing the layers along the face of these natural walls, they show much tendency 
to change, and it is only by close observation and great care that an accurate correlation 
of different sections can be made, and considerable variation is to be expected where 
much distance intervenes. 

This changeableness will be manifest by comparing the preceding section with the 
two following, both taken from the same quarter section (S. W. qr. Sec. 25, Mukwa). 


Fie. 32. 


1, Earth. 


2. Magnesian limestone. 20 inches. 


3. White sandstone. 3 inches. 
4. Magnesian limestone. 8 inches. 
5. Oolitic silicious limestone. 7 inches. 


6. Magnesian limestone. 9 inches. 
7. Sandstone. 8 inches. 


8. Thick even-bedded magnesian limestone. 24 inches. 


9. Oolitic silicious limestone. 5 inches. 
10. Sandy magnesian limestone of irregular bedding and texture. 20 inches. 


11. Irregularly bedded sandstone, marked with iron. 22 inchos. 


Total thickness, 10 feet and 6 inches. 


1. Earth. 


2. Yellow sandy and oolitic magnesian limestone. 18 inches. 


8. Green sandstone. 4 inches. 


4. Oolitic magnesian limestone, as above. 2014 inches. 


5. White sandstone. 3 inches. 
6. Oolitic magnesian limestone, as above. 9 inches. 


7. Yellow sandstone. 4 inches. 
8. Sandy silicious limestone. 13 inches. 


9. Oolitic layer. 3 inches. 
10. Sandy and Oolitic limestone. 13 inches. 


11. Yellow sandstone, marked with green. 15 inches. 


Total thickness, 8 feet and 614 inches. 


The increase of silicious matter in the latter is very noticeable. This is perhaps due 
to the fact that the ledge from which the section is taken here approaches within a half 
mile of the Archean outcrop of granite in this town, previously described. As it arose 
into the Lower Magnesian horizon, it might perhaps rationally be supposed to produce 


280 GEOLOGY OF EASTERN WISCONSIN. 


such a modification of the limestone in its vicinity. But the fact of changeableness is 
nevertheless a general one. 

Through Hortonia the course of the ledge is eastward, in which direction the forma- 
tion slowly dips, until in the town of Ellington it is covered by the St. Peters sand- 
stone and Trenton limestone, which, standing out in a similar escarpment, seem to 
form a continuation of the Lower Magnesian ledge. 

It has already been remarked that the course of the streams in this vicinity is peculiar. 
The Wolf river, when it arrives opposite this rock barrier, turns sharply to the west, 
while a little stream traverses the township of Ellington in an almost direct line parallel 
to this ledge, and enters the Wolf river at the point of its sudden flexure, This little 
stream lies in the level bottom of a valley averaging about a mile in breadth. On its 
south side, in sections 25 and 26 of the town of Ellington, highly fossiliferous limestone 
of the Trenton period reaches from near the flood plane of the valley upwards, 35 feet or 
more. On the opposite side of the valley, in section 24, there arises from the same flood 
plane, a mural cliff of Lower Magnesian limestone to the height of more than 50 feet. 
The accompanying figure presents the relations of these formations: 


Fia. 34. 


Observed. 
deal 


1. Potsdam sandstone. 2. Lower Maynesian limestone. 3. St. Peters sandstone. 
4. Trenton limestone. 


The rock forming this Lower Magnesian cliff is a very hard, silicious dolomite, of 
almost flinty texture, striking fire readily from impact of the hammer, and yielding a 
resonance and fracture more like quartzite than ordinary limestone. Its distant bedding 
joints are very obscure, in the main body of the cliff, while irregular vertical fissures are 
numerous and conspicuous. Geodes of limpid and opalescent quartz are scattered through 
it. These characteristics pertain in full only to the cliff in question. To the east a low- 
ex ledge of the more usual coarse, silicious limestone extends some distance into the next 
township, and a similar ledge on the west, curves to the north, and is lost under the 
drift. But it soon reappears and extends with insignificant interruptions onward to the 
vicinity of the Wolf river. The strata, like those on the south side of the valley, rise in 
that direction, so that near the river the upper face of the Potsdam sandstone is brought 
considerably above the flood plane, and a profile section across the valley at Stephens- 
ville would show a very unequal elevation in the Lower Magnesian strata. 

Still further to the westward, within about two miles of New London, two conspicu- 
ous mounds, known as North and South Musquito Hill, rise about 200 feet above the R. 
R. grade at the depot. Their main mass is sandstone, but they are crowned with calca- 
reous strata. On the western brow of the south hill the uppermost layers exposed are 
thin, banded, arenaceous and odlitic, and are succeeded below by two feet of shelly, rot- 
ten, mottled layers, underlaid by sixteen inches of thin-bedded, flag-like rock, under 
which again lies a foot of hard, broken, chippy rock, which in turn rests upon quartzose 
sandstone beds of 6 inches to 24 inches in thickness. The actual exposure of the sand- 
stone is confined to a few feet, but the precipitous slope indicates its presence in conside- 


LOWER MAGNESIAN LIMESTONE. 981 


rable thickness. On the south face an exposure exhibits the same section, with some- 
thing of the usual tendency to variableness. 

On the north hill, near the crest, a quarry has been opened in straw colored, calciferous 
strata, whose bedding, as exposed, ranges from 2 inches to 12 inches in thickness. Cer- 
tain layers are somewhat greenish, and green spots abound in others. The slope below 
affords occasional glimpses of gray and green sandstones. 

It may be stated incidentally, as an interesting fact, that a loose block of Trenton lime- 
stone was found on the summit of this hill. 

The character of the magnesian limestone reposing on the summits of these hills dif- 
fers somewhat, it will be observed, from that of the lower beds of the Lower Magnesian 
limestone on the opposite side of the Wolf river, and may not belong to precisely the 
same horizon, but it is evident that it cannot belong to a higher, and if it does not be- 
long to the same geological level, must constitute an intercalated band in the Potsdam 
sandstone. But the elevation of the junction of. the sandstone and limestone on Mus- 
quito Hill was estimated to be 100 feet higher than the junction of the sandstone and 
limestone on the opposite side of the valley. It appears then that for a distance of about 
twenty miles (how much more is not known), the formations on the north side of the 
valley are notubly higher than on the south side. While it is possible that all this 
may be due to a southward dip of no great’ magnitude in itself, but quite unusual in 
these formations in this region, especially in that direction, it seems more consonant 
with all the facts of the case, to suppose that the valley represents the line of a fault 
with a downthrow on the south side. 

It is in this region that the stair-like border of this and the higher formations is most 
conspicuous. From the eastward-bearing ledge just under discussion, the western limit 
ot the formation runs in its irregular zigzag way, almost due north to Lake Shawano, 
where it turns again nearly due east along the south side of the Oconto river. 

Passing by for want of space several ledges that occur in the towns of Black Creek, 
Cicero, Lesser and Hartland, which will have value as the country develops, we find at 
the angle made south of Lake Shawano, the following beds forming the summit of a 
bluff 133 feet high, the lower portion of which is Potsdam sandstone. (Sec. 34, 8. E. qr., 
T. 27, R. 16 E.) 


Earth. 

. Rather thin bedded, shaly arenaceous magnesian limestone, 4 feet. 
. Bluish irregular magnesian limestone, containing geodes of quartz, 3 feet. 
. Compact silicious limestone, 1 foot. : 

Grayish white magnesian limestone, 8 inches. 

Cherty magnesian limestone, 1 foot and 6 inches. 

. Light gray magnesian limestone, 3 feet. 

. Olitic layer, 2 feet. 

. Concealed, 3 feet. 

10. Odlitic layers, 3 feet. 

11. Light colored magnesian limestone, partially exposed. 

12. Slope. concealing sandstone. 


OONAARwre 


At Oconto Falls the following section is shown: 

1. The uppermost portion exposed consists of grayish buff, silicious dolomite, of me- 
dium hardness, somewhat uneven texture, beg in part minutely granular crystalline, 
and in part earthy, containing frequent cavities varying from the size of a pea to that of 
a walnut. These cavities are sometimes partially lined with quartz crystals, but these 
miniature geodes are so much less prevalent than in the layer below, which is studded 
with them, and with clusters of quartz crystals, as to make this a distinguishing feature. 
The bedding is irregular, but as exposed in the face of the gorge, the lay2rs are from one 


282 GEOLOGY OF EASTERN WISCONSIN. 


foot thick downwards. The rock weathers to a granular, sandy surface, much pitted 
from unequal resistance to the elements, and showing lines of deposition, 5.1 feet. 

2. A group of beds very similar to the above, but characterized by a much greater 
abundance of crystalized quartz, lining the numerous small cavities, or forming small 
clusters. There is no distinct line of demarkation between these and the above layers, 
11.7 feet. 

3. Below the above lics a thick bed of impure conglomeritic dolomite, the component 
fragments having an almost flinty hardness and fracture. It presents the appearance 
of having been formed of fragments of silicious dolomite imbedded in a matrix of dolo- 
mitic sand and mud, which afterwards cemented, and in a measure, coalesced. On 
weathering, the constituents are brought out conspicuously. The more compact trag- 
ments seem to contain a considerable percentage of silica disseminated through them, 
while segregations of quartz, much oftener in the crystalline than the nodular form, are 
very numerous, and, standing out upon the weathered surface, give it a very rough as- 
pect. This layer by its hardness offers great resistance to erosion from the volume of 
water pouring over it, but when undermined by the removal of the softer rock below, 
it falls in huge masses, sometimes 20 feet in maximum diameter, which lie in the chan- 
nel for ages before complete removal. The prevailing color of the rock is dark gray, 
mottled by the-white quartz, and the variously colored fragments of which it is composed. 
The thickness of the bed is varying, that measured as an average being 4.7 feet. 

4. Underlying the above is a very hard, impure dolomite of a dark gray color, mottled 
with lighter hues, and of more uniform texture than that above, but still not homogene- 
ous, while some portions are studded with small geodes and clusters of quartz crystals. 
It is not subdivided into regular beds, but is much fissured vertically. 9.7 feet. 

5. Still lower lies a stratum of less hardness, much finer and more uniform crystalline 
grain, and more distinctly laminated, so as to present a horizontally banded appearance. 
It has a bluish gray cast on the fresh, somewhat conchoidal fracture, distantly stained 
with dark purplish brown iron spots, but weathers to a dirty gray. The quartz segrega- 
tions descend from above into the upper layers of this. 4.7 feet. 

An analysis of this stratum by Mr. G. Bode gave: 


Carbonate: Of: ime s2<e'sas-< ae tece sie oe-0y bbe dd ew nb awe on peborata des 49.414 
Carbonate of magnesia, ....... 0. eee e cece eee e see eceeeescuscece 39.784 
UEC 5 wise. sucee aae xe Ge a. geaiier eo eress BEG Aeiase eealgl rae a ees hear aetuerndeatnininte: 7.638 
AVarainialis 2 ieca sieges te ipl decane d 04 54 2's RAO to mh a hee 1.473 
£G)-416 (680) 2510) 0 area ay 1.691 

100.000 


6. Below this follows a bed of green and purple shale and argillo-arenaceous dolomite, 
having the following composition: 


Carbonditenot lim é).iiusiecdaccuasenmasnvmae dam vane eeaets vee oe Soke ee 29.370 
Carbonate:of magnesia s...s0cicnxccniediies dena vbiee's iw daaoeseuw ves 18.860 
BiliCah a aieticutaek anda Dauscleltees Sites socuens. seusieveaaecs. exam Atcesere bate ee & 37.798 
SATA al seis Betas eras ccsopeuateyaverainuind) angipaonuiet ade vorbteratansen ire ae eee 9.621 
OxXIGE-OF ION as ianea awit Gch acta omar ctrcaeeueminatene vate ee tea ee tee 4.351 

100.000 


This shale very closely resembles that of the Eureka section, and probably belongs tc 
the same horizon. It is to the softness of this shale and the ease with which it is eroded, 
that the falls are due. 2 feet. 


LOWER MAGNESIAN LIMESTONE. 983 


7. A yellowish or grayish dolomite of very rough, irregular, granular crystalline and, 
earthy texture, containing geodes and almost devoid of bedding lines. 6 feet. 

8. At the base of the above, are two thin layers that present a virescent hue, caused 
by small green spherules imbedded in a gray rock. Associated with these are a greater 
or less number of odlitic spherules, some ocherous, and others in which the center is yel- 
low and the exterior green, which suggests that the coloring matter may be a ferrous 
compound of iron which oxidizes to the hydrated ferric form. On the weathered portion 
of the rock these little spherical bodies are wholly or partially dissolved out, giving a harsh, 
minutely pitted surface. Those that are partially dissolved, show a radiating structure 
somewhat resembling some of the Foraminifera, but the rays are not reducible to any 
definite numerical system. Aggiegations of similar problematic forms, not green, but 
usually white, occur in and upon the surface of the layers, disposed precisely as the 
white odlitic masses are in the layers below, some of which show clearly a concretionary 
structure, making it probable that all are so. They deserve more study than it has been 
possible yet to give them. The same layers contain many illy preserved remains of 
what appear to be an undescribed species of Salterella and also an undetermined Gas- 
teropod having a low broad coil. The gray portion of the rock is a mixture of earthy 
and crystalline granular material, rather soft, and has an easy regular fracture. 6 inches. 

9. This fossiliferous layer graduates below into a very peculiar dolomitic and silicious 
rock, in which the concretionary structure attains an unusual development. Alnost the 
whole mass is formed of vanously sized concentric segregations of chert and dolomitic 
material. They are not unfrequently two or three feet in diameter, and resemble coarse, 
gigantic Stromatopora. 2.2 feet. 

10. This rests upon a dark gray dolomite, similar to that immediately above the con- 
cretionary layer, but contains aggregated masses of white odlite, and is itself somewhat 
odlitic from the presence of yellowish and dark gray spherules. The white ones are of 
large size, and upon fracture and abrasion show their con:entre structure. They are 
aggregated so as to form flat or nodular masses similar to those usually assemed by chert 
in this and the higher Silurian formations. 16 inches. 

11. Closely associated with this below is a layer of a pistachio-green cast formed by 
abundant green spots, with which are mingled a less number of yeliow, orange and red- 
dish ones, the rock mass being gray. Aside from the colored spherules, it is slightly 
odlitic and rather soft, possessing a regular easy fracture. The Salterella occurs here 
also. 3 inches. 

12. The base of the exposure is formed by a dark gray, very impure, and for the most 
part odlitic dolomite. The oGliths are generally darker than the mass of the rock, and 
the larger ones are seldom perfectly spherical, but incline to the forms usually assumed 
by chert nodules. Ocherous spherules occur, and occasionally red hematite ones. In 
some layers, quartzose sand is abundant, forming seams or lenticular masses. Geodes, 
both of quartz and calcite occur. The bedding is very irregular. 5 fe +t. 

Total exposure, 53.2 feet. 

The falls have a vertical descent of 22 feet, with a fall of 10 feet on the rapids above, 
and a greater amount below. 

A few miles north of Stiles, on Jones creek, a thinner band of shale, very similar to 
that described above, gives rise to a diminutive imitation of Oconto Falls, though the 
layers are not specifically identifiable with those of the preceding section. The dip is 
undulating, so that though shown for some distance along the stream, but a small verti- 
cal thickness is exhibited. 

The upper portion of the formation is displayed at several points between Angelica 
and the Oconto river; at Ordway’s ledge and vicinity, about five miles north of Stiles; 
and on the south side ot the main Peshtigo river, from above the mouth of the Little 
river to near the bend above Potato rapids. At these several points the uneven nature 


284 GROLOGY OF EASTERN WISCONSIN. 


of the superior face of the formation is shown to be still a prominent fact. The last 
mentioned point is 120 miles from that at which this feature was first. described, show- 
ing that this is not a local or exceptional character, but one that attaches to the forma- 
tion throughout this portion of the state, and to some extent, at least, beyond. 

‘As the formation passes across the Menomonee river into Michigan, it affords us & 
parting glimpse at the Grand Rapids. The section is closely similar to that at Oconto 
Falls, and will not be here repeated. A full description is given by Dr. Rominger in his 
report on the Paleozoic Rocks of the Upper Peninsula of Michigan, p. 72. 


Economic Considerations. — Many portions of this formation fur- 
nish stone well suited for heavy masonry, as locks, piers, founda- 
tions, ete. Its heavy beds, somewhat silicious character, and free- 
dom from shaly matter, render it enduring, while it is wrought with- 
out difficulty. Other portions are adapted to ordinary construction, 
and exceptional portions are fitted for cutting. 

The rock is burned at numerous points for guecklime, and when a 
judicious selection is made, which is not always the case, with good 
results. The mass of the formation is not adapted to this purpose, but 
some parts are exceptionally pure dolomites, and properly burned, pro- 
duce a most excellent lime. Selection becomes a matter of much im- 
portance, and as it is equally so with other formations, and other por- 
tions of the state, the volume on the general geology of the state will 
contain specific information and directions that will assist in choosing 
a suitable stone. 

Some of the less pure portions produce a lime that forms a slightly 
hydrauli¢ mortar, suitable for general construction, but whose infe- 
rior whiteness reduces its value for finishing purposes. In some cases,: 
where the rock is burned at a low heat, the hydraulie property be- 
comes sufficiently marked to be very serviceable in many cases where 
common quicklime will not answer, and where the more expensive 
cement is too costly. Iam informed by Hon. Wm. Starr, of Ripon, 
that formerly, lime of this class from the Lower Magnesian limestone 
at that place was used for cisterns with success, and that in removing 
the foundations of a mill that had stood many years exposed to water, 
the mortar made from this lime was found in excellent condition. 

An anulysis of the rock which constitutes a portion of one of the 
mounds previously described, taken from the N. W. 4 of the N. E.4 
of Sec. 20, Ripon, gave the following result: 


Carbonate of Tinie s seins es sates xc aos rgd ean eh Meo anos 4 ck acetates 51.68 
Carbonate of magnesia......... cece eee ees cccnceees seventecenens 40.98 
BeSGUOKIDE OF THOM aints. gastric idisceKle Jeacwie piein vein iecdvratecten ueateanaeh ga siccend 0.60 
GA Vr an LTA coi nia sss Sino atiacdate sey cova Suto ses celdes cova oohig oh casera one pe heeoeateatntanee 3.09 
SUL Gabe cays ose isan weve. wishaphsyla onda iasaiate cenndd aac eee ls te WAN Re oT ate ooete: dues 3.16 
"Wiatet vas isa seawied vw g tame nimnaensewin id suelel cn dulueanneaabecue ss 0.70 


ST. PETERS SANDSTONE, 285 


Insoluble in acids, 6.17 per cent., or nearly the entire amount of 
silica and alumina. 

Messrs. Blish & Barlow manufacture a hydraulic lime from rock 
belonging to this formation, found in the N. W. $ of Sec. 26, town of 
Poygan, Winnebago county. 

The following analysis by Prof. W. W. Daniells, shows it to be an 
impure dolomite: 


CarbonaterOf Lime eis cits. gcisidciingeodsamgeleaeecciesaieaen even hess 49.747 
Carbonatesof magnesia... noccines ubaweteabeaayeddgardeee¥ewe beeaa 88.189 
‘Jrisolabble: sai Beil s.aiste sis crciajahie s Sisars itunes nce sinc nud actsan tase’ uwheaeela dienadyestes 9.442 
Sesquioxide of iron and alumina.... 2.00... ccc c eee ccc ee en ee eeeee 1.587 
Water dass cadknteuer commana Gack dbo san nna peg tumonmknatatne 1.190 

100.155 


The insoluble residue consisted of silica, 5.808, and alumina, 3.639. 
The manufactured product is used in the vicinity, and in the neigh- 
boring cities. 

Some of the argillo-arenaceous dolomites, associated with the shale 
belt of this formation, have a composition approaching very near that 
of some of the well known cement rocks of the country, as will be 
seen by reference to the analysis of Layer 6, at Oconto Falls, previ- 
ously given, which was made with this fact in view, and which de- 
serves consideration, though the stratum at that point is unfavorably 
situated. 


ST. PETERS SANDSTONE. 


Upon the billowy surface of the Lower Magnesian limestone, filling 
up its troughs, and in most cases surmounting the crests of its prom- 
inences, lies the St. Peters sandstone. This formation has usually 
been described as a very uniform deposit of purely quartzose, inco- 
herent, pebbleless, non-fossiliferous sandstone. All these characteris- 
tics fail in eastern Wisconsin. 

Owing to the unequal surface of the Lower Magnesian limestone pre- 
viously described, its thickness, instead of being remarkably uniform, 
is precisely the opposite. It is known to vary within the district un- 
der description from two hundred and twelve feet down to a single 
layer of sand grains. It ranges from zero to one hundred feet or 
more — within a quarter of a mile, in one case, at least, and changes 
in a similar rapid and remarkable manner at many other points. In 
the instances of its entire disappearance, its thickness is not sufficient 
to overtop the prominences of the lower formation, and the Trenton 
limestone above rests directly upon the Lower Magnesian limestone, 


286 GEOLOGY OF EASTERN WISCONSIN. 


while in the immediate vicinity, observed depths of sandstone of fifty- 
four feet, eighty-two feet, and one hundred feet have been noted. 
This irregularity appears to be greatest from Dodge county north- 
wards. In thesouthern part of the district, and, so far as the Artesian 
wells enable us to judge, in the lake shore region, a greater degree of 
uniformity prevails. In other words, the unevenness of the Lower 
Magnesian surface seems to have been greatest near its margin, or 
near the shore line of the ocean at the time of its deposit; and as it 
recedes to the eastward and southward, it becomes more uniform. 
Setting aside, for the moment, a large number of exceptional cases, 
arising chiefly from the foregoing peculiarities, the rock may be de- 
scribed essentially as it is found to be elsewhere, being composed of 
well rounded, rather uniform, transparent, incoherent grains of quartz, 
Fra. 35. forming a very friable rock. 
Calcareous and argillaceous 
mm matter are almost entirely ab- 
» Ny sent. White, yellow and gray 
are the most prevalent colors, 
but red, brown, pink and 
green are not uncommon. 
Sometimes the rock is beauti- 
fully variegated and in other 


a _ 
iy 


AN 
\\ sya 
NTT i WW, 
a" 


N 
N\ me 
Sean \\\\ AN 
r — ‘ io 
| Dia 


, 
ut 


cw" 


94 
"wntuanongatS 
ain 


aun 
A ae 


SuoWING CoLoRATION oF St. Parnes Sanpsronz ar C28CS it is banded in a dis. 
ate jointed and irregular way, 
remaining portion o win, ined enaeckea with pink, PTOUCIDg a very interesting 
and unique effect. This is 
imperfectly illustrated in the accompanying figures. In the upper 
part of the formation, irregular concretions of iron ore oceur, which, 
on weathering, present a dark brown, glazed surface, which leads to 
the popular impression that they are of volcanic or meteoric origin. 
In structure, the St. Peters sandstone is finely laminated, fre- 
quently in oblique and cross lines, and shows at some points fine ex- 
amples of ebb and flow structure. The bedding is usually obscure. 
Vertical, oblique and irregular fissures frequently traverse the forma- 
tion, cutting it into huge, irregular masses. 

The exceptions to these general characteristics arise chiefly from 
the relation of this sandstone to the irregularities of the underlying 
formation. Where it adjoins the sloping sides of the limestone 
mounds, it has derived from them ingredients not possessed clse- 
where. More or less of calcareous matter would necessarily become 
mingled with the sand during its deposit. The amount observed is 
not so great as might be expected, and sandstone within a few fect of 


ST. PETERS SANDSTONE. 287 


limestone dipping under it at an angle of 25°, and rising thirty feet 
above it, has been observed to be almost perfectly free from calea- 

Fre. 36. reous matter. It is to be re- 
= marked, however, that the 
arching form of these lime- 
stone mounds, and the con- 
= : centric nature of the external 
. = : layers are most admirably 


wy: g=5d'«‘—QdbpQ—pn4 6 == adapted tu resist erosion, and 
Suowine TnE CotoraTion or St. Perens Sanpstone that by the nearness of these 


AT RIPON. 
domes to each other, they 
would afford mutual protection from violent wave action. Conglom- 
eritic and brecciated rock, formed by fragments of the limestone im- 
bedded in the sandstone, have been observed at several points, but 
only in very close relation to the limestone. 

A much more prevalent modification, especially to the northward, 
consists of thin seams of white argillaceous material interlaminated 
with the sand and, to some extent, diffused through it, giving it a 
schistose character. It then possesses considerable coherence, and is 
found in large tirm masses on the slope below the ledges of Trenton 
limestone. At some points, ferruginous matter mingles with the cal- 
careous and argillaceous ingredients, forming a variegated rock not 
unlike the red and purple shales of the Mendota beds. 

In addition to the modifications arising from the Lower Magnesian 
limestone, the Archean rocks contribute others, which have perhaps 
been sufficiently described in connection with the quartzites of Port- 
land and Waterloo. 

At several points in Rock county, the passage of the St. Peters to 
the formation above is attended by an alternation of sandstone and 
calcareous rock. The sandstone just below the calcareous bed is 
marked with fucoidal impressions and the base of the calcareous layer 
contains abundant Scolithus tubes. The calcareous bed is of a green- 
ish gray cast containing a large percentage of insoluble, argillo-arena- 
ceous material, in addition to the evident quartzose grains that are 
more or less freely scattered through portions of it. This has not 
been observed to attain a thickness of more than four or five feet. 
The upper portion is usually shaly and appears at some points to 
have been eroded before the deposition of the stratum of sandstone 
above. This latter is thin and mixed with argillaceous material on 
which sometimes supervenes a thin seam of carbonaceous matter fol- 
lowed by the fossiliferous Trenton limestone. At the most northern 
point at which the junction was seen, the sand mingles freely with 


288 GEOLOGY OF EASTERN WISCONSIN. 


the calcareous layers of the Trenton, for several feet above their base. 
At most other points the usual abrupt transition was observed. 

Organic Remains. Previous to the present year (1876) there has 
been no published announcement of the existence of fossils in this 
formation. In the Fourth Annual Report of the Geological Survey 
of Minnesota, Prof. N. H. Winchell describes a Lingulepis, found 
near Fountain in that state, in the upper beds of the formation. 

In my unpublished report of 1873, Scolithus borings were de- 
scribed as occurring in rock in the town of Waterloo, referred to the 
St. Peters sandstone. In 1874, this was confirmed by finding well 
preserved tubes of the same in the town of Beloit, in strata belonging 
to the upper part of the formation. Fucoidal impressions were also 
found at the same locality. In 1875, Scolithus tubes were seen in 
sandstone referred doubtfully to the base of the formation. 

In a synopsis of my report for these years, three hundred copies of 
which were printed and distributed at private expense, in the early 
part of January, 1876, the existence of organic remains in this for- 
mation was announced. This form of announcement will not probs- 
bly be regarded as sufficient to justify a claim to priority, in this in- 
teresting discovery. The organic remains so far have been found ex- 
clusively where the sandstone was compacted by some cementing ma- 
terial, which justifies the belief that the absence of fossils throughout 
the greater part of the formation is due to want of preservation and 
not to original absence of life in the depositing sea. 

Method of formation. The existenve of the remains of marine 
life demonstrates that the fossiliferous portions at least are submarine 
deposits, while the well rounded character of the grains, the ebb and 
flow structure, the shaly laminations, the conglomeritic portions and 
its relations to the adjacent formations leave no doubt that it belongs 
to the common class of oceanic sand deposits. 


Extent and Local Descriptions. The St. Peters sandstone enters this district from 
Illinois and from the Lead Region at the southwestern corner of Rock county. Owing 
to the ease with which the sandstone is eroded, it usually occupies only a narrow belt 
close under the protecting ledges of the overlying Trenton limestone, and appears on 
the map as a narrow border to that formation. In some places, as in Rock county, 
where it is represented as occupying more ample areas, it is quite probable that if the 
drift could be removed the sandstone would be found absent at some points. The pre- 
glacial rivers undoubtedly cut entirely through it, but their position cannot now be ac- 
curately mapped. 

In Rock county it may be readily identified, since it seldom shows itself except under 
a protecting shelf or crown of Trenton limestone, whose characteristic fossils are easily 
recognized, and by the simpler fact, that it is the only sandstone exposed in the county. 
Its upper portion is amply displayed in the western portion of the county, where the 
Grift is light, but presents so great similarity that it will be unnecessary to enter into 


ST. PETERS SANDSTONE. 289 


local details. A feature occurs in the north part of the township of Magnolia, of this 
c unty, deserving notice. A small stream, known as Allen’s creek, flows westward 
along the line separating sections 4, 5, and 6, on the north, from sections 7, 8 and 9, on the 
south. On each side there is a range of bluffs capped with Trenton limestone and under- 
laid with St. Peters sandstone. The junction of the two formations on the south side 
is, by aneroid measurement, 155 feet above the stream, and on the opposite side, in sec- 
tion 6, 82 feet, showing a difference of 123 feet. This superior elevation of the south 
bluff is maintained as-far to the east as the two can be compared. In section 7, about 
midway between the two bluffs, there is a very sharp east and west ridge of hard sand- 
stone, intersected in every direction by a network of silicious seams that stand out prom- 
inently on the weathered surface, as though the rock had been extensively fractured and 
subsequently reunited by silicious cement. This ridge rises 50 feet above the junction 
of St. Peters and Trenton on the north side of the stream. These facts are illustrated 
by the accompanying figure. 


“Era. 37. 


SHOWING THE RELATIONS OF THE ST. PETERS SANDSTONE AND TRENTON LIMESTONE, MAGNOLIA, 


In this quiet region of gentle southeastward dips, these phenomena are unusual, 
though insignicant in general geology. They are equally explainable by supposing a 
flexure of the strata or a fault. 

At the railroad cut near Magnolia station, the transition from the St. Peters sand- 
stone to the Trenton limestone is well shown. The main cut consists of the limestone, 
the lower 3 or 4 feet of which are more or less sandy. Below this lies 8 inches of sandstone 
containing seams and nodules of iron oxide and sulphide, doubtless all originally pyrites. 
This layer of sandstone rests upon 4 feet 4 inches of impure sandy conglomeritic lime- 
rock, full of Scolithus(?) tubes. Below this, continuing to the base of the exposure, is 
an incoherent sandstone, mottled and banded with yellow, orange and green colors, and 
exhibiting oblique and horizontal lamination. A similar transition may be seen at nu- 
merous other points in Rock county. From this county onward, the general course of 
the formation is due north for about sixty miles, and then east of north for more than 
one hundred miles. Its irregularity of thickness in tracing it nortuward first becomes 
pronounced in the western part of Dodge county, and it is first known to be entirely 
cut off by the contact of the limestones, below and above, in the southern part of Green 
Lake county, notwithstanding which, and frequent subsequent interruptions, it main- 
tains an existence for more than 120 miles to the northward. It was last observed within 
about four miles of the Michigan line, where it had a thickness of 20 feet. Beyond that 
point it is concealed by the drift. 

The formation is not recognized at all in the recent geological report of Michigan, 
although the foregoing facts offer a strong presumption that it exists there. Under the 
impression that has formerly prevailed concerning the uniformity of this deposit, the 
finding of the Trenton limestone on the Escanaba river, resting directly upon the Lower 
Magnesian, would justify the inference that the St. Peters sandstone was essentially 
wanting in the Upper Peninsula of Michigan, but with the light now possessed, the fact 
of contact at that point has little significance in relation to the question of the presence 
or absence of the formation in question. 

Wis. Sur. —19 


290 GEOLOGY OF EASTERN WISCONSIN. 


Economic Considerations. The greatest prospective value of 
this formation is doubtless its water-bearing capacity, it being, as has 
already been shown, the great source of Artesian fountains in this 
portion of the state. In view of this fact, the foregoing developments 
in respect to its nature possess emineut practical importance. 

For some years geologists have habitually recommended the sand 
of this formation for the manufacture of glass. Its value for that 
purpose is now being put to the practical test. A factory has recently 
been established at Omro for that purpose. Thesand is derived from 
near Waukau. A six pot furnace has been erected having a capacity 
per month of 800 boxes of 100 feet each. At present the manufacture 
is confined to window glass and shades. The results thus far attained 
are reported as highly satisfactory. 

In the town of Waterloo the sandstone has sufficient compactness 
to serve as @ building stone, but usually it is too soft. This latter fact, 
however, permiits its extensive use as sand for mortar, and similar 
purposes. At most localities it can be dug with pick and shovel, the 
mere handling being sufficient to reduce it to sand. On account of 
its cleanness and sharpness, it is much superior to most drift sand. 


TRENTON GROUP. 


Upon the St. Peters sandstone there lies an extensive series of lime- 
stones and shales, which represent the Trenton period. 1t consists of 
three main divisions, which are recognized in geological history as 
epochs. The lowest member is known as the Trenton limestone, the 
next in order as the Galena limestone, and the uppermost as the Cin- 
cinnati shalesand limestone. These are firmly linked together by fos- 
sils common to the three horizons, and in the northeastern part of the 
state it is exceedingly difficult to discern any satisfactory line of de- 
markation between them. In the southern portion, however, they are 
well distinguished, and will receive consideration in the order named. 


TRENTON LIMESTONE. 


Subdivisions. The Trenton limestone proper, as it is developed 
in the southern portion of the district under consideration, consists of 
four subdivisions sufficiently well characterized to be valuable aids in 
the study and discussion of the formation, and in the practical appli- 
cation of the results of the survey. 

Adhering as closely as the nature of the case will admit, to the 
terms already in use, these will be distinguished as follows: 


TRENTON LIMESTONE. 291 


I. Uprrr Buus Bens, thickness, 15 feet. 


=r} II. Urerer Burr Bens, thickness, 55 feet. 


III. Lower Buvz Bens, thickness, 25 feet. 


IV. Lower Burr Bens, thickness, 25 feet. 


It has been customary to divide the Trenton limestone of this state 
into the “ Buff limestone” and the “ Blue limestone,” and in the Lead 
region the latter and some higher beds form the “ Glass rock,” “ Brown 
rock,” and “ Green rock.’’ These latter terms are based upon litho- 
logical characters that do not prevail in southeastern Wisconsin, and 
hence the use of these terms would be undesirable even if their appli- 
cation within the Lead region was sufficiently well defined to justify 
their extension to other localities. 

To continue the unmodified use of the terms Blue and Buff lime- 
stone, and to rest with this twofold subdivision, is open to serious 
objection, as experience has shown. 

In the first place, the color distinction made between the two is 
not applicable without qualification, since more than half of the up- 
per portion usually designated Blue limestone is quite as persistently 
buff as the lower division. The unleached interior of the thicker 
beds, in all the subdivisions, is blue, and that was doubtless the origi- 
nal color of the whole furmation, but the two divisions designated in 
this report as Buff are habitually leached to much greater depths 
than the remaining two, and are less associated with bluish green 
shales, which give to the latter a bluish or greenish aspect. Applied 
as now suggested, the terms blue and buff become reasonably appro- 
priate and very convenient. 

In the second place, the chemical distinction, viz.: that the lower 
division is a dolomite, and the remainder a limestone, does not hold 
good. An analysis of chippings from unweathered layers, represent- 
ing the whole thickness of what has heretofore been called Buff lime- 


292 GEOLOGY OF EASTERN WISCONSIN. 


stone, and is now called the Lower Buff beds, exclusive of the argil- 
laceous layers at the base, shows 36.41 per cent. of carbonate of 
magnesia. A similar analysis of the Lower Blue beds shows 38.39 
per cent. of carbonate of magnesia. A like analysis of the lower 
13 feet of the Upper Buff beds gives 43.30 per cent. of magnesic car- 
bonate, and one of a higher stratum, 34.86 per cent. These analyses 
were all made from rocks whose exposure to leaching and weathering 
was as nearly as possible equal, and from adjacent, where not identi- 
cal, localities, all being from the vicinity of Beloit. 

From these it appears that the quantity of magnesia varies but 
slightly, and. that the entire amount is large, so that the term dolo- 
mite is applicable here as well as to the calcareous formations above 
and below, while the Blue limestone of the Lead region is a true lime- 
stone, containing but little magnesia. 

In the third place, the paleontological distinction heretofore 
drawn does not hold good. The Buff limestone has been regarded as 
characterized by great numbers of Gasteropoda, Cephalopoda and 
Lamellibranchiata, especially by species referable to Zellinomya, 
Cypricardites and allied genera. But this is at least equally true of 
the Upper Buff beds of this report. 

The following species catalogued in the report of 1862, as belonging 
to the Lower Buff limestone, have been found in the Upper Buff beds 
of this report: 

Cypricardites Niota, C. rotundatus, C. ventricosus, Modiolopsis 
superba, Tellinomya nasuta, T. ventricosa, Murchisonia helicteres, 
Pleurotomaria (Raphistoma) Nasoni, P. subconica, Trochonema 
umbilicatum, Raphistoma lenticularis, Cyrtoceras annulatum, C. 
eugium, Oncoceras Lycus, O. Pandion and O. plebium. 

Only one of the list given in the report of 1862 as from the Buff 
is known to me as occurring exclusively in the Lower Buff, while 
three have been found in the Upper Buff that have not been observed 
in the Lower. The majority are common to the two subdivisions, 
and to this number several allied species have now been added. 
Columnaria alveolata, also regarded as peculiar to the Lower Buff, is 
found in the upper beds. 

The strata at Rockton, which belong to the Upper Buff beds, are 
referred to the Buff limestone of previous authors,! and a similar par- 
donable confusion of the two members has undoubtedly been ex- 
perienced by other writers on the geology of this region. 

These facts are dwelt upon to this extent to demonstrate the ne- 
cessity for the introduction of a new classification, and of new terms 


15ee pp. 89, 90, Vol. V, Geol. Rep. of Ill. 


TRENTON LIMESTONE. 293 


in lieu of those that have already found a place in the literature of 
western geology. 

It is not presumed that the distinctions here made have any wide 
geographical application, and hence the terms in common use have. 
only received such qualification as the geology of this region demands. 

The term deds has been substituted for limestone, since, in the 
opinion of the writer, these divisions do not rise to the dignity of 
what are technically known among geologists as epochs, to which 
grade the more significant term should be confined, unless there are 
special lithological reasons for its use otherwise. While it is very. 
much in the interests of science, and its practical application, to sub- 
divide the several formations as far as the facts will permit, and thus 
give to our discriminations and descriptions as much of exactness as 
possible, much confasion is introduced into the general literature of 
the science, if each of these minor members is clothed with a formal 
title. 

1. The Lower Buff Beds. It has already been observed in connec- 
tion with the St. Peters sandstone, that a slight alternation of sand- 
stone and calcareous layers occurs in the transition to the Trenton 
limestone, there being above the main body of sandstone a calcar- 
eous layer of about four feet thickness, overlaid by a bed of sand- 
stone two feet or less in thickness. Above this there follow the 
Lower Buff beds. Their usual thickness is from eighteen to twenty- 
five feet. At some points the formation seems to be made up of 
three main strata, the lower one, more or less shaly toward the bot- 
tom, of about four feet thickness, the middle one seven feet, and the 
upper, twelve. These are less distinctly subdivided into beds from 
two feet in thickness downwards. When these distinctions are not 
observable, the layers are of a similar heavy bedded character, except 
when affected by the action of the elements. The texture is some- 
what irregular, arising from an uneven association of earthy and 
erystalline material. The general aspect is earthy, but crystalline. 
particles compose the greater part of the mass. The color, as seen in 
natural ledges and superficial quarries, is a light yellowish buff or 
gray. The interior of thicker and less exposed layers frequently has 
a bluish cast. 

The rock is composed of carbonate of lime and magnesia, a con- 
siderable percentage of silicious and alnminous material, and an io- 
significant ingredient of iron and the more common salts. Crystals of 
calcite and occasionally those of pyrite occur in cavities. 

The fossils of this division are abundant, although less so than in 
the upper divisions, especially the blue beds. 


294 GEOLOGY OF EASTERN WISCONSIN. 


The following is a partial list of the species that lived during the 
deposition of these strata: 

Buthotrephis succulens, Streptelasma (Petraia) corniculum,a new 
species of Stictopora and one of Trematopora, a Lingula, resembling 
L. obtusa, Orthis disparalis, O. perveta, O. subquadrata, O. tricenaria, 
Streptorhynchus deflectum, S. filitextum, S. deltoideum, S. planum- 
bonum, Strophomena alternata, S. camerata, S. camura, S. imeras- 
sata, a new species of Rhynchonella, Tellinomye nasuta, Cypricar- 
dites Canadensis, C. rectirostris, C. rotundatus, CO. subtruncatus, 
C. ventricosus, C., n. sp., Modiolopsis superba, Helicotoma planu- 
lata, Raphistoma lenticularis, R. Nasoni, Pleurotomaria subconiea, 
Trochonema ambiguum, T. umbilicutum, Murchisonia tricarinata, 
MM. bicincta, Subulites elongatus, Bucania bidorsata, Bellerophon 
bilobatus, Pterotheca attenuata, Orthoceras anellum, O. junceum, O. 
vertebrale, O., n. sp. 0. Beloitense, Oncoceras Pandion, O. plebeium, 
Gyroceras convolvans, Lituites occidentalis, Illenus taurus, Cer- 
aurus pleurexanthemus and Leperditia fabulites. 

It is impossible in the present state of our knowledge to name any 
single fossil of common occurrence that is peculiarly characteristic 
of this geological horizon The abundance of Lamellibranchiates, 
Gasteropods and Cephalopods, and the fewness of the Corals and Bry- 
ozoans sufficiently distinguish it from both of the Blue beds above, 
but not from the Upper Buff beds to which this division bears astrong 
resemblance paleontologically as well as lithologically. At some 
points the Lower Buff beds develop something of a shaly character at 
the base, and are highly fossiliferous, in which cases the facies of the 
fauna strongly resembles that of the Blue beds, which are likewise 
shaly. It appears from all the facts that there was an alternation of 
conditions in the depositing Trenton seas, and that when the condi- 
tions were such as to favor the formation of limestone simply, the life 
above characterized predominated, and that whenever the conditions 
changed so as to cause a deposit of shale interleaved with layers of 
limestone, the brachiopodous and coralline fauna prevailed. These 
subdivisions then signify rather physical mutations of a more or less 
local nature, than wide spread changes in the life-character of the period. 

2. The Lower Blue Beds. The upper surface of the preceding di- 
vision is at most points well defined, and upon its thick beds rest an 
alternating series of thin, impure limestone layers and thinner shaly 
leaves. These are usually grouped into more massive beds, and where 
removed from the action of surface agencies, the shaly portions often 
possess sufficient coherence to bind the limestone layers into beds of 
respectable dimensions. 


TRENTON LIMESTONE. 295 


The average thickness may be put down at from twenty to twenty- 
five feet. The limestone is varying in texture. Usually it is a mix- 
ture of earthy material and minute crystals, but sometimes has a 
compact crystalline structure, and occasionally a coarse granular one. 
Some layers are little else than a mass of fossils. The color is bluish, 
or grayish, weathering to light gray or buff. 

The shale is a bluish green, and aside from mingling with the lime- 
stone somewhat, it forms seams and partings between the layers. 
These are seldom over two inches thick in the southern part of our 
province, but attain more considerable dimensions at the north. A 
notable amount of carbonaceous material is sometimes associated with 
this shale. It is usually very highly fossiliferous. 

In chemical composition the limestone layers do not essentially 
differ, so far as tested, from the Buff already described, being an im- 
pure magnesian limestone. The analysis previously referred to in- 
cluded only the limestone layers, the shaly partings being excluded. 
Including these, probably one-third of the whole mass would be found 
to be silicious and aluminous material. 

Besides the bluish green cast that the shale gives to the mass, it has 
served to protect the limestone from the leaching action of percolat- 
ing water, so that it also oftener retains its original bluish hue than 
the beds below and above, and renders the name applied to it not in- 
appropriate. It is characterized by a much greater abundance of fos- 
sils than the beds below. These differ from those below in the 
much greater abundance of Corals, Bryozoans and small Brachio- 
pods, especially the Orthide. Murchisonia gracilis appears in 
great abundance near the base of this division. It is not found in 
my somewhat extensive collections from the Lower Buff, which indi- 
cates its rarity, though perhaps not absence, from that horizon. Bed- 
lerophon bilobatus is very abundant, though not confined to this 
horizon. This division comprehends, in greater or less numbers, a 
large proportion of all the species found in the Trenton limestone of 
this region. 

3. The Upper Buff Beds. This is the thickest and most important 
subdivision of the group in the Rock river valley, reaching a vertical 
dimension of fifty-five feet. It is less uniform in its several parts 
than the two preceding, and is less easily described in general terms, 
and the reader will perhaps find the detailed description of the see- 
tion at Beloit, given subsequently, under the head of local deserip- 
tions, more satisfactory than the general statements here made. The 
most prevalent kind of rock is a rather heavy bedded limestone, ob- 
scurely banded and mottled with light gray and buff, giving the 


296 GEOLOGY OF EASTERN WISCONSIN. 


whole a light, yellowish buff aspect. The gray portions are more 
compact and crystalline than the buff, which are porous and earthy 
although beautifully bespangled with glistening crystalline facets. 
These characters apply more particularly to the lowest and uppermost 
members; the latter is distinguished by the presence of nodules of 
chert. A portion of the intermediate layers, while retaining some- 
thing of the nature above described, becomes much more irregular in 
texture, and possesses a very rough fracture, which gives the ledges 
in the quarry a brecciated appearance that is increased by the pres- 
ence of cavities. 

Another portion is more homogeneous in structure than either of 
the preceding kinds, and has a very noticeable conchoidal fracture, 
resembling in this respect the glass rock of the Lead region, from 
which, however, it differs in having a less compact and more earthy 
texture, caused by the presence of from 12 to 15 per cent. of alumin- 
ous and silicious material. It is lined with obscure reddish stains, 
probably of fucoidal origin. This constitutes two bands, two to four 
feet thick, lying near the center of the division and separated seven 
or eight feet from each other. They thus constitute reliable land- 
marks in correlating partial exposures at distant points, and, if intel- 
ligently used, will prove a serviceable guide to the quarryman. 

The life at this stage was, as has been remarked, very similar to 
that at the time of the deposit of the Lower Buff beds, but was more 
prolific and varied. Nearly sixty species are known to occur in these 
beds, and it is presumable that the actual number is much larger. 

Of these, between fifteen and twenty have not been found in the 
Lower Buff beds, but until more thorough search has been made it 
would not be wise to regard them as diagnostic. The occurrence of 
Halysites at this horizon is especially worthy of remark, as being the 
lowest point at which it has yet been authentically reported in the 
western series. 

4. The Upper Blue Beds. These are so similar in general charac- 
ter to the Lower Blue Beds. as not to need extended description. 
They differ from them chiefly in those cases where they take on a 
coarse granular character, approaching that of the Galena limestone 
above, to which they constitute the transition. The degree in which 
they are thus modified varies with the locality. At several points 
there are only four or five such transitional beds, and at other points 
the whole division shows something of this character. 

An abundance of Brachiopods, Bryozoans and Chetetoid corals 
form the leading feature of the life of this period. Its general aspect 
is more manifestly similar to that of the Cincinnati shales above the 


TRENTON LIMESTONE. 297 


Galena than that of the beds below. ZLeptana sericea is a very abun- 
dant fossil, which has not been observed to be true below. 


Local Descriptions. In the vicinity of Beloit are a number of natural and arti- 
ficial exposures that are so fortunately situated at different elevations as to exhibit the 


Fie. 39. 


entire thickness of the formation, and yet, an equally fortunate cir- 
cumstance for the students of geology of that locality, their correct 
correlation is attended with something of difficulty, and is only ac- 
complished by careful and industrious study. By combining the 
partial series shown at the various points, the following general 
section for that vicinity may be constructed: 


Upper Buus Bens. 


A. <A greenish blue impure limestone, chiefly earthy and sub- 
crystalline, but in part granular, beds thin and separated with 
shale, very fossiliferous. Estimated thickness, fifteen feet. 


Urrer Burr Bens. 


B. J. In general a fine grained, impure limestone, of earthy or 
subcrystalline texture, the former a light buft,the latter gray, com- 
bined so as to give an obscure banded and mottled appearance 
quite peculiar. Nodules of chert are present, which distinguish 
it from the rock below. Beds, thick and uniform, fracture, easy and 
regular in the upper two-thirds, while that of the lower part is 
very rough and angular, as though from a brecciated structure; 
more impure than the upper portions. A shaly layer, 7 feet from 
the base, contains carbonaceous seams with Graptolite markings. 
Twenty-two feet. 

II. Layer of homogeneous structure, conchoidal fracture, and 
earthy texture, but sparkling with minute crystals; med and spot- 
ted with obscure reddish fucoidal stains. Two and one half feet. 

III. Combines to some extent the character of the layers above, 
being less homogeneous than the last, and more so than the pro- 
ceding. Some layers, very fossiliterous, the remains being grouped 
more or less in colonies. Horizon of the Halysites. Seven to eight 
feev. 

IV. Similar to II, but the characters more marked. Three to 
four feet. 

V. Similar to I, but not cherty. Texture toward the upper part 
more irregular than below. Nineteen feet. 


Lower Buus Beps. 


C. Thin-bedded impure limestone of varying earthy and crys- 
talline texture, interleaved with shaly partings, the whole having 
a bluish-green or gray color. Very fossiliferous. Twenty- -three 


feet. 
: Lower Burr BeEps. 


D. Thick-bedded, buff limestone, of rather coarse texture, 
somewhat shaly at the base. Fossils not very abundant except in 
the shaly portions, Twenty-three feet. 

Transitional layer of sandstone, 2 feet. 

Transitional layer of impure limestone, 4 feet. 

St. Peters sandstone. 


298 GEOLOGY OF EASTERN WISCONSIN. 


At Clute’s point, near the east line of Sec. 10, town of Beloit, about four miles north of 
the city, the upper portion of the St. Peters sandstone and the lower part of the calcare- 
ous transition bed is shown. About a quarter of a mile southeast of this, in See. 11, N. 
W. qr. of S. W. qr., the transition stratum is better shown, together with the layer of 
sand above and the bottom layers of the Lower Buff beds. About an equal distance 
further south, near the high bluff that overlooks the river, cherty layers, B, I, and a por- 
tion of those above are shown. ‘The latter partake quite decidedly of the characteristics 
of the Galena limestone, and are less shaly than usual. Passing over the high hill to a 
ravine on its southwest flank, the Galena limestone and some of the upper transitional 
layers may be found. Nearly a mile further south, at the large quarry near the C. & 
N. W.R. R., a portion of the St. Peters sandstone, the calcareous transitional layer, the 
interstratified layer of sand, the shaly layers of the Lower Buff limestone, one of which 
is especially crowded with Leperditia fabulites, the heavy Lower Buff beds in full, and the 
Lower Blue beds, may be seen in magnificent vertical exposure. 

A partial analysis of chippings from the entire thickness of the Buff and Blue layers 
at this point, exclusive of the thin ones at the base, shows the following composition: 


Buff. Blue. 

Ensolublerresidués js -saicu vines aces as oie ed es assy ees 5.74 10.29 
Soluble: BiltCaivek Gus date Geeienerwusteres Sadev asd ee canan’ed 1.96 1.75 
Sesquioxide of iron and alumina................eee cee eee 3.27 1.60 
Carbonate of wnapnesidicrscccsesvyeace See bie been ke acne 36.40 38.39 
Carbonate of lime, etc., by estimate.............ceeeeeeee 52.63 47.97 
AL Oba eshir ceipsceucttenth cassian Geiun deed oxoaace saeioaie eaten +. 100.00 100.00 


In a ravine a little south of this the upper part of the Lower Buff and the lower part 
of the Lower Blue beds are shown in a small quarry. Still further south along the rail- 
way, another large quarry exhibits a considerable portion of the Lower Buff and Blue 
beds, and below, near the track, the St. Peter sandstone is slightly exposed. Several 
minor openings along this line of bluffs display limited sections. A mile or more to the 
southeast, at Carpenter's quarry, on the line between sections 26 and 27, the lower por- 
tion of the Upper Buff beds—B. V, IV, III and a portion of II, of the preceding sec- 
tion —are extensively wrought, the lower beds especially being a desirable building- 
stone. The ravine below this quarry has gullicd into the Lower Blue beds, and shows 
their character wherever suljected to the full action of atmosphere, frost, and water. 

A partial analysis of the strata B. V and B. IV, at Carpenter's quarry, shows their 
chemical nature to be as follows: 

Upper Buff. 


B. IV. B.V. 

Insolublerestdié se. 45.ns sda aecsnccset a eescwce eaeauts 12.50 3.42 

HOLDS. SilCa esas cckany Qos Movie ewig ak ees sou sao wes 1.87 1.99 

Sesquioxide of iron and alumina..............eeeceeeeeee 2.23 1.42 

Carbonate of magnesia....... 20. sec e eee e cece eee eeuceece 34.86 43.87 
Carbonate of lime, etc., by estimate ...............e.. eee 48.54 49.30 ° 

TO bal caste sy wera sasciwigta wis winictati sy acalhaa wd lutiocale’os Sedeaoioners 100.00 = 100.00 


A mile and a half farther southwest, Hess’ quarry appears to lie across the layer 
marked B. H, in the section, and to include some of the layers above and below, thu 
latter being especially prolific in fossils heretofore classified as characteristic of the Buff. 
At Hanchett’s quarry, a short distance south of this, the present exposure reaches from 
about three feet below the bed marked B. IV, to about the top of B. II. A little over 


TRENTON LIMESTONE. 299. 


a half mile northwest of this point, at Smith's quarry, the junction of the Upper Blue 
beds and the Galena limestone with a few feet above and below is shown, completing 
the series. This junction may also be seen between Turtleville and Shopiere. 

The quarries at Rockton, Illinois, present a magnificent section of the Upper Butf beds 
from layer B. IV upwards to the lower portion of the Upper Blue beds. 

These statements are given thus specifically that there may be the fullest opportunity 
for verifying and utilizing the statements of this report, and that there may hereby be 
furnished a basis for the more accurate study of the vertical, and, to some extent, hori- 
zontal range of the exceedingly interesting fossils of these beds, which it is hoped will 
be prosecuted by the geologists of the region. A series of collections carried on for years 
under the favorable opportunities afforded by continuous quarrying, in which the exact 
locality and horizon should be carefully noted, could not fail to show valuable results. 

Over one hundred species of fossils are known to occur in these beds, among which the 
following identifications have been made: 


Buthotrephis succulens. Raphistoma Nasoni. 
Steptelasma corniculum. * Trochonema ambiguum. 
Cheetetes lycoperdon. Trochonema umbilicatum. 
Cheetetes discoideus. Trochonema Beloitense, n. sp. 
Stictopora elegantula. Plurotomaria subconica. 
Stictopora, n. sp. Murchisonia bicincta. 
Schizocrinus nodosus. Murchisonia gracilis. 
Ptilodictya recta. Murchisonia helicteres. 
Lingula, sp. und. Murchisonia pagoda. 

Orthis perveta. Morchisonia tricarinata. 
Orthis plicatella. Cyclonema percarinatum. 
Orthis testudinaria. Subuljtes elongatus. 

Orthis pectinella. Clisospira occidentalis, n. sp. 
Orthis tricenaria. Helicotoma planulata. 
Orthis bellarugosa. Maclurea Bigsbyi. 
Strophomena camerata. Metoptoma perovalis, n. sp. 
Strophomena alternata. Bellerophon bilobatus. 
Strophodonta, sp. und. Bellerophon Wisconsinensis, n. sp. 
Streptorhynchus deflectum. Bucania Buelli, n. sp. 
Stzeptorhynchus subtentum. Bucania punctifrons. 
Leptena sericea. Bucania bidorsata. 
Rhynchonella, sp. und. Pterotheca attenuata. 
Ambonychia attenuata. Hyolithes Baconi, n. sp. 
Ambonychia, n. sp. Gyroceras, sp. und. 
Ambonychia lamellosa. Cyrtoceras annulatum. 
Cypricardites Niota. Cyrtoceras corniculum. 
Cypricardites rotundatus. Cyrtoceras eugium. 
Cypricardites ventricosus. Cyrtoceras Neleus. 
Cypricardites, n. sp. Oncoceras abruptum. 
Tellinomya nasuta. Oncoceras Alceus. 
Tellinomya alta. Oncoceras Lycus. 
Tellinomya Iphigenia. Oncoceras Pandion. 
Tellinomya levata. Oncoceras plebeium. 
Tellinomya ventricosa. Oncoceras, sp. undescribed. 
Modiolopsis superba. Oncoceras, sp. undescribed. 
Modiolopsis plana. Orthoceras anellum. 


Raphistoma lenticularis. Orthoceras niulticameratum. 


300 GEOLOGY OF EASTERN WISCONSIN. 


Orthoceras junceum. Worm borings. 

Orthoceras planoconvexum. Jllenus ovatus. 

Orthoceras Beloitense. Asaphus Barrandi. 
Orthoceras 2 sp. undes. Asaphus lowensis. 
Orthoceras vertebrale. Ceraurus pleurexanthemus. 
Endoceras annulatum. Encrinurus sp. undes. 
Endoceras proteiforme, Leperditia fabulites. 


Gonioceras anceps. 


In the vicinity of Janesville are a number of extensive quarries and natural expo- 
sures that display the three lower members of the formation quite extensively. At the 
quarry, a mile and a half west of the city we find, at the base, heavy buff layers, con- 
taining but few fossils, and representing the Lower Buff beds. The complete thickness 
is not shown. On these repose thinner bedded, eminently fossiliferous, blue and gray 
beds attended with shaly layers and seams. These are the Lower Blue beds, in thick- 
ness, 22 feet 9 inches. These support about 13 feet of light buff colored limestone, of 
uneven structure — owing to earthy or soft granular spots and occasional cavities — rather 
irregular fracture, giving an earthy surface with crystalline spangles, and containing 
but few fossils. Beds one foot or less in thickness. These constitute the lower portion 
of the Upper Buff beds. The following species were observed at this point, nearly all 
belonging to the Blue beds: Buthotrephis, Cheetetes lycoperdon, Crinoid stems, Stic- 
topora (two new species), Ptilodictya, Trematopora, Lingula attenuata, Orthis perveta, 
O. tricenaria. O. sp. new (like O. testudinaria), Streptorhynchus deflectum, Strophomena 
camerata, S. incrassata, Rhynchon-aella, n. sp., Ambonychia lamellosa, Tellinomya n 
suta, Cypricardites rotundatus, C. ventricosus, Modiolopsis plana, Helicotoma planulata, 
Raphistoma lenticularis, Trochonema umbilicatum, Murchisonia helicteres, M. tricari- 
nata, Pleurotomaria subconica, Bucania, n. sp., Pterotheca attenuata, Hyolithes Baconi, 
n. sp., Orthoceras junceum, O. vertebrale, O., n. sp., Endoceras, Proteiforme, Cyrtoceras 
Pandion? Gomphoceras? Asaphus Barrandi, Illenus ovatus, Ceraurus pleurexanthe- 
mus, Leperditia fabulites and Beyrichia. 

At the lower railroad bridge at Janesville, the whole of the Lower Buff limestone is 
shown resting upon the St. Peters sandstone, and overlaid by about 80 feet of the higher 
beds, which are here less fossiliferous than usual. A section of this exposure is given in 
the report of 1862. About two miles above the city, Rock river cuts through the lower 
part of the formation and into the St. Peters sandstone, and a ravine coming in on the 
east, through which the road ascends from the river, exposes a large part of the higher 
strata, so that by combining the sections, nearly the whole of the series may be studied. 
Fossils are abundant in the usual layers. 

Farther up the river, above Fulton Center, the lower strata crown the bluffs with 
weather-worn outliers, while nearer the water's edge the St. Peters sandstone discovers 
itself. They become somewhat cavernous at one point, a rare feature in this region. 
The following fossils were collected along the ledges on the west side of the river: 
Chetetes, Streptelasma corniculum, Stictopora, n. sp., Orthis perveta, O. tricenaria, 
Streptorhynchus deflectum, Strophomena camerata? S. incrassata, Rhynchonella, Telli- 
nomya nasuta, Cypricardites Canadensis, C. rectirostris, C. rotundatus, C. ventricosus, 
Modiolopsis superba, Raphistoma lenticularis, Trochonema ambiguum, Pleurotomaria 
subconica, Murchisonia tricarinata, Bucania bidorsata, Pterotheca attenuata, Orthoceras 
junceum, O. vertebrale, Ormoceras, Illenus taurus, Leperditia fabulites. 

The lower beds are also exposed at the outlet of Lake Koshkonong. In the west- 
ern part of Rock county there are numerous outcroppings of this formation, most fre- 
quently of the lower beds; but occasionally also of the higher ones. The railway cut 
near Magnolia station exposes the Lower Buff beds, and furnishes an excellent oppor- 


TRENTON LIMESTONE. 801 


tunity for studying its character and fauna, which is very similar to that already given. 
The uppermost layers of the Trenton, and its junction with the Galena limestone above, 
may be seen satisfactorily in the N. E. Jy of Sec. 31, and in the 8. E. 4 of Sec. 19, 
town of Union, where a new species of Stictopora, and one of Trematopora, Ptilodictya 
recta, Orthis perveta, O. testudinaria, O. tricenaria, Lepteena sericea, and Ceraurus pleu- 
rexanthemus indicate the character of a fauna very abundant in individuals, though not 
especially so in species. At the lower quarry belonging to Mr. Krump near Ft. Atkin- 
son, the upper portion of this formation is again shown, though the layers are some- 
what lower than the above. About two miles below Jefferson, on the west side of Rock 
river, a little stream has cut down to dark mottled, fine grained, rather thick beds that 
are capable of receiving an excellent polish. Their lithological affinities are with the 
upper half of the formation. 

Near Aztalan are several quarries showing the junction of the Lower Buff layers and 
those above. The fossils collected were chiefly Buf species. The surface of the rock is 
beautifully polished and striated by glacial action. 

On the north side of Red Cedar Lake in the town of Oakland, and in the vicinity, on 
the west, the lower beds are displayed, showing a somewhat less firm rock than usual. 
The first mentioned locality affords Schizocrinus, Stictopora, Orthis perveta, O. plica- 
tella? O.tricenaria, Streptorhynchus felitextum, Strophomena incrassata? Zygospira 
modesta? Raphistoma lenticularis, Pleurotomaria, Subulites elongatus and Cyrtolites. 
To which the others add Buthotrephis succulens, Strophomena camerata, Cypricardites 
rotundatus, Orthoceras vertebrale, Ormoceras and Gonioceras anceps. 

The most interesting exposure of the Trenton limestone in the town of Waterloo is 
at the quarry of Mr. David Crump in section 85. The lower four feet are of thick bedded, 
very serviceable rock, above which lies one foot of thin shaly stone, succeeded by six feet 
of somewhat irregular layers of medium thickness, upon which are two feet of even 
bedded stone overlaid by two and a half of thin, greenish, shaly material. The lower 
portion is to be regarded as representing the Lower Buff layers, and the upper ones 
the Lower Blue limestone. The following species were’ collected in a limited time at 
this locality:. Buthotrephis succulens, Graptolite-like bodies; Chetetes, Streptelasma 
corniculum, Orthis tricenaria, Streptorhynchus deflectum, S. planumbonum, Stropho- 
mena incrassata, a new species of Rhynchonella, Tellinomya ventricosa (young) Cyp- 
ricardites rotundotus, and anew species, Raphistoma lentieularis, Pleurotomaria sub- 
conica, Murchisonia bicincta, M. helicteres, Orthoceras annellum, O. vertebrale, and frag- 
ments of Ormoceras and Cyrtoceras. 

The Trenton formation outcrops in the towns of Shields, Portland, Elba, Lowell, Cal- 

amus, Beaver Dam, Westford, Fox Lake and Trenton, in Dodge county; but the ex- 
posures in all cases are slight, and for the most part belong to the base of the formation. 
While they subserve a very useful purpose in supplying their respective regions with 
building material, they add little to our knowledge of the formation, and possess but 
small interest to the geologist or general reader. 
‘ In the townships of Mackford and Green Lake, in the county of Green Lake, more’ 
frequent and extensive exposures, both natural and artificial, occur, particularly in the 
vicinity of the lakes that beautify those towns. According to the general rule already 
observed, they are chiefly the lower beds, and are caused to stand forth by the easy 
degradation of the sandstone below. 

In the vicinity of Ripon the Lower Buff limestone is well displayed. One of the 
noticeable peculiarities in this neighborhocd is the unequal elevation of the base of the 
formation. While resting, so far as observed, conformably upon the St. Peters sand- 
stone, the junction is found at varying altitudes. One of the lowest points is at ‘‘ The 
Falls,” within the city. These falls are caused by the waters of Silver creek pouring 
over the lower ledges of the Trenton limestone and excavating the softer sandstone be- 


302 GEOLOGY OF FASTERN WISCONSIN. 


low. By following up the stream, a strong dip to the north of east may be observed. 
Fossils are not abundant here, and but few species were collected, although the quarry- 
ing and natural exposures afforded ample opportunities. A few rods west of the busi- 
ness center of the city, the lowest layers of the formation are about 40 feet higher than 
at the falls. Along the bluff, in the western part of the city, the same layers are 25 to 
30 feet higher still, from which point they dip to the south until they disappear beneath 
Crystal creek at a lower point than that at which they occur to the east in the southern 
part of the city. To the west of this, toward Green Lake, the base of the formation is 
more nearly horizontal. In section 5 of the township of Ripon, about three miles north- 
west of the city, the junction in question occurs at a lower elevation, if an aneroid meas- 
urement is to be trusted, than at any of the preceding points. 

All these variations may be readily accounted for by supposing a changeable dip of 
a few degrees; but they are nevertheless unusual in this formation. As the floor of the 
formation has its greatest elevation at and in the vicinity of the pomt where it rests 
upon the domes of Lower Magnesian limestone previously described, and has a lower 
elevation as it recedes from this point, it is reasonable to suppose that the phenomena 
may be due to that relationship. 

The following species representing the fauna of the lower beds of the formation weve 
collected in this vicinity, the quarries of Mr. Coombs and Mr. Corlis proving most pro- 
lific: Buthotrephis succulens, B. gracilis, Chetetes, Streptelasma corniculum, Retepora, 
Trematopora, n. sp., Lingula, like L. obtusa, Stictopora, Orthis perveta, O. tricenaria, 0. 
subquadrata, Streptorhynchus deflectum, S. deltoideum, S. filitextum, S. planumbonum, 
Strophomena alternata, S. camura, S. incrassata, S. tenuistriata, Rhynchonella, n. sp., 
Tellinomya nasuta, Cypricardites rotundatus, C. subtruncatus, C. ventricosus, C., 0. Sp. 
Modiolopsis superba, Helicotoma planulata, Raphistoma lenticularis, Trochonema am- 
biguum, T’. wnbilicatum, Pleurotomaria subconica, Murchisonia bicincta, Holopea, Sub- 
uutes elongatus; Orthoceras annellum, O. junceum, O. vertebrale, O. planoconvexum, 
0., sp. new, Cyrtoceras (Oncoceras) plebeium? C. Pandion, C. or Gyroceras (outer cham- 
ber only), Ormoceras, Gyroceras convolvans, Lituites, Illenus taurus, Enerinurus, Lep- 
erditia fabulites, Ceraurus pleurexanthemus. 

North of Ripon, the formation soon becomes doubly covered with drift, being over- 
laid not only by the original glacial deposit of rubbish, but also by the later lacustrine 
clays, and hence it presents itself at the surface even more rarely than before, so that 
our attention is not again demanded by the meager and scattered exposures until we 
reach the vicinity of Neenah and Menasha, where a cluster of interesting quarries 
oceur. Leaving out of consideration those directly south of Neenah and north of Me- 
nasha, which are referred to a higher horizon, we find a belt of quarries beginning with 
Thompson's in Sec. 29, Neenah, and extending north to the county line, which possesses 
the general lithological characters of the Upper Buff beds, which have already been ful- 
ly described. The following list of species, however, collected from this belt, shows 
several forms not observed in that horizon in the southern part of the state, but which 
are common in a higher position and which therefore give special interest to the fauna 
of these localities: Two new species of Chetetes, Streptelasma corniculum, Columnaria, 
a new species of Stictopora, Schizorinus nodosus, Lingula quadrata? Orthis lyna, O. 
plicatella, O. subquadrata, O. testudinaria, O. pectinella, Streptorhynchus deflectum, S. 
filitexctum, Strophomena alternata, S. incrassata, S. camerata, Leptena sericea, Zygo- 
spira recurvirostris, Rhynchonella Anticostensis, Raphistoma lenticularis, Pleuroto- 
maria subconica, anew species of Murchisonia, having a lofty spire, Endoceras pro- 
teiforme, an undetermined Gyroceras and Leperdita alta? were secured in the limited 
time that could be devoted to collection. ‘ 

In the vicinity of Mr. Verbeck’s residence, near the southeast corner of section 18, 
Menasha, are several small quarries that possess interest from their position and char- 


TRENTON LIMESTONE. 803 


acter. At the quarry just east of his honse, the rock consists of thick bedded, light 
greenish blue, or gray limestone containing some argillaceous material distributed 
through the mass in thin leaves, forming a rock quite similar to that which prevails in 
the bed of the Lower Fox river. Between the heavy beds are greenish blue argilla- 
ceous shales containing fossils, the small Brachiopods of the Blue beds predominating. 

Opposite this, on the south, a few feet of rock of a similar nature but more fossilifer- 
ous, are underlaid by a partially exposed bed of dark blue crystalline rock. About forty 
rods west of this is another shallow quarry displaying apparently a lower horizon. The 
mass of the rock here has a rather brittle, compact, crystalline texture of dark, slightly 
bluish gray color, and irregular or sometimes vitreous or conchoidal fracture. In the 
lower strata, there is much chert, distributed in layers of nodules which are white or flint 
colored and fossiliferous. The rock also contains frequent small geodes, the cavities be- 
ing lined with calcite and occasionally pyrite, or rarely by zinc blende. The walls of 
fissures are also sometimes lined with calcite and pyrite. A short distance to the north- 
west of the quarry first mentioned the beds present the more usual characteristics of the 
argillaceous portions of the Blue limestone as seen farther south. The strata at these 
several quarries dip at an angle of about 2° to the southeast. 

Passing on to the north about ten miles we find in the S. E. qr. of section 28 of the 
town of Center, a partially exposed low dome of rock, reminding us forcibly of the 
Lower Magnesian mounds previously described, the more so because that formation lies 
about tavo miles distant. The beds are exposed on the east and south sides, in which 
directions they dip, but it is not certain that the uncovering of the other sides would hear 
out the impression of a mound with quaquaversal dip, given by an approach from the 
east and south. It may be here remarked that the dip of the Trenton in this region is 
greater and more varying than in the southern part of the state, though even here the 
inclination rarely exceeds 7° or 8°. The rock at this point is a bluish gray argillaceous 
limestone, with shaly partings and very fossiliferous, the following species, many of 
them represented by a large number of individuals, being gathered by the writer in a 
half hour: Buthotrephis succulens, Spongoid bodies Astylospongia? a new species of 
Cheetetes, C. discoideus, Streptelasma corniculum, Schizocrinus nodosus, a new species of 
Stictopora, Orthis lynx, 0. subquadrata, O. testudinaria, a new species of Orthis, Strep- 
torhynchus, Strophomena alternata, Leptena sericea, Zygospira recurvirostra, a new 
species of Rhynchonella, Raphistoma lenticularis, an undetermined cast ot Murchisonia, 
containing a fragment of Subulites, resembling S. brevis, Bellerphon bilobatus, Buca- 
nia (fragment), Orthoceras and Illenus taurus. 

In describing the Lower Magnesian limestone in the region just west of the last local- 
ity, its relations to the Trenton were dwelt upon, and in view of that relationship, it may 
be profitable to here record the occurrence of the following species in Secs. 25 and 26, 
town of Ellington, immediately over against the escarpment of Lower Magnesian lime- 
stone: Paleophycus cespitosum, Schizocrinus nodosus, Orthis lynx, Streptorhynchus 
deflectum, Strophomena alternate, S. incrassata and an undetermined species of Khyn- 
chonella. 

By reference to the maps it will be seen that the formation passes north through the 
townships of Freedom, Osborn, Seymour, Maple Grove, Lesser, Angelica, Little Suam- 
ico, Pensaukee, Stiles, Oconto, Peshtigo and Marinette, as those townships are now con- 
stituted. The exposures in these towns are scattered and meager, and represent chiefly 
the lower member of the formation. They possess much local value as a source of 
building material, but in their present undeveloped condition they add but little of 
knowledge or interest to what has already been said, although they indicate that the 
characteristic peculiarities of the formation at the south undergo something of modi- 


fication. 
It is the barrier interposed by this formation, that causes the Peshtigo river to make 


304 GEOLOGY OF EASTERN WISCONSIN. 


a detour to the eastward in range 31, and gives rise to Potato and Place’s Rapids, where 
the river crosses it, the former due apparently to the more resisting Lower Buff beds and 
the latter to the Upper. 

The second series of rapids encountered in ascending the Menomonee river are attrib- 
utable toa similar cause. It is much to be regretted that at this extremity of our dis- 
trict, two hundred miles from the point where our study of the formation began, there is 
not an equally extensive and fortunate exposure of its several members, that compari- 
sons might be made which would exhibit the changes it has undergone in thickness, 
lithological character and organic contents. Instead of this we have only a few feet 
poorly exposed in the banks of the Menomonee river. A portion of the rock at the 
rapids is a deep blue, heavy, crystalline limestone, weathering smooth and breaking into 
rectangular blocks, while other portions are quite irregular in texture, being composed 
of combined earthy, crystalline and shaly material, with partings of the latter material. 
The bedding is thin and the layers for the most part uneven. On the whole, while not 
differing essentially from the general characters of the formation as seen elsewhere, it 
presents an exceptional aspect in harmony with the suggestion already made, that this 
formation in common with the accompanying ones below and above has changed, in a 
subordinate degree, its pecuharities. The following species indicate the character of 
the fauna: A new species of Cruziana, Buthotrephis succulens, undetermined Fucoids, 
Cheetetes lycoperdon, Monticulipora allied to M. frondosa, Crinoidea (Cyathocrinus? ), 
columns of Schizocrinus nodosus, a new species of Stictopora, Ptilodictya recta? Orthis 
testudinaria, V. tricenaria, and an undetermined species, Streptorhynchus filitextum, S. 
planoconverum, Stryphomena incrassata, Rhynchonella, Zygospira recurvirostra, Penta- 
merus hemiplicatus, and Trilobitic remains (Asaphus).? 


Industrial Considerations, This rock is extensively quarried for 
the purposes of common masonry. At the great majority of places 
the quarries are only superficial and the layers thin, and associated 
with much chipstone. As greater depths are reached a better class 
of building stone is usually found, because the rock has been less sub- 
ject to surface action. It is to be observed, however, that with the 
same amount of exposure the layers in the interior of a hill, which ap- 
pear firm and solid, would become split and broken, like those that 
outcrop. The change that is seen in tracing a layer back into the 
hill is brought about by the atmosphere, frost, percolating water, and 
similar agencies, and is not due to the original nature of the rock. 
This fact affords a means of judging of the endurance of the rock, 
and, applied to most of the beds of this formation, shows that their 
power of resisting the elements is limited. This is especially true of 
the Blue limestone, which is inferior to the Buff, and which is to be 
avoided as far as circumstances will permit. It is a matter of expe- 
rience that two quarries may be opened with what appears to the 
proprietors an equally good prospect, one of which will soon reach 
regular, even courses, with little waste material, while the other only 
develops thin layers with much shale and chipstone. Such would be 


* Compare list from the same locality in the Michigan Report, Paleozoic Rocks, 1872, 
p. 62. 


GALENA LIMESTONE. 308 


the’ case if one were located in the horizon of the Buff beds, and the 
other in that of the Blue. The facts here given should assist in avoid- 
ing mistakes of this kind. The Upper Buff beds furnish the best 
quality of building stone, unless thick layers for heavy masonry are 
desired, when the Lower Buff also furnishes good material. Very 
little of this formation is well adapted for cutting, though the lower 
portions of the Upper Buff, and some parts of the Lower, are well 
suited to rough-dressed, course-work, its soft color, when tastefully 
relieved by appropriate pointing, cappings, and cornice, producing a 
very grateful effect. Itis a significant fact in this connection, that 
in the vicinity of Beloit, where, as stated in the local descriptions, 
quarries have been opened at nearly every horizon of this formation, 
none are now habitually worked, except those lying in the lower two- 
thirds of the Upper Buff beds. ; 

This limestone is burned at some localities for quick lime, but ex- 
cept as a source of local supply when communication is poor, such 
use is not to be recommended. The ten to twenty per cent. of im- 
purities which it usually contains are not only so much waste mate- 
rial, as ordinarily manufactured, but if the heat is allowed to become 
excessive, the impurities unite with the lime, producing a neutral 
product. Burned at a low temperature, this difficulty isin a measure 
avoided. Some of the more impure, yet homogeneous portions, would 
probably produce a water lime that would fall into the class known as 
“limes slightly hydraulic,” or perhaps a grade higher. 


GALENA LIMESTONE. 


Reposing on the Trenton beds just described, lies the Galena lime- 
stone; so named from the double fact that in the southwestern part 
of the state, where it has its most characteristic development, it is the 
chief formation that bears the lead ore, Galena or Galenite, and that in 
the vicinity of the city of Galena, it is extensively displayed. 

General characteristics. In chemical constitution, the rock con- 
sists essentially of carbonate of lime and carbonate of magnesia, united, 
molecule to molecule, and hence it is, strictly speaking, a dolomite. 
In addition to these main ingredients, there is always present a vari- 
able quantity of silicious and aluminous material, and also some 
iron. Iron pyrites, calcite, zine blende and galenite are not unfre- 
quently associated with it in the district under consideration, while 
in the Lead region these exist in great abundance, and others than 
those named are associated with them. 

The dolomite of this formation exists usually in an imperfectly 

Wis. Sur. —20 


306 GEOLOGY .OF EASTERN WISCONSIN. 


crystallized granular form, while the silicious and aluminous mater- 
ial has an earthy texture, and when abundant, gives the rock a shaly 
‘structure. These earthy ingredients are usually distributed in seams 
or partings between the layers, and in thin leaves in the mass of the bed. 
These being insoluble are left as a clay when the lime and magnesia are 
dissolved away, giving rise to a clayey soil, or crevice filling according 
to circumstances. When the rock is ground up by glacial action more 
of the soluble parts are retained and a most excellent marly clay soil 
results. In its more manifest characters and typical form, this de- 
posit may be described as a heavy bedded, irregular, coarse textured, 
gray or buff dolomite, containing frequent cavities lined or filled with 
the minerals already mentioned, and weathering in a very irregular, 
fantastic way, owing to inequalities of structure. Nodules, and occa- 
sionally continuous sheets of chert or flint are a prominent feature 
of some portions of the formation. When exposed at or near the 
surface, the rock usually presents a decayed, rotten appearance, 

As a general description, this is applicable in eastern Wisconsin as 
far north as Dodge county. At that point the formation begins to 
undergo a change. The modification consists mainly in the intro- 
duction of more clayey material in the form of shaly leaves and part- 
ings. The effect of this has been to render the rock more impervious 
to water and atmospheric agencies, and hence, its original blue or 
gray color is more generally preserved, and to this is added the green- 
ish or bluish hue of the shaly material, so that the rock, instead of 
being light yellowish gray or buff, is usually greenish or bluish gray. 
With the increase of argillaceous material there is also an increase of 
fossils. This may be partly due to the more perfect preservation that 
was afforded by the nature of the rock, but it is probable that the 
change in the oceanic conditions that caused the increase of clayey 
material also had its effect upon the life of the period. 

Without entering into a full discussion of the causes that produced 
this modification in rock and fauna, it may be observed that the ty- 
pical Galena limestone, viewed as a whole, arches over the low broad 
anticlinal axis, which stretches southward from the more ancient 
vocks that form the elevated country in the northern part of the state, 
and that, whatever may be true of the western horn of this arched 
crescent, as it enters the trough between the Wisconsin and Minne- 
sota axes, the eastern horn becomes depressed and modified as it 
reaches the margin of the great basin oceupied by the Lower Penin- 
sula of Michigan and adjacent regions. It will be subsequently 
shown that there is, and was at the time of deposit, a marked depres- 
sion of all the formations in this region, and that they were all mod- 


GALENA LIMESTONE. 807 


ified by the change of conditions which this depression caused, aid- 
ed by the protection which the projecting axis above mentioned and 
its associated reefs afforded. The change in the Galena limestone is 
gradual and progressive for 40 or 50 miles, beyond which its nature 
as modified becomes constant for nearly a hundred miles to the lim- 
its of the state. 

Organic Contents. For a complete list of the fossils found in the 
progress of the survey in this formation, the reader is referred to the 
general table of fossils of the Trenton, Galena and Cincinnati forma- 
tions, where may also be obtained a convenient view of their distribu- 
tion, and for a knowledge of their special distribution and associa- 
tions, reference may be had to the lists given in the local descriptions 
that follow. In addition to these, only a few general remarks need 
here be made. The “ Lead Coral,” Z2eceptaculites Oweni, is the most 
characteristic fossil, and, from the ease with which it can be distin- 
guished, furnishes a most convenient and reliable guide. It is not, 
however, always to be found in limited exposures of the formation, 
though it is very widely distributed. A large coiled shell, having a 
high spire, known as Murchisonia bellicincta is almost equally 
characteristic in this region and is more abundant. This species is 
regarded as identical with Ifurchisonia major, whose typical locality 
Hes in this horizon in the Green Bay region. Two somewhat similar 
fossils, Pusispira ventricosa and F’. elongata are, so far as yet deter- 
mined in this region, confined to this formation. Lingula quadrata, 
a phosphatic shell, is also regarded as characteristic, though it 
is not strictly confined to this horizon. Several other species, so far 
as present knowledge goes, are found only in these beds, but their 
distribution is not sufficiently general and well ascertained to justify 
regarding them as distinguishing species. The majority of the spe- 
cies, as we should expect, are also found in the adjacent formations. 
Of the 75 species collected from this formation, setting aside doubt- 
ful forms, 19 are confined to it, 42 are also found in lower strata, but 
not above, and 14 are found both below and above. These state- 
ments relate only to the collections made, and it is to be considered 
that owing to practical difficulties, the collections from the adjacent 
strata above are léss full than from those below, and that from the 
immediately superjacent beds there are no collections, because no ex- 
posures in this region. 

Thickness. The average of several estimates gives this formation 
a thickness of about 160 feet, with a variation from about 125 feet to 


200 feet. 
Industrial value. While this is the formation which is so pro- 


308 GEOLOGY OF EASTERN WISCONSIN. 


ductive of lead and zine in the southwestern part of the state, there 
is little reason to expect that it will prove so in the region under con- 
sideration, for, although the ores of those metals occur not unfre- 
quently in small quantities, no indications of valuable deposits have 
yet been developed. 

Analysis shows that much of this formation from Dodge county 
southward is a comparatively pure magnesian limestone, and is well 
adapted to the manufacture of quicklime. It is used for this pur- 
pose at Watertown, Ft. Atkinson, Whitewater and elsewhere. It is 
estimated that 40,000 to 50,000 barrels are burned annually. It is 
much to be preferred to the Trenton beds which are sometimes 
burned in the immediate vicinity. 

In the southern portion of the district it furnishes an inferior 
building stone, owing to its granular character, but as it undergoes 
modification farther north, it becomes better suited to the purposes 
of construction. At Waupun, Oshkosh and other localities, it is 
rough-dressed for course-work with very satisfactory results. At 
other points, especially Duck Creek and Kaukauna, the heavy beds 
are well suited to the more massive kinds of masonry, and have been 
used in the construction of the government works in that region. 

Distribution and Local Details. The more exact surface distribu- 
tion of the Galena limestone is shown on the maps of the accompa- 
nying atlas. Viewed in a comprehensive way the formation may be 
said to constitute a broad, nearly north and south belt, having a jag- 
ged, irregular outline, and forming the floor of the great Rock river 
and Green Bay valley. 


Beginning at the south, according to our habit, we find on the west side of Rock river, 
in Rock county, about a dozen small areas of this formation, capping the higher prom- 
inences. Only afew feet of the base of the formation are present at these points. 

In the eastern part of Rock county, and the western part of Walworth county, the 
Galena limestone has a more ample development, though largely concealed by drift. The 
rock in this region has essentially the same characteristics that distinguish it in the Lead 
region, being a rather heavy bedded, coarse, uneven textured, granular, buff dolomite, 
containing more or less of chert, and weathering to a very rough exterior. Fossils are 
not abundant, and are usually in the condition of obscure casts. The most extensive 
exposures are found where the westward flowing streams have formed gorges in crossing 
the strata. 

The Western Union Railway passes through one of these, in the town of Turtle, 
about midway between Beloit and Clinton Junction, and has added several fine cuts to 
the natural exposures made by the stream. 

In the town of Bradford, the Turtle creek has excavated a passage through this for- 
mation, leaving vertical escarpments of moderate altitude, surmounted by steep slopes, 
rising from 80 feet to 100 feet above the stream. Fissures analogous to those of the 
Lead region occur here, but no trustworthy indication of valuable lead deposits were 
seen. A few fossils were collected here, including Receptuculites Oweni, an undeter- 


GALENA LIMESTONE. 809 


mined species of Streptelasma, a new species of Lingula, Orthis lynx, O tricenaria, a 
Strophomena, Cypricardites rotundatus, C. subtruncatus, C. ventricosus, Raphistoma ton 
ticularis, Trochonema umbilicatum, a new species of Murchisonia and Orthocerus junce- 
wm, The most southerly exposure of this formation, seen in Walworth county, was near 
Sharon Mills. Between this point and Whitewater, deep drift conceals it. Near 
the latter point, several quarries have been opened, from which a supply of building 
stone and lime are derived. The rock here is of a more decided buff color than is com- 
mon, and is marked with peculiar concentric wavy lines of a redish hue. It is soft, po- 
yous, granular, uneven in texture, and much decomposed on the surface, but is more 
cohesive and enduring than its appearance would indicate. There is evidence of a con- 
siderable fauna at this point, though the preservation of the fossils is usually poor. 

The following identifications have been made, a portion of them based on specimens 
from the private collections of Mr. L. C. Wooster: : 

Receptaculites globosus, R. Oweni, Astylospongia, casts of the cup of a Zaphrentis, 
Cornulites-like tubes, Lingula quadrata, a Monomerella, Orthis lyna, O. perveta, or equi- 
valvis, Streptorhynchus deltoideum, Strophomena alternata, Ss. camerata, large form, S. 
camerata?, small ventricose form, Atrypa bisulcata, Rhynchonella capax, Ambonychia 
erecta?, A. lamellosa, Cypricardites ventricosus, Raphistoma lenticularis, Trochonema 
umbilicatum, Pleurotomaria, resembling P. Occidentalis, Murchisonia bellicincta, or M. 
major; M. bicincta, and anew species, Holopea paludiniformis, H. near H. obliqua, 
Fusispira elongatt. F. ventricosa, and a new species of Ecculiomphalus, Maclurea 
Bigsbyi?, and two n. sp. Conularia Trentonensis, Orthoceras planoconvexum, and two 
undetermined species, Cyrtoceras (Oncoceras) plebeium, and two undetermined species. 

Passing by several minor exposures, we find about two miles southeast of Fort 
Atkinson, quarries situated in the lower portion of this formation, and a little to the 
north (Sec. 10, S. E. qr., T. 5, R. 14), a quarry in the Upper Blue limestone. The rock 
from the former furnishes a good lime and an ordinary building stone. On the west 
side of Rock river, in the towns of Jefferson and Oakland, are several patches of 
Galena limestone, forming the nucleus of the prominent hills of that region. On the 
east side of the river, the heavy drift accumulations effectually conceal the formation. 

About two miles north of Watertown, in the 8. E. qr. of Sec. 20, town of Emmet, 
Dodge county, is an extensive quarry displaying this formation, which still maintains 
the characteristics already described. Cavities in the rock are rather more than usually 
abundant, and are usually lined with calcite, or more rarely dolomite, and occasionally 
with zinc blende or galena. Iron pyrites also occur in nodular erystallizations, many 
of which are desulphurized in whole or in part. 3, 

Chert, as usual, is abundant, more particularly in the upper layers. Fossils are rare. 

An analysis by Mr. Bode of chippings from the several layers representing a thick- 
ness of fifteen feet, shows the following composition: 


Carbonate of lime.... sec cece eee e eee e ence eee e erent ee ten serene 54.051 
Carbonate of magnesia .......e. conse eee teen eect ete ee eeenene es 44.139 
Gili Geisaaiscaasnietersiaats Meiers Noa giseuindidedes tain bbs ME aS aE A eC INE 1.564 
Alamina .. ccc ccc c cece erect ene e nett ene e een een eeeatennes 0.072 
Oxide Of 1ron .... ec ec cece eee cece teen eee n nent ree tne e cnet ennes 0.174 

100.000 


From which it will be seen to be a nearly pure dolomite, aside from the chert, which 
was excluded from the specimens analyzed. 

As far north as this point, the rock of this formation has maintained a very constant 
character, and, as remarked before, closely resembles the Galena in its more typical 
localities. To the north of this point it begins to undergo a change, For twenty-five 


310 GEOLOGY OF EASTERN WISCONSIN. 


v 
miles northward the change is slight. The rock becomes somewhat more firm, compact, 
and serviceable as building material and of a gray or blue cast rather than buff. It is 
also somewhat more argillaceous. ; 

In the vicinity of Fox Lake and at Waupun, this change has become quite pro- 
nounced, resulting in a rock, much superior to that farther south, for purposes of con- 
struction, though less serviceable for quicklime. If the formation be traced along its 
western margin, that is, along its base, the modification of its characteristics is found to 
be very gradual, Along the upper margin, there are but few opportunities for ex- 
amination. 

At Seven Mile Creek there is a flat weathered exposure that reveals little, save the 
fact of change in the direction indicated. Moore’s quarry in the western part of the city 
of Fond du Lae displays a rough, coarse, thick bedded rock of irregular texture, con- 
taining cavities lined with calcite and pyrite, and somewhat, though not remarkably, ar- 
gillaceous. While different from the rock at Watertown and southward, it still retains 
a noticeable resemblance to it. Receptaculites Oweniand Murchisonia bellicincta (major) 
occur here, as well as at Waupun and other points in this region, and leave no doubt as 
to the horizon to which these beds belong. At Moore's quarry the strata have been 
forced up into a sharp anticlinal axis, from which the beds dip equally in both directions 
at an inclination of upwards of 10.° The trend of the axis is northwest and southeast. 
It is manifestly a case of disturbed strata, but the extent of the distubance is unknown, 
as the excavation is very limited. It is interesting chiefly because such features are 
very rare in this quiet region. While sloping and undulating beds are not at all un- 
common, they almost invariably carry with them evidences that they were so deposited 
rather than folded or tilted by subsequent force. 

Beyond this point, so far as known to me, the Galena formation has not been mapped 
by previous investigators, and most, if not all of the rocks north of this point, now re- 
ferred to that horizon, have heretofore been placed either in the Trenton series below, or 
the Cincinnati above, and lest the position now taken should be misapprehended, it 
must be borne in mind, that it is simply claimed that the beds in question belong to the 
Galena horizon, and are a continuation of the unquestioned strata of that formation as 
found to the southward, and since they are the exact stratigraphical equivalents of the 
lead-bearing beds, they are mapped and described as being a modified form of that sub- 
division of the Trenton group. Whether the term Galena limestone should be applied 
to this group of strata as far as they are directly traceable, or whether it should be lim- 
ited to the lead-bearing portion, or whether 1t should apply to that portion which has 
the same lithological character as the lead-bearing portion, but is not itself productive, 
as for instance, that portion now described, or whether it should be extended as far as a 
sunilarity of organic remains is found, which would include a portion whose lithoiogical 
characters differ from the typical Galena limestonc, is not here discussed, and is a mat- 
ter of little practical importance, except as a means to a clear understanding of the facts. 

But it is a matter of much importance to ascertain precisely what becomes of the lead- 
bearing formation as it recedes from the productive area in southwestern Wisconsin, 
since it adds to our knowledge of the conditions under which the formation had its 
origin, and which, itis commonly held, determined its metalliferous character. About 
two miles southwest of Oshkosh are quarries that possess unusual interest, on account 
of their relation to this questiou. Two kinds of rock are displayed by the excavations. 
The lower portion, consisting of an exposure of 1514 feet, is formed of regular, uniform 
layers from 4 to 10 inches in thickness, rarely more or less, of a crystalline, compact, 
hard, brittle, subtranslucent, magnesian limestone, marked at intervals with irregular 
argillaceous seams of a deep blue color, occasionally tinged with green. These shaly 
partings are usually clustered about the bedding joints, to which they probably stand in 
the relation of cause. Aside from these seams, the mass of the rock is a dark bluish 


GALENA LIMESTONE. 311 


gray. The specific gravity is high. Geodes are common, and are usually filled with cal- 
cite in a great variety of forms of crystallization, and with pyrite, also in unusual variety 
of forms and colors. Zine blende is also quite common, and more rarely, Galena. This 
combination otten gives to these geodes a very beautiful and interesting appearance. 
Sheets of 1ron pyrites, filling vertical fissures, sometimes traverse the quarries. Zinc 
blende is sometimes found in small lumps in the interior of the beds. Fossils are some- 
what rare in this portion, Receptaculites Oweni being most frequent. Columns of Schiz- 
ocrinus, and a fragment of an Hndoceras were also found by diligent search. 

The upper portion of the quarry consists of alternating beds of limestone and shale, 
the whole having a greenish gray color. The limestone is much more impure and less 
crystalline than that below, and of a less firm character. These beds, and more especi- 
ally the associated shales, are quite fossiliferous. Among the species represented are 
the following: 

Small spherical bodies (sponges?), Cheetetes lycoperdon, C. discoideus, a new species 
of C. (branching form), Zaphrentis (res. Streptelasma multilamellosum), Schizocrinus 
nodosus? (large size column), Homocrinus, a new species of Stictopora, a new species of 
Trematopora, a new species of Lingula, Crania scabiosa on Streptelasma, Orthis lynx, 
O. plicatella? O. testudinaria, O. tricenaria, Streptorhynchus deltoideum, Strophomena 
alternata, S. camerata, S. incrassata, Leptena sericea, Zygospira recuvirostris, a new 
species of Rhynchonella, Ambonychia radiata? Cypricardites (internal cast), Tellinomya 
(internal cast) Euomphalus, Murchisonia bellicincta = M. Major, Bellerophon. biloba- 
tus, Illenus taurus (pygidium), Calymene senaria, Harpes? (fragment of cheek spine), 
Ceraurus pleurexanthemus. 

A specimen of Receptaculites Oweni was found in the rock pile, adjacent to the quar- 
ries, and was believed to have come from the upper layers. 

Tt will be best to reserve a discussion of the interesting facts here presented until the 
data furnished farther north are before us, and while noting on the map the position 
and stratigraphical relations of these quarries, pass on along the strike of the formation 
to the vicinity of Neenah. 

About a mile southeast of this place, the rock comes to the surface and is quar- 
ried tothe depth of afew feet. Like the upper portion of the quarries at Oshkosh, 
there is an alternation of impure limestone and shale. There is also present a coarse, 
granular crystalline rock of firmer texture than the remaining layers. The dip isirreg- 
ular, varying from 8° downwards. Some layers, especially the shaly ones, are quite fos- 
siliferous. The following species occur here: 

Buthotrephis succulens, Graptolites, Cheetetes lycoperdon, and anew species having 
a branching form, discs of Schizocrinus, plates of Crinoids, two new species of Tre- 
matopora, two new species of Stictopora, a Ptilodictya, Lingula quadrata, Orthis lynx, 
O. pectinella, O. testudinaria, and a new species, Hemipronites Americanus, Strepto- 
rhynchus deltoideum, Lepteena sericea (small one) Zygospira modesta; anew species of 
Rhynchonella, an undetermined species of Ambonychia, and of Euomphalus, Raphis- 
toma lenticularis (small), Helicotoma planulata, Murchisonia bellicineta, M. Gracilis, 
Conularia Trentonensis, an Orthoceras, a Cyrtoceras, Leperditia fabulites, Illenus 
Towensis, I. taurus, Calymene senaria and Dalmania callicephatas. 

The facies of this fauna, as well as the nature of the beds, show a somewhat wide 
departure from the character of the typical Galena limestone, and a close alliance with 
the Upper Blue beds of the Trenton; but the facts yet to be given will, it is believed, 
justify the position to which they are assigned. 

Three miles north of this, in the town of Menasha (Sec. 11, Ehf. of S. W. qr.), are two 
quarries only a short distance apart, but owing to the irregular nature of the dip, it ig 
not clear precisely what relation they sustain to each other. The quarry south of Mr. 
Tunt’s house consists of impure argillaceous greenish blue limestone, alternating with 


312 GEOLOGY OF EASTERN WISCONSIN. 


shaly layers and partings, closely resembling the upper beds at the Oshkosh quarries, 
and carrying about the same fossils. , 

‘The more recently opened quarry north of this, so far as developed at the time of my 
visit, showed a more granular rock, abounding in chert. It is important to note that 
here, Receptaculites Oweni, R. Iowensis and Murchisonia bellicincta, fossils that charac- 
terize the Galena horizon, occur, associated with Chetetes Lycoperdon, a new species of 
Chutetes having a large branching form, Streptelasma corniculum, Schizocrinus nodo- 
sus, anew species of Stictopora, Orthis lynx, O. testudinaria, O. disparalis, O. pectinella, 
O. tricenaria, Strophomena incrassata, Leptena sericea, a new species of Rhynchonella, 
Raphistoma lenticularis, a Helicotoma, resembling H. planulata, two species resembling 
Murchisonia bellicincta, one resembling M. gracilis, and one like M. percarinata ; a Belle- 
rophon, a doubtful form of Holopea puludiniformis, and an undetermined Orthoceras. 

From Appleton to De Pere, the Lower Fox river forms a succession of rapids over 
the heavier and more resisting ledges of this formation. A description of the beds at 
Kaukauna will sufficiently indicate the general character of the whole. At that point 
the layers vary from 6 to 30 inches in thickness, and have a dip of from 114° to 2° to the 
S.of E. The rock is of a dull bluish green or gray hue, and is characterized by very thin, 
shaly partings between some of the layers, and by thin, irregular, argillaceous lamine 
through the body of the rock, not sufficient however to notably impair its strength or 
powers of resisting atmospheric influences, since bowlders, that have apparently been ex- 
posed since the drift period, are still sound. Aside from these lamine, the rock has a 
crystalline character, impervious, and compact in general, though it contains a few cav- 
ities, some of which are lined with calcite, and occasionally, pyrite. The beds are ver- 
tically fissured at intervals, affording facilities for easy quarrying. Some of these fissures 
are lined with calcite or pyrite. 

These layers contain comparatively few fossils. ‘The most conspicuous and character- 
istic are Marchisonia bellicincta (major), Lingula quadrata, and Fusispira ventricosa. 
With these are associated several other species, already mentioned as occurring at Osh- 
kosh, Neenah and Menasha. At Little Chute, a Climacograptus, nearly allied to C. typ- 
icalis, occurs, and also north of this, in equivalent strata on Duck creek, but is not known 
to be found at any other horizon. An analysis shows this rock to be a dolomite, with 
about 8 per cent ot impurities, consisting chiefly of silica, alumina and iron. 

Duck creek, which runs nearly parallel to the Fox river, has also cut away the drift 
and displayed this formation, At the village of Duck Creek, near its mouth, the mas- 
sive beds are strikingly similar to those at Kaukauna, both in lithological characters 
and in organic contents. Murchisonia bellicincta, Fusispira ventricosa and Lingula 
quadrata are again the most noteworthy fossils. Farther up the stream, the beds are 
more argillaceous and alternate with shaly, very fossiliferous layers, closely resembling 
those already described. The leading fossils are graptolitic remains. Chetetes lycoper- 
don and a large new species of the same genus, Streptelasma corniculum, Pleurocystites, 
Glyptocystites Logani, a Trematopora, Lingula quadrata, and a species resembling L. 
attenuata, Orthis pectinella, and a new species, Strophomena alternata, S. incrassata 2 
Ehynchonella capax, Raphistoma lenticularis, Trochonema uinbilicatum, Murchisonia 
bellicincta and Dalmania callicephala. 

Duck creek, as well as the Fox river, runs along the line of drift movement, but in the 
opposite direction, The glacier moved up these valleys and planed, polished and 
grooved the surtace of the rock in the most beautiful manner, as may be observed at 
any favorable locality. In this planing process, the softer portions of the rock were 
doubtless excavated deepest, leaving the more resisting portions prominent, and these 
portions form the rapids on these streams, and are the parts chiefly observed. The 


more shaly portions are not observed at all on the Fox river, and at but few localities 
on Duck Creek. 


GALENA LIMESTONE. 313 


The Big Suamico river has likewise denuded this formation at afew points. The most 
noteworthy of these is at Flintville, and as the section here best illustrates the peculi- 
arities which the formation has assumed, it may be described in some detail. 

1. The lowest rock seen is a bed of soft, bluish-green, disintegrating shale, only par- 
tially exposed. 

2, Above this, is a three-inch layer of coarse, blue, granular, half crystalline limestone, 
mixed with earthy, argillaceous material, and at all points very full of Orthis testudinaria. 

3. Upon this, rest 10 inches of soft, bluish-green, decomposed shale, containing num- 
ulitic forms of Chetetes and Streptelasma corniculum. 

4, Above this, lies a four-inch bed of deep blue, coarse-grained, crystalline magnesian 
limestone, mixed with more or less of yellowish, earthy matter, the whole having a high 
specific gravity. This layer is characterized by the presence in unusual numbers of 
Receptaculites Qweni, the characteristic fossil of the Galena limestone, while other fossils, 
except minute crinoidal discs, are rare. 

5. Upon this, repose 2 feet 10 inches of shale and impure limestone, easily decompos- 
ing on exposure, and containing many branching forms of Chetetes, Streptelasma cor- 
nicul um, Orthis lynx, O. plicatella, Leptena sericea, and other fossils. 

6. Next above, occurs a 10 inch layer, similar to No. 4, but more massive, and marked 
by irregular lamine of a dark, dirty greenish, argillaceous, and apparently carbonaceous 
material, giving a somewhat fetid odor under the stroke of the hammer. 

7. Five inches soft shale, similar to No. 3. 

8. A four-inch layer, similar to No. 5, but more markedly bine. 

9. An irregular layer, about 2 inches thick, that is little else than a mass of the stems 
of the branching Chetetes. The numulitic forms, as also Brachiopods and Trilobites, are 
present. 

10. About 1 foot 6 inches of shale, containing Chwietes in abundance, especially the 
more hemispherical forms. 

11. Above this, lie about 3 feet of thick bedded, massive dolomite, very similar to that 
previously described at Kaukauna and Duck Creek. It contains Receptaculites Oweni, 
besides Orthis plicatella, O. lynx, Leptena sericea, Strophomena alternata, Raphistoma 
lenticularis, and fragments of trilobites and crinoids. 

The entire collection made at this locality, which is given below, shows an interesting 
mingling of those species that are characteristic of the Galena limestone in its typical 
localities, with an abundant Trenton fauna not found at this horizon in the Lead region. 
Cruziana? Receptaculites Oweni, Cheetetes lycoperdon, and three new species, Strepte- 
lasma corniculum, two new species of Stictopora, Lingula attenuata ? Philodops truncata, 
Orthis lynx, O. plicatella, and a form with bifurcating ribs like O. fissicosta, O. testudi- 
naria, Hemipronites Americanus, n. sp., Strophomena alternata, S. incrassata ? Lep- 
tena sericea, Zygospira recurvirostris, a new species of Rhynchonella, Pentamerus 
(Camerella ?) hemiplicatus, Raphistoma lenticularis, Murchisonia bellicincta (slender 
form), Murchisonia (slender form like M. gracilis, round volutions), F'usispira elongata, 
Bellerophon bilobatus, Cyrtolites Dyeri, Endoceras proteiforme, Illenus taurus, I. 
Iowensis, Asaphus, Calymene senaria, Ceraurus pleurexanthemus, Dalmania calli- 
cephala, Spherocoryphe, sp.? and Proétus? (fragment only). 

This formation, without noteworthy modification, is again exposed by the Little Sua- 
mico river, and outcrops along the shore of G-een Bay, south of Pensaukee, and, al- 
though largely concealed by drift, borders the bay northward into Michigan. 

Its last appearance in the state is at the lower rapids of the Menomonee river, a little 
above Marinette, where a few feet are expysed in the channel of the river. Itis here 
a bluish or greenish gray, impure dolomite of rather coarse, uneven, partly crystalline 
and partly earthy texture, containing some cavities lined with calcite. Fossils are not 
abundant. Dr. Rominger, in the Michigan report, cites the following: ‘‘Lingula 


314 GEOLOGY OF EASTERN WISCONSIN. 


quadrata, Leptena camerata, Streptorhynchus filitextus, Murchisonia major, Bucania 
expansa, Trochonema umbilicata, Maclurea (large casts, three inches in diameter), Con- 
ularia Trentonensis, Dictyonema (a species with very delicately reticulated fronds ex- 
panding from a transversely-wrinkled hollow cylindrical stem, with a shining carbon- 
aceous surface); also indistinct specimens of Cheetetes frondosus and Crinoid stems are 
included in the rock,” p. 57; to which may be added a new species of Stictopora, Ra- 
phistoma lenticularis, a Murchisonia allied to M. gracilis, but larger, a Pleurotomaria, 
and an Orthoceras. 


In the way of recapitulation, it may be observed that a comparison 
of the fossils that have now been enumerated, in connection with the 
several localities, shows, (1) that there are a considerable number that 
range throughout the whole Trenton period, including the Cincinnati 
epoch, and are, therefore, of no service in discriminating between its 
subdivisions; (2) that there is another portion whose occurrence is 
chiefly confined to the strata below; and (3) that there are a few that 
are not authentically known to occur either above, or below, the horizon 
under consideration, and may be regarded as characteristic of it. Of 
this latter number, Receptaculites Oweni and Murchisonia bellacineta, 
or major, are the most constant and reliable. Lingula guadrata, al- 
though rare in other beds in this region, does not appear to be strictly 
confined to this subdivision. Fusispira ventricosa, F’. elongata, and 
an intermediate form, are, perhaps, to be added to the list, as they range 
from Walworth to Oconto county, and are not found in the collec- 
tions of the survey in any other stratum. 

It will be seen that the change in the nature of the rock com- 
menced in Dodge county, and was essentially completed in Winnebago 
county, being gradual and progressive through 40 or 50 miles; and 
that it consisted mainly of the addition of shaly or argillaceous mate- 
rial; and that the increase in the variety and number of the fossils ac- 
companied the increase of the clayey ingredient. 

By a comparison with the formations already described, and those 
remaining to be treated, it will further be seen, that they also undergo 
some modification at essentially the same latitude, the cause of which 
can be better understood when all the facts are before us. 


THE CINCINNATI SHALES AND LIMESTONES. 


The Galena limestone is succeeded by a series of shales and lime- 
stones, constituting what will be known in this report as the Cincin- 
nati group, a name now quite generally adopted for this geological 
horizon, although there is still some difference of opinion as to the 
lower limits which should he assigned to the application of the term. 
It here includes all the beds known to lie between the upper surface 


THE CINCINNATI SHALES AND LIMESTONE. 8315 


of the Galena limestone, and the upper limits of the Lower Silurian 
formation. 

General Character. The shales that form so prominent a member 
of this group are of a varied character. One kind is little else than a 
slightly indurated green or blue clay, often very fine in texture, eon- 
taining but little sand, or other hard material, and being, chemically, 
little else than silicate of alumina. This graduates, by the addition of 
fossils, iron pyrites, caleareous and silicious matter, and, occasionally, 
crystals of gypsum, into a variety of impure and changeable shales. 
Another class has 1 more slaty structure, having been deposited in 
delicate laminze of fine sediment, not so largely clay as the above. 
These split with great ease and regularity into thin, brittle plates. 
Still another kind has a more arenaceous character and regular bed- 
ding, giving it somewhat the appearance of a fine grained sandstone. 
These three general classes include many minor varieties. 

The associated limestone is also varying in nature. A portion has 
a coarse, granular, crystalline texture, mingled with earthy, or ocher- 
ous matter, while another portion is compact, crystalline, with leaves 
of argillaceous matter variously distributed through it; and still other 
portions are silicious or cherty. These several forms often give place 
to, or graduate into shale. The limestone occurs at all observed hori- 
zons, but, except at the northern extremity of the exposure, is much 
less in quantity than the shale. Near Little Sturgeon Bay, the cal- 
careous material is much increased, and limestone predominates. 

The npper part of the formation is chiefly composed of the clay- 
shales and limestone. 

The slaty and arenaceous shales are found at lower horizons. Their 
special positions and distribution may be found among the local de- 
tails. 

The thickness of the formation may be placed at 200 feet, with an 
ascertained variation from 165 feet to 240 feet. There are reasons for 
believing that the extreme range is somewhat greater. 

Life. Sea weeds représented the plants, and Radiates, Mollusks, 
and Articulates, the animals. 

The most noteworthy feature is the remarkable abundance of Chaete- 
toid Corals and Bryozoans at certain localities. Upwards of 30 species 
were collected from the shale thrown out of two shafts of no consid- 
erable depth. Other Corals, than those related to Cheetetes, are far less 
abundant. Brachiopods are next in prevalence, the genera Orthis and 
Strophomena predominating. Lamellibranchs and Gasteropods are 
rare, and Crustaceans and Crinoids limited to a few species. More 
specific facts will be given with the local details, and a full list, ex- 


816 GEOLOGY OF EASTERN WISUONSIN. 


cept some new or doubtful species, may be found in the table of fossils 
of the Trenton period. 

Industrial value. This formation makes two notable contributions 
to the soil derived from it, either directly, or through the medium of 
the drift. The one arises from the clayey members of the formation, 
and furnishes an argillaceous constituent to the soil. They usually 
contain, also, some lime, which, with the interstratified limestone, adds 
a caleareous ingredient. The other has its origin in the arenaceous 
shales, which give rise toa somewhat sandy soil. The two mingle 
for the most part, producing an intermediate and excellent soil. In 
portions of the towns of Ottawa, Eagle, Palmyra, and La Grange, 
however, the sandy element is objectionably prevalent. 

The decomposing shales are used in the manufacture of brick, of 
which they make an excellent quality. Some of the clays of this 
formation possess an exceptionally fine texture, and are much freer 
from sand, or grit, than most drift clays, and hence are to be recom- 
mended for those purposes that require such a clay. These chiefly 
lie in the upper part of the formation. 

It may be remarked, in view of the unwarranted expenditures that 
are likely to be made under false advice, or superficial knowledge, that, 
however much any portion of this formation may resemble, in general 
aspect, any portion of the Coal Series, there never has been, and there 
is no likelihood that there ever will be, any workable deposit of coal 
found either in, or beneath it. No reliance whatever is to be placed on 
the physical nature of the rock. The fossils found in it, which, in this 
and other formations, are given with unusual fullness, demonstrate 
the utter folly of enterprises looking to the discovery of coal in or be- 
neath this formation. 

Distribution and Local Details. The most southerly point at which the Cincinnati 
beds have been observed in outcrop is near the middle of the south line of Sec. 9, in 
the town of Eagle, Waukesha county. The exposure at this point is very slight, and 
consists of impure limestone, a portion of it having an carthy and a portion, a granular 
crystalline texture, full of small cavities, and speckled with ocherous spots. A sufficient 
number of imperfect fossils are present to determine the position of the rock, which is 
near the upper face of the formation, but not immediately beneath the Niagara lime- 
stone, there being a bed of clay or clay-like shale between. In this vicinity the drift 
contains many blocks of a fine-grained, dark clay shale, ard a lighter colored, olivaceous 
gray, arenaceous rock, having a somewhat shaly structure. The two kinds are not un- 
commonly united in one bowlder, but the former soon disintegrates on exposure. The 
slaty portion also contains many comminuted fragments of Lingula, provisionally iden- 
tified as Lingula Maquoketa, and of indistinct graptolitic remains, similar to Clima- 
cograptus. As this is a very soft rock, and the blocks are little worn, and are essen- 
tially confined to this vicinity, where the glacial moraine crosses the Cincinnati belt, it 


is safe to conclude that it forms one of the members of the Cincinnati group at this 
point. This is confirmed by the fact that precisely similar rock occurs between 150 and 


THE CINCINNATI SHALES AND LIMESTONES. 817 


175 feet below the base of the Niagara limestone, on the east side of Lake Winnebago, 
and is found at other points, constituting a portion of the series, 

In the adjoining section (Sec. 10, N. W. qr.), the Niagara limestone, which consti- 
tutes Hinkley’s quarry, rests upon a dark blue, hard clay, constituting the upper mem- 
ber of the formation. The transition is abrupt, as is befitting the junction of the Lower 
and Upper Silurian formations. 

North of this, the formation is concealed by drift, and, except as occasionally struck 
by a well, is not again accessible to observation until Roberts’ quarry, on the south side 
of Pewaukee Lake, is reached. This quarry, like the last, is in the lower beds of the 
Niagara limestone, and has for its floor the clay.like shale of the formation under con- 
sideration. Fortunately for the geologist, however unprofitable for the owner, some 
“experienced miner,”’ in his ‘‘ practical’ wisdom, had discerned in this the Coal forma- 
tion (!), and expressed the belief that coal would be found beneath the shale 3 80 a shaft; 
was sunk, from which was thrown a remarkable abundance of beautifully preserved Low- 
er Silurian fossils, but, it is needless to say, no “fossil fuel.” The shaft and boring to- 
gether reached a depth of 50 feet, and showed an alternating succession of blue shale, 
and gray, yellow, and blue limestone, associated with some erystalzed quartz, and with 
considerable iron pyrites. Among the fossils collected from the material thrown out of 
this shaft, there were found no less than siateen species of Cheetetes, nine of which are 
regarded as new, With these are associated two species of Stellipora, one of De- 
kayi, two of Stictopora, several new species of Trematopora, a Fenestella, a Retepora, 
an Alecto, and two of Callopora, making nearly thirty species of Bryozoans and Corals. 
Of other forms, there were found five specics of Orthis, six of Strophomena, Crania seti- 
gera, Zygospira modesta, Pterinea demissa, Calymene senaria, an IUcenus, a new spe- 
cies of Beyrichia and one of Ortonia. These all came from the upper 10 feet of the shaft. 

Passing onward, the formation 1s again effectually concealed, till the town of Aship- 
pun is reached. In Sec. 6 of this town, and Sec. 1 of the adjoining town of Lebanon, 
small streams have denuded arenaceous beds identical with the rock described as occur- 
ring in the drift in the town of Eagle. At other points in this vicinity the presence of 
the formation is sufficiently indicated, even though it does not display itself in actual 


outcrops. 
At Hartford, these shales underlie the iron ore bed, and are penetrated by cellars, 


wells, and other excavations. 

The portion here exposed is the upper stratum, and has its usual characteristics, being 
a blue, clay-like, fossiliferous shale, containing some limestone. 

The following list of fossils will be of local interest: Several species of Chetetes, 
among which are C. annuliferus, C. rhombicus, and a new species, Stictopora fragilis, 
Orthis testudinaria, O. subquadrata, O. occidentalis, Leptena sericea, Strophomena uni- 
costata, Rhynchonella capax, and some undetermined forms. With more favorable 
exposures, this locality would doubtless prove prolific in interesting species. It may be 
remarked as a practical suggestion, that the iron ore beds, when present, always lie 
above this formation, except where disturbed by the ditt. 

Beneath the mines at Iron Ridge, and in the vicinity of the upper portion of the 
formation, is a light greenish blue, scarcely indurated clay, not very fossiliferous. Be- 
low this the shale is darker and more full of fossils. As usual, interstratified beds of 
limestone are present. The upper surface of the clay mingles with the iron ore above 
for one or two feet, rendering it too impure for use. 

The following interesting collection was made at this point: Chetetes rhombicus, n 
sw., C. briareus, C. punctatus, n. sp., and several other new or undetermined species, 
Alveolites, n. sp., Aulopora arachnoidea, Alecto inflata, Stellipora antheloidea, Sticto- 
pore. fragilis, a Helopora, a Lingula, Orthis testudinaria, O. lynx, O. subquadrata, 
and an undetrmined species, Strophomena unicostata, an undetermined Strepto- 


318 GEOLOGY OF EASTERN WISCONSIN. 


rhynchus, Leptena sericea, Rhynchonella capax, and a new species, 2. perlamellosa. 
Beneath the ledges in this region, the Cincinnati beds approach near the surface, but 
are rarely exposed on account of their soft nature. It is to this fact, chiefly, that the ver- 
tical ledges owe their origin. The soft clays and shales were easily carried away during 
the drift period, leaving the firmer Niagara limestone projecting above. Since the dritt 
period, the springs that issue so numerously at the surface of these clays have worn 
them away still farther, and the limestone from above has fallen in huge blocks and coy- 
ered the slope at the base of the cliff. So that not only in the region we are now 
speaking of, but for a hundred miles northward, the Cincinnati formation will chiefly 
manifest itself by a slope, covered with debris, at the base of vertical walls of limestone, 
known in all this region as “‘The Ledge.”’ Occasionally streams cut through this loose, 
concealing material, and display portions of the formation. An interesting case of this 
kind occurs in the town of Herman, where a beautiful brook tumbles over the step- 
like layers of Niagara limestone, and finally plunges into a gorge excavated from 
the shales under consideration. Only a few feet of blue clay and a yellow arenaceous 
shale are, however, exhibited. A similar instance occurs in the N. W. qr. of Sec. 21, 
Taycheedah. The falls at this point wash out of the clay large numbers of aggrega- 
tions of crystals of iron pyrites. These are usually globular, but sometimes take varied 
and fantastic forms. A considerable deposit of travertine, of modern origin, occurs at 
this point. 

South of Clifton, on the east side of Lake Winnebago, upwards of 175 feet are oc- 
cupied by this formation, above the level of the lake. How much it extends below is 
not known. The upper portion is chiefly concealed with fallen blocks from the clift 
above and other debris. At the lake level there appears a dark chocolate brown shale, 
alternating with impure limestone and shale of lighter color. The dark shale contains 
many comminuted fragments of Lingulas. 

Above this, liesa bed of limestone, about eight inches thick, of mingled crystalline and 
earthy structure. Upon this, rests a dark chocolate brown, slate-like shale, splitting 
with facility into soft, brittle plates. Many water-worn fragments of this stratum aro 
heaped up by the waves on the beach below, and present an exaggerated illustration 
of the difference between the rounding effects of beach action and of running water. 
In the former case, the effect of the waves is, to cause the fragments to move up and 
down the sloping beach, and if they were originally flat, as in this case, their tendency 
is to slide, rather than roll, and the result is a round, disk-like, but not globular, form, 
and this is very markedly the case at this point. On the other hand, the effect of run- 
ning water is to roll, rather than silde, the fragments, and hence, to produce spherical 
pebbles. This distinction, may be studied with profit, in connection with the drift de- 
posits. Above the slate-like beds, lies a yellowish gray shale of homogeneous, some- 
what arennceous texture, and having a conchoidal fracture, giving the rock the appear- 
ance of having an obscure concretionary structure. 

Beds higher than these, and lower than those previously described, are slightly ex- 
posed in Lot 59, Stockbridge, where shales and limestones constitute the section and Orthis 
occidentalis, 0. tricenaria, Strophomena alternata, and Rhynchonella capax, the chief 
features of the fauna. An extraordinarily large specimen of the lastnamed species was 
found, by Mr. King. at this locality. In Brown county, several of the streams that 
‘come down from above the ledge denude, to some extent, the Cincinnati beds. One of 
these forms the beautiful Cascade Falls, east of De Pere, where the shales underlie the 
iron ore deposit, and will be again mentioned in connection with that formation, and 
another, east of Green Bay, forms a succession of rapids over greenish blue shales and 
limestones. 

On reaching Green Bay, the formation is better exposed in its upper portion, but its 
base here, as elsewhere, is concealed. The escarpment of limestone that forms Whit- 


THE CINCINNATI SHALES AND LIMESTONES. 319 


ney’s Bluff is underlaid by about 65 feet of this formation, consisting, so far as ex- 
posed at the time of examination, mainly of blue shale, but including, also, some beds 
of limestone. A portion of the shale consists of a bluish, drab-colored, scarcely indurated, 
clay, of very fine texture, nearly free from sand and similar impurities, and is, in this 
respect, much superior to most drift clays, and is worthy of attention, as an excellent 
clay. Crystals of gypsum, of the variety Selenite, are found at this locality. 

North of this, the formation is quite changeable in nature. This may be well ob- 
served along the clitf that lines the shore of Green Bay, south of Little Sturgeon Bay. 
On the western curve of the point, at the mouth of the latter bay, where the formation 
last displays itself in force, the entire exposure, 15 feet, is of a hard, compact, fine 
grained, laminated limestone, showing mud cracks. 

. Following along the shore southward, a most interesting series of minor changes and 
fine exhibitions of the manner in which this class of rocks are deposited, is presented for 
study, and is worthy of note here for the benefit of students of geology, since nowhere 
else in the state are equally good opportunities for the study of shale deposits afforded. 
Degrees of induration, from that of ordinary clay, to rocks of almost flint-like hardness, 
varieties of lamination, from that which is so delicate and uniform as to indicate the 
most quiet depositing waters, up through various degrees of undulation and irregularity, 
to ripple marks, eight inches from crest to crest, and an inch high; together with mud 
cracks, so pronounced and regular as to sometimes cause the surface to resemble a pave- 
ment of octagonal bricks, may be observed, while the cliffs are banded and variegated 
with various shades of blue, green, gray and purple, the whole indicating great variety 
of conditions and of material, within a limited area. 

The formation is here much more calcareous and more firm and resisting in its nature, 
and, at the same time, less fossiliferous than at any point observed to the southward. In 
some of the lower layers exposed, there is much chert in large nodular or lenticular 
masses. 

The following section is perhaps as nearly typical as any that could be selected to rep- 
resent the formation at this extremity of its area: 


1. Hard, fine grained, compact, argillaceous limestone, in beds 10 inches 

or less in thickness, some of them weathering rough and irregular. 

IA DOU cia thivecoteinsse io exe slows oie salepeerwe te Bac eonidiemeedeneereReecens 9 ft. 
2. Similar, but harder limestone, marked with undulating and contracted 

laminations; some shaly layers interstratified; bluish gray in color, 

lined with red .....-....eeeeeeeee oud dis ere wine cnnid ne wumrsieiausma mnie 7 £t.6 in. 
8. A group of shales of varying color and texture, the most prominent of 

which are finely laminated and slaty, splitting up on exposure into 

scales and plates, while some are more clay-like. The group in- 


cludes limestone layers ......... Laid plais aby gray Anite min hier Sere nedierece 16 ft.8 in. 
4, Thick bedded, blue, cherty Limestone, with some argillaceous impurities 
in the form of lamine and partings.......+....cceeesee eer eenees 5 ft.8 in. 
5. Very similar to the above, but harder...........+.0.seeseee chelates 1 ft. 14in. 
6. Thin bedded, broken, irregular, nodular, quite cherty, calcareous layers. 
xpos einrscedce tice se aoa Sake dG saat eehaanae Dawe eee 33 
Total -abouticcd vases o683b polateinws vases sis foisnane ileteae poe 44 ft. 


At the point west of Little Sturgeon Bay, the‘formation sinks beneath the waters of 
Green Bay. 


820° GEOLOGY OF EASTERN WISCONSIN. 


FOSSILS OF THE TRENTON PERIOD. 


I 
. . . [o) 
GENERA AND SPECIES, alAalmala = 
Bla]/8!/] 3a] 4 
ares 
alalPplele 
PLANT. 
Paleophycus ceespitosum nee * 
 PTACIS: . seuventuaeeuss * * 
Pi tabullare wise cece ceuieinnes cmad|eeeayaees lacie) 
Py UNG: BP iewceurewinewaredaseaswads ex ewne sodaleavallrex sine s|| 
Cruziana, und. sp anew lake g * 
Buthotrephis needles Lies aver neenawenwes oe * 
Be Und: SPikdscus eesgherassealanasoen aoe Saini sects lneeisifeewel| OF 
Phytopsis tubulosa .........0ceeee seeeees * 
FORAMENIFERA. 
Receptaculites globularis......-......ee0005 MS rs (ee aera | ere 
Re HOWONSIS ss lescsesn es pcarans eee eames s 23a ss Benny tne lala daiel losevace 
Rig Owe nitive cssuiase:. cet seigvas/eaapele ve acatacass sees . 
PETROSPONGIA. 
Astylospongia? und. sp......-.ceeeee eee eee pAceallot a alieece lies ave 
GRAPTOLITIDA, 
Buthograptus laxus............ceeseeeeeee areal aad bell poansrellltatraca 
{ Hranaosrapias oy pionis 2 Peewee nase ANE Sahai seas lieseseow| leaves | earns 
ii onan tae cue tee Cae 
Diplograptus Peosta............00eeeeeeeee LtRellndevalersieel duce |i 
Graptolitic bodies, gen. and sp. und........ Lape ecac call pisusre [leveaev||) 
CORALS. 
Cheetetes annuliferus, n. sp........... eee. Seeks [baie ell eaves 
Cy AUTOS cise cng cise tes 3afvarje LesasaesNecaneoanlhasrae 
C. briareus............ inva eaete 
C. discoideus . occa 
Op JAM Gals ccaas ci iintues i ienet ond eadumieAtan ios oahag 
C. lycoperdon * | ox 
C. mammulatus Pe Pete een Ore 
©. SOx tO icveesscee singe teaiace nm nemanaeawtes tases cus saosavt [banaets a Gis liars 
C. pavonius........... eee eee e eee eereee pica ics | anarallgoe.s 8 
Ce POlYPOrUS; Ne iSP4 we esvienawariseancces. ver flares tous tb eee | sere 
© pulchellus:s.cn.ceseonasncannneeie Gis ‘subi ovat hora rossi i sea 
C;, ‘punctatus; We sp eeisscae sneesdceevi ase ake seacgs ale 
C. rhombicus, n. sp.........c cee eee e ee eee sever atar tas 
Os POM OBUD eases Fane ha BGs Mey aint eons nike ave’ set 
Oe GUS OSS iis cpp oarisagn ealweteries hes nace 14.5sless i 
C. n.and und. sp..........000. : * 
Monticulipora Dalei.. : 
UNG SE cee-ire we ivevarawraaisre shavcieic ae aivavere oats 
Stellipora Tpivstoretl; 


| Galena proper. 
| Galena modified. 
| Cincinnati. 


ne ace 


FOSSILS OF THE TRENTON PERIOD. 


Fosstts or THz TRENTON PErRIoD — continued. 


| 3 (ts 
we) sg le} s] e] Bs 
GENERA AND SPECIES. ala lain, leis 
eleie| eis] e| 
ele ele elas 
elisieplplla|iisis 
: CORALS — con. 
Stallipordiy We BPs vescie sede ye Peden cee meres roerbiardel aca sanuifiaecaell +s leexs 
AI VOOLLES, Me Bsa wiors'es coda. We are Ss eae ee i ARs [ties laren fnaptaces | OBER SOE eS 
Dekayi, sp. res. D. aspera.....-... 0... cece naa | Meal havepees evetscies | oe 
Streptelasma (Petraia) corniculum ......... Sadredly creeall OF ecwane st 
8. (Zaphrentis) multilamellosum .......... 4 wilace eval bsnvanahnnacsce: | BOS 
S) protundim: iesisic cnwnsewrasennes cea bah |leeeval i nada lene dV 
Ss ANd pSPse sees saga aa antrresi the Snes Pe rae aie rere Die: 
Columnaria alveolata ......-.6 eee cece eens Paved lester eapalineecenes | et 
Gy Und: Spysctouackenssane gratioes saed ane es jibes teas lheapel tae 
Zaphrentis, und. sp.......... eee cece eee ee dont eeha' ts gh) aerine [ee 
Coral resemb. Calceola ...-...--....0e es eee sev dle aore|| eit lneacal| tee 
WavOsibes, scissor caw ateciuurs ous tsa dx vas actual, Sane! ncevacelbece sian] 
Cornulites-like tubes, gen. and sp.und....... sogsall series lindane Manes [taints 
CRINOIDEA. 
Schizocrinus nodosus * | * 
Poteriocrinus, und. sp ® 
Cyathocrinus, n. sp. ?. «.-.-. * 
omocrinus, und. sp are 
Lichenocrinus, sp sree aswidlive- aaah scaaee| le Sears 
Crinoids, gen. and sp. und. ......+-.--..65- as-is treat rad eye -eiase ll E 
CYSTID ZA. 
Pleurocystites squamosus? .......eeeeeeeeee Shea Lesa wagleade laa 
Glyptocystites Logani, .....-..ee. scence ee rated eee * 
BRYOZOANS. 
Trematopora sp. res. Gorgonia perantiqua ...)...-]....]-.--| * || .* 
T. new and und. species.......--.++++eees  haees|s ate * 
Stictopora elegantula.........6.-+eeeeeeeee seal] OE || Bes tle BE [Pedaaey 
S. fragilis... cece cece centre e cece nenes mpesilkeealesaal en's a|lseas |eeen| eden 
Si. PATMOSA cele egy voce ne arene Mn aaa Gore corer penal hed g hl Se we alclene's ||| AE oie 
Ss. We SPNO; Tyee dg etesain ae dacniayey ates mays * * i] * 
GS. n.sp. No. Q...-:26 ceeeeeeeceereeeeees csal| ® * 
GS: n. Spi NO Bi vier eecerene ster ews poe eae gexall 
Ptilodictya recta, .... 0+. .eereceeeeeeeeeees * | OR * 
UNA. SPECIES «0. ee eee eee eee ee eect ee eee * 
Clathropora flabellata ve 
Callopora und. sp sa% 
Fenestella, und. sp cee 
Retepora, und. sp * 
Alecto inflata. 6. .ccescce cere eeeeeee 
Aulopora arachnoidea eneelecers 
Helopora, und. sp..-+esee cree rece ee ce eeeee ara la 
Paleschara? und. sp....esseeeesee veeeeeee eget gece an 
BRACHIOPODA. 
Lingula alternata .......+-seeeeee ene e aeons se ecallcciecalines fesse Fes 
L. maquoketa ...----+sse.eeeeeeeeee vesfoeesfeceefeceefeee [feed iouretegss 
L, quadrata.....sceee cee eeee eee e ese eneee Hgts noel aiton|eeuullll 


Wis. Sur. —21 


| Cincinnati. 


we RK 


* 


Cn 


322 


GEOLOGY OF EASTERN WISCONSIN. 


Fosstts oF Tin TRENTON PERIOD — continued. 


GENERA AND SPECIES. 


| Lower Buff. 


Lingula, sp. res. L. obtusa,..............00- ‘edly: aeatalltardna.c 
Lingula, two new species............ ... 6. svete tesatavalavonal| alansie|| hep 
iy AATAGL SS Yip cxtcsed <phcevnaicn drarayavarawnartnachapeibnyu satel siya eee sean desatid 
ine leiea a, SIs shana diarercensacione aaecatanatonls saree astavteoil e-totl pares|| [shade el farses] 
Pholidops AUT CAL Es cerah sl what swinane cdSichaviesadeetaienstobahess agrlauiei|avavens 


L 


BRACHIOPODA — (con.) 


| Lower Blue. 


| Upper Buff. 


| Upper Blue. 


| Trenton epoch. 


| Galena, proper. 


Crania scabioga.......-.cceeceeeceeeceeeee sass voll Sabsere[eadpalteersiell| eae ol leas 


C. 
C. 


Seu 


PARR DDK DDS 


Strophomena all Geert cites fase nis Seo petaneracacansiiesestaner Ue 
AMG U Ger. cvas ithe <secsctiasetoviacd Bay elaxevevesh ata carey acacersi] s 


SOLID CTA i seh. erace coca aver ses ervtegrecerergcaelaals wane Sarees eed res ee | ee | aS 
TBs SP ovecsieverteeneitviearnctacto shsaohomiavavetsse Ingieceiees a ivele crave) Robo acnts 

Schizocrania filosa.... 6... se eee eee eee eee sus aet| ete ocd a sea 
Monomerella sp. undes........... 0.000000 Papers (pairs (ese 
RTs Beller eos a isesa sieht hess dee Ogeechee aR er Viecllensead aa e 


CIS PAPAS: oF sassioectealQeeee wevbaceaceSaieses 
Ella 


CQUIV ALVIS jose: o/e.0:5: 9 are stssstia elastase egal Se ee) ee eee 
FRATICAICONISIS cose ace sinensis penis ahiarsnadnersigrerans tail iseiess [hoa 


ynx 
occidentalis. . 


testudinaria..... 0.2.2... cc ec eceeenees sapidke ; 


sp. res. O. 6 hybrida 
sp. res. O. borealis. . 
new species........ 


Und, SPCClES ec oe oo. esis e eouredawd Sears eign lees 
Hemipronites Americanus,n. sp...........5. Ae a 
Eee mics deflectum......+:+.--+--- i 
COLEGVA CUE 2, 5:cccsasccinns duasashed diteacceonascievalecens td ee eae 
HMO XUUI: & iSstos so aceees dehuiatarda nGranesenas sir | ener epee 


planoconvexum ...........0cceeee eee 


Planumbonumy 0.03.0. cence ce cen eens ad es 
FOCUS gre Sotsieieseteadacissureacawane hale ater, ee 


sinuatum. . 
subtentum. . 
CWO: BPs estas vece-caade siPNeeteve gare aye 


Me BDeoe ere ee cee ees eee ec ener eres eeees atujets 


meridionalis, n. sp 


¥*e xe xe! 


* 


HR RR RR ERR HK 


eX KHER * RID 


NIUPONGcawdeaa nese o sere igs aes Ls ahead Sera ns ade 


| Galena modified. 


* 


| Cincinnati. 


Come wee oe ER Ee 


a rs 


FOSSILS OF THE TRENTON PERIOD. 


FossiLs OF THE TRENTON PERIOD — continued. 


s\le|3s 
é : 2 . } B, Be 
HS 8 ela 2) s 
GENERA AND SPECIES. a/S)a)/S lal &] 4 
S/ E/E EVE) Elz 
a £ |i 'e 
Sislsis lay sis 
BRACHIOPODA — (con.) 
Zygospira modesta....... cece eee eee eeeee Me call) Oe 
G.  PECULVILOSULE dis acah acrgieé 5-8 £4ed Hees Be ewes seed aan | ee 
Ady pa: DISUICAA Mr meg cases sieled bp Satna mesures [eens] Loeeigl| wauice| areardd als |] *® 
Rhynchonella Anticostensis......-.......- swaaileeeefasienlivesndl Py) || oe 
CAPAX ec wah awe eho ead Sea eare un [ease [ees tne oar # * | ® 
Bic f lam Gar Pina sire a civics diesen vi hacaemeibGl acon dn oe bare ack sate 
Ri nai8piy NOs Vas swisiecdensenmeds sucnits a ares aval ececaalll CBs Ihewwn| OF 
R. perlamellosa, n. BPs ar wee wasp oan as weit [ose eral nada lho mal lingers [at aoe 
Pentamerus hemiplicatus .......--..ee.e0s ecg eaeubacra sara] oF o| * 
LAMELLIBRANCHIATA. 
Pterina demissa . ...... eee ee ee ee eee eee eee |ltuceyal staal toll eutotll aaadele 
Ambonychia attenuata ..........0e.eeeeeee racalvsagl © Maeda he 
Ay. tectarncs coe bavesdses cee sue dee eae salexeeli gue ss 8 * |e], 
A. lamellosa..........- jovetuersdsaeaxes sag oe |e 2 * |, 
A. planistriata........0csc ccs ee cen etee elec cleceelenee ial leo ee 
Ay PAdAta eos ccedadinndeaessviveeies oes |se00 |e ae loot *2|| # | * 
yO ) 6 ed ed * ® laws 
Tellinomya Iphigenia ca | ops lowes 
T. alta Laealne oeleese * roe 
T.  lirata sascleies aol | eee 
T. levata x te pase cal | (eae es 
T. nasuta came ace * ae 
EPL Ont MIC OSEhe-s Sra? woiscienesaiiere anion anneceee uel iene * ) * |» * eee 
T. neand und, spiicaccccsvewece deeeeees sc acasl dabeorcn viral eaateead| | OR Moa ore 
oa Canadensis,........0s0eeeeeee * beeen 8 oll ee clee es 
Gy” Ni Otay. w-canaiecieaiiacala ee Were oie,aers naan [aes * | oe] & BMWs aleaxe 
C. x |r | ow || # x |, 
C. & * a an ree 
Niodtblepis faba anthee * 
M. pl * 5 
M. * * * 
M. und. and n. sp a = 
Euomphalus, n. sp?..-.--+es eee eens eee es obs vesalllteeal 
Ecculiomphalus, und. sp.. vessfees ef ce eftas tenes ® leaee 
Raphistoma lenticularis......--.+++.+++++++ * | Oe | OR * | 8 
R. SOME ges ieee iosaeuaeaewsis Vises ase Biers tee RL OR [eee el] # aw 
Helicotoma planulata.....-..--+s+eeeeeeeee a a * 
ne |) eee vewefere ef] * tals 
H.. sp. und... cee eee e eee tee ete e cence feeealenealeees gaeal| Ef 
Trochonema ambiguum ......-.-- ‘acts nees OE leis * slew 
T. Beloitense, n. sp.-.+-eseeeeeeeee scenes steel * als 
T. wumbilicatum ....-.:0ecee cece ee eeerees * | oe | m - | os 
T. ves, T. lapicidum..........+.-.+.+++ Se mulonsallsgen (see e||bese)] ™ 
Ye A) altace a ia 


oie: 


2d GEOLOGY OF EASTERN WISCONSIN. 


Fossiis OF THE TRENTON PERr1op — continued. 


a} HS 
Hl ES Sie ey eis 
GENERA AND SPECIES. a;e;Fals, eyes 
ai/slelsail£is 24 
EEL ALAVE/S]4q% 
Sl8i/b Si a/ss 4 
GASTEROPODA. — (con.) 
Eunema? pagodum ............e see e eee ee sige eee ete baal) A, [Ete 
Pleurotomaria depauperata..........60ee0 0s sietie| ee HeeNellagcesl| Ce : safes 
Py Nita: casceeavwetn cele ainstin cere aan wee Peete roe a) nce ey eee | ce eee | | 
Py “SUbCONIGB nae secmsemiew cede nedecammuete Re [RE | Re seca RE Ns Sscall eaaoes sl doecave 
Py nd: Sp. is.p-cous ve cdemtaviea mers ot aeeatate pieotis jot ep aar we econ | lay aah adeevell oe 
P. sp. res. P. occidentalis............--56- schoo dell Osea oa eels Saal Peakaga so 
Cyclonema percarinatum ........-0..6000 6s ee Pee (reer | mean (eeecer | Recerca | aoe 
Murchisonia bicincta..... .......665- sy har BO lesa] Fl sail | oe 
M.  bellicincta=M. major...............06- ies Pomeel eater fowcealiteaaey: * 
My \prracilisn i: aneawensac cena “anes sore waeudlli® 22, enssesge fiers aa re) ed 
M, “helicteres 00:1 2ccmenameswsomoat noes 6 sue, TEE SB eg all Ae a Seca hag 
MM, PaBOdaivesnisuninie sonra vox a vas dann x45 faced Py A Tecayeelll | seete 
MM. percarindtal? 2059s 4 x5 + o424o Sa Gee 4 sbarsueifticse jlwavetstlasmiecel| fee ae|| 
My -Sermilatey a issiavsouae so ot ean xine do oie 4% soreca ese FE Tae HL Eleva eail tee eal wane 
Mi.) AHICATINATAe mifwalonnacaya sine eee es eek BP Wd oe coal Re Poa sl lave taal cease 
MG, ‘three: t's @piiaiencctanvomey gangs eae ees ss se ais: fectisjal lev asnve |acreral| [eves (PRP [vecenall haere 
Holopea;obliqiaisc scisieae maax sacs x4 x3 4448 ees HED leversceliacecn.o:t oatad |) SRS IN) cena |) Ro hess 
H. paludiniformis........... ce eee eeeeee satecey SMa Sass ieee | ORS a Fo heats 
2 MING, SPictinexignaunieas gargs cannes oe as e054 sco fas fl oc oyene' Uaeaieceel| anatie sil [anes oP |Iiiarea 
Subulites ClONgatUS .asse vies deavieeasoees * * lok |i] ® eas 
Calisospira occidentalis, n. sp.........0-.00. scacava|s Ro lace aval asqca| B| cece y |lawcees 
Fusispiraclongata. .ce:2 4246s seer ses eucaae ivan || erro seal oteal| eveeal) * 
Bb. SONG COSAcisaitaivad Aandad eS) AG Vee RE EE davascos|ucntecadllesuiceuell aresteal| [teaxeace | OF aan eae 
Das at, Sinclar aud etal ras ¥uosa es Stok Gwe Sr avallieceratsil scaeecal| weal aces || gas co | eae 
Waclirer Biesiat seein aeiteeka mak oie eaneee dace: Se lexpealhagsael |, S| EP Salhegea 
My Camerata; DSPs ssee's4 bee dnesd peau wesd Lee deve Seat ll Raab a sven liast ce) | OE etl Kee 
M. subrotunda, n. sp........e.e eee e eee eee deni wae elicrarseal aperey: (ll Seetive| | OR ae 
pisteptoms 3 res. M. patellitormis........ ecosd «|e Sedeell srereiel | gacetall loosd haloes * 
onan mie SPs seeceiaesedansecans bees ceoeleceell * . 
» HETEROPODA. 
Bucania bidorsata.........-..cccceseveseee * | oR | & lax, 
Buellin, spricaqsweesvases vexewueeas es * od 
DOR PANSA re yaydics pied give Baan eek eae EEA aval. cee | aceralllalaretea| tC Oretavers 
B puneiifonmis.- ee eee ee pee ee ee Bel oe 
SDisvlossis cece weed ayer at ses kets * 
Banant biUObwhisiee Siceageace dee een teu aa lasso teats saci * 
Wisconsinensis, n. 8p... 2... cc ee eee eee x [oe toe | ox ra eee | [eae 
Bie’ UBC sepsis ats wees ee ct-euaind gee aed BAER E eta | ce vhiceowil| FF Ihocnall|) 
Cyrtolites compressus.....-...-......e cece prgale cele eea |e aa alll HE esl levees 
Oy. ADYOMiai es seateaisucieteely veut ganebovtue jvedleetaleses[seasl[eaatalaces|| & 
PTEROPODA. 
Conularia Trentonensis...............00.00- onal iees ee alesa lek ca | 
Hyolithes Baconi, n. sp.................00. see sf OF RS alll 8 7 
Pterotheca attenuata............cec eee eae x | oR | x x 7 < 
Ecculiomphalus undulatus.............. 00. Be Nake 
(a! eee ee ee eee ere * fe See Gs ss 


FOSSILS OF THE TRENTON PERIOD. 


Fosst_s oF THE Trenton PErtop — continued. 


e|3 

GENERA AND SPECIES. me | 

5 | 5 

§]8 

CEPHALOPODA. 

Orthoceras amplicameratum..... 0 .....--- gee atau 

OQ: aellimiasscan akan sae ece Ueeeseues * | # 
O. capitolinum < ces. cone see ede ae Gees save beasts 

Q, jUNGEOM, <. vecse secs eke ee ayees eee res ee 

QO. planoconvexa...... ss cece cence ee eeeeeee #2) * 
O. multicameratumn « Avecsiliovw oye 

QO. vertebrale.......... ey # 

Q. TSP Pen. vena s ees oe * ; 

Op Wd: Sse s ee cate ss oe cas baa 6 Ooi oes oe seal: 

QO. (Ormoceras) Beloitense, n. sp.....+-+-+- * 7) OR 
Ormoceras tenuifilum?...........e sees eee pier iets 

UNG. SPrivs oes casa k se a5 555 Here Re ee * * 
Endoceras se umlatonn D Ya seae Soe NSE Ome sge= liege 


E. proteiforme..... 0... cece cere cece eeeeee fetes 


| 
alm 
BR) 8 
a | 
P}P 


x 


ee KH! 


Hie Ud: SPidw aig. sass aie ayers are oe aha laevis wet See 


Cyrtoceras annulatum . : sata] ORE Nhe 
Cy, SCAM ied we has tis san cam ME eS : sus esa) | 8 
Ce seomiculum:» o.c0.40.04 sn eeantecmaaneas : ae aa oe 
Ch SUG ised on das ane cn ae ea epee 5 PEA SBE These 
Cy Weculosuiiiese dics eccke ts acesedacesots sites easel atl eewsae 
C. macrostomum .....--- eee eee e ee eens fasevel esansa eis’ Se 
Cs “Neleusiicauaa, ov cnt beenedants toad aera oem site eeators |) TET Wes 
C. und. BP... se se ee see cere reese cen eernes sui [gaseed | sea fees 
Ce Und) SPri acs ccesnise ce tesneu a sneeneartes seal’ FE essai as 
Oncoceras Alceus deavellSetess |! OE bere 
O. abruptam fa, ll ageas|| Ae lit 
O. Lycus... 2... eee e cree ener e eee cree es atexe) 5) |) 8 [ies 
Q):. Pan dhOniies si sus vecisiee bee adits et nace Ae) || IB Nes 
QO. plebeium #2] #1) ® les 
* 


O. Wd. Spire ec cee cece cece es tree eee ee eee Nees 
Ascoceras or Cryptoceras, und. sp..-.+-+++++ wens] es eae aleced lar 


Gyroceras convolvans....+-+-+++eseeereeeee 
G. duplicostatumn. sp 
Gonioceras ANCEPS.-- +++ eee ee ee 


G. occidentale ......-scccrce rece ceseennes saek 


Lituites occidentalis......-..eeceeereeeeeee 


L. Robertsoni.......scccceeecceececeerees Os 


Gomphoceras, und. sp .+-+-+ sees secre ener Suelo ease ot 


CRUSTACEA. 


Leperditia fabulites ...----.+eeeee eee eceeee * | # | F 
Tllenus crassicauda ?. . ielstt al esol Len all os, 
J, Jowensis....cccccccecesscceeeereserees Picked esters eeoaaee 
T, GVEUS secs wa sin'e crete bag) a esa Barase eco ea senegal (ES | Oe 2 
T.. taurus.icssese cas Serene aici suréeeea abs # >| geal eee ales’. 
J, und. spose seeeeecerecesee eres eeenerens tevalwwee| & . 
Asaphus Barrandi.......+-+eeersseereeeres aoe |) | : 
AL Gigas... ccs cece cere eect erent e eee e es savage Sseie A] ek as 
A. Towensis...++-+ee+- eee PE 5 2 
AL De SPeeee cece eeeeees ie saliseaa 
A. sp. Und ..... sees eee ee ee eeee j eslaes 


Qalymene senaria..---- eiaae ene 


| Trenton Epoch. 


HERE EHH E HR KK Y KS 


XEN HD KKH RHEE! 


* 


SRE RE HR! 


* 


| Galena proper. 


* 


Harpes, und. sp.-++++e+reeere gpeezae touug ae ccaiaialleaaies fan's 4 | anes | [Pee alee ae 


| Galena modified. 


ee ¥! 


| ‘Cincinnati. 


826 GEOLOGY OF EASTERN WISCONSIN. 


FossiLs oF THE TRENTON PERIOD — continued. 


a wt 3 
ee re re ee ee a 
Hl S/e 2a] 2/2 i 
GENERA AND SPECIES. alma /alHallal | ais 
H mH a HW 9 3 oS A 
o @ | o © =i a a ‘ 
FP) ERIE EV 4S/4]¢ 
° - . 
a alee lyalsol ols 
CRUSTACEA — (con.) 
Dalmania callicephala ..........-6... 2006 ewsallleisiag lame evel sae | eee 
IDs. Means .00reeurewsergde case OP tei Hewes leg aati coal cvlldis’s fll sways 
Ceraurus pleurexanthemus a lit SPT. esau 6 sah The ae 
Encrinurus, n. sp. 2... eee eee eee f ss * Neel Sesieus 
Spherocephalus? und. sp.....--- coves saclives|easollacmellaaece SE Meese 
Proétus, und. Sp... ++ esse eee e ee eee eens evadlesssneas [ssa s|leoualllcase] F Moca. 
Beyrichia, und. and n. Sp..--+--+ essere ee eee sanye| Se sailesad laaevall * 
ANNELIDA. 
Ortonia, n. SP..0.0- sees eee ee neers eee e es peecliavelavecleace| lenewellacecale * 
Serpulites-like tubes.......seeee cece ee eeeee sat nade aneai's oes |freasi 


Z 
Z 
2 
© 
a 
ae 
Z 
Ss) 
s 


CLINTON IRON ORE DEPOSIT. 32 


“ad 


CHAPTER VIIL 


UPPER SILURIAN. 


CLINTON IRON ORE DEPOSIT. 


It has already been incidentally stated, that, at certain points, the 
Cincinnati shales were overlaid by an iron ore deposit, while much 
more frequently it was observed, that the Niagara limestone rested 
directly upon them. Wherever the iron ore occurs, it is found to be 
capped by Niagara limestone. The phenomenon presented, then, is 
that of a separation of the shales and limestone, at some points, by a 
bed of iron ore, coming in between them, and growing thicker till its 
maximum is reached, and then thinning out and disappearing again, 
forming an irregular lens-like mass. 

As yet there seems no authentic instance of organicremains having 
been found in this deposit, althongh I was shown fossils, said, with 
undoubted truth, to have been taken from the ore, but they were pro- 
bably found in the disturbed drift ore, as they were Cincinnati species, 
specimens of which were ascertained to have been driven up by 
glacial forces into the mixed mass overlying the Mayville ore bed. 
We are left, then, without the valuable criterion which fossils afford 
for determining the age of this important formation. But there is, 
nevertheless, no occasion for doubt on this subject. Its stratigraph- 
ical position fixes its age within very narrow limits. The limestone 
above belongs to a very low horizon in the Niagara group, and, indeed, 
it has been regarded by some eminent geologists as belonging to the 
Clinton epoch, and it probably is the approximate equivalent of the 
upper portion of the Clinton beds of New York, but as will be seen 
hereafter, there is no good reason for separating this limestone from 
the great mass of the Niagara group, with which it is intimately con- 
nected. There is a sharp line of demarkation between the ore and the 
limestone, at most points, so that there is no reason for assigning the 
ore a higher position than the Clinton epoch. 

While, as already stated, the clay below mingles somewhat with 
the lower layers of the iron deposit, the ore “ takes on” layers at the 
bottom, so that its beds are in a slight degree unconformable to those 


328 GEOLOGY OF EASTERN WISCONSIN, 


below, which constitutes a reason for not grouping the iron beds with 
the Cincinnati series. 

Within the limits to which stratigraphical evidence thus confines 
this formation, there can be no hesitancy in referring it, on litholog- 
ical grounds, to the Clinton epoch, since that epoch is characterized 
from Ohio as far eastward as Nova Scotia, and as far southward as 
Alabama, by a similar deposit of odlitic iron ore. 

As this formation is developed only at certain localities, we may 
profitably omit further general remarks, and give place to detailed 
local descriptions. 

By far the most important development of this formation occurs at 
Iron Ridge, in the township of Hubbard, Dodge county. The main 
deposit is included in Secs, 12 and 13 of that town. The locality is 
characterized by a north and south ledge facing the west, and over- 
looking the lower land in that direction, from a height of about sixty 
feet. The upper twenty feet or more of this ledge is composed of 
heavy, rough beds of Niagara limestone. Beneath this lies the ore 
bed having a varying thickness, the average of which is perhaps fif- 
teen to eighteen feet. 

This leaves the base of the ore at a most convenient elevation above 
the lower land adjoining on the west, giving the most ample facil- 
ities for drainage, loading the ore into cars, or supplying the ad- 
jacent furnace. The accompanying topographical map, for the data 
of which, as well as many other favors, 1 am indebted to the kind- 
ness of Supt. W. C. Sterling, will show the situation more precisely, 
and the chromo-lithograph (Pl. X), which has been accurately 
sketched from a phovograph, will give a more vivid conception of the 
relations of the ore and the method of mining, than can be conveyed 
by description. The mine, of which only a small portion is shown 
in the plate, is situated a short distance west of the center of Sec. 13. 

Near it is the furnace, and a little further west is the village. 
Three-quarters of a mile north of this, is the Mayville mine, on what 
is known as the Mayville Ore Bed, though the village of Mayville is 
four miles anda half distant. The working force at this point, at the 
time of my investigations, was in charge of G. Rt. Hood, to whom I 
am indebted for various favors. 

Having thus before us the essential geographical features of the 
location, and the general situation of the ore bed, we may give our at- 
tention more specifically to the deposit itself. 

The ore occurs in regular horizontal beds, varying from about 3 to 
14 inches in thickness. The dip is slight and varying in direction. 
Near the furnace, it is northward; at the Mayville Ore Bed, it is south- 


PLATE, XI 


TOPOGRAPHICAL MAP 


of a portion of the 
IRON RIDGE MINING PROPER 


Chielly trom data furnished. 
oy 
Supt W. C. Sterling, 


o) 


Qontour lirtes 5¢t.apart vertically. yg 
- S| 


dine. 


1873. 
Scale, 40011; 


Toe Muavavicgs Trio. & Baca Go. 


CLINTON IRON ORE DEPOSIT. 329 


eastward; and north of this, it is again northward. This, in connee- 
tion with the fact that the thickest portion of ore oceurs at the highest 
elevation, near the center of the deposit, seems to indicate that appre- 
ciable, though slight, flexures of the strata have taken place at this 
point since their original deposition. 


Fig. 40. 


NortH anp Soura SEcTION THROUGH THE InoN ORE Deposit, IRoN RipGE. 


1. Cincinnati Shale. 2. Iron Ore. 3. Niagara Limestone. 


The ore, as a whole, must be classed with the hematites, although 
it contains a notable amount of water in combination, and gives a 
streak varying from a dirty red to a yellowish brown, and, except the 
upper layer, which differs from the main body, seldom gives a bright 
scarlet streak or powder. The hydration is not uniform, however, 
and is most marked where the ore is most exposed, and seems to be a 
process in progress, rather than an original characteristic. The water 
collected in, or issuing from, the mines is colored to a bright scarlet, 
although a spring issuing beneath is almost free from indications of 
iron, as indeed are all the springs in the vicinity. They cannot be 
relied upon, then, to indicate the presence of this iron deposit. The 
ore consists chiefly of small lenticular concretions, whose average 
diameter is about one twenty-fifth of an inch. They are less uniform 
in size than would appear to casual observation, being of all dimensions, 
from one tenth of an inch in diameter to those that are very minute. 
There occur also in all of the layers, but more numerously in the 
lower ones, larger concretions which are usually more or less lenticu- 
lar in form, though frequently otherwise. These seem to be largely 
composed of argillaceous material. From this conecretionary or 
odlitic structure, the ore receives its popular names, “seed ore,” and 
“shot ore.’ The coneretions are bound together by just enough of 
adhesive ore powder to give the mass a somewhat firm coherence, and 
the result is a soft, granular rock. The little lens-shaped concretions 
lie, as would naturally be anticipated, chiefly upon their sides, giving 
to the rock a ready cleavage in a horizontal direction. These facts, 
together with the vertical joints and frequent bedding lines, render 
mining remarkably easy. The prevailing color is a dark reddish 
brown. At certain points it becomes purplish and even bluish, as at 
the Mayville Ore Bed, where the term “blue ore” is applied. 

The top layer, from 3 to 8 inches thick, differs markedly from the 


330 GEOLOGY OF EASTERN WISCONSIN. 


rest of the deposit. It is dark purple in color, much harder and more 
compact than the odlitic ore, and is not lenticular, though sometimes 
incorporating a few concretions. It gives a bright scarlet streak and 
powder, has an irregular or conchoidal fracture, and much higher 
specific gravity than the main mass. It contains, as noted by Dr. 
Percival, scales of specular ore. 

At the mines, the bedded ore varies from 15 to 254 feet in thick- 
ness. To this, at the Mayville Ore Bed, there is added a considerable 
depth of drift ore increasing the thickness to 40 feet or more. 


Fie. 41. 


PROFILE SECTION AT THE MayYvILLE ORE Bev. 
a. Cincinnati Shale. 0. Bedded Ore. cv. Drift Ore. d. Niagara Limestone, Cupping Ore. jf. Mixcd 


Drift. 

The accompanying section (fig. +1) shows very inadequately the ar- 
rangement of the undisturbed and drift ores, and of the ocherous 
drift, gravel, bowlders, and disturbed and undisturbed limestone, as 
seen at the time of my visits. It was taken just when the drift, in 
the progress of mining, was giving place to undisturbed limestone, a 
point most favorable for study. It will be noted that the various 
bands of drift material extend from the left (north) obliquely upwards 
to the right, and that at the left, the upper dark layer of ore is swept 
away, and at the right, it is broken up in a peculiar way very imper- 
fectly illustrated in the figure. 

The force that produced the disturbance and intrusion of the ore 
into the econimon drift seems to have come from the west of north, 
and to have been massive in character. It is but another characteris- 
tic instance of glacial action. 

What may have been the original extent of the ore deposit to the 
westward cannot now be ascertained. That portion has been swept 
away by the dennding agencies which formed the valley lying in that 
direction. To the southward and south-westward, the same agencies 
have limited our knowledge. To the eastward, the deposit thins out. 
To the northeastward, there rises a high ridge, underlaid by a consid- 
erable depth of limestone, which has thus far limited explorations in 
that direction, since the immense quantities of ore already developed 
leave no necessity for further exploration at present by the company 


CLINTON IRON ORE DEPOSIT. 831 


owning the land. The deposit may be traced a mile and a quarter to 
the northward from the furnace, where it is lost under the hills that 
rise in that direction. It has been found in a thin deposit, two miles 
farther on to the west of north, in the town of Williamstown. It has 
also been found a mile to the east of the furnace. Though it is diffi. 
cult to give even an approximate estimate of the amount of ore here 
deposited, it is at least safe to say that it is to be reckoned by millions 
of tons, and, though not absolutely inexhaustible, is at least adequate 
to all anticipated wants for a long period to come. 

Both open and underground mining have been made use of, but 
the former method has been found the most economical. 

The position of the ore, outcropping along the face of a terrace, at a 
convenient elevation, rendering drainage, “stripping,” loading into 
cars, or the furnace, convenient, the soft character of the ore, its hor- 
izontal bedding of medium thickness, the ease with which it may be 
bored and blasted, its situation in a rich agricultural and heavily tim- 
bered region, and its railway connections, combine to render this lo- 
cality unsurpassed in the advantages it presents for mining, reducing 
and shipping the ore. 

The following table of analyses shows the chemical nature of the 
ore: 


S|] | 
= a od o 

ANALYSES OF S ee aelede| oat ob 28] = 
Iron RipGE Ore. Bs 2 gh aan Sp 3.9 Zn| os 
| 28! Bolas] 22] 22] 88) 43 
O|5,8| 536.25) 563) 53) Oe CE 

| pal pleas) Ml FA LP) eS 

a} OQ im | AQ joa) ia) 
Loss by heat at 212°................ ssiosa’ ts |ideate Sv Plevacoca Mev toes 2.00) 3.00) 2.00)..... 
Specific gravity. i... sue seca sess |een tees vee ue Gullo SSeS 2.94) 3.07) 2.99) 3.03 
Peroxide of iron.......e..eeseeeeeee 72.50/74. 40/79. 25) 76.74/77 .34/78.75)41.67/76.51 
Carbonate of lime .........-..+..05- 0.56] 6.72) 6.81]..... 0.55) 2.00/15.48} 0.75 
Carbonate of magnesia...........++. 0.64; 0.41) 0.14)..... 6.64/trace.| 8.25|trace. 
Oxide of manganese.......--.+0.0-- LAO seh ioe gases 1.05) 3.50} 3.30} 2.56) 8.10 
AluMiNaiecccs oes 4 eee 6 Sia a 6 ey we 8.40} 2.26] 2.49} 4.00) 5.00) 4.50/12.74] 5.21 
DUCA dieccctaeeee sae sees Aawes Ser atn 7.75] 9.11} 6.18/10.09) 8.57) 6.40/15.12/10.13 
Water and loss ..-...eee esse eeeeee 8.75) 3.10] 4.00)....- 2.65)..... 2.65]..... 
BUOY eiecadie idinteuiioe tae tens a8 o.tans awa arals Sowa lenwe lee ae 6.00)..... 3.00)..... 4.30 
TOSS o-svcid cp sevasticubseidvanel niece 8: esnpaieed sos neea G75 40k SiS | CTI mee QD Qa scenes Ls eins [aaee s 
Phosphoric acid .......eseeereeeeeeeleneee 1.00} 1.18)..... 2.75} 0.75) 1.53}..... 
100.| 100.} 100. 100.} 100.| 100.} 100.; 100 
Metallie: Tromsiesvicneise na aw ane «lence [erceone Reatollegeeertes 54.14/54. 13]/29.17/53.56 


In his report, Dr. Jackson says, that the lime and magnesia are 
combined with the silica and not with carbonic acid, so that the above 


332 GEOLOGY OF EASTERN WISCONSIN. 


table should read, lime, for carbonate of lime, and magnesia, for car- 
bonate of magnesia, so far as his anslysis is concerned. 

I am indebted to the kindness of Supt. Sterling, for the following 
relating to the iron interest at this point. The whole amount of 
ore shipped from July 1, 1869, to January 1, 1872, was 178,842 tons; 
the amount in 1872, 82,371 tons; in 1873, 48,706 tons; total for 
the three and a half years, 304,919 tons. This ore was shipped to 
Chicago, Joliet and Springfield, Ill, St. Louis, Mo., Wyandotte and 
Jackson, Mich., Appleton, Green Bay and Milwaukee, in our own 
state, and Zanesville and Newburg, Ohio, as well as to various other 
points in small quantities. 

The cost of mining the ore (1873) is from 50 to 75 cents per ton. 
The value of the ore, delivered on the cars, is from $1.50 to $2.00 per ton. 

The average furnace-yield of metal, from the ore, is 45 per cent. 

The furnace at this point is 40 feet high, 9} feet across the boshes, 
uses 4 or 5 tuyeres, as occasion may require, makes use of the hot blast, 
blown by steain power, burns charcoal — the average cost of which is 
114 cents per bushel — and has a capacity of about 3,500 gross tons 
yearly. No flux is used. 

The composition of the pig-iron product is shown by the following 
analysis, by E. T. Sweet, kindly furnished by Prof. Irving: 


Per ceut. 
TOT oi 5g Sh GUE Se Rate Sie Sates cecal Behar aloe emma edetecs 95.784 
Phosphorus...+.. 00sec cee cree eet nese eee eee eee tener ee een eee 1.675 
Graphite... 060i ccc c cece e enn eter ener rete nen ene ee ener e ences 1.379 
Combined CarbGn wacicsnwisa nr enue nrcd doer Re redier Semsewsa ees 0.849 
TT a 8S a eee eee cng hae aa cpg sh aba aanolalos yn ayaa whet tbiaca done 0.491 
Sulphur... .. 0.06 cere cece cee eet ence ence etree eee ee neeenenes 0.108 
Manganést yi s0dscnacesosS3e2 59208 4220 490 Wha Re Eee Dee a Hees a eles Trace. 

100.286 


In 1849, a blast furnace was established at the village of Mayville 
for the reduction of this ore. Iam indebted to Mr. James Scoular 
for the following facts concerning its present capacity and workings 
(1873): Height, forty feet—nine feet in the boshes; uses four 
tuyeres, the hot air blast, charcoal as fuel, and steam and water com- 
bined, as power. The vharge is seven hundred pounds of ore and six- 
teen bushels of charcoal. The ore used is from the north opening at 
the Mayville Ore Bed. Limestone and lean ore have sometimes been 
used asa flux. Sandstone was being tried. The yield is thirteen or 
fourteen tons of iron per day, being about forty-two per cent. of the ore. 

Hartford. The deposit at this place is altogether similar to that 
at Iron Ridge. It is, however, much inferior in both vertical and 
lateral extent, and if the numerous statements collected concerning 


CLINTON IRON ORE DEPOSIT. 333 


the wells of the place, with such observations as were possible, can be 
trusted, much more uneven. The bed underlies the southeastern por- 
tion of the village. In the southwestern portion, the denuding agen- 
cies have swept away the overlying limestone and the ore, if it ever 
existed there, and have substituted adrift deposit. On the north side 
of the Rubicon, the horizon of the ore has been depressed by an ap- 
parent fault, so as to occur at a considerable depth below the surface 
of the river. There seems good evidence that the deposit reaches ten 
or twelve feet in thickness at some points, but rapidly thins out, so 
that the average thickness for the area over which it occurs probably 
does not exceed two feet. The accompanying section will show the 
general nature of the deposit and its relations. 


ramee Fre. 42. 


Rubicon 
ipa 


PosITION 4ND RELATIONS OF THE IRoN ORE AT HartrorD. 
NV. L.—Niagara Limestone. C. S.— Cincinnati Shale. 


Besides the deposits at Iron Ridge and Hartford, and their vicinity, 
drift ore, of precisely similar nature, occurs in the town of Stockbridge. 
The deposit is small and lies upon the west side of a ridge of moder- 
ate height, the exterior of which, at least, is drift. A well in the 
vicinity is said to have reached iron ore, eighteen inches in thickness, 
beneath limestone. 

At the Cascade Falls, east of De Pere, the formation again appears. 
Its situation beneath the Niagara limestone and above the Cincinnati 
shales is shown in the accompanying figure. The fall 
wus, is caused by the fact that the iron ore is more easily 
worn away by the action of the stream than the lime- 

z7=— stone above. The shale is somewhat more resisting 
than the ore. The maximum thickness of the ore is 
five feet. On the east side of the gorge, its base was 


Fie. 48. 


, at the fall, and to the west of it, that full measurements 
, could be made. Just east of the fall, the thickness, 
: == measured as accurately as the nature of the case 
Cascapz Farts, near Would admit, is four feet, eight and one-half inches. 

pain Just west of the fall it is four feet nine inches. A. 
@. Cincinnati shale. Jitt]e farther on where the wall of the gorge curves 


v. Clinton iron ore. 5 : z ' 
c. Niagara limestone. toward the north, it reaches its maximum of five fect, 


304 GEOLOGY OF EASTERN WISCONSIN. 


and still farther on, it is reduced to four feet six and one-half inches. 
Near the point of greatest thickness, there are slight indications of 
“taking on”? layers. The ore at this point is very similar to that at 
Iron Ridge. The odlitic concretions are somewhat larger on the aver- 
age, and of a slightly duller color, and there is a greater amount of 
argillaceous material present. Upon the bed of lenticular ore, there is 
a highly pyritiferous layer that seems to represent the dark layer at 
Iron Ridge. Along the shore of Green Bay, south of Little Sturgeon 
Bay, this geological horizon is marked by a somewhat continuous bed 
of ore, or ocherous rock, of a few inches thickness. It very rarely pre- 
sents an odlitic structure, or other characteristic of the deposits already 
described, but it is identical with them in geological position, and 
must he regarded as their stratigraphical equivalent. 

It appears, then, from the foregoing facts, that this iron ore occurs 
at widely separated points, and that between these it is entirely want- 
ing, or is represented only by a rusty seam between the limestone and 
shale. There can be no doubt that it was a marine deposit, for in ad- 
dition to the evidence of the beds in this state, the equivalent forma- 
tion elsewhere contains the remains of marine life. It appears alto- 
gether probable that the ore was deposited in detached basins, over 
which, and over all the intervening region, the Niagara limestone was 
afterwards laid down, enclosing the detached deposits between it and 
the shale below in the form of lenticular masses. This ore is to be 
sought for only between the Cincinnati shales and the Niagara lime- 
stone. The line along which the junction of these two formations 
comes to the surface will be found traced with much care on the 
accompanying maps. To the east of this line, the horizon of the ore 
lies beneath the Niagara limestone, and, so far as geological evidence 
goes, is as likely to be found at the base of that formation, at any 
point over the broad area occupied by it, as at the points where its 
base has come to be exposed at the surface by denuding agencies. Of 
course the value of a bed of ore, found at any considerable depth below 
the surface, would be very seriously affected by its unfavorable po- 
sition. 

While it is probable that beds of this ore do exist at points not yet 
discovered, it is prudent to bear in mind that deposits of the thick- 
ness of that at Iron Ridge are very rare, there being but a single 
known instance of a thicker deposit in all the wide range of the Clin- 
ton formation, though beds of less depth are profitably mined; and 
while it is legitimate to hope that further profitable discoveries may 
yet be made, it is the part of wisdom to exercise due caution in the 
expenditure of time or funds in exploration, and to be guided by an 


PLATE, XII 


TNO ey 
TNOLS qu : ; 
BA NXVS Svs 
= s OLL St ‘LS 
AN OLS mary) NON Das 


( Beans 
wv NT A TY 9 


LLYN NY) Nie 


i 


UDI) JO JINIT 


SPpog PLU 
ae comedies 


ae 


SPIT ti0)3.4 7 ; ; - 
pag 72.10) LonNo7y a OLS INIT === a 
: )VUVOVIN 


“Pog Dv soy 


1p "YAH ieee emmy  eqneeses aca Sees | 
So rep Pupiyy PT IO PPT 
WIA S oe eel wee 
Ss5 ee SS 
A oes ee 7727) 
| re brvogays’ 
oLel 
uyite quel) o) Sa [8 

AQ 


STIAM NVIS OLLUV 


Ag wnoys sv 


UDDADGIYS' OP WONIUMING? UO) UAIISD {| MOLY 
a1140e8d 


D241. np 


YO | ULtT 


WH 


womnunyt’ Di 7f 


Fit Minwaten birin & Bxcin.Ca. 


NIAGARA LIMESTONE. 335 


intelligence derived from careful study of the geological facts relating 
to this interesting formation. 


NIAGARA LIMESTONE. 


The shales and iron ore deposits, that have last been described, lie 
along the eastern margin of the great Green Bay and Rock river val- 
ley, and are to a large extent overhung by beetling cliffs of craggy 
limestone that form the western projecting edge of the Niagara for- 
mation. 

The strata, that thus jut out along this border, form the lower mem- 
ber of an extensive and important limestone group, that occupies 
nearly all the region between this border and Lake Michigan. The 
strata dip to the eastward, so that the higher members of the series 
appear in succession in that direction. All these members are mag- 
nesian limestones, or dolomites, some of them being among the purest 
known. 

The belt occupied by this formation has a north and south extent 
of about two hundred miles. In the course of this extension, its 
character undergoes a change, so that its nature at the two extremi- 
ties is quite different. And it is a most interesting fact to note that 
this change takes place at the same latitude as that at which the 
changes that we have previously noted in the lower formations, espe- 
cially the Galena limestone, take place. At the north, there are six 
subdivisions, sufficiently well marked and persistent to justify their 
being named, described, and mapped separately. At the south, there 
are four such subdivisions. It should be observed that these are de- 
nominated subdivisions of the Niagara limestone. They are not re- 
garded as distinct formations, or as having the grade of epochs, as that 
term is usually understood, but they are nevertheless well character- 
ized subordinate divisions of a formation of more than ordinary im- 
portance, and it is believed to be of much value to industry, as well 
as science, to give all the exactness and precision possible to its inves- 
tigation and description. The names given to the subdivisions are as 
follows, placed opposite to each other for convenience of comparison: 


Niagara GRovp. 


At the South — At the North — 
1. Guelph Beds. 1. Guelph Beds. 
2. Racine Beds. 2. Racine Beds. 


4, Lower Coral Beds. 
5. Byron Beds. 


4, Mayville Beds. ‘6. Mayville Beds. 


38. Upper Coral Beds. 
3. Waukesha Beds. 


836 GEOLOGY OF EASTERN WISCONSIN. 


The term Guelph has been applied to the uppermost beds on ac- 
count of a similarity of fossils to those of the Guelph limestone of 
Canada, to which the Wisconsin formation is probably equivalent. 
The recognition of this equivalence is due to Prof. Whitfield. 

The Qacine beds are the equivalent of what has been known as 
the Racine limestone,! except that the upper portion is now separated 
as Guelph, and the reefs and associated rocks west of Milwaukee, 
which have been referred to a lower horizon, are included in it. 

The lowest strata of the Niagara series are named Mayville heds 
because they have their maximum development and finest exposure 
south of that village. For the strata that lie between these and the 
Racine beds, in the southern part of the state, the term Waukesha 
limestone, which has been previously applied to a portion of them, 
has been adopted with modifications. The white limestone, that lies 
upon the Mayville beds, in the northern portion, receives its name 
from the township of Byron, where it is extensively utilized for lime, 
building stone, and flagging, and where occurs the only fossil yet 
found abundantly in it. The Upper and Lower Coral beds have been 
thus designated from the preponderance of coralline forms among 
the fossils found in them. 

The accompanying plates (Plates XI{ and XIIT) will show the po- 
sition and relations of these subdivisons very satisfactorily. Plate 
XIII is based upon the facts developed in sinking the Artesian wells 
at Sheboygan, Milwaukee and Western Union Junction. They were 
sunk after my investigations upon this formation, and confirm in a 
most satisfactory manner my conclusions. The plate also illustrates 
a number of other interesting geological facts, among which is the 
northward dip of the strata. It also furnishes valuable data in ref- 
erence to Artesian wells. 


MAYVILLE BEDS, 


As already indicated, these beds form the lowest member of the 
Niagara series throughout its whole extent. They possess the same 
general character throughout their entire area, and, in this respect, 
differ from the rest of the group. The rock of this member is, in 
general, a rough, coarse, gray, magnesian limestone. There is consid- 
erable difference, however, among the several layers that compose it, 
and some of these maintain their peculiarities with great persistency, 
so that it is possible to distinguish them at points one hundred miles 
or more apart. This makes it possible to describe a section which 


'Geology of Wisconsin, 1862, p. 67. 


PLATE, x] 


inberlint 


PROFILES 
TC. Cha 


a 5 
3 N 5 
“Gy ‘¢ 
Ae AY 
i SS 
uy 
it § EI, 
ans : 
S Ss Fs i 
& AQ si s 
qh: : ie : 
) S re Re < 
= 3 é Hs : : 
2 & S i : & ) 
As § S y | 3 
3 S g S | > ii 
5 8 Re qe 4 
pos 5 S5 dh i} =e ti ss 3 nl 
- gs SM 2 a / 
S as 4 SMM SE 8 SRS Sy ah 
2 mS 83M Bee te 3) di 
: : se 1 ae S2 fH 
=) eau z Hn i yy o Ae 
Sanus TH g = Ea 
iS $ = i if fl & [ & ah 
it 5 5 ~ / ff} S If x Hl) 
Hees § = Eh =i 
= Ss oF S 
fe | | Sa 
s i g) Hae 
5 y r 
: 3 H ; in 
ai ae 
ity = s a; 
= BI Fea 
= s, 
Sk, 
i 


Lower Coral Beds 


A: HW 
eal 
LM ita 
Y 
: i 
geea2e22es Gne88 5 


NIAGARA LIMESTONE. 837 


will be applicable in a general way to the formation at all points, and 
will be of practical service, as some layers are valuable and others 
comparatively worthless. It will, however, be impossible to readily 
distinguish all these layers at every point. 

The lowest stratum consists of from four to ten feet of shaly, im- 
pure limestone, usually of a yellowish gray, but sometimes of a 
greenish hue. The beds, at some points, attain sufficient thickness 
and soundness to be serviceable as building stone. At Iron Ridge, 
this stratum either disappears or loses its characteristics. 

Upon this lies a stratum of hard, heavy-bedded magnesian lime- 
stone, usually gray in color, and generally characterized by prominent 
vertical fissures and obscure and distant bedding joints. It does not 
make good quicklime, and is of comparatively little value as a build- 
ing rock. It varies from six to twelve feet in thickness. The third 
general stratum is composed of three parts, as found in most places. 
The lower one consists of broken fragments of limestone imbedded 
in a greenish, bluish or yellowish, marly clay. More or less of chert 
is present. The middle portion consists of compact, sometimes 
cherty limestone, in even beds, from four to fourteen inches thick, 
and serviceable for building stone. The upper portion is a repetition 
of the lower. The three portions are not to be distinguished, how- 
ever, at all points. The chert is sometimes almost entirely wanting, 
as in Oakfield, and sometimes is a very prominent feature, as in Ot- 
tawa. The entire stratum varies from five to thirty-five feet in thick- 
ness. In the town of Taycheedah, there occur at the bottom of this 
stratum a few regular beds that are marked by an abundance of Stro- 
matopora, very imperfectly preserved. They should probably be 
grouped with the above, as Stromatopora extends into its layers. 

This stratum is overlaid by an even bedded limestone, usually quite 
hard, compact, fine grained, white or light gray, often nearly a pure 
dolomite, and a valuable rock. At the same horizon, or just above it, 
in Taycheedah, Empire, Ashippun, and less distinctly at some other 
points, there occurs a reddish yellow, granular crystalline dolomite, 
called by the workmen and residents “sandstone.” It is, in fact, an 
unusually pure dolomite, so that if the term is understood to imply 
that the rock is silicious, it could scarcely be more erroneous, since 
the amount of silica is not more than about one-fourth of one per 
cent. It is, however, a fine example of calcareous sandrock. The 
grains are chiefly minute crystals, that show no evidences of wearing 
action, and have evidently not been disturbed since their crystalliza- 
tion. The interstices between the crystals are to a considerable ex- 
tent unfilled by any matrix, making the stone highly porous, and, in 

Wis. Sur. —22 


338 GEOLOGY OF EASTERN WISCUNSIN. 


some cases, rendering it liable to disintegrate to a calcareous sand. 
It occurs in heavy beds, is easily quarried, cuts with the greatest fa- 
cility, and is much used at Fond du Lac for cappings, etc. It is 
probable that this and the preceding rock are to be referred to the 
same horizon, as they seem to graduate into each other at some points, 
and to replace each other, mutually, at others. 

Upon this rests a stratum similar to the second in being charac- 
terized by thick beds and vertical fissures, but differing from it in 
being less hard, and in possessing a highly brecciated structure in 
some localities. To the position just above this is to be referred a 
layer containing many obscure casts of a Pentamerus (Gypidula), 
very similar to the species occidentalis. This stratum is succeeded 
above by the white, even-textured limestone of the Byron and Wau- 
kesha beds. 

As a whole, the Mayville beds may be readily recognized by their 
thick bedding, uneven structure, and the rough, craggy, pitted sur- 
face of the weathered ledges, when taken in connection with their 
position. It is the best exposed member of the Niagara group, as 
it forms a chain of craggy cliffs, upwards of a hundred miles in 
length, though broken down and concealed at frequent intervals. 
The greatest observed thickness is one hundred feet. The aver- 
age thickness is probably not more than siaty feet. The chemical 
composition of some of the more important of these beds is shown 
in the following table: 


ANALYSES. 
I I Iii. IV. Vv. VI. 
Carbonate of lime......-+-..- 50.52 50.54 58.95 55.03 54.91 55.18 
Carbonate of magnesia....... 40.97 40.37 44.28 44.3 42.77 41.70 
Sesquioxide of iron.....-...-- 0.77 1.02 0.30 0.31 0.43 0.57 
Sesquioxide of alumina.....-. 3.49 2.67 O10: wanes 0.46 0.18 
SiliCann.acne ance aae eens 3.57 4000 eaaek asa dagen wheat 
Jnsoluble residue........0..00 ceeee te eee 1.23 0.26 1.385 1.73 
WiALei senaretenedd oases 0.48 0.70 trace 0.29 0.26 0.45 
T Gta atoissermotebcectreracyires er 99.80 99.82 99.86 100.23 100.18 99.81 
Per cent. of impurities........ 7.83 8.21 1.63 0.57 2.24 2.48 


The rock for the first analysis was from the shaly beds, at the base 
of the formation, that are used for making waterlime in Williams- 
town (N. W. $ of N. E. $ of Sec. 27, T. 16 N., R. 19 E.), and the sec- 
ond was from similar beds found in Stockbridge (N. E. + of See. 11, 
T.19 N., R.18 E.). The third was from the limestone used at the 
Appleton iron furnaces for flux, and obtained from the lower 20 feet 


NIAGARA LIMESTONE. 339 


of the formation at Clifton, on Lake Winnebago. The fourth was 
from the so-called sandstone near Taycheedah. The fifth, from the 
upper layer, aud the sixth from the lower layer, at Audley’s quarry, 
in the town of Delafield (Sec. 20, 8. E. 4). The limestone in the last 
named instance included many nodules of chert, which were excluded 
from the samples analyzed, one object of the analysis being to ascer- 
tain the chemical nature of limestone associated with well-defined con- 
cretions of chert. The above analyses were executed by Prof. Daniells. 

It appears that in all cases, the carbonates of lime and magnesia 
exist essentially in the proportions necessary to form dolomite, so that 
these beds may be said to be true sedimentary dolomites, and the re- 
maining constituents may be regarded as impurities, and are so sum- 
med up for convenience, the water being disregarded. It will be ob- 
served that the Taycheedah “sandstone” is remarkably pure. This 
will be again noticed in the discussion of economic considerations. 

Life. The remains of the life of the period are very illy preserv- 
ed, and it is only rarely that fossils can be found sufficiently well-de- 
fined to be satisfactorily identified. In most cases, only obscure casts 
remain. It is not to be inferred from this, however, that the life of 
the period was actually meager. On the contrary, it was probably 
abundant. The conglomeritic character of a portion of the beds shows 
that the material was subjected to much grinding action by the waves 
of the depositing seas, and makes it probable that the greater portion 
were comminuted in the process of deposit, while the crystalline na- 
ture of the rock suggests, that the process of crystallization may have 
obliterated some that escaped comminution, and cavities having the 
form of fossils show that some others have been removed by solution. 
From the nature of the material, some of the identifications are neces- 
sarily doubtful, and are so indicated. 

In the following table, the occurrence of the several species, at the 
more important localities, will be found systematically and compactly 
arranged. Students and collectors will find this a convenient form, 
A table will be found at the close of the description of the Niagara 
group, in which the fossils of this member are compared with those 
of the other beds, which will also be found instructive. 


3840 GEOLOGY OF EASTERN WISCONSIN. 


FOSSILS OF THE MAYVILLE BEDS OF THE NIAGARA GROUP. 


& 
> ia) 
ae Bs 
3 © | “wa 
oes 2 |e 
aS E ; a | ad 
GENERA AND SPECIES. Blea a 2) 
aaa We) _ . 
e/2/S/8/E/B/2 
si /2/2/2/8) s/2e 
|S | 3 | 2 a} 
ala|b/2| s/s 
HiFls|4|/2z/a|4 
PETROSPONGIA. 
Stromatopora concentrica....-..sceeccesereeerecs | [a ee ae oe 
CORALS. 
Favosites Niagarensis..........cscescsesesceeeees BP Recah s ele | oe | o® 
PAV OSUSES ois cactige sihiiacianatd wing reen Saraaieynera ios chase harsh sraravel| ater 
Astrocerium Venustum..... ee. cece cece eect e ween Bb eens 
Halysites catenulaatus .........eceeeeee seer eeeee eaigg larsnra averse)! Slr OR beccviel| 
Helilites pyriformis .......+....:-+eeeeee ees slwdion + oR Neral ara a 
Diphyphyllum cespitosum . $8 Sistas sex [ieovap 
Zaphrentis, und. sp........ * a | ce 
Cyathophyllum, und. sp ...--.-..cceceeee eeecene oan erst * 
Chonophyllum Niagarense..........6. cee ee eens vag ail seared eae] 
AMplERUS, UNG 6:40. .cecsu verse dees seeaw asad Sean sees lewoalhecese|| OF 
BRACHIOPODA. 
Orthis flabellula ia ian es * 
QO. res. O. hybrida sseislleiealll SF cod of 
Strophodonta striata .... Be eae sega ava ee 
Strophomena rhomboidalis gr | | eae Be Ne a 
Meristina, res. M. cylindrica os eeaheaery a ee 
Retzia aprinis=Rhynchospira aprinis eged| 8 scat be cevas 
IAN aiy Bs. ISPD Za arenace, ans gracaaret waves raters ayatacelaiaes aslo iexate saa eee 
Pentamerus fornicatus.... .... aaeel nak 
P. oblongus.... ...-.... Sisson eeeansene sae whe ¥ iva sia 
Gypidula, res. G. occidentalis,H. but smaller iacera| see 
Stricklandinia, und. s ee shea 
Leptoccelia planoconvexa, me * 
GASTEROPODA. 
Euomphalus Racinensis......... .....eesseeerees Noe ease * 
Buena, Und. Spieciors.c suawiewereinnagenivarernicctornrse : Sedalleieas * 
CEPHALOPODA, 
Ormoceras, prob. O. vertebratum..... .... Saatrealewaleen ieaere| eelelteried| A ol ORE oe 
CRUSTACEA, 
Tllenus, res. I. Barriensis.........0. csc eseeenees © lewealauaalocedieeesl tidutees 


Economic Value. From the analyses already given, it will be 
seen that some portions of this formation are remarkably pure dolo- 
mites, while others are notably impure. From the description already 


NIAGARA LIMESTONE. d41 


given, and, more especially, from the local details that follow, it will 
appear that these several portions occur in such a way as to require 
some discrimination, if the best quality of rock is to be.chosen; and 
it is hoped this report will furnish some assistance in making a suit- 
able selection. 

Kilns for the reduction of lime have been established along its en- 
tire length. These vary in construction, from mere rude domes of 
bowlders to approved patent kilns. And yet some of each class were 
found abandoned, while others were doing a profitable business. It 
was observed that, in many cases, an impure rock had been burned. 
In some instances, this was pardonable, as no better was exposed in 
the vicinity, and the local demand warranted the use of such as was 
accessible, until improved means of communication supplied a supe- 
rior article from other sources; but in other instances, it is evident 
that the failure was due to the use of inferior rock, when a superior 
ore existed in the immediate vicinity. 

Properly selected, a very excellent lime may be made from this 
formation. A considerable quantity of stone may be selected, in 
which the impurities are less than one per cent. of the wholes much 
additional may be found, in which they are less than two per cent., 
and an inexhaustible quantity, in which they do nst exceed three per 
cent. The large percentage of magnesia is an advantage, for it is a 
well established fact that dolomite makes a stronger cement than 
simple limestone. At many localities, the better class of rock is 
used, and an excellent product obtained. Practical suggestions in re- 
lation to selection will be found in Vol. I, where they are given to 
save constant repetition. Numerous statistics relating to the in- 
dustry were taken; but they could not be made sufficiently complete, 
accurate, and uniform to justify publication here. 

At some localities, it is claimed that the lower beds of this forma- 
tion are suited to the manufacture of hydraulic lime, and analyses I. 
and II, given above, were made to ascertain upon what basis this 
claim was founded. The composition, it will be seen, is quite differ- 
from that of the celebrated hydraulic cements, and would ot justify 
an expectation that this rock would produce an hydraulic lime that 
would have more than a local market. It will doubtless furnish a 
serviceable substitute for the more expensive cements, for certain 
purposes, where common fat lime will not answer. 

Rock obtained from Clifton is used at Appleton as a flux for Lake 
Superior iron ores, and is said to work satisfactorily. The rock is 
obtained from the fallen masses on the slope below the cliff, which 
consist of a mingling of the several strata. The analysis above given 


842 GEOLOGY OF EASTERN WISCONSIN. 


represents the better quality found in the rock pile at the furnace. By 
comparison with that from Taycheedah, it will be seen that the lime- 
stone used is not the purest that is accessible to Lake Winnebago, and 
this fact may be worthy of the attention of those interested. 

For the purposes of ordinary masonry, this formation furnishes an 
abundance of readily accessible material, and it is extensively used 
for such purposes. The granular stratum furnishes an excellent stone 
for cutting. Its rich cream color gives it a very pleasing effect. 
Rock obtained east of Horicon marsh is wrought at the State Prison, 
at Waupun, and quarries have been opened upon this stratum, east of 
Found du Lac, from which a supply of cut stone, for that city and 
other points, is obtained. 

Distribution, and Local Descriptions. By consulting the maps, 
it will be seen that these beds occupy an irregular belt, stretching in 
a nearly north and south direction, from the [linois line, in Wal- 
worth county, to near the extremity of the peninsula east of Green 
Bay, where it dips beneath the surface of that body of water. Most 
of the localities here mentioned lie on the extreme western margin 
of this belt, and show the projecting edge of the formation. 


~ The point at which the formation enters this state from Tllinois, or leaves it in that 
direction, if you please, is deeply concealed by drift, but there is abundant reason for 
believing that it crosses the line from the towns of Walworth and Linn, as represented 
on the map. 

On the north side of Lake Geneva, the limestone approaches the surface, but does not 
actually outcrop. The most southerly point where the western limit of these beds is ac- 
curately determined by outcrop is in the 8. W. qr. of Sec. 10, town of Eagle in Wau- 
kesha county. South of this point, the outline, as mapped, is based upon topographical 
and drift evidence, and can only be regarded as approximate. At Hinckley’s quarry, in 
the above-named section, four feet of thin bedded, impure magnesian limestone, having 
an even fracture and light, yellowish gray color, blotched with green in places, espec- 
jally between the layers, form the base of the quarry, and rest upon the Cincinnati shale. 
Above these are nine feet of thicker bedded limestone of coarser and more regular tex- 
ture, and marked by walnut-sized cavities, lined with yellow granular matter. 

These beds, when exposed in natural ledges, as they are in the vicinity, weather to a 
very rough, ragged exterior, due to the irregularities of their structure. 

In this region, the great drift moraine, previously described as the Kettle Range, over- 
lies this formation, and it is only here and there that it displaysitself. Near Hinckley’s 
quarry, the ledge swings round to the east, and disappears beneath the drift ridges. It 
emerges again in Secs. 11 and 14 of the town of Ottawa. The rock here is char- 
acterized by conspicuous nodules of white chert, which are very abundant in some 
layers. 

At Hunter's quarry (Sec. 11, 5. E. qr.), the lower three feet exposed is a moderately 
hard, compact, gray, magnesian limestone, marked with iron stains. Upon this lies a 
somewhat peculiar shaly layer, which may he described as chipstone imbedded in a 
clayey matenal. Above this are two and a half feet of more solid rock, the upper por- 
tion of which is cherty. This is overlaid by another shaly, or chipstone layer, similar to 
that below, but cherty; and this in turn is surmounted by a few rotten buff layers that 


NIAGARA LIMESTONE. 348 


complete the exposure. The two chipstone layers are worthy of note, as they may be 
recognized more than a hundred miles to the northward. 

In Delafield, the next town north, notwithstanding the drift, the formation discovers 
itself at several points, though nowhere in great force. Its character is essentially as in 
Ottawa. At the quarry near the village, the two shaly layers are observable. 

At Audley and Graham's quarry (8. E. qr., Sec. 20), a few layers of dark, gray 
crystalline limestone, containing much chert, are burned for lime. The analysis of this 
has already been given. At Roberts’ quarry, south of Pewaukee Lake (S. W. qr. of S. 
W. qr., See. 24, Delafield), the beds are more close-textured and silicious than at the 
points previously described, and the chert is more distinctly arranged in layers along 
the bedding joints. The exterior of the layers is buff, while the interior is blue, the lat- 
ter sometimes appearing as a well-defined rectangle, surrounded by a border of buff, 
when a block has been broken across. The whole was undoubtedly once blue, and the 
buff has been caused by leaching, and the peroxidation of the iron present. 

The formation again disappears beneath the drift, and is next seen m the town of 
Ashippun, in Dodge county, where it forms a few ragged outlying ledges. The most 
noteworthy of these lies in the west half of Secs. 6 and 7. It rises about fifty feet above 
“the grade,” at its base, though the vertical ledge only presents a face of about twenty 
feet. 

The bedding joints are very obscure, and the layers are traced with difficulty, so that 
the rock presents a very massive appearance, but a general section, somewhat as follows, 
may be made out. Six feet exposed at the base consist of a hard, but porous, dolomite 
of uneven texture, made up of fine and coarse grained patches, mottled gray and buff 
correspondingly. This is overlaid by from 4 to 6 feet of very hard, compact, flintlike 
limestone, much fissured vertically. Upon this rest 7 to 8 feet of a reddish buff, gran- 
ular, somewhat friable, magnesian limestone, the granules consisting of small crystals 
of dolomite, the spaces between which are mostly unfilled, giving a porous structure. 
Chemically, this is a very pure dolomite, and should be burned for lime instead of either 
of the other layers exposed at this point, as it would not only produce a superior quality 
of lime, but would burn easier. This is undoubtedly the equivalent of the ‘‘ sandstone *’ 
layer near Taycheedah, and is the most valuable portion of the beds under consideration. 
This is overlaid by 6 feet or more of brecciated rock, consisting of subungular fragments 
of a gray magnesian limestone, imbedded in a yellow, granular matrix of similar chem- 
ical nature. 

North of this, the margin of the main body of the formation recedes to the castward 
as far as Hartford. Near this place are several limited exposures of these beds, one of 
which, on the farm of Mr. Blodgett, is interesting on account of the fossils it contains, 
a list of which has already been given. The rock is a light colored, granular dolomite 
of irregular texture. 

Passing by several outcrops in Herman, we find at Iron Ridge, reposing on the ore 
beds, 6 feet 8 inches of buff magnesian limestone, in beds of 8 to 16 inches thickness. 
Upon this, lies a layer 6 feet 8 inches thick, the bedding planes of which are very obscure, 
so that it appears like a single layer, while vertical fissures are frequent. This is over- 
laid by 2 feet 10 inches of thin bedded magnesian limestone, which gives place above to 
a shaly layer, composed of rotten chipstone, mingled with a greenish blue clay. The 
whole is capped by about 6 feet of broken, frost-riven limestone. As the mining pro- 
gresses backward from the face of the ledge, the thinner beds will douhtless be found 
uniting into thicker and more solid ones, and the disintegrated rock will give place to 
that which is more firm, with corresponding changes in color and general aspect. 

From this point northward, there is no dearth of outcrops. The Kettle Range has 
receded to the eastward, and there is left only the usual drift deposit, through which 


the formation boldly thrusts its jagged edge. 


b44 GEOLOGY OF EASTERN WISCONSIN. 


About two miles south of the village of Mayville, there is a precipitous cliff 100 feet 
in hight, exhibiting the full extent, and more than the usual thickness of this subdivision 
of the Niagara group. Owing to the difficulties of measuring on the vertical face of the 
cliff, the thickness of the beds is only approximately given from aneroid measurement. 

At the base, are 5 feet of the usual thin bedded, shelly, light colored layers, disinte- 
grated back from the face of the ledge. 

Overhanging this, is 12 feet of hard, semi-translucent dolomite, not separated into dis- 
tinct beds, but rifted with vertical fissures, which do not, however, extend into the beds 
above or below. This supports 7 feet of shaly and cherty rock, lying beneath 4 feet of 
thick bedded limestone, which is in turn overlaid by 23 feet of shaly and cherty layers, 
the three forming the shaly or chipstone group, previously described. 

Upon this, lies another stratum of about 23 feet, in which the vertical fissures are much 
more pronounced than the bedding lines. 

This is surmounted by a somewhat thicker group of soft, white, granular, crystalline 
dolomite, some layers of which contain many casts of fossils, particularly of Gypidula. 
The top of the ledge is formed of white, fine-grained, crystalline dolomite, closely re- 
sembling the rock of the next group above, to which it probably belongs. 

In crossing the east branch of Rock river, the boundary again swings to the eastward 
as in the case of the Rubicon, and in the course of this detour, manifests itself in several 
low ledges. 

Returning from this deviation, the formation enters upon a succession of precipitous 
ledges that extend to Little Sturgeon Bay. These are all so like each other, and so sim- 
ilar to those already described, that it will not be necessary to repeat the details of their 
structure. From near the village of Kekoskee, the ledges succeed each other in stair- 
like order, shifting westward till the margin of Horicon Marsh is reached, when they 
stretch northerly to its extremity, where, forming a continuous rampart, the line curves 
rapidly to the eastward through the corner of Oakfield, and onward in crenate outline 
through the town of Byron. 

The direction of the ledge is now in the line of dip, and the beds under consideration 
rapidly drop down and are soon surmounted by the white walls of the Byron beds. 
Turning abruptly northward, in the northwest corner of the town of Eden, the chain of 
ledges extends through the western part of Empire, the Mayville beds again emerging 
and forming the rocky rampart, while the white Byron heds retire to the eastward. 
Opposite the southern extremity of Lake Winnebago, the crown of the cliff, at some 
points, is formed by a very pure, granular crystalline, cream colored dolomite, locally 
known as asandstone. The constituent grains are small crystals of the carbonate of lime 
and magnesia, usually quite firmly compacted, but sometimes loosely aggregated, leav- 
ing numerous interspaces, which render the rock very porous and disposed to crumble 
to a calcareous sand, whence the local name. It is probably due to the misapprehension 
of its real character, growing out of the use of the name sandstone, that it has not been 
more extensively used for the manufacture of lime, instead of the much inferior rock 
that has been employed. Aside from this important stratum, the formation continues 
essentially as previously described. The chain of cliffs skirts at a little distance the east 
shore of Lake Winnebago, rising more than 200 feet above it. Toward the northem 
extremity, the ledge approaches the lake and directly overlooks it. 

Between Lake Winnebago and Green Bay, the formation is more broken down and 
covered, but on reaching the eastern shore of the latter, it reappears in bold relief, crown- 
ing and protecting the more perishable Cincinnati shales, and giving a picturesque 
outline to the bay shore as far north as Little Sturgeon Bay. It forms the rocky sum- 
mit of Whitney's Bluff, where it is wrought for various purposes. ‘The most northern 
place where it is extensively used is on the shore west of Little Sturgeon Bay, where 
a pier and kilns have been constructed. At this point, many of the general features 


NIAGARA LIMESTONE. B45 


o 


noted in Waukesha county are still discernible though the texture and composition hera 
are superior. North of this point these beds drop down to near the level of the waters 
of Green Bay, and alternately appear and disappear with the nndulations of the strata, 
as far north as the Light House point opposite Chambers’ Island, where they finally 
disappear beneath the waters of the bay. 


BYRON BEDS. 


Reposing upon the coarse textured Mayville beds last described, 
lies a somewhat thicker series of beds, bearing a strong contrast to 
them in color, texture, stratification, and general character. The 
ledges of the former ure rough in aspect and dull in color, those of 
the latter are usually smooth and white. The texture of the former 
is generally coarse, and often very uneven, that of the latter is always 
fine, and sometimes so close and compact as to be lithographic in 
character. The transition from the one to the other is usually ab- 
rupt and well defined. These facts eminently justify the distinction 
here adopted. 

To describe somewhat more precisely, it may be remarked, that the 
color, where not white, is a light gray or creain tint, sometimes lined 
or mottled with pink in a very handsome manner. The texture is 
usually either very close and compact, or very fine grained. In the 
former case, it is hard and has a somewhat glassy fracture, and the 
edges of the fragments often appear translucent, Such portions 
often have a grayish water hue. The other class usually has a regu- 
lar or conchoidal fracture, and is opaque. Some portions are finely 
laminated, and where these lamin are colored, as sometimes occurs, 
a beautiful effect is produced. 

The bedding is either thin, producing excellent flagging, or attains 
more considerable dimensions, and furnishes cutting and building 
stone. Some of the strata are habitually undulating, and some, in the 
weathered ledges, are excessively fractured in a conchoidal manner, 
while others are vertically fissured. 

Argillaceous partings are occasionally present, and the rock, though 
rarely, becomes shaly. Muderacks and ripple marks were observed. 

The following analysis of rock taken from Butler’s quarry (Sec. 10, 
Byron), made by Prof. Daniells, for the survey, shows it to be a near- 


ly pure dolomite: 
yP Per Cee 


Carbonate of lime.... .cccseccccscrcccrcnceecnceeeracencccseeneees 54 

Carbonate of magnesia... . 60... cece eee eect et eee e eter ene e anaes 44.48 
Sesquioxide of 10 ..-.. see eee cee cece teeter eee ee ere e ene e arene oe 0.26 
Sesquioxide of alumina..... cece eec cece ee te sence eee e een eneeee serve 0210 
Insoluble residue... 2.6.50 ce cee eee cece eee eter en eter rent eeeee 0.67 
Water... ccc ccc cee cece ew ere ween eee e ee en reece esereereecreeare 0.41 


346 GEOLOGY OF EASTERN WISCONSIN. 


Fossils. These are very rare. At Butler’s quarry, in the town of 
Byron, Leperditia fonticcla is abundant, this being its typical local- 
ity. Fucoidal impressions are occasionally met with, and an undeter- 
mined Zaphrentis was found near Sturgeon Bay. 

Thickness. The greatest observed thickness, not including the 
transition beds above, is 110 feet; inelnding that portion of the transi- 
tion beds most allied to this division, its maximum thickness would 
reach perhaps 140 feet. 

Distribution. The formation presents so great a degree of uni- 
formity that local sections and descriptions will be unnecessary. 

In delineating the outcroppings of the beds below, we were carried 
northward to near the extremity of the peninsula east of Green Bay. 
We may secure continuity of thought and save ourselves mental trans- 
portation by taking up the distribution of this division at that point. 

It was stated that at Little Sturgeon Bay, the Mayville beds dipped 
down to near the water’s edge. On doing so, they are at once sur- 
mounted by the Byron beds, in full force. These form a series of 
bold, picturesque cliffs, extending to the extremity of the peninsula. 
Two of these cliffs stand like pillars of Hercules, at the mouth of Big 
Sturgeon Bay, and each of the harbors north of this, on the west side 
of the peninsula, is guarded by at least one such Cyclopean sentinel, 
and one stands by Death’s Door at the extremity. South of Little 
Sturgeon Bay, this formation lies a little back from the rocky escarp- 
ment that faces the Green Bay valley, and its strata are beveled down 
to the general surface of the country, so that it displays itself less 
conspicuously. The belt which it occupies at the surface lies next 
east of the Mayville beds as far south as Washington county. South- 
east of Fond du Lae, it again comes out to the margin of the valley above 
referred to, and forms the white cliffs in the towns of Empire, Eden, 
Byron and Oakfield. In this region, the base of the formation is thin 
bedded, while in the upper portion, the beds are thicker. South of 
this, the formation again recedes from the chain of ledges, and, at a 
very unfortunate point is lost beneath the drift of the Kettle Range. 
This drift moraine crosses the strata under question obliquely, and ef- 
fectually conceals them from view for thirty miles. On the other side 
of the range, the beds at Pewaukee are the nearest exposed rock east 
of the Mayville beds. 

The upper strata at this point are very similar to the Byron beds 
in color, texture and composition, but in fossils, they are closely rela- 
ted to the Racine limestone, while the Byron beds contain but few 
remains of any kind, and are separated from the Racine by the Coral 
beds, containing an abundance of fossils, less closely related to the 


NIAGARA LIMESTONE. 847 


Racine fauna than those of the Pewaukee beds, so that there is here 
presented a novel and interesting question of equivalency, that will 
be more fully appreciated when all the facts are before us. 

The strata under consideration are designated Byron beds in this 
report, only so far south as they maintain their distinctive character. 
They have been regarded by some geologists as the equivalents, in 
part, of the Clinton strata of New York. In reference to this ques- 
tion, the attention of geologists is called to the fauna of the Mayville 
beds, which lie between these and the Clinton iron ore beds, which 
shows that there is no good reason for separating these from the Ni- 
agara group. 

Economic Considerations. The purity of the rock of the Byron 
beds admirably fits it for the manufacture of lime. It makes a strong 
and white article, that sustains an excellent reputation. In selecting 
for this purpose, the granular variety is generally to be preferred, 
from its superior purity, and because its somewhat porous nature al- 
lows the carbonic gas that is discharged in the burning to escape read- 
ily, thus facilitating an easy and complete calcination. 

In the towns of Oakfield and Byron, kilns have been established, 
that manufacture an excellent lime, some of which is shipped to the 
Chicago market. To the northward, where the formation is so abun- 
dantly displayed, it is but little burned, as the local demand is as yet 
small, and shipment by water is attended with risk. 

The thicker beds furnish an excellent building stone, either rough 
dressed, for ordinary masonry, or cut, for the finer classes of work. 
In some instances a color as white as statuary marble may be ob- 
tained. 

In the town of Brillion, and less notably at some other localities, 
the strata are beautifully mottled and banded with pink, producing 
a handsome ornamental stone. It is fine grained and close textured, 
though not entirely free from minute pores, and possesses sufficient 
hardness to be capable of taking a fair polish. It will not take rank as 
a high grade of marble, but should find a place as an ornamental stone. 

As considerable sums have been expended on this series of lime- 
stones, in search of marble, it may be well to remark here that this is 
an undisturbed sedimentary formation, lying very much as it did 
when deposited by the ocean, and, while it has erystalized to a large 
degree, there is no evidence that it has undergone any unusual degree 
of heat or pressure, and there is no reason to expect that any portion 
of it will present that indurated and perfectly crystallized character 
that is shown by metamorphic rocks, to which class the better grade 


of marble belongs. 


3848 GEOLOGY OF EASTERN WISCONSIN. 


The thinner beds of this formation furnish an excellent flagging. 
The compactness and fine grain of some layers fit them for litho- 
graphic purposes, but they are apt to be marred by occasional small 

cavities or other flaws. 

Transition Beds. Above the Byron beds, as they are developed 
in the Green Bay peninsula, there lies a series of alternating, coarse 
and fine grained strata, that are transitionary in character, and mark 
the passage from the fine textured Byron beds to the coarse textured 
Coral beds above. They may be briefly described as follows, in 
descending order: 

Beginning at the base of the Lower Coral beds, there occurs ae a 
hard, tough, conglomeritic dolomite, of bluish color, mottled with 
lighter hues, which weathers into creases, rather than pits. It has a 
close, but uneven texture, and contains some argillaceous partings, 
and a few cavities. No fossils were seen except in the upper layer, 
and here only one, not observed elsewhere. This consists of mi- 
nute, vertical, cylindrical canals, somewhat regularly interspersed 
through the rock, but separated from each other by several times their 
own diameter. The general appearance is similar to that which 
would be given if a small, distant-tubed Syringopora were to be en- 
tirely removed by solution, leaving only its external cast in the rock. 
It seemed to be confined to a single layer, which was traced 2,000 feet, 
for the purpose of securing the dip, which was found at this point — 
southwest shore of Sturgeon Bay —to be nearly 80 feet per mile, 
southwestward. 

Below this portion, the rock is uniform in texture, close, compact, 
fine grained, regularly bedded, smooth on the weathered exterior, 
even in fracture, and is of grayish or white color. No fossils were 
observed in this portion. 

Below this, there are thick, heavy, granular beds of coarse, crystal- 
line texture, and irregular hardness, in general, quite similar to the 
Lower Coral beds in lithological characters, but containing few or 
no fossils. The observed thickness of these, taken together, is about 
30 feet. 

Below this, there is more or less of alternation between the thin 
bedded, compact rock, that characterizes the Byron beds below, and 
the thick-bedded, coarse-grained rocks that represent the formations 
above. The conglomeritic layer is the only one that is not, in its na- 


ture, allied either to the Lower Coral beds above, or to the Byron 
beds below. 


NIAGARA LIMESTONE. 849 


LOWER CORAL BEDS. 


A considerable portion of the transition beds just described are to 
be regarded as belonging to this division. The rock of this forma- 
tion is a rough, heavy-bedded dolomite, not unlike the Mayville beds, 
The layers are sometimes very massive, 12 to 15 feet intervening be- 
tween distinct bedding joints. In one case, a brecciated reef-like out- 
lier, 18 feet in height, showed no bedding lines. This massive struc- 
ture is an occasional feature of this formation. 

In texture, the rock is coarse, crystalline, granular, and usually rath- 
er soft. Occasional layers are marked by argillaceous seams and par- 
tings, and by bands or scattered nodules of chert or flint, or by 
silicified fossils. The softer portions usually contain frequent cavi- 
ties, doubtless formed by the removal of fossils. These, together 
with the irregular hardness of the rock, give to the weathered outliers 
a very rough, craggy, pitted exterior. The prevailing color is gray, 
verging toward blue, white, and yellow, at times occasionally en- 
livened by markings of red, pink, and purple. 

Much of the rock is a nearly pure dolomite, admirably adapted to 
the manufacture of lime. Some portions are, however, quite silicious 
or argillaceous, and the discrimination recommended in reference to 
the Mayville beds is to be observed here; indeed, the economic re- 
marks made with reference to that subdivision are generally applica- 
ble here, and need not be repeated. 

Organic Remains. These are abundant and consist very largely of 
corals, among which the genus /avosites predominates. Brachiopods 
are next in abundance, among which Pentamerus is most prevalent. 

The following table shows the leading species and local distribution 
in a compact form: 


350 GEOLOGY OF EASTERN WISCONSIN. 


FOSSILS OF THE LOWER CORAL BEDS OF THE NIAGARA GROUP. 


— iat 
mt . 
oe Se 
RB |x a 
5 a wot Es 
GENERA AND SPECIES. #5 Bs 4 
eG lpea| & 
tet (iG | oS 
mS a) 
PETROSPONGIA 
Stromotopora concentric. ..+-6. ceeeeeeereee per 
CORALS. 
Favosites favosus ....+++++++- sadnednee eh ea Jan aa as 
F. Niagarensis ... ......0+0sseceeeeee eee EP eh BE 
Astrocerium venustum......eseeeeeeee cerns cefecsedees 
Halysites catenulatus ....... . sess eee neers a | * : 
H. catenulatus var., microporus, n. var.....- ned [eis 
H. catenulatus var., macroporus, n. var...-- dag leas 
H. agglomeratus .. 00.0... cece eee ee eee ames 
Diphyphyllum cespitosum......--.- -.++ +: pealee4 
Syringopora Dalmani ......-..----e seer eee oes 
i, MING, BPs dcotuare saan. walbnd Ayeratatoun dared aye otiene - 
Cystostylus typicus, n. gen. and sp. ...---+-- 46 
Cyanthophyllum, und. sp.....-..-++e. seers ah 
Amplexus, und. sp.......-2eeeeeeeee cee 7 * 
Zaphrentis, und. sp. ......2eseeeeee ceeeeee eanlt Fp 
Aulacophyllum, und. sp. ..-. sess eeee ee eens 48 
Chonophyllum, und. sp.....-..eeeeeeeeeeeee : 
BRACHIOPODA. 
Dinobolus Conradi ........-+.0+seee esse ee eee ge4e| oS fatee 
Trimerella, res. T. grandis......+..--..++.+0- Pea a ee 
Meristina, Und. SP... ese ccscncie estes eee inee dees was at |e sie 
Pentamerus bisulcatus...............0000000 en en eee 
PR. (OblONGUsa sas rtie Seeks ey toe cake tata teas * loves] # 
P.. VONGCOSUS: | caecesoc tase ses thee ee ees meee leeael: oF 
Siricklandiniscs.ince aga seeds ease weexene s * 
GASTEROPODA. 
Straparollina, und. apc) issc.2ssarvecenasase ss ee ie 
Trochonema, und. sp.............. seh th Het Gti yaa = 
Pletrotomaria, Nesp. sestca ssodiaaetsee.a se Se tered SE 
B.. und: Spars eawen eemmewey emer Ades pace te Saya) 
Murchisonia Hercynia ......-..-..eeeee eee eee ea ead 
Bucania trigonostoma....-...eee cece ee eee ee er es 
CEPHALOPODA. 
Orthoceras abenwits.) cscceeoesccsaie aciwnces oe eee Por 
0: Onds SP waaeenwmanyncat gases suduatee secu serena | 
Discosorus conoideus ....... 0... c cee eee eee Petes) 
CYTOCePAR weve sanunneanaasnsiasovieraciaccies etal 
Phragmoceras labiatum, u. sp..--+-e-.2.s0eee * 
CRUSTACKA, 
lenis), und), sPsseeveiersearniec western wed |neen # 


| Cato (Mendhks). 


* ee 


al 

f= a 

g| 4 

n a 

S/ Ele 

£ & & 

OIM|A 

x 

* wee cae 

x | « | * 

* wee 

* * 
7 

lee slnaies 

* woe es 

- * | 


NIAGARA LIMESTONE. 851 


It is difficult to state definitely the thickness of this subdivision, 
for, as already seen, its lower limit is not well defined, and it is equally 
difficult to fix precisely its upper boundary. 

The greatest thickness, directly observed, was 48 feet, but this does 
not inelude any of the transitional beds, and probably not all others, 
as the section was incomplete. If we include that portion of the beds 
of passage below and above, which is most nearly allied to this divis- 
ion, the maximum thickness will be about 70 feet. 

This formation is very closely related to the Upper Coral beds, and 
the distinction between the two is less marked than that between the 
other subdivisions of this group. It will therefore be a matter of con- 
venience to describe the Upper Coral beds, and then consider their 
extent and local developments conjointly. 


UPPER CORAL BEDS. 


These beds directly underlie the Racine limestone at the north, and 
are separated from them by a sharp line of division, readily distin- 
guishable wherever observed. 

The rock is a rather thin bedded dolomite, generally of a buff color, 
as seen in exposures, but, in its unweathered condition, often grayish or 
bluish. It is usually suberystalline, of fine grain, compact, and hard, 
but occasionally earthy. It shows a tendency to split into irregular 
rudely lenticular flakes. It contains much silicious material in the 
form of chert, flint or silicified fossils. The chert is usually white, 
and in the form of nodules, but graduates into dark, translucent vari- 
eties, which pass into flint, resembling that of the chalk beds of Eng- 
land. The carbonate of lime, that originally constituted the material 
of the fossils, has been replaced in many cases by a whitish, chert- 
like material, and in others by translucent and transparent forms of 
eryptocrystalline silica, while the cavities are drusy with quartz. 
Silicified fossils are more common than the unchanged form, and on 
weathering, these project from the surface, giving the rock a very 
rough, harsh exterior. The stone is of little value for construction or 
lime. Some layers make a tolerable flag. 

Organic remains are exceedingly abundant in this formation, among 
which corals mostly predominate. About thirty species were collect- 
ed, and many of these occur in great number. ‘The state of preserva- 
tion is often very fine, owing to silicification. The more important 
localities are tabulated below, and a full list of species and their range 
will be found in the general table of fossils of the Niagara group. 


852 GEOLOGY OF EASTERN WISCONSIN. 


FOSSILS OF THE UPPER CORAL BEDS OF THE NIAGARA GROUP. 


GENERA AND SPECIES. 


aunee, 8. 14. 
Scarboro Creek, T. 24 


R. 24, 8.30. 
T. 24, R. 24, 8. 28, 


| Cato, 8. 27, N.E. qr 
| Cato, Clark's Mills. 
| Cato, 8. 5, N. E. qr. 
| Gibson, Smith's ledge 
| Sturgeon Bay, T. 27, 


| Forrestville, 8. 17. 
R. 26, 8. 9 
| Bailey's Harbor. 


Cato Falls. 
| Kew: 


PLANTA, 


Buthotrephis, undsp.... -... sravall esesehe!|eseuels, | Omeeae eaasvsel @ wecelleae el aces 


PETROSPONGIA. 


Stromatopora concentrica..... Bec lecaysna| Oe ms 
S. und. sp....... Assessor Uctvatell eng cited tease Susaee lela Gasser 


' CORALS. 


Favosites favosus......+..eee+ A osctia| leech F liorealtewau |) 
F. Niagarensis added aeall Bees: Bees 
F.  favosus,var.with larger cells}....}....|....feee-[.... [eee efeeee| * 
Be WHY SPiv eine ain eencocoremsimsieveres ei...) # f..ef ll] | oF | * 
Astrocerium venustum........ Peer eee (ee 
Bes WAGs BBieiniecers cele rcarevelarein siete] TE | levewvond oreeil| v's capil evasion bell ahaae der eee alfissereca tageese 
Michelina? undes. sp......... da dal deseaeus ly oeerd eiortpalte Sea eee andl uaeel| gators [ante-allsras aces 
Alveolites, und. sp........... ete fccuads tioned cttee lt oS ail weal Stall) ae eS 
Halysites catenulatus Drahnunerasela Deka lmoetiemwalingeealy AP (Mh a cead ance anaes leeoell ae 


*¥e xX * 
HX XH * 


H. var. microporus ......+4. stale eee O eral eed Mathias fond allteS sce 
H. ct ea bh tecdeasien ta Veal VR acral tetes| batons Sra town lacie vee a ee all gra 
FA. “MMs, Bis. s/2 aie oe ain eels dae aioli esx hacehead |taetegel ioe aie be arr acevo acae aes ase roll 
Halislites pprlornaia ba GES EER stale oiaif ears. |e 8 ed scars beaterallt crore Bd bape Fe 
Thecia, und. sp. with small cells]....)....)....].---] ® Jo...f..../..../ * | * 
Aulopora, und. sp......+...6- siesta coed [c. @a ca iecaval wteters [ac stare ete eallaauane [wate si esoets 
Cladopora reticulata.......... Scakeaa bie, Scelecscnle [ese ire) crdredefarnrs-S | malaealy dxayia| ee Ie 
GC. Und apis axe etaswaee se Gave Bua Scallle.oduallt avaral|stira Levea-al|in satel ia cillageotel| 2 
Syringopora compacta ........ isabel is exalieee a [peeu eee sf cow ale assent’ HF. Heaece| 5 
S. Dalmani sccasec tecoca HM acclceny|ducle|| Mi WadaalecsismaieMe. Ty © 
Cyathophyllum, und. sp...... Sess bentinceeevelp “OR I eg Herateeel adios gi OM | eabacallatecess 
Zaphrentis sp. res. Z. gigantea |....J}..../....J.---]....{ * f..../....] * 


* Hof 


K.. Und, Sprseorssaviassonaa Nose | RP Te de ae Toll [Ly 


* 


Aulacophyllum, und. sp....... piesk | neo. deolft da celles aoabararecall oaae lia aa 


Amplexus fenestratus, n. sp... sO an | podlecsr avulyew Weel deco ltise? 


A, “Und. 8p. vi cane ceed sey Hees egal OE few eu OF 


Streptelasma calyculum....... ena lentoeasall, MP iets dM lig ua liens exon sbeciac 
Chonophylluim, und. sp....... cael F- Neeallectalleweel F esae| ORY | OR 


Cystiphyllum Americanum....]....] * 


Gr Niggarenie wesseseesss. TED eel aes Bel ree Ba 


Gy Ud Bp. hea hasan n kee cedsleeeeleeealaeerlececlecedlhesabesnc[eea | 
Strombodes pentagonus ...... sco ay| eokballnaeallecs aval 4 ocalvesere | 6 dpa | 


Diphyphyllum czespitosum . . AS ies ree ine) [eee ae Sascatl nese ldeadt wey 


Cystostylus typicus, n.sp.. .-| * |....)....[..--f... sh eeel ce cleeeclecee | ® 
(ironies UMA we nican teria clyudalexgeluc dhvcalesetlecedlec ke. ay 


NIAGARA LIMESTONE. 353 


FossiLs OF THE UprER Conan Beps or tum Nragara Group — continued. 


ui . o th 
ae eae wees 
Ale) ja lSlae [S86 |, 
. fs 5 . Sa 
A | ‘a alala fes|%|4 esl 4 
GENERA AND SPECIES. ele tale lal silane] g Bo 4 
al/O|S la) al 8 isxi= |S [ssl 2 
sloleltelé| 8 lBSiai Bla ® 
S/8)/8/83/ 2) F ae a] # q s 
os eS 3 S | ia o/138 : is] am = 
ClOlOlO;/olM lA H) & ja a 
BRACHIOPODA. 
Orthis flabellula............. Hiateales salted “EX Vecwcelosealle oeelleaaa'| oe Ie athena 
Strophomena, n. sp.... .....- ew aliaealrcoateelece ol! Locus cesdae ase leamd ns 
Atrypa reticularis........ ... oe elavnual BE Veksavellaaacern btide'sllats wallace dal 
Pentamerus bisinuatus ....... Rema eeedlacced OE [SB Mey ecle eval GE [a aale eae 
Pe Oblongus: | :essy. av aenees shits ea | SEP iccantis acess hadamalt PE | 2S eel neta) SF 
P. ventricosus.............. hee Ray ecal| A | ctenalbesesal worse [aneterc aos nea ales 
Bip Nesp keacees uate cnet aa leae lees wile aalvseal see. |\ 2 Sees| sevslaeesles as 
Stricklandinia, n. sp ....... Fei bees ince ad ataiail a ia erateymal sane [i A 1 (ees eae Ol en ate sees 
Ds UNG SPijenee vases ssgeisians biases ofas 2| Samia) a vale oA vada tere |) OP 
Rhynchonelloid shell..... .. * 
GASTEROPODA. 
Loxonema,..iscisseiswursalees iesatesisesw ell oR 
CEPHALOPODA. 
Orthoceras, und. sp........+.. soarefeicealocarl| eiedlerveltsesfosaa| OF * 
CRUSTACEA. 
Illeenus, pygidium ofan und. sp.|....[..0s{eee efor epee efeeeelececfeseefecealeoee] * 
Bronteus Acamas ...-..+-+.05 sites | FD | rae fea alike.) seats seleaaleniccs[ tas aesiew 
INCERTA SEDES. 
Huronia annulata........... * | ox 


The greatest thickness of this formation actually observed is 75 
feet. Its maximum thickness is estimated at 90 feet. 

Distribution. Beginning at the north, we find the central, and, to 
a great extent, the eastern portion of the Green Bay peninsula occu- 
pied by the Coral beds, the lower division, of course, lying to the 
westward. Extending southward, they constitute an irregular belt, 
occupying a median position on the Lake Michigan slope, and ceasing 
to be traceable as distinct subdivisions in the southern portion of 
Fond du Lae county. 

Local Details. Near the eastern entrance of Porte de Morts, the coral beds pre- 
sent themselves in vertical cliffs, facing the lake. The exposure belongs chiefly to the 
upper division, and presents, in certain portions, more than the usual amount of cherty 
material. In general, the beds are highly fossiliferous. Silicified specimens of Penta- 


merus oblongus, of rare beauty, are occasionally met with. 
At Bailey’s Harbor, the Upper Coral beds are exposed in nearly their entire thick- 


Wis. Sur. —23 


854 GEOLOGY OF EASTERN WISCONSIN. 


ness, constituting three terraces, rising in succession from the lake shore. ‘The ledges 
here are extremely fossiliferous, and this locality is already known in the literature of 
the science. The uppermost ledge is capped by a few layers of the Racine limestone. 
South of Jacksonport, along the lake shore, the Upper Coral limestone is again ex- 
posed, presenting a thickness of twenty feet, with its usual characteristics and abundance 
of fossils. 

In the vicinity of Sturgeon Bay, several exposures, both of the Upper and Lower beds, 
oceur. In Sec. 9, there are several slight outcrops of the upper strata, which are here, 
ag usual, quite cherty and contain an abundance of silicified fossils, among which the 
coralline forms predominate. In Sec. 5, near the village of Sturgeon Bay, the upper 
portion of the Coral beds have a slight exposure, overlaid by a few of the Racine beds. 
The junction between the two is here sharp and well defined, the uppermost layers of 
the Coral beds being highly fossiliferous, a fact which does not seem to be universally 
true, as at several other points the beds lying immediately beneath the Racine lime- 
stone are comparatively free from fossils. North of the village, near the mill, the Lower 
Coral beds are shown imperfectly, but in considerable thickness. Still farther north, 
along the cliffs facing the bay, at various points, partial sections of the same beds are 
exposed. On the opposite side of the bay are numerous partial exposures of the Lower 
Coral beds overlying the Byron beds. Following the outcrops of the formation south- 
ward, Greening’s ledge, in the town of Forrestville (8. W. qr. Sec. I7), is worthy of 
note for the remarkable abundance of fossils which it presents. Passing by several 
minor exposures, we find, on Scarboro creek, in the town of Casco, and in Sec. 28 of the 
town of Pierce (T. 24, R. 24), the Upper Coral strata presenting their usual thin, irreg- 
ular, cherty outcrops, and characterized by an unusual abundance of well preserved 
silicified fossils. The latter locality is remarkable for the great number of Favositoil 
corals, large masses of Syringopora, and frequent specimens of Strombodes, in associa- 
tion with an abundance of the more usual forms. In Sec. 14, in the town of Kewaunee, 
at the mill of Mr. Stramsky, the uppermost layers of the Coral beds are found immedi- 
underlying the Racine limestone. They are here more homogeneous and less cherty 
than at most localities to the northward, and much less fossiliterous than the corres- 
ponding beds at Sturgeon Bay, only five or six species being observed. In the valley of 
West Twin river, several notable exposures of this formation occur. In Sec. 28, town of 
Gibson, a vertical thickness of about forty feet, belongmg to the lower division, is ex- 
posed. The upper portion of the ledge consists of very heavy heds of coarse, rather soft 
dolomite, characterized by fine specimens of coral. The lower portion of the ledge con- 
sists of a harder and more compact rock of finer texture, very prolific in Pentamerus. 
In the vicinity of the junction of Mud creek with the West Twin river, particularly in 
Sec. 18, Cooperstown, ledges that appear to represent the transition from the Lower 
Coral beds to the Byron beds find ample exposure. The following section is observed 
near the center of Sec. 13. 


1. At the top, a broken, grayish white dolomite, mottled with pinkish 
red, of porous, rather hard, brittle, crystalline texture and uneven 
fracture, in beds of 18, 11g, 15 and 1314 inches, respectively. The 


lower layers are more compact than those above...............065 4 ft. 10 in. 
2. Harder laminated dolomite, of slightly porous texture, gray, lined 

WIth Pilko. ss hese Gapa saves eet eueTeteeeesyssaxe es aaeeaam vais 1 ft. 5$in 
3. Similar to No. 1, but more coarse and porous in texture, and rougher 

ii General ABPCCl. casa Peace ese Poa eas ed can Doane a darned 2 ft. 2hin. 
4, Similar to No. 2, but not distinctly laminated. In beds of 714, 12 and 

Tl anches respectively.:cc. vetese ei ievessanaa dex anaes ca deatied uns 2 ft. 63 in, 


uv 


5. Rather soft, granular dolomite, of sandy appearance, streaked with 
white and yellow, and distinctly blotched with copper red...... .. 6 in, 


NIAGARA LIMESTONE. 355 


6. Rather hard, compact dolomite, mottled with purplish, pink and 

white, containing a few very small drusy geodes. Weatherssmooth, 1ft. 6 in, 
7. Coarsely porous dolomite, of uneven texture, prominently mottled 

with scarlet, pink and purple, and containing corals and drusy 

geodes. Marked with stylolites........... 0... cceecceecee ee wees 2ft. 3 in. 
8. Rather hard, firm, laminated dolomite, rather thin bedded, having a 

brittle, uneven fracture. In successive beds of 934, 13, 9, 13, and 

OMG INCHES s sae cuwanea ax cere ye edseeeacd fist seed ee sedans onde cane 4ft. 2hin, 
9. Very fine grained, compact, flint-like dolomite, of smooth, hard, semi- 

conchoidal fracture, and bluish and yellowish gray color. In beds 

of 11, 744, 444, 5, 346, 41%, 9, 614, and 7 inches respectively....... 4 ft. 103 in. 
10. Compact, but more granular crystalline than the above, of whitish 

gray color. In beds of 9; 6, 9, 81g, 219, and 11 inches, the lowest 

of which is banded with purple...... 00... 0... cece ee cece ese cece 3 ft. 10 in. 


In the vieinity, higher and more fossiliferous beds find linited exposure. In Sec. 25 
of this town, there is a peculiar outlier of 181 feet vertical exposure, presenting nv 
well-defined bedding. The rock is a rather hard, coarsely brecciated, light colored 
dolomite, weathering very rough, and containing few fossils. It resembles some of the 
brecciated portions of the Lower Magnesian limestone previously described, but more 
especially the reef structure ‘of the Racine limestone, yet to be considered. 

Passing by a number of minor outcrops in this vicinity, in Sec. 5, of the town of Cato, 
is a notable ledge arising to the height of 46 feet, which consists of heavy, regularly 
bedded dolomite, of coarsely brecciated structure for the most part, but, to some extent, 
coarsely granular, and containing abundant cavities of various sizes, often filled with 
calcite, many of which are evidently the result of the entire or partial removal of fossils. 
Corals are present in abundance. In the N. W. 44 of the N. W. 24 of the same section 
is an isolated ledge of somewhat similar character, but rather more thin-bedded and 
compact, and differing from the former in the presence, in some layers, of much chert, 
in which fossils, most beautifully silicified, are abundant, Pentamerus oblongus being 
the predominating form. In Sec. 6 of the same town, on the farm of Mr. J. Mendlik, 
is a conspicuous ledge, consisting of very heavy bedded, rough, inegular dolomite, of 
varying hardness, usually rather soft, brecciated for the greater part, white or gray 
in color, and variously mottled and streaked with pink. The structure is very irregular. 
The rock contains many corals, especially those belonging to the genus Favosites, and 
a few other fossils. 

Another noteworthy ledge occurs near the middle of the south half of Sec. 36, town of 
Richland. The following section, in descending order, was noted at that point: 


1. Hard, white, compact, somewhat cherty dolomite, containing occa- 
sional cavities, and showing a slight tendency to separate on the 
weathered surface into thin beds...........0. ee ceee eee cence eee 10 ft. 

2. Hard, grayish white dolomite of uneven texture, and subcrystalline, 
irregular fracture, marked by numerous argillaceous, lamellar part- 
ings, and a few geodes. Weathers irregularly into deep pits. In 


layers of 3 feet 4 inches, 2 feet 6 inches, and 3 feet..........+...-- 8 ft. 10 in. 
3. A softer and more granular stratum, containing Cyathophylloid corals, 
which were not observed in the upper beds....----. ++: eeeeee cree 3 ft. 2 in. 


4, A stratam of irregular, grayish white, shaly dolomite of uneven tex- 
ture, which weathers into rough creaseS......+++eee sree ee eeerees 4 ft. 


396 GEOLOGY OF EASTERN WISCONSIN. 


5. White, rather soft, granular crystalline dolomite, of more even tex- 

ture than the above, and better suited for cutting. Weathers smooth. 

In layers of 10 to 13 inches........ cece cece cece ee eee eee n een e ee 2ft. 11 in, 
6. Vnin, regular bedded, white, granular crystalline, rather soft, some- 

vhat shaly dolomite, in layers from 3 to 9 inches in thickness, par- 

tially concealed .......... cee ce cece enter e cere een een eeeaee 3 ft. 9 in, 
7. Pure, opaque white, saccharoidal dolomite, of medium hardness and 

even texture, weathering comparatively smooth. In layers of 13, 

16, 17, 36, 16, and 10 inches, which occasionally unite or subdivide. 9 ft. 
8. Granular crystalline dolomite, of medium hardness, somewhat un- 

even texture, white and pale orange color, mottled and mingled. 


Layers not always well defined.........--eeeeee eset eee etn ener ees 6f. 6 in. 
Motal Pi saies hoReid dina weceas eke sss eROe av tao ts Hast elas 48 ft. 2 in. 


At Cato Falls, on the Manitowoc river, thinner and more homogeneous beds, belong- 
ing toa higher horizon, appear in undulating stratification. At Clark’s mills, two 
miles below, similar thin beds, in broken ledges, form a wall along the bank of the river, 
rising from 10 to 15 feet in hight, and are characterized by abundance of corals of the 
genus Farosites. Near the old mill, a short distance below Clark’s mills, on the left 
hand side of the river, occurs a slight outcrop, the top of which is very cherty, and con- 
tains silicified fossils, the most conspicuous of which is the remarkable Cyathophylloid 
coral, Amplecus fenestratus, u.sp., which attains a foot or more in length, and two or three 
inches in diameter. A short distance down the river, from 20 to 25 feet of impure, brec- 
ciated limestone is overlaid by about 12 feet of cherty rock containing the above men- 
tioned coral, the whole, from its hardness, giving rise to the rapids. It is worthy of 
note that these two localities are the only ones at which the above fossil has been found. 
South of the Manitowoc river, the formation is overlaid for a considerable distance with 
the glacial accumulations of the Kettle Range, and effectually concealed from observation. 

In Secs. 2 and 11 of the town of Ashford, Fond du Lac county, the railroad exca- 
vations again bring. the formation to our notice. In the former section, the rock is 4 
sott, yellowish dolomite of irregular texture and bedding, and is specially interesting for 
the variety, abundance and peculiarity of its fauna, as will be seen by reference to the 
table. The cut in Sec. 11 presents a rock whose lithological characters are not essen- 
tially different from the preceding, but which contains a very great abundance of Penta- 
merus oblongus, in great variety of size and form, and an almost entire absence of the 
fossils which characterize the preceding location. At the village of Elmore, in the samo 
township, a quarry exhibits a heavy bedded rock of much more firm and homogeneous 
texture, the sole, but abundant, fossil of which is Pentames wus oblongus, in unusually largo 
and fine hae, 

In the N. W. 1j of Sec. 6, in the town of Kewaskum, at Kuhn’s quary, is a porus, 
granular, ceeteitne dolomite, containing an abundance of Favositoid corals and Penta- 
mverus oblongus, and probably represents the horizon of the Lower Coral beds. South- 
ward from this point, the formation is lost under the Kettle Range, and we do not again 
sec it, or what may be supposed to be its equivalent, until we reach the vicinity of Pe- 
waukee. On the Sheboygan river, at the village of Rockville, there is a slight expos- 
ure of the upper portion of the Upper Coral beds, presenting a more than usually dark 
gray color, with more or less of chert, and containing but very few fossils. The drift 
in the vicinity, however, is prolific in those species which are so abundantly present far- 
ther to the north. 


NIAGARA LIMESTONE. 85T 


WAUKESHA BEDS. 


The term Waukesha limestone was selected many years since by 
Dr. Lapham, to designate the thin bedded strata that occur at Wan- 
kesha, and their equivalents elsewhere. This term was also adopted 
by Prof. Hall, in the report of 1862.2 It seems therefore desirable 
to retain a name that has already become fixed in the literature of the 
subject, althoagh we shall be compelled to restrict its application, and 
to entertain, to some extent, different views as to its relations. 

There are at Waukesha three classes of limestone. In the quarry 
near the college, the upper fourteen feet consist of a soft, yellowish, 
coarse-textured dolomite, that has been identified with unquestioned 
correctness, as the equivalent of the Racine limestone. This reposes 
upon regular, even beds of a hard, compact, fine-textured, crystalline 
dolomite, of gray color and conchoidal fracture. It is characterized 
by the presence of much chert in the form of nodules, distributed 
chiefly in layers, coinciding with the bedding joints. These strata 
abound in Orthoceratites, but contain few other fossils. They consti- 
tute the type of the Waukesha beds, The transition to the Racine 
beds is quite abrupt, but does not correspond to a bedding joint. 
From three to four inches of the base of a thick layer are of compact 
rock, like that below, while the remainder has the open texture and 
fossils of the Racine beds. 

Passing by several intermediate quarries, for the moment, we find 
at the lime kilns, two miles above Waukesha, a fine display of the 
Racine limestone reposing upon similar cherty flags, which form the 
sole of the quarry. The transition is accomplished in a manner pre- 
cisely similar to that above described. 

In the road, south of this quarry, the porous Racine rock appears, 
but one hundred yards beyond, and at the same elevation, oceurs a 
light colored, hard, compact, close-grained, suberystalline dolomite, 
resembling closely the Waukesha flags, except that chert is absent. 
A few rods further, a quarry has been opened, exposing these strata 
more satisfactorily. In addition to the close textured rock, there are 
layers of mottled blue and white color, and irregular, lumpy struc- 
ture, such as are associated with the even-bedded rock in the vicinity 
of the Niagara reefs near Milwaukee. Several openings follow at 
short intervals, including the main quarry of Mr. Hadfield, all of 
which exhibit the same character. This is also true of the several 
quarries on the opposite side of the Fox river. T have elsewhere dem- 


1See Owens’ Geological Survey of Wisconsin, Jowa and Minnesota, p. 455. 
2 Geology of Wisconsin, 1862, pp. 56-64; also note on pp. 446-448. 


858 GEOLOGY OF EASTERN WISCONSIN. 


onstrated that the coarse, open-textured Racine limestone graduates 
horizontally into a precisely similar compact rock, and am therefore 
inclined to consider the weight of evidence as favoring the conclu- 
sion that such is the case here. In this view, the flags and thicker 
even- bedded rock, on either side of the Fox river above Waukesha, 
would be regarded as belonging to the Racine beds, being the strati- 
graphical equivalents of the coarse-grained Racine layers. The only 
undoubted members of the Waukesha beds are, then, the cherty flags 
near the college and at the kiln. 

Farther up the stream, in Sec. 31, Menomonee, similar cherty flags 
make their appearance, and they also occur in the drift at intermediate 
points. 

At Pewaukee, the upper strata consist of a white, fine-grained, but 
porous crystalline dolomite, having a conchoidal fracture. In this 
portion occur the crinoids Caryocrinus ornatus, Hucalyptocrinus 
crassus, L, colatus, E., n. sp., and the trilobites, Z2le@nus Loawus and 
L. pterocephatus, n. sp., in association with several Orthoceratites and 
other fossils, thus manifesting a noticeable affinity to the Racine 
fauna. 

The lower layers at this point are more argillaceous and silicious, 
and of more irregular texture, with patches of cherty material. Ha- 
lysites, Favosites and Pentamerus occur in these beds. In one por- 
tion of Mr. Pelton’s quarry a layer is almost entirely composed of 
a large Pentamerus oblongus, imbedded in white dolomitic material, 
forming a rather heavy bedded rock of uneven texture. It lies near 
the base of the quarry, but from its situation and the undulating na- 
ture of the strata, its relation to the impure layers above mentioned 
are not apparent. It is quite possible that, as suggested by Prof. 
Whitfield on paleontological evidence, the upper portion belongs to 
the Racine, and the lower to the Waukesha horizon. The list of fos- 
sils, collected at this ponit, is as follows: Stromatopora concentrica, 
Favosites favosus, Astrocerium venustum, Halysites catenulatus, Za- 
phrentis, Omphyma, Caryocrmus ornatus, H'ucalyptocrinus crassus, 
Lf. celatus, E., n. sp., Streptorhynchus subplanum, Strophomena 
rhomboidalis, Spirifera nobilis, Meristina Maria, Atrypa reticularis, 
Pentamerus oblongus, P. ventricosus, Orthoceras annulatum, O. 
alienum, O. medulare, O. crebescens, Gyroceras Hercules, Gomphoc- 
eras nautilus, n. sp., Lilenus Towus, and I. pterocephalus, n. sp. 

An interesting feature of this locality is a mound of rock lying a 
short distance west of the main quarries which rises ten or twelve 
feet above its base, and has a diameter of only a few rods. It con- 
sists of very irregular beds, coalescing promiscuously with each other 


NIAGARA LIMESTONE. 859 


and dipping irregularly in all directions. The rock is, for the most 
part, hard, compact, white, and, in some portions, cherty, and con- 
tains a few Brachiopods. It evidently owes its origin to irregulari- 
ties of deposition and not to upheaval. 

Johnson’s quarry in the town of Genesee, presents a vertical 
exposure of more than 25 feet, of a beautiful white, fine-grained 
dolomite, in beds of 20 inches thickness and less, having an eastward 
dip of one foot in sixty. Near the base a layer possesses the mottled 
color and uneven texture above decribed. Fossils are rare in this 
location. A few rods distant on the opposite side of the road, a 
quarry displays very similar beds, but they are rather more por- 
ous in general and abound in chert in certain layers which is 
rare or absent at the former locality. They are also more fos- 
silferous, though not abundantly so. The following species were 
collected: Of Crinoids, Caryocrinus ornatus, Eucalyptocrinus 
crassus, und FE’. celatus; of Brachiopods, Orthis flabellula, Spirifera 
plicatella, Atrypa reticularis, Rhynchonella Indianensis; the Gas- 
teropod, Platyostoma Niagarense,; of Cephalopods, Orthoceras an- 
qulatum, O. alienum, O. columnare, O. medulare, O. n. sp. Cyr- 
toceras Orcas, Gyroceras Hercules, and the Trilobite, [llenus towus; a 
a fauna very closely resembling that of Pewaukee. 

In the rise of the hill, immediately to the east, the typical, yellow, 
eoarse-grained Racine limestone appears, as it also does in the adja- 
cent ridge on the south. It is probable that many of the prominent 
hills in this region contain a core of Racine limestone; though deeply 
overlaid by the almost universally prevalent drift. 

Closely allied strata occur at Castleman’s quarry, in the town of 
East Troy, but no distinct fossils were found. The locality is widely 
separated by deep drift from all other outcrops. 

Returning to the vicinity of the typical locality in Waukesha coun- 
ty, we find in Sec. 34, of the town of Lisbon, a formation that may be 
said to be identical in character with the upper strata at Pewaukee. 
To the east and northeast, in that and the adjoining town, are numer- 
ous openings upon white, or light colored, fine-grained, even bedded 
dolomite, with few or no fossils, which renders their place in the 
series somewhat doubtful. 

As the horizon of the Waukesha beds is traced northward, it plun- 
ges beneath the deep drift of the Kettle Range, and on emerging be- 
yond, the Byron beds and the Upper and Lower Coral beds are found 
to occupy the space between the Racine beds above and the Mayville 
below. The cherty flags at Waukesha most closely resemble the up- 
per portion of the Upper Coral beds, which occupy the same strati- 


360 GEOLOGY OF EASTERN WISCONSIN. 


graphical position beneath the Racine strata, but nowhere in the 
southern counties is there manifested that abundance and variety of 
coralline forms that distinguish the formation to the northward. 
The Pentamerus beds at Pewaukee bear a closer alliance to certain 
members of the Lower Coral beds than to any other member of the 
northern Niagara series, while the white, compact, chertless beds bear 
so striking a lithological resemblance to the Byron beds, that they 
have been sometimes regarded as equivalents. But to satisfy all these 
affinities would be to impose incredible, if not impossible, demands up- 
on the stratigraphical relations of the southern members, besides, the 
affinities are not by any means unequivocal. 

The facts seem to be that in this case, as with the lower formations, 
the deposits in the southern counties differ from the corresponding 
ones in the northern counties, and that the Waukesha group of strata 
is the equivalent of the three more ponderous northern members that 
lie, like it, between the Mayville and Racine horizons. 

On Plate X of the accompanying atlas, white lines have been used 
to designate, in a general way, the surface area of each of the sub- 
divisions of the Niagara group. Within the spaces included be- 
tween these lines are often limited — and occasionally considerable — 
areas of a higher member occupying the summit of prominences, or 
of a lower member, reached by deep erosion. Within the general 
area of the Waukesha beds, patches of Racine limestone occur, as al- 
ready cited in Genesee. The white lines for this subdivision were 


drawn so as to include all of the known cherty flags belonging to this 
horizon. 


RACINE BEDS. 


Overlying the Waukesha beds at the south, and the Upper Coral 
beds at the north, is a magnesian limestone to which the term Racine 
has been applied, from its important development at that point.’ It 
has an extent of about 200 miles, reaching from Illinois to near the 
extremity of the Green Bay peninsula, and attains a surface width of 
thirty miles. In its southern portion, where it rests upon the Wau- 
kesha limestone, it consists of reef-like masses of conglomeritic rock, 
which, on the denuded surface, appear as mounds or ridges, and which 
graduate into various kinds of porous, granular, irregularly bedded 
rock, or into fine grained, compact, even-bedded strata, the whole con- 
stituting a formation of exceedingly irregular structure. In its 
northern portion, where it reposes on the Upper Coral beds, it pos- 
sesses a much more uniform character. On account of these pecu- 


1 Report of 1862, p. 67. 


NIAGARA LIMESTONE. 361 


liarities, it is thought best to depart from our usual order of deserip- 
tion, so far as to vonsider, first, the local peculiarities of the formation, 
after which we may, with more satisfaction, indulge in generalizations 
and draw conclusions. 


Local details. At Racine, whence the formation takes its name, as exposed at the 
rapids of Root river, it is a blue, gray or buff, brittle dolomite, having a somewhat glassy 
fracture, suberystalline structure in part, and earthy in part, and contains many geodic 
cavities, filled with calcite and pyrite, and sometimes mammillary deposits. Its texture 
is uneven, being sometimes granular and again brecciated, usually coarse and porous, 
but sometimes fine and compact. It is frequently stained with iron oxide, and, in places, 
is quite pyritiferous, especially in the fissures. The bedding is also irregular, but usually 
rather heavy, ranging from five feet downwards. In the south quarry at this point, be- 
longing to Mr. Horlick, there is a small mound of highly porous blue rock, without vis- 
ible bedding, full of fossils, from which it doubtless had its origin, after the manner of 
reef formation. It is surrounded on all sides hy bedded rock. ‘The dip at this point is 
varying in amount and direction, as shown by the following record of observations in 
different parts of the three quarries near the rapids: 


EAST QUARRY. 


Dip Sh. Direchion et weisa Gide hl vote ecieaenameem ene N. 47° W. 
Dip 7°. Mie” tient tae 5 nfo GaGa dahana leds ces ancyeaei tu Suaan a avtad seat ge eae a N. 40° W. 
Dip 1°. KC) C lenaleeuiotslneds tne ape h aoe eV EE Ree N. 55° W. 
Dip sigs, (Sh Sickest eetoask SOR Rares Ce ere ee W. 45° § 
WEST QUARRY. 
Dip 5°; Direchoniss 4 w.1504 209 somone a teen suet oe aa seminaries N. 65° W 
Tipe.  8~ “axcaloan omc debe anaheieenemenimeieeanseiae N. 11° W. 
Dip 2°. MISS? 5 Toca ageaa stave use bane wears etiam saasie easmeanas eae N. 30° W 
Dip 1° WE 0 ic stheniylled. abso niin ain apsincesaeaueaaanioe: N. 63° W 
NORTH QUARRY, WEST SIDE. 

DipO®.. Directionsy:.<2isscsisseeeeeeeer esta ease cereus Seer eee 
Dip 1°. 1A cia sin Weare ates ada miendudaumtbieenenoaaeeEKE 8. 80° E, 
NORTH QUARRY, EAST SIDE 
Dip 0°. Direction....... cee cee cece serene eee n eect eee nee ences 
Dip 1° TOIT Ay vv ee a he aie ct Aetna iat LD nea cea tina N. 30° E 


It is understood, of course, that these measurements were made in different parts of 
the quarries, and on different layers, and they doubtless do not in all cases represent the 
true dip; i. e., the maximum inclination, as the exposure often did not render the 
demonstration of this possible. But the general fact of irregularity is sufficienty shown, 
and it is to be noticed that the average dip is to the N. W., a direction opposite to the 
general dip of the formation. — 

Fossils are very abundant, in the form of imperfect casts. At Vaughn's quarry, less 
than two miles distant, the first six o eight feet, as it lies in the beds, is deep yellow in 
color, verging to orange and red on the one hand, and to pale buff on the other. Below 
this the color varies from ashy-gray to grayish-blue. The upper layers are apparently 
thinner bedded than those below, though this is probably only the effect of the elements. 
The lower layers are heavier, but do not often exceed a foot in thickness. The beds are 
but obscurely defined, so that it is difficult to trace a given one’for any considerable dis- 
tance, or to ascertain the dip with any precision, There is an almost entire absence of 


862 GEOLOGY OF EASTERN WISCONSIN. 


shaly partings or lamine of clay, so that the chipstone are comparatively free from the 
marly or clayey matter common in quarries. This is only true of the lower layers that 
have not been affected by inwashing from above, and by the immediate action of the 
surface elements. ; 

The vertical joints are prominent, and in some portions frequent, and are usually 
smooth, and coated with calcareous and pyritiferous deposits. 

The rock is porous and geodiferous; the former condition being largely due to crin- 
oidal remains imperfectly preserved, and the latter perhaps in part to the same cause, 
also, the portion removed being the calyx. The material filling the geodes is chiefly cal- 
cite and pyrite, both of which appear in abundant and beautitul forms. The pyrite 
takes the tabular form of crystallization to a large extent, and the calcite seems to pre- 
fer the form known as dog-tooth spar. Crystals of this an inch or more in length are not 
uncommon, 

The rock is quite brittle and sonorous, and presents a saccharoidal appearance on the 
freshly fractured surface of the unweathered layers. A bluish green, argillaceous ma- 
terial is found in obscure, irregular partings. 

In fossils, it is far less prolific than the rock at the Rapids. 

At the quarries belonging to Mr. Trimbone, in the town of Greenfield, Milwaukee 
county, the rock is chiefly a light buff, porous, granular, brittle dolomite, rather soft, 
and in some cases almost friable, and at points disintegrating to a calcareous sand. A 
little calcite in crystals, but no pyrite was seen. The fracture is rough, but usually 
along the line indicated by the application of the force, the manner in which the force is 
applied, rather than the nature of the rock, determining the line of fracture. 

But in the southeastern quarry, the rock differs considerably from the rest, bemg 
harder, finer, more compact, less brittle, and bluer. 

In general, the beds are from 144 to 3 feet in thickness, but readily split into thinner 
layers. The beds, though in general regular and somewhat uniform, not unfrequently 
thicken, and curve, or undulate. Indeed, the last feature seems to be a common char- 
acteristic when any considerable area is considered, so much so as to render any attempt 
to get the general dip, by local observations, utterly futile. These undulations are not 
regular, nor do they present a system, as though due to some common cause, as contrac- 
tion or upheaval, but are in a sense inharmonious with each other. The phenomenon 
arises, doubtless, in irregularities of deposition, and not in subsequent folding or other 
disturbance. A little careful study is decisive on this point. One of the clearest illus- 
trations of this is to be found in the southeastern quarry, where the lower bedding joints 
can be traced in a straight line beneath the apparent folding. The next ones are lost in 
a thick unbedded mass, over which the upper layers pass on a considerable curve. 

Passing by the Milwaukee region for the moment, we find near Cedarburg and 
Grafton, excellent examples of the irregular nature of this deposit. At the village of 
Cedarburg, most of the rock is a soft, porous, granular, minutely crystalline, dolomite, 
varymg in color from white to light cream. Occasionally, cavities of the size of a 
walnut or larger appear, but they are not frequent. The beds are from 2 feet to 41% feet 
thick, but not well defined, nor are vertical fissures regular or prominent. The local 
dip varies from 1° to 343° in a southwesterly direction, but is changeable. 

Other portions are harder and more compact, some of which, however, when mined 
back from the exposed surface, become softer and more granular, at variance with the 
usual fact. 

A half mile to the east, near the center of Sec. 26, a very soft crystalline rock, called 
sandstone, from its friable and granular nature, occurs, having a strong dip to the west- 
ward. Following down the stream a short distance, we find a hard, brecciated and geodif- 
erous rock of bluish cast without apparent stratification. 

This gives place almost immediately to a granular rock similar to the preceding, but 


NIAGARA LIMESTONE. 863 


‘the bedding joints become entirely lost, and, in an exposure of 20 feet, none are visible 
Vertical seams occur at intervals, which are disposed to change to an angle of 45° sills 
the horizon, and to pass obliquely across to the neighboring fissure. 

If Wwe pass on eastward about half a mile, we find a rock, at a somewhat higher ele- 
vation, of a more earthy structure, belonging to the Guelph horizon, but when we reach 
the Milwaukee river, below the rapids, we again find the granular rock, as before, but 
distinctly bedded and dipping northward. In a few rods, the layers become harder and 
are almost as soon lost in a brecciated, unstratified mass, whose superior hardness hag 
given rise to the rapids. This mass is made up of fragments of rock cemented by com- 
minuted debris of a dolomitic character, which renders the distinction of the fragments 
from the matrix often obscure. This breccia graduates almost imperceptibly into hard, 
compact layers, as we proceed up the river, and these in turn soon give place to granular 
rocks again, the strata dipping northward for a distance, and then rising, as illustrated 
in the accompanying figure. 


PROFILE SECTION ALONG THE MILWAUKEE RIVER, BELOW GRAFTON, SHOWING THE CHANGEABLE 
NaTURE OF THE Racine LIMESTONE. 


a. Soft and granular; }. Close-grained and hard; c. Brecciated; d. Hard and compact; e. Granular. 


At the dam near the south line of the 8. E. qr., Sec. 24, Grafton, the granular dolom- 
ite is developed in its most characteristic form, becoming a well marked calcareous sand- 
rovk. 

Above the dam, a harder rock of closer but irregular texture ensues, but at a some- 
what higher level, and belongs to the Guelph horizon. 

Near the center of the east line of Sec. 33, Cedarburg, there is an outlier of rough, coarse 
brecciated dolomite of light gray color. It is composed of fragments of compact rock, 
the spaces between which are filled with a yellow pulverulent material. As the ruck of 
the vicinity has been swept: away, leaving it about 30 feet higher than its base, it is prob- 
able that it was surrounded by the softer granular beds that are prevalent in this neigh- 
borhood. 

Throughout. Ozaukee and Washington counties, this formation is chiefly represented 
by rocks similar to those already described, but to this remark there are conspicuous ex- 
ceptions. 

Near the south line of the 8. W. /4 of Sec. 35, Germantown, there is a quarry of 
considerable lateral extent, though it exposes but about 8 feet vertically. In the western 
portion of the quarry, the upper 13 inches consist of a. hard, close-textured rock, but 
full of rough, irregular cavities. Below this, and not definitely separated from it, are 
23 inches of porous, granular rock of the Racine type, showing, on the weathered edge, 
oblique and cross lamination. (e of Fig. 45.) Below this, are 5 feet of bluish white, 
very fine grained, compact dolomite, in beds averaging 6 inches in thickness. (f of 
Fig.) The distinction between this and the rock above is sharp and clear, so that it 
may be accurately traced, even where the bedding joint does not correspond to the junc- 
tion. Traced to the northeast, the porous layer of the Racine type is reduced to 18 
inches within 25 paces. It has also lost much of its porous character, having changed 
so as to be less different from the upper portion, and being now broken up into irregular 
layers. Five paces farther, this layer is reduced to six inches, and has still farther 
changed in character. (g.) Ten paces farther, it is no longer recognizable, both it and 


864 GEOLOGY OF EASTERN WISCONSIN. 


the layer above having changed so as to be scarcely distinguish- 
able from the compact rock below. Farther on, the difference 
becomes still less, a few cavities, and a slightly greater irregu- 
larity in the subordinate layers, being all that distinguishes 
them from the layers below. (h.) At the farthest point to 
which these layers can be traced, no geologist would think of 
separating them from the layers below, thus making it a clear 
case of thinning out and transformation. These layers are es- 
sentially horizontal. 

If we now return to the point in the southwestern part of the 
quarry, whence we started, and take 69 paces to the southwest, 
we find the rock exposed in the road as follows: 

First, a compact limestone, similar to that in the quarry, dip- 
ping eastward at an angle of 6°. The upper layer is 8 inches 
thick, underlaid by one of 4 inches. (d.) The rock for 5 paces 
is then covered, beyond which it again appears. The upper 22 
inches of this are divided irregularly into beds. the superior por- 
tion of which is as compact as any seen at the quarry, but the 
lower is somewhat more porous. This dips11° N. of E. Under 
this lie 5 inches of porous rock, but not of the most pronounced 
class. Under this, again, lie 2 inches of similar kind; beneath 
which, again, there are 54g inches of limestone, containing 
many cavities of the size of an almond, and similar to the upper 
layer described at the quarry. Under this lie 1814 inches of the 
more pronounced and typical, porous, granular rock. (c.) Here 
again the section is interrupted by 8 paces of unexposed surface, 
when a porous, granular rock succeeds, having a dip of 14° N. 
of H. (6.) There are about 26 inches of this, the irregularity of 
the structure making it difficult to measure exactly. Below this 
come 6 to 8 inches of a rough, irregular, brecciated, rather 
hard and tough, but somewhat porous, rock, containing large 
and small crinoid stems, like those common in the Racine beds. 
The section is again interrupted for 4 paces, when a rough, very 
irregular, brecciated, porous rock tollows, constituting a confused 
mass, similar to the rock mounds near Milwaukee and Wauwa- 
tosa, yet to be described. (a.) In this, Ill@nus ioxus, fragments 
of Atrypa and Rhynchonella, crinoid stems, and an Orthoceras, 
were found. This exposure continues 18 paces. The whole sit- 
uation is imperfectly represented by the accompanying figure. 

It seems to be possible to draw but one rational conclusion 
. from the foregoing facts, viz: (1) That the last mentioned ireg- 
‘ ular mass stood as a reef in the depositing sea; and (2) that the 

alternating layers were deposited on its slope, while (3) these, 
in the more quiet waters at a little distance from the reef, were 
replaced by a deposit of finer silt, which formed the compact 
layers. The unusual phenomena of cross and oblique lamina- 
tion in limestone harmonizes with this view. 

Within a mile from this point, there are several exposures of 
the compact rock. In the south half of Sec. 36, this even tex- 
tured, compact variety is associated with a layer of the same 
general color and composition, but having a sort of lumpy 
structure, a kind of conglomerate, in which the pebbles and 


Fie. 45. 


SHowine PEcutrarn Structure DescripeD IN TUE ACCOMPANYING TEXT. 


y 
] 


ay 3 


Z1 


NIAGARA LIMESTONE. 365 


matrix were of the same material, and blended in solidification. This association here 
is an important link in the chain of evidence, as we have a precisely similar association 
with even textured layers, near Milwaukee, which have been heretofore excluded from 
the Racine group. 

The position of these beds is also to be taken into account. To the northeast, north- 
west, southwest and southeast, are outcrops of the characteristic granular rock, within 
from one to four miles, with nothing in the topography to favor any other view than 
that taken. 

About four miles to the southeast (middle N. line Sec. 29, Granville, Milwaukee 
county), we find a mound of confused, unstratified rock, having a north and south axis. 
The rock is dirty buff in color, and soft, granular, and almost pulverulent in texture. 
Eighty-five paces to the southeast of this, is a similar, but much smaller, mound, on 
the north side of which a quarry has been opened in even bedded, rather soft and porous 
dolomite. the layers of which dip into, or under, the mound at an average angle of about 
4°. Pentamerus (Gypidula) multicostata abounds in these layers, and, in the larger- 
mound, is associated with other Niagara fossils. 

Near Milwaukee there are three mounds or ridges of rock that have attracted much 
attention, and which seem to be regarded as exceptional phenomena, but which, I think, 
in the light of preceding and subsequent facts, should cease to be so regarded. One of 
these, known as Moody’s quarry, is located in 
the Fourth ward of the city of Milwaukee, in 
the side of the bluff facing the Menomonee 
river. Another is situated in the grounds of 
the National Military Asylum, and the chief 
and most noted at the station Raphu, near 
Wauwatosa, and commonly referred to the 
SuowinG THE STRATIFICATION aT MoopY’s Jatter locality in the literature of the subject. 

QUARRY, MILWAUREE, The distance from the first to the second, on an 
air line, is 214 miles; from the second to the third, a little more than two miles, and 
from the first to the third, less than 31{ miles. Lines joining them thus would form an 
obtuse-angled triangle. Within this triangle are two quarries of regularly bedded, 
horizontal limestone. One of these, Storey’s quarry, is about two-thirds of a milu 
northeast of the outcrop in the Asylum grounds, and the other, about the same distance 
from the Raphu or Wauwatosa mound. Only a few rods west of the last, there are sim- 
ilar horizantal beds, having a very close relationship to the mound. These mounds are 
similar in character. The most striking peculiarity, aside from their external form and 
stratigraphical relations, is the great irregularity of their structure. The stratification 
is ohscure, and sometimes apparently wanting. The rock has an irregular texture und 
varying, but frequently glassy, fracture, and contains many cavities of varying size and 
very irregular form. These are sometimes drusy with crystals, sometimes coated with 
stalagmite, or, again, filled with pulverulent material. The color is also varying, but usu- 
ally bluish or yellowish. In composition, it is nearly a pure dolomite, and that from 
Schoonmaker’s quarry is used successfully as a flux for iron at the Bay View furnaces. 

As the quarries near Wauwatosa furnish the best exposures, are the most fossilifer- 
ous, and have been the subject of most discussion, it is desirable that we should enter 
somewhat into particulars in reference to this interesting locality. If we place ourselves 
at the extreme western exposure, known as Busack’s quarry (see Fig.), we shall find a 
section showing heavy, well defined, nearly horizontal, slightly argillaceous beds, of a 
uniform, compact grain, medium hardness, smooth conchoidal fracture, and 
bluish gray color. Interstratified with these, are layers having the lumpy nature pre- 
viously described as occurring in Sec. 36, Germantown. The layers dip eastward to 
about the middle of the quarry, from which they rise, but not uniformly, for at this 


Fie. 46. 


rather fine, 


366 GEOLOGY OF EASTERN WISCONSIN. 


point an east and west axis occurs, having the general trend of the ridge farther east, 

and with which it probably has a definite connection. An east and west section in this 
part of the quarry would show a dip to the westward, and a north and south section would 
exhibit the layers curving gently over this axis. But as we 

trace the rock eastward, it changes in nature. Near the east- 
ern extremity, the upper layer becomes sl'ghtly irregular in 

bedding, and rather soft, and granular in texture. 

Below this is a layer from 22 to 24 inches thick, divided 
into sublayers, somewhat irregularly, and occasionally show- 
ing lines of deposition. To casual observation, it appears to 
be a compact, fine-grained, even-textured dolomite, but 
closer inspection shows it to contain many small cavities, 
that are angular and sharply defined, and are the result of 
the removal of minute fossils, in which the rock abounds at 
this point. Aside from these, the rock is as previously de- 
scribed, with occasional seams of argillaceous material. Be- 
low this, the rock is similar to that in the western part of tho 
quarry. In the extreme southeastern portion exposed in con- 
nection with this quarry, the rock becomes quite irregular in 
structure. 

There ensues at this point, unfortunately, an interruption 
of several rods in the exposure, so that this incipient change 
in structure cannot be traced to its consummation. 

Passing this interval, we find at the western extremity of 
Mr. Schoonmaker’s quarry, at the surface, a cellular, even 
textured, regularly bedded rock, similar to the last described, 
but of lighter color, and more distinctly granular nature. 
This dips southward at an angle of about 15°. As the face 
of the quarry curves round to the south, the whole section is 
composed of similar rock down to and beneath the water 
that occupies the bottom of the quarry at this point. But 
these lower layers dip less and less, until they become hori- 
zontal, and even slightly incline toward the irregular mass. 
If we trace these lower layers toward the ridge, their inclina- 
tion somewhat increases as well as their thickness — th’s 
latter sometimes markedly — until they are lost in the ob- 
scure structure of the reef, or disappear at the surface. 

As we pass eastward along the fave of this ridge, now well 
exposed by quarrying, the dip of the ill-defined layers in- 
creases gradually to 54°, when the stratification can no longer 
be clearly distinguished. This obscurity continues for 80 
paces. There are some indications of horizontal bedding in 
this space, and also some that the dip is to the south, and 
that the exposure is along the strike of the strata, but neither 
observation is altogether trustworthy. 

East of this, blue and lighter colored bands indicate a dip 
of about 30° eastward. This continues for about 35 paces, 
the observation at the eastern extremity showing a dip of 
31° in a direction E. 10° to 15° 8., this being the dip as ea- 
posed, not necessarily the full amount of the true dip. The 
same qualification is true of the other observations made cn 
dip along the face of this exposure. 


Jchoonmakers @ uarry 


Fie. 47. 


RELATION OF THE MouND AND HortzontTaL LOYESTONE NEAR WAUWATOSA. 


NIAGARA LIMESTONE. 367 


Ten paces of unexposed face succeeds, followed by 90 paces uncovered, which shows an 
obscure dip of about 30° E. of 8. Again 30 paces are concealed, bepond which a face 40 
yards in length succeeds, whose dip is 33° E. of 8. After another interruption of 60 
paces, we find the last exposure of about 10 paces length, whose very obscure strati- 
fication mdicates a dip to the 8. W. The ridge reaches a hight of about 45 fect above 
the sole of the quarry. 

Near the summit of the ridge, at its western extremity, is a slight outcrop apparently 
in place, and seeming to dip to the northwestward (20°, N, 30° W.). If this be reliable, 
we should infer that the ridge was comparatively narrow, as the exposure lies only 17 
paces back from the face of the quarry. 

The trend of the ridge, as estimated from the exposures, is a little to the north of 
east. 

The rock at Storey’s and Schwickhart’s quarries, within the triangle before 
mentioned, is closely similar to that in the western part of Busack’s quarry, and the 
same remark may be made of the fossils, which consist mainly of Ovthoceratites. 
But in Busack’s quarry, where the strata approach the reef, the fauna is much ampli- 
fied, and we find Halysites catenulatus, an undetermined Trematopora, Streptelasma 
and Fenestella, Stephanocrinus gemmiformis, Orthis biloba, O. elegantula, Strophomena 
rhomboidalis, Streporhynchus subplanum, Atrypa reticularis, Rhynchonella neglecta, 
Platyceras Niagarense, Orthoceras annulatum, a new species of Phragmoceras, found 
also in the adjoining reef, a Gomphoceras, Calymene Niagarensis, Encrinurus ornatus, 
and a new species found also at Zimmerman’s quarry, IWlenus Ioxus, and Bronteus 
Acamas. a 

From all the foregoing facts, it may be regarded as fairly demonstrated that theso 
horizontal beds were laid down simultaneously with the formation of the mounds. The 
cellular nature of the rock of the latter, and the uncompressed condition of fragile fos- 
sils, are fatal to any theory of upheaval, or other violent action. 

About five miles northwest of this, at Zimmerman’s quarry, in Section 7, N. E. qr., 
Wauwatosa, there is an even-bedded limestone of compact or minutely cellular texture, 
very similar to that of some layers in the eastern part of Busack’s quarry already de- 
scribed, and to which they are equivalent, as shown by the contained fossils. As quar- 
ried, the layers are thin, but the true beds are of more considerable thickness, a state- 
ment which is true of most or all the flags and apparently thin-bedded. strata of this 
region. A few miles farther to the ucrthwest, at Howard’s quarry, and. at several 
other points in Menomonee, quarries of white and gray flags, and even-bedded, com- 
pact, fine-grained, chertless limestones occur, that seem to belong to this horizon. At 
Howard's are found Halysites catenulatus, Atrypa nodostiiata, Orthoceras annilatumn, 
O. medulare, Phragmoceras Nestor, Illenus Ioxus, Calymene Niagarensis, and several 
undetermined forms. At other points, fossils arerare. In the adjoining town of Lisbon, 
as already mentioned, are similar strata, whose exact stratigraphical position is some- 
what doubtful. From the fact that the compact, even-hedded rock that unquestionably 
belongs to the Racine horizon is evervwhere, so far as known, free from chert, while 
the strata immediately underlying the undoubted Racine beds at Waukesha are highly 
cherty — and the same is true of the layers beneath the Racine in all the northern coun- 
ties—the presence or absence of chert is entitled to some consideration as a distinguish- 
ing feature. From its nature, however, | am disinclined to rigidly apply it as a diag- 
nostic character, and, besides, such application would, in some .cases, lead to strati- 
graphical difficulties. It may be best, however, to provisionally regard the chertless 
beds as belonging to the Racine horizon. and the cherty flags to the Waukesha beds. 
If this rule be followed, most of the rock exposed in the town of Lishon, and a portion 
of that in Pewaukee, would be regarded as Racine. In justification of the fact that any 
doubt remains, it is to be remarked that this is a region of almost universally prevalent 


868 GEOLOGY OF EASTERN WISCONSIN. 


drift, and that exposures of the rock are few and of limited extent, and it is further to 
be remembered that these are distinctions between subordinate divisions of the same 
epoch, and involve discriminations not often attempted with equal detail. 

In the northern counties, the formation is mach more uniform, both in the character 
of the rock and of its organic contents. Asa type, or at least standard of comparison, 
we may select a limited but characteristic section from the town of Kewaunee (T. 23, 
R. 24, Sec. 14, 8. hf). 

1. Top Layer. A hard, compact, rather fine-grained, grayish white, even 

bedded dolomite, of somewhat uneven texture, weathering into 

creases, rather than pits, and quite fossiliferous, especially abound- 

ing in Brachiopods.........+ees secret eee eee e tet e ener cree eens 1 ft 10 in. 
9. Somewhat similar to the above, but coarser, softer, more uneven in 

texture, more inclined to be granular, and containing fewer fossils. 


It weathers into pits rather than creases.......--.+- esse eens eeeee 1 ft 2in. 
3. Similar to the last, but still more soft and granular, and more irregu- 

lar in bedding and texture...-.----. eee eee cece eee eee e ence ees 2 ft 4 in. 
4, Similar to thé abové:.s.c.cs0caecks ciuaweenieesunereeevenude® seuss 3 ft 6 in. 
5. Thin layers, belonging to the Upper Coral beds .........-2++++ee+0+ 11 ft. 


Although some of these layers are described as soft and granular, they do not possess 
these qualities in the same degree as that at Cedarburg and similar localities. 

At Wilmot’s quarry S. E. qr., Sec. 32, Pierce (T. 24, R. 24), about five miles from the 
above, we find a rather soft, somewhat granular dolomite of subcrystalline structure, ir- 
regular fractnre, rather thick, scarcely even heds, of bluish and grayish white color, 
with occasional stains of yellow and red, weathering to a yellow or buff, 

All of the rock referred to this formation in Kewaunee county is very similar to the 
above. 

One more example, from near Sturgeon Bay, Sec. 9, 8. E. qr., T, 27, R. 26, will 
suffice for this portion of the formation. This outcrop consists of a whitish, somewhat 
granular, porous dolomite, of subcrystalline structure. It is heavy bedded and weathers 
into pits and creases. but not conspicuously so. The weathered surface shows white 
lines about one-half inch in width that are usually parallel to the bedding. These cor- 
respond to thin laminw of a more compact, homogeneous, cryptocrystalline rock, appar- 
ently of essentially the same chemical composition as the rest. Some portions of the 
rock instead of being granular, are close and flintlike in texture, although enclosing 
numerous small cavities. On the average, the rock is of medium hardness and irregular 
fracture. 

The formation throughout Door county does not essentially differ from this, except 
that at some points it verges more toward the coarse-grained saccharoidal marhles. 

Speaking in general terms, the formation is possessed of quite constaut lithological 
characters north of Sheboygan county. 


Summation. It appears, then, that in the southern counties there 
are three well marked classes of limestones, with intermediate grada- 
tions, one class, consisting of very irregular, often brecciated or con. 
glomeritic dolomite, forming masses that usually appear as mounds, 
or ridges of rock, of obscure stratification, a second class, formed of 
pure, soft, granular dolomites, a part of them calcareous sandrock, 
and a third class, consisting of compact, fine grained, regular, even 
beds. We have demonstrated that the three forms change into each 
other when traced horizontally. They were therefore formed simul- 


NIAGARA LIMESTONE. 869 


taneously. The view that best explains these facts is, (1) that the 
mounds and ridges were ancient reefs, and (2) that the granular sand 
rock was formed from calcareous sands, derived by wave-action from 
the reef, and (3) that the compact strata originated from the deposit 
of the finer caleareous mud that settled in deeper and more quiet 
waters, the whole process being analogous to, if not identical with, the 
coral formation of the present seas. But before pursuing this analogy 
farther, it will be well to consider the evidences of life found in these 
rocks. While some of the reefs, or at least that portion of them that 
happens to be exposed to examination, present only a few fragments 
of fossils, others are prolific in organic remains, and some of them are 
remarkable for the richness and variety of their fauna. The reef near 
Wauwatosa (Schoonmaker’s quarry), is a striking instance of this. 
There have been collected from it, chiefly by Dr. Day, probably not 
less than two hundred species. Of these there have been identified 
28 Corals, 8 Bryozoans, 4 Crinoids, 19 Brachiopods, 11 Gasteropods, 
9 Lamellibranchs, 24 Cephalopods, and 16 Trilobites. And an ex- 
haustive examination of the collections would doubtless much increase 
the number. The specific character of these will be seen by consult- 
ing the accompanying table. This locality is especially notable for 
its Trilobites. At the quarry in Milwaukee, Corals are proportion- 
ately more abundant in number of individuals. At Noessen’s quarry 
near Saukville, where there is a mingling of Racine and Guelph 
faunas, some portions of the rock are little more than a mass of coral 
remains imbedded in calcareous sand. 

Of the granular varieties of rock, that which is nearest allied to the 
reet rock is peculiarly notable for an abundance of Crinoids. The lo- 
cality near Racine is preéminent in this respect. Upwards of thirty 
species have been identified from this one locality. These are associ- 
ated, as will be seen by consulting the table, with a large number of 
Corals, Brachiopods, Gasteropods, Cephalopods, Trilobites and a lesser 
number of other forms. Very similar faunas are displayed at Green- 
field, Waukesha, and elsewhere. The more purely granular sandrock 
seldom contains many fossils. 

The fauna of the compact strata is distinguished for the conspicu- 
ous presence of the straight and curved Cephalopods with compara- 
tively few associates. The Cephalopods are abundant, as already 
noted, in the reefs and crinoid beds, but are overshadowed by the 
number and variety of other forms, while in the compact rock, they 
greatly predominate. 

It appears then, (1) that upon the reefs there swarmed a vast variety 
of life; (2) that upon certain banks or shoal areas there was also great 

Wis. Sur. — 24 


3870 GEOLOGY OF EASTERN WISCONSIN. 


abundance and variety, among which the erinoid family attained un. 
usual prominence; (3) that over areas of submarine sand-flats there 
either was little life present, or, from the porous nature of the rock, it 
has been illy preserved, and (4) that over the deeper areas, that de- 
posited fine calcareous mud, the gigantic Cephalopods held sway. 
The counterpart of all this is to be found among the coral reefs of to- 
day. Vivid descriptions, almost specifically applicable to the forma- 
tions in question, save in the modern aspect of the life, may be found 
in the writings of Prof. Dana and Mr. Darwin on recent coral forma- 
tions. A few quotations from the excellent work of the former on 
Corals and Coral Islands, may find a place here by way of illustration 
and confirmation. 


‘*Generally the barren areas much exceed those flourishing with zodphytes, and not 
unfrequently the clusters are scattered lke tufts of vegetation in a sandy plain. The 
growing corals extend up the sloping edge of the reef, nearly to low tide level. For ten 
to twenty yards from the margin, the reef is usually very cavernous, or pierced with 
holes or sinuous recesses, a hiding place for crabs and shrimps, or a retreat for the echini, 
asterias, sea-anemones and mollusks; and over this portion of the platform the gigantic 
Tridacna, sometimes over two feet long and five hundred pounds in weight, is often 
found, lying more than half buried in the solid rock, with barely room to gape a little 
its ponderous shell, and expose to the waters a gorgeously colored mantle. Further in 
are occasional pools and basins, alive with all that lives in these strange coral seas. 
The reef rock, when broken, shows commonly its detritus origin. Parts are of compact, 
homogeneous texture, and solid white limestone, without a piece of coral distinguishable, 
and rarely an imbedded shell. But generally the rock is a breccia, or conglomerate, 
made up of corals cemented into a compact mass, and. the fragments of which it con- 
sists are sometimes many cubic feet in size.’ “Besides corals, the shells of the seas con- 
tribute to it, and it sometimes contains them as fossils, along with bones of fishes, 
exuvia of crabs, spines, and fragments of Echini, Orbitolites (disk-shaped foraminzters), 
and other remains of organic life inhabiting reef grounds.” 


Speaking of the masses of coral rock thrown upon the beach by the 
waves, he says: 


“On moving these masses, which usually rest upon their projecting angles, and have 
an open space beneath, the waters at once became alive with shrimps, crabs and fish, 
escaping from their disturbed shelter; and beneath appear various Actiniz, or living 
flowers, the spiny echini and sluggish biche-de-mar, while swarms of shells, having each 
a soldier crab tor their tenant, walk ott with unusual life and stateliness. Moreover, 
delicate corallines, Ascidize and sponges tint with lively shades of red, green and pink, 
the under surface of the block of coral which had formed the roof of the little grotto.” 


In other portions of the same work, there are frequent descriptions 
or references to sandrock, solid limestone, and various conglomeritic¢ 
forms, that might almost have been embodied as a portion of the lith- 
ological description of this exposure of the Racine limestone. It does 
not appear, however, that Corals played so conspicuous a part, relat- 


NIAGARA LIMESTONE. ‘871 


ively, in the formation of these ancient reefs as they do in modern 
ones. In the northern counties, the Racine strata present no indica- 
tions of this reef formation, but in Ozaukee and Washington counties 
it becomes pronounced and extends thence southward until, south of 
Racine, the formation is concealed completely beneath the drift. The 
line of reefs is unquestionably sixty miles in length, and may be 
much more. From their position they must be regarded as of the 
nature of barrier reefs. It is worthy of remark here that the reefs 
terminate at the north at that point at which the underlying forma- 
tions undergo the modifications previously described, and it is partic- 
ularly worthy of notice that this is the point where the Waukesha beds 
give place to the Byron and Coral beds, from which it appears that 
the discrimination of these subdivisions has an historical and dynam- 
ical importance. The consideration of the industrial value of this 
formation will be found following the treatment of the Guelph beds. 

Dr. F. H. Day, of Wauwatosa, through years of industrious accu- 
mulation, has gathered, from the several localities of this formation 
in the southeastern part of the state, a very extensive collection, that 
is exceedingly rich in new, interesting, and typical forms. He has 
very kindly furnished the survey a list of species found at the several 
localities, which is incorporated in the following table. The species 
given on the authority of Dr. Day are marked thus +, those of the 
survey, thus, *. 


72 GEOLOGY OF EASTERN WISCONSIN. 


FOSSILS OF THE RACINE BEDS OF THE NIAGARA GROUP. 


> 3g 
=> wa 
oe ie a 
: :v 
F ,| ¢ |dzlgeig— 2 ee 
GENERA AND SPECIES. | & Z\4 SESE ae E a /2G/28 
op 5 2 > > Dey|e& 
al/e|S|4 |ESlESiesl 8 | 8 |B 138 
ao] -d cay 2B |S4/2 4/28) 2 SB S| em 
) co) S|) R a eogia S| & 3 
a 5 Raa H 4 | o 
2\é|é |= ESE2SS) 3) 5 Base 


| Sturgeon Bay. 


PLANTA. 


Arthophycus .........4. Siacall Af Naasacp fener e | 4.8 


Buthotrephis, und. sp... .- * essed | Poleeses|, Pl) Spal aes 
PLACUIB.s.6 cece cee e es | estate| 8 Seco  eeeranr Pils pails 

B. flexuosa......--.000- ee eee ere rece i a 
FORAMINIFERA. 


Receptaculites hemispheri- + 
CUS: Sate ieesd eae deoe sty 
R.  infundibuliformis....}°°°"|"" 7" 


kx 


— 
* 
—- 


PETROSPONGIA. 


Stromatopora concentrica.|....]----| Ff] * | +] *t] fF] #* [eee] * 


CORALS. 

Favosites favosus ........ coed! SE | Pleswal FBR] AP ben +e 
F. Gothlandicus ....... raccs[eete! “Plasec| A T T ie. sate 
F. Niagarensis......... wove) FE | FE [saarel HF] Spb OE OP lewd 
Wey pbiblabiag gested 2 atsecscrsiatces iesaleaes| AP lee wohinaellova sly sues ais 
Astrocerium constrictum..|....J.---] fF ]....[ * ] Fl +i. ibe 
A. venustum........... sessfeeee| PF lsaecl FY] PF LPT ® [aul # 
Halysites catenulatus..... eel HE] oT] Pl ti] ] ep] ® foe fe 
H. var. microporus ..... nae Mola dare case liieallaieace [Sete Ile sepia 
ii, var. macroporus..... oeeal|> cay rea reer ail opaeaue 
H. agglomeratus ....... Begone Pe liecwes Sa tall Bsn 
Heliolites pyriformis ..... cent! 8 leaeeleemelecci| RR | ® siavel team 
H. macrostylus .......... wana needle sa sliesnalace |) Poles Pa eee rere 
Thecia, und. sp.......... azesleesa] OP [esaalaedal oF «| sachet] Gates 
Cladopora reticulata...... pad [eee easels Pia Mlieraictst| kahve 
Ccenites lunatus.......... foal Tt leaeeleetiotesccal hol cF alle oie | cars 
Syringopora compacta....|....J...-[....[....) 2.) HP few. sag |waces 
BS. Dalmanties.c0sagesas aa selesea ley Mine eeeal “tll eaees Sed leeae 
Db. infundibula; ne ispies sf ex sveslgesciacs. [icevell I 21s Segleaws 
8. verticillata... ... ... Stzale ces. Bere pear eee a eee be eva OF 
DiphyphyHum cespitosum)....) * J....J....f...) fF] Ff. 3 

sp., with larger col’s..|....]  * |.. jasleeoe, FL OF hee wes 
D. sp., with smaller col’s.|... | * |. aasave catch php llacsuesd| ag “se 
Eridophyllum, und. sp..../.,..] * |. asso fiaia. are ea avabll Whadene lee a 
Gyathooiy ives, wd. spew<lasscf # | seesfeses| Pp] BE #] # 
Omphyma, und. sp......--|....) * |. aeeh SP ecsconal | OR es é 
Amplexus Shumardi...... Sete RE Taacs| ya aal seal teeta Ae die : 
A. und. sp..... PEG BEANR ee vets] EP igesl eased. coal (eee ee F 
Zaphrentis, und. sp....... sol TL PT] TF] tl ti] ¢ yo #f.. * 

Spi Yess Zepipan ted. <2 e)2a2laass.s bose | Se all cencvy [bias llega aed Lecce 
Streptelasma calyculum...|....) + | * tT) oF] Fh. 
Aulacophyllum, und. sp... amaalll oT Ff fos 


Cyathoxoma Wisconsinen- 
eee er ee vad) Elva alae tee aallestcalins call pacaloaeallos 
Chonophyllum Niagarense.|....J....] f [....fe... peeeeen raes e 
Cystiphyllum Niagarense..]....|....)..../..../.... I i 

Strombodes pentagonus...|....[....]....[...lee. T 


NIAGARA LIMESTONE. 373 
Fossits oF THE Racing Beps or THE Niagara Group — continued. 
meta a = a 
j , | 2 [22/24la-] 8 s lao sé 
GENERA AND SPECIES. fe os |S |S eiS slSal s g_|gaj® 
a || 8 (8 s/sass) 2] ¢ jasiss] 8 
g b |G) |e Sle Sled) 8 Btls a! ¢ 
Al 8/ 8 )/S [SES S/25) & |S |e l/e8l & 
E| 3) 2) 2 alesee| 2 |e lEsleel 2 
Ala l|é|F ESEQSS Ss /5 Mae) s 
CRINOIDEA. 
Saccocrinus Christyi....... ese ed EN ae $ leew. 
S. semiradiatus.........{...-) *p | ft] *F peal | 
Marcrostylocrinus striatus.|....| *f | T | *f |- dies 
Melocrinus Verneulii.... |....| *F | +] *f |-- fe issesess [a 
Glyptocrinus armosus..... soci RP) Ae RE Harte, aoe 
Ge NODINSewiswk waco eins ssouniall ETE] EE WAP asada Seidel apetenaile 
Glyptaster occidentalis....]....| *f | T | *F J- yaieaal aval 
G. pentangularis........ geos| Fe) SB SPL se Cees 
Lampterocrinusinflatus...|...-| *f | T ].---{- Reena aaeesihe 
Eucalyptocrinus ccelatus..|-.--| * J-.--| * |}. saya esveusieatl 
E. cornutus .......0..../e0-- | PLR es +P lewsnite 
E. cornutus,var. excavat's Pell Eo POF seat odorata garel 
E. ChaSSUS. <6 65603692 557s 3 a na a + |. 
E. obconicus.........-5- er |] oF] tye. Adc 
E. ormatus ...--..-..0 ee sia (a al a oe 
Hho Mi, Sp eneteadoybicsvescnd Fuel ares ck I tI 
Platycrinus, und. sp.---.- sage] OF nes ai 
Rhodocrinus rectus......- oe Ti ae les 
Cyathoerinus Cora.....+-- eH lo. ] + |. 

. pisiformis.........+-- * + | ig 
C. Waukoma...-.....- : + | #4 f.. 

Stephanocrinus gemmifor- 

Rages hsien oo co ewe coool ELE LET * | AE, — 
Caryocrinus ornatus...... deat t as a % 
Ichthyocrinus subangularis). - - . 5 a eee Be t 

CYSTIDEA. 
Crinocystites ornatus...... tei { fe Heol ececare|lseictels 
| OA | A -3) nr * tt] tye t |. 
Apiocystites imago....--- wena] T fesse] T feveelee eel 
Echinocystites nodosus. ...].---| *f | TT] T [ece-[ers +f 
Gomphocystites clavus.---[..++Jees-fersefeeeetes filets 
G. glans.....-..5.-2+6e- anal HR to] Ae |veee| OT fs 
Hemicosmites subglobosus |. - - - He P| ceallntealega'e ete 
Holocystites cylindricus...|.--.} *t | T | *f |-- 
Il. ovatus.....---.+e-e ete eee local RI coe 
H.  scutellatus.......++-. ull geal hae { 
H. Winchelli......--.-- 5 ied a 
H. abnormis.......--+++ fel ste] a es 
H. alternatus....----.-- +] oT] THe 

BRYOZOA. 
Lichenalia cencentrica....|----| *ff----} * | T] T ii ae 
Sagenella membranacea..|.---|-.+-{ T ]---- + i o Dey 
Fenestella, und. sp eee | OT] OF fee] FT te 
F. elegans......-+- lawealestaliecalioasiad! YF 248 
Retepora, und. sp..--- sleeves! oF A ot] oT 
Polypora incepta......++- pees! pos besge|! Plos 


BYES 


GEOLOGY OF EASTERN WISCONSIN. 


Fossiis oF THE RACINE BED OF THE NIAGARA GROUP — continued. 


GENERA AND SPECIES. 


BRYOZOA — (con.) 


Stictopora, und. sp........feee fees afeeeefeee feeee 
i dont. 


Cheetetes lycoper 


Trematopora, und. sp...+.|....|-+.. 


BRACHIPODA. 


Trematis, n. sp....-+..-- aoe 
Dinobolus Conradi........ ae 
Trimerella,sp.res.T.grandis]... 

Orthis biloba.... ......-. ene 


elegantula........... 


HYD: cocevreceainisarecarecs 


O999990 


las 


“ce 


thomboidalis 
semifasciata, 


s. 


8. nobilis 


AN tntntam 


plicatella............ 
8. ‘© var. radiata... 
Meristella Hyale 


Cyrtia myrtia............ 


ucleospira pisiformis.....].. . 
Retzia? und. sp........... 
Meristina Maria........../. 


M. nitida 


Pentagonia, n.sp......... etiolated | och 


Atrypa congesta 


Atrypa nodostriata....... Soave 
reticularis....... sasgeral eae 


‘A. 
A 
R. 
R. 


| Burlington. 


flabellula..........-. ee 


Dy vensvecesci eine shor chs oe 
oblata(?).........0.. seatslioxs 
© pectinellacn vce cases sien Se 
Streptorhynchus subplanus|.... 
Discina discus............ stig 
Strophomena patenta..... sis 
DS. protundavicc evapora De 
8 small var.....].. 


inconstans=........ ae 


Niagarensis.......... vatyalte 


We BP nysonw adware das leseee 
Rhynchonella cuneata....|.... 
Indianensis.........../.... 


Fichwaldia reticulata... Hee 


* 


ERE: : 


x et 


* 


6: * . 
% Rp 


% 
eR: 


ee 


Pentamerus fornicatus....|....{.... 


% 


x ee 
PEE pepe 


Kop 


= 
Fe 


* 


os 


| Greenfield. 


wy OS 


fxs! 


ae oateee sale tee ieee ie al ‘ 


(Zimmerman’s.) 


| Waukesha. 
| Wauwatosa. 


& 
7 


MS ao ae 


| Wauwatosa. 
(Schoonmaker’s.) 


x 


Faeroe ee a 


+e Bape # 


x 


a 
| 
5 F 
Bb 
a (3) ~| 2 
Say a & | sa] 
Sl s Se enaieae 
M4 Al 6 -{aGleR] & 
smb a | g |ax eo] ¢ 
eo) & iol a g| 2 
S| o/8 las 8) & 
FS) | 2 /esleal § 
os] © & | o oe act 
AS) A | Oo MAME] m 
excl alteare Peakae * 
© Vexcales ods ne 
eee oe * 
eae ie 
* slew ee % 


5) Spee, Ne 


NIAGARA LIMESTONE. 875 


Fosstts oF THE Racine Beps or THE Niagara Grovur — continued. 


o| 2| |e 
< ke i < 
a] sy be 
g :| @ |S eiSela 1 8 =| & 
GENERA AND SPECIES. | § SIS ISESeISal g S| Pa 
ls || 2 Es 8/2e| 3 | 8 |24/42| 2 
ei q BIE o/e's| Ss e”./38 
a [ck ® 5/8 RelES! & & S|Br on 
5/8 | S| 8 |S Elscles] 8) 8 |ESIRE| 
Ale |S/2 ESEZES Ss] 6 WaMee! s 
BRACHIOPODA — (con.) 
Pentamerus bisulcatus....]....[-..efeeeefeeeefeeed PF] fd. pee ea 
P. oblongus..........-. sae. Pb AN al t [sees] * oe.[ * | ® 
P. pergibbosus....- .--J-++-feeeefees-feeeefees-f ot | of]. juealleees 
P. ventricosus .......... veel EL PL * | * | ee] pL. ie oo ake 
Anastrophia interplicata .J.--.| * [.---[....) * [oe--[e---]- salevss 
* * 


Strcklandinia,und.spi+s<|es ea) eecfeces) ecee|ot ae }s 24.0)! teee|enes| pees 
Gypidula occidentalis ....J----] ft |eee-}e.--[ee--] Ft] t 
LAMELLIBRANCHIATA. 


Pterinea brisa. ......---++ Spans i +] #4] + 
Ambonychia acutirostra ..]..-. 4 rene 


. ee 


Paleeocardia cordiformis ..|..-.|.- 
Modioiopsis Dictzeus ....- ee 

NileSls weiwenieeleee's pre 
M. subundata ......... niet 
Ma. ‘recta, seoscncew ses se oa 
Amphiccelia (Leptodo- 

mus) Leidyi...-... 
Leptodomus undulatus, 


 —pengecen te 6 
mh ne 


GASTEROPODA. 


Platyceras Niagarense ..|-.--| t+] +] *t |e.--] ® | tT] * [ece-feee-[eeeefeeee 
Platyostoma Niagarense .| .--| *t{ t| *t ]----L Ah] t | ee-feeeefeeeefee ee} eee 
Euomphalus eae n | ox 

lus) mopsus ...-+-+++ Wanchai hese e 


Racinensis, n.sp.- --|---- (gets | Seealeirwe leaiee [+l ice 
E. und. sp. .-.--ee ee eee iewsl ace |bewelaves i asiy Sy RI sea * | % 
Straparollus solarioides ..|..-.| * |... |-.+-]. “cca hake as aves oes 
Pleurotomaria axion ....|....J.---| + |... |. eal ofS eas 
Pleurotomaria Idia ...... veel MET Ff] fF deel Ft { seks : 
Pe Hal@l esos aoa “a note] OF [eeaaltawales val) axe ‘set . 
P. occidens .....--+--+- were] FET OF wale AP | eaze i aisle . 
Pi gga a, pecuseen os 950 el tL td + eaatille : 
P.  subtilistriata ........ spacal ipdaceces|« v-exallsoes fs6 j 
Xenophora antiqua ....--. dbacel weassecl teak Redcat mao oer Wes é 
X. trigonostoma........ Adena lattes dg eal Stee 1 é 
Bucania angusta ........ seed { ti] +t ti] t 3 
B. trigonostoma... .... silads se. [ae |e : 
Trochonema Fatua....... stave) Seas ease see als is 
Cyclonema elevatum ..... vaseatal EA ica goal ecseatiel| dears be “ 

pauper .-.....-e. eee ga ee TR) aaa fousesiall ares . 
Loxonema Leda....-..--] --+| ft] ft feeee]eeee ‘ 
Metoptoma .......-....- seaal of feset|. -F leweals 2 
Bellerophon expansus..-.. pecaioeavlensalesar AP ae 
Marchisonia bellicincta ..|..-. { fi |sawelowas 
M. Laphami........+.- sees + | t ° 


376 GEOLOGY OF EASTERN WISCONSIN. 


Fossits oF THE Ractne Beps or tur Niagara Grovur — continued. 


GENERA AND SPECIES. 


Burlington. 


GASTEROPODA — (con.) 


Murchisonia macrospira...}.... 


M, (mMylittascecssscenews Saale eaa 


CEPHALOPODA. 


Orthoceras abnormé...... sais 
alienum ...........-. ots 
annulatum.......... ne 
columnare .......... Saas 
crebescens.........6. ee 
ue PAM 355 84. svi ee 
medulare ........... ewe 
Niagarense ......... avehe 
. trochleare .......... ee ee 
Ormoceras, sp. res. O. ver-|.... 
tebral@.:acescacscecccs sxieive 


oogosoce 


* xX * 
i a se 


Greenfield. 


—S 


| Waukesha. 


Gomphoceras septoris.. .J....[....f....feees 


(hr, SCPIIGHD coe ene c ances idee 


Gs MIS Pieccrcssbeysaclees dere) wine 


Oncoceras Orcas ...... F 
QO. gibosum........ 0. 


Cyrtoceras brevicorne ....].... 
>. arcticameratum .....J.... 


Vigidum...........04 ne 

bo (Me SDitus. eaten oe wa ee Wate 
Phragmoceras, n. sp...... jeeel es 
Gyroceras Hercules....... ere 


C 

C. Ries 
C.. lucillum...... 0665650. : 

C. 

C 


Trochoceras Bannisteri .. . 


T. Des Plainense....... ves 
T. Gebhardi. .......... aes 
T. costatum ........... pees 


T. occidentale . 
Lituites, und. sp. ........ 


CRUSTACEA. 


Illenus Barriensis........ oes oc 
I. corniculus ........... Be Slee: wealllea.aves drsrens 
I. Daytonensis ......... doalies salle 


I. imperator ........... 
L, ANSIPINS wsnenen aa news 
I. Toxus ....... 
Calymene Niagaren 


Ce Wail or eesensrcas aon ease 
Phacops, n. sp. ....--.+-. ha 


Dalmania vigilans ....... coat |aeny 


Ceraurus Niagarensis ....|.... 


SEES eee 


Be i ei 
eS Sa ck 


sts! 


Sten i ieee eee 


| Zimmernian’s. 


ye 


| Schoonmaker’s. 


eS 5 
Reet 


od 


+ 


oe RET 


| Moody’s. 


apse 


| Monomonee Falls. 


| Grafton, S. 25. 


Kewaunee, 8. 14. 


Kewaunee, 
(Wilmot’s.) 
| Sturgeon Bay. 


Sl FER ca crsndl sea 


NIAGARA LIMESTONE. 817 


Fossits oF THE Racine Beps or THe NraGARA Croup — continued. 


. 3 Net = 
a | @ so | a 2 oer 
lal ale! [gig Lele 
GENERA AND SPECIES. S s/ 8 E gi .| 2/2; 8 18s = 
g/€/8)8)2/o) a] 2) 2 lad] 3 
a/e/s)ala/2l2] 2] € [Bel 2 
a} & S| 5 s | 5 
ala/Slela/el/2iSlélsie4 
CRUSTACEA — (con.) 
COrannrns eis ie vase vice eee ees vast (lace Wows FE lenatenll acs. |eiete wits ceeds cuales tera. 
C.D. 8p... veeee eee Saas TE WE ess feat BO ie ee 
Encrinurus ornutus....... ieeelees lara theca | OF Mi aaalanes ere 
KE. Nereus.....-..-..0-- ae antl isinreelh sia 32.4 lhe als somal aninna dus 
Hy Ty SPrisswudaneace ¢oy iis hal acme aot savas | RE is 2a ale iss 
Lichas breviceps.......... srssetalitie eaenes | 3 orale awe |) SF Tees oe 
L. _ phlyctonodes ...... same Sh Faia oo]! ath” llactane es 
Bronteus Acamas........ sate) Mt Bh) ape ewee hn 
B. Laphami, n. sp...... aie eva RR AL pease | see deel eos. sal ecnneelf vena % 
Spheerexochus Romingeri.]. ..| * |....] *+ fete Pee 7 
Leperditia: asec. saws eee. wo@ ail watalbeced) OF 2 Be eee . 
Acidaspis ............66. aod Py A gia LS acess : 
Harpes tringula........-.. aus ans [eatealeatoai ce |e 
Asaphus, und. sp......... Hears midaelews vfeewdiaeg | 1% 


THE GUELPH BEDS. 


_ The Guelph limestone constitutes the uppermost subdivision of the 
Niagara Group in Wisconsin. In its lithological character, it does 
not differ essentially from the Racine limestone, being in general a 
rough, thick bedded, irregular dolomite, usually quite free from im- 
purities, and of buff, gray, or blue color. The distinction between the 
two subdivisions is a paleontological rather than a physical one. In 
the latter respect there is less difference between these than either of 
the other members of the group. There was evidently no marked 
change in the physical history of the region, but the sare conditions 
continued from the beginning of the deposit of the Racine limestone 
to the close of the formation of the Guelph beds. In the interval, 
however, the life underwent a change by the introduction of the 
species that characterize the Guelph horizon. This introduction was 
gradual, so that many localities show a mingling of the two faunas. 
The right hand white line on the maps is intended to bound this 
formation, and is drawn so as to include localities presenting these 
mingled species. In doing so, however, it was necessary to include 
some of the reefs and sandrock deposits whose physical history is un- 
questionably identical with the Racine reefs. The propriety of doing 
this may be questioned. 


Local Details. The mound and quarry in Granville and the Guelph beds near 
Cedarburg and Grafton have. been mentioned in the description of the Racine lime- 


378 GEOLOGY OF EASTERN WISCONSIN. 


stone. In the former case the formation is so similar to the reef structure of the Racine 
limestone that it is quite possible it should be so grouped, as has been done in description. 
In the latter case, however, there is a nearer approach to a lithological distinction than 
elsewhere, the Guelph beds being more regular and compact than the subjacent Racine. 
Gasteropods predominate among the fossils. 

At Noessen’s quarry, north of Saukville, (Sec. 26, N. E. 34), there is a limited open- 
ing upon an ancient reef, exposing a rock of varying character, a portion of it being very 
soft and coarsely granular, while other portions are compact and fine grained. Some 
portions are made up almost wholly of Crinoid stems and Corals, while others are brec- 
ciated. In color the rock is buff, weathenng to a deeper and more reddish hue. Corals 
and Crinoids are abundant, and only extensive quarrying is needed to make this locality 
valuable to the collector. The fauna shows a mingling of Guelph and Racine species. 
The locality is rather to be regarded as Racine than Guelph. 

At the light-house point, near Sheboygan, we find a hard, mottled, bluish dolomite 
of suberystalline, rather compact, but not uniform texture. A concentric structure, de- 
veloped in blue and white, is frequent. This and the mottling, brought out by the pol- 
ishing of the glacier, and swept by the waves, give the surface a unique beauty. The 
gencral dip is to the southward, but after passing a low axis north of the point the slope 
isin the opposite direction. Near Sheboygan Falls, the rock is similar, though at a 
few points, a tendency toward the granular character, so common to the south, is mani- 
fested. 

At Roth’s quarry, N. W. 4 of 8. E. ¥¥ of Sec. 9, Sheboygan, the greater portion of 
the rock in the main quarry east of the kiln, is a thick bedded, bluish dolomite, quite 
hard and comparatively free from cavities, but with occasional geodes of calcite and 
more rarely iron pyrites. Some portions are beautifully laminated. Other portions are 
more granular and lighter in color, and approach somewhat the granular rock found 
farther south. In general aspect and lithological character, it somewhat resembles the 
rock of Vaughn's quarry, near Racine, already described. This and all the rocks of this 
vicinity, have but a meagre content of fossils. A few rods west of this, there occurs a 
hard, shaly, bluish, magnesian limestone with argillaceous partings and lamine. Tho 
layers are undulating and the dip various. 

At Rabie’s quarry (middle N. 14 Sec. 7, Sheboygan), occurs a rock that differs from 
any found elsewhere in the degree of development reached by certain tendencies of this 
much varying formation. The vertical exposure is but slight. The upper layers are 
rather even and compact in texture, but below, the rock is highly brecciated with much 
argillaceous matter associated as a sort of matrix. The dolomite is a deep blue, while 
the argillaceous matter has a greenish cast, thus giving the rock a much deeper color 
than that of other portions of the formation. These layers are very geodiferous, the 
frequent cavities being drusy with calcite. The bmiliancy of these, in strong contrast 
with the deep color of the rock, led an interested party to believe that there was silver 
present, and a little iron pyrites scattered sparsely through the rock, raised even brighter 
hopes, which we were seemingly cruel, but really kind, enough to dissipate. 

At Howard’s quarry, on the Sheboygan river, the rock is very irregular, both in bed- 
ding and structure. It varies from a soft granular, to a hard, almost flint-like dolomite. 
It contains many cavities, and weathers to an exceedingly rough, pitted surface. The 
more granular rock is white, and the more flint-like, bluish. The bedding is too obscure 
and irregular to give any reliable dip. The rapids here, as in most other cases within 
this formation, are due to the changeable nature of the rock, and not to the fact that a 
uniformly soft layer underlies a harder one, as is commonly true of falls. 

In the town of Carlton, Kewaunee county, we find the most northern exposure of 
this formation yet recognized. It consists of a soft, granular, disintegrating, cream or 
buff colored dolomite of irregular bedding and structure. The fauna is peculiar, in the 
presence of large Gasteropods and Lamellibranchs. 


NTAGARA LIMESTONE. 


379 


The following table shows the character of the fauna, of the forma- 
tion, and at the same time the distribution of the species among the 


several localities: 


FOSSILS OF THE GUELPH BEDS OF THE NIAGARA GROUP. 


>; Lae > 5 5 6 
g FFs 6 je /2 
GENERA AND SPECIES. g sf gle | pS air) 
a |daldelevlbe ze lea 
er Se ana 
gE faslaslenieuleee & 
aij is 8 6 |8 |é 
PETROSPONGIA. r 
Stromatopora concentrica.....+....eeees Dawahieealimeelorseleses | Ae i 8 
CORALS. 
Favosites Niagarensis Ae ees 
F. occidens, 1. Sp..-++e-ee esse eee * | 8 
Astrocerium venustum . issice | aiiara al eeoaea scale 
Alveolites, und. Sp....++ sees eee ee cree asics | ioe solace wel * 
Cladopora, und. Sp...++-++0+ seers eee eee cain 3 | ihe Pema] ea4 |yuyaslites auallissweete 
Halysites catenulatus......+0.++eeseeeee sdagecal sea dull eee ae eee 
H. catenulatus, var. microporus ....2.--| * feces|oeesfeeee[ereefeoesfenee 
Cyathophyllum, und. sp. .-.----- AS asec ee reed ere i da 
Amplexus annulatus, n. sp..-+-- ++ -+eeees Sasa ess | Cec s Veale. || OF 
Chonophyllum magnificum .....+.--+--- asalietle woaleavalgwerlaied|avies 
Cystiphyllum, sp. res. C. Niagarense..... ist Meese [eta * 
Diphyphyllum, und. sp...-+-+-+ -+++-+- Ses legend]: eared eats lf 
Zaphrentis, und. Sp..-+--+ + ceeeeeeeeeee Ded rcvalllGhaxe htavsiat lion coecll ereas oe heveters | eee 
CRINOIDEA. 
Eucalyptocrinus ceelatus ......+-.se.ee- ieaalees dyonalpeenleany|ese's| 
E. ornatys.... - eee eee oc ales 4a vnanl woes pras * 
Glyptocrinus nobilis......-..2+-.eeeeee. sealed oa | shots * 
BRACHIOPODA. 
“Monomerella prisca....+++--++- 521) rene OO | san 
Orthis elegantula ......--++++. * ahuleeere 
Strophomena profunda seats) wate des 2a 3m 
S. rhomboidalis.... +++. ss0reee eee ee cee eee ss Jes (eye 
Spirifera plicatella, var. radiata........-- ward wedeoa he eoaed Pawns say 
Meristella Hyale=-Charionella Hyale..--+ |... .J-++-J-++ [eeesfenseferes * 
Retzia, nud. sp. .seeee rere eee ere eeee x gratis lee eal cacao aap cil enna 
Atyrpa, und. sp eee eee TPES Rois crear TOT  yaalll* Salles as Pee heer 
Rhynchonella cuneata ....++++++essseeee es ee x | # 
R. neglecta ...---ese eee e eee e eee ee es * 
BR. pisum .... e022 cece eer ee ree eees _ dugellsavere leew a lle~arallla ose's [are wal Keo 
Pentamerus oblongus...--++++eeeeeeeeee juno aaa [eereabannes 
P, ventricosus.... sees cere e cette eee E scac [ee aeoweleesaleeicelesal 
PP. und. sp.....eeereereeee re reee cease alee aca sabaes x) Slee: 
Gypidula (Pentamerus) multicostata ...- * | #2)... | * | * 
Go occidentalis........+seeeee cee ceeds Mone Melgar 1 
LAMELLIBRANCHIATA. 
Meyalomus Canadensis. .---++++++see+ chtscar taalar 4 [tank ave feces te lace Xfi] OC [EEN 
Ambonychia acutirostra..... Basle : * on 
Rensseleeria, 0. Sp. .see-eeeceeceeeees 04 |crnalewarepenres |? of 


(Howard’s.) 


| Sheboygan Falls, 
| Carlton, Sec. 28. 


Xx we * i DP ptt 


* 


380 GEOLOGY OF EASTERN WISCONSIN. 


Fossits or THE Guetry Beps of THE NIAGARA Gnrour — continued. 


gid me & FR lg |e | 
2 ME lee). ld |e 
GENERA AND SPECIES. af Fo S| SS of =| Sut Se el oe 
rd (sal sals lee Se ee Be | 3 
Figs |é (2-4 sles! 
8 ERIlENISR\CHIEA/e ale a] 8 
a | bel Q d o 3 a 
oid 16 © OO |} |ja fe |S 
GASTEROPODA. 
Cyclonema? magniventrum, u. Sp..-++ pied esleeealae st pda aene es pele sae Ras 
sp. res. UC, pauper... .- eee eer eeeeee aes see “ue ee = ays 
Holopea elevata .......e0ee eee e eee eens panes waleeee ave ster 
H. Guelphensis..........--.+-+f ee eeee od Co nite ans ahi 
H, armioniad caze.i ees caaecs dee ewan s or eres sve “ 
Loxonema magnum, u. SP. -.. ee eee ee eee vase aes “7 el eee 
Murchisonia Boydii ...---.-- ++eee seen savefeees d+ [aa Raye Ges 
gigantea, n. Sp.- +--+. sees eee e eens ee a ies lhe 
M. Hyyreitiasyccssavews Oorceaeeseenen Sass gfe eee) * 
M.. To@anile ics seais seals caine’ vosreges sauce) sole alee a2 |e setcshamass [ae eeallee shy 
ta #9 * * 
M. longispira.....-...seee eee ee eee eee sib alaetell FB ls sea é “o 
M. macrospira.......s.ee cece ee ee eee Send Oo Ge Oe Ce oe ne 
My. Me BPs s cada yn esis eee ee nteneg ete nage pietaliass | dartel ewe ie asl Gees : 
Platyostoma Niagarense ..........+--+-+ opal SP Ileoes sina’ |sieaes ; 
Pleurotomaria axion......-.-. sees eee ee shehiee eneea ovate esas das 
Pi Hale? 2 'sse oe eee Gees reese eases ¥ ciaise acer Blea aes 4 avers 
Pi VIA saisinsievednes scete.gionas bro anateeas a orernince liane eae fescue # ) see] * oer 
Straparollus Hippolyte ............6. .- Nate aN snaoiallh, SE | |Gcaente | evden Gee ene Fi 
Gi. ‘SOLAIOIMES sree saaneicnaiigy gran treraierane motes erie dedeaid 6 Gass fecsieresl ease tteseasel|? OP chess * 
Trochonema Fatua....-... 6.50.0 eeeees Sasgvel Sect lecerdys luexsealeuctsalheweaie oP vee 
Subulites ventricosus..........+eseeeeee sae) etso alle s.aya) eave * 
CEPHALOPODA. 
Orthoceras abnorme....-......- seen ee rer salen SES | FF trees ina se 
NNUAL 4 iss-gees vAlea madam anes | e's (asta call: HR  ceee sala tise 
QO. Carltonense, n. sp. ss. cece cece eee walegll exter ik Scaleweceol | lacie Mesetere * 
Os: CYEDESCEMSs oie se enioe saree seme eas sactiall esas [elaalnnere faataraliccsiass (OS ie 
Gomphoceras, und. sp.. ..--...ee. ee eee keesleaesy To ll cacdleees sires 
Cyrtoceras arcticameratum............4¢ ai ealicas laeeeiocanl, 2 save 
Gh. Vaterale:siccyiet ackigea debed seek site nes csdslessa loa chal eaael F aie 
Cy rectus 8p a ie ee'e vie Waseda sas Pegs | eed ered | ertets eeear ere 
Ce Med UI 6 denies peewee sedis atlas evedileasaleaaial wee MH lereg esac |h moltieres 
Phragmoceras, und. sp...... seeeeeeee suvelessslioorlimulessaleasslseesiaee| * 
CRUSTACEA. 
HMisantis Toxts:nacctscs:suarieaisisinn aaa alee aur 2 * basa ae 
Bronteus Acamas ....-...eececeeseeeues : * ‘ 


InpustriaL VaLug or tur Wavuxesua, Ractne anp Gurtexn Bens. 


Lime. Probably the Niagara limestone surpasses all other forma- 
tions in the interior of the continent, in the amount and excellence of 
the quick lime produced from it, and certainly the formation no 
where surpasses the purity and adaptation to lime manufacture that 
it attains within the_region under consideration. The excellence of 


NIAGARA LIMESTONE. 881 


certain portions of the lower members in this respect has already been 
considered, and the higher members now claim attention. 

The following analyses show that the first great essential, purity, is 
possessed in a high degree: 


; I. IL. Il. IV. 

Carbonate of lime. ... 6.6... .. cece cece cece eens 52.86 52.16 55.23 55.41 
Carbonate of magnesia............ecceeeeeevees 42.98 45.50 43.52 48.48 
Sulphate of Nimes 0s ass dew ees amiledceead seed aieas 0.10 0.05 ..... 
Phosphate of lime.... 2.0.0... ccc cess ees ec eevee eeeee 0.12 0.10 ..... 
Sesquioxide of iron...... 0.0.00. ce ceee cece ences 0.32 ' 
Sesquioxide of alumina.......-.... ceesee eee ee seen oe ai ie 
DillGarsigi tease tes eie's dav a dies HORM EMNR ead eas GMeee. AGRA. ieee 0.50 
SUl PMs centred nats Se one sa uae sabe amentieseaeues Gately Trace Trace, ...-. 
Wateiie oo 2’ Fil. d sender dedaide tw ae es 0.49 0.67 0.25 Seoue 
Insoluble residue........... 0... c cece cece cece es 3.44 0.28 0.40  ..... 

A Otall 4 pis state eaianies oe < kai eee td sek as ate res 100.09 99.65 100.47 100.00 


No. 1 is from the Pentamerus layer at Pelton’s quarry, Pewaukee. 
This layer is not now burned for lime, the upper layers, which are 
purer, being used exclusively. No. II is from Mr. Horlick’s, and 
No. III from Mr. Beswick’s quarries, Racine. All the foregoing 
analyses are by Prof. Daniells. No. IV is an average of six analyses 
of as many layers of Mr. J. Druecker’s quarry, near Port Washing- 
ton, by Mr. Bode. It will be observed that the average insoluble res- 
idue of those that are used for lime is less than one-half of one per 
cent.; or, if the alumina and iron be included, but little over one per 
cent. These are not analyses of exceptional specimens, but are be- 
lieved to be fair averages of the rock used for the market product, and 
inexhaustible quantities of equally excellent material are readily acces- 
sible. The material used by the leading lime-burners at other points 
is of essentially the same excellent quality. 

Aside from chemical purity, a certain degree of porosity is desira- 
ble, since it promotes the ready escape of the gases and secures a 
uniform and complete reduction without an excessive heat and the 
consequent partial vitrification of the surface and loss of strength. 
It likewise facilitates complete slacking when used, thus tending to 
reduce the liability to slack in the wall, which is the annoying habit 
of some limes when carelessly used. The more minutely and uni- 
formly porous the rock is, the better. The formation under consid- 
eration presents abundant deposits that possess this desirable quality 
in an eminent degree, and this kind of rock is now almost exclusively 
used, the practical experience of burners having led to this, without, 
perhaps, fully appreciating the reason for it. 

Owing to these excellencies, the Wisconsin limes produced from 


882 GEOLOGY OF EASTERN WISCONSIN. 


this formation enjoy a high reputation, and are largely used in the 
Chicago market, notwithstanding the distance. When visited, the 
kilns of Messrs. H. & Y. ©. Pelton, of Pewaukee, were producing 
1,200 barrels per week, which was shipped to Chicago, Grand Haven, 
Sparta, Des Moines and elsewhere. At the kilns of Mr. Ormsby, of 
the same place, 2,000 barrels were being burned per week, about one- 
half of which was shipped to Chicago and the rest mainly to the La 
Crosse region. Messrs. Colville & Ormsby, of Lisbon, were burning 
700 barrels per week. Messrs. Horlick & Sons, of Racine, manufac- 
ture from 60,000 to 75,000 barrels per year, which is sent to the west 
and south, and to Michigan. Their business is so extensive as to re- 
quire a branch house in Chicago. Mr. Beswick, of the same place, 
burns upward of 18,000 barrels per year, which is used chiefly at points 
on the Lake Shore railroad. Mr. Vaughn, of the same place, pro- 
duces from 600 to 1,000 barrels per week, which is mostly sold at 
Chicago. At Waukesha, the Messrs. Hadfield burn and ship exten- 
sively. Mr. Johnson, in the town of Genesee, burns sufficient to sup- 
ply the local demand. Mr. Trimbone, of Greenfield, produces from 
60,000 to 80,090 barrels per year, which is chiefly consumed in Mil- 
waukee. The kiln of Mr. Druecker, near Port Washington, has a 
capacity of 250 barrels daily, the product of which is shipped to 
Chicago. At Mr. Roth’s kilns, near Sheboygan, 1,600 to 1,700 bar- 
rels per year are produced. At numerous other poiuts, there are 
kilns of capacity sufficient to supply the local demand. Probably 
400,000 Larrels may be considered a fair estimate of the total amount 
of lime burned per year from the Niagara limestone. 

Building-Stone. While this district yearly exports large quanti- 
ties of brick and lime, it continues to import more or less of build- 
ing stone. This is due less to the necessities of the case than to the 
want of development of our own resources So far as there may be a 
demand for silicious sandstone, there will probably continue to be a 
a necessity for going outside of our district, though not outside of the 
state, but the formation under consideration is capable of furnishing 
excellent material for both massive and ornamental construction. 

The careful, and in many cases, elaborate descriptions of the texture 
and bedding of the members of the formation, given under the head of 
local details, need not be repeated, and our attention may be confined to 
a few localities that especially deserve mention. The quarries of the 
Messrs. Tadfield, near Waukesha, afford excellent, compact, fine- 
grained, white, or light-gray beds, 20 inches or more, in available 
thickness. The rock has a reliable conchoidal fracture and can be 
dressed with as much ease and facility, as is attainable in so firm a 


NIAGARA LIMESTONE. 383 


rock. It is admirably adapted to use as dimension stone of various 
kinds, particularly for trimmings with white brick, with which its 
color harmonizes beautifully. 

A white and most excellent rock of similar texture is wrought at 
Johnson’s yuarry, Genesee, and is worthy of high commendation. 

Near Cedarburg, at the quarry of Messrs. Schleifer & Anshuetz, a 
white, granular, crystalline rock occurs in massive deposit without ev- 
ident bedding joints, so that blocks of any required dimensions can be 
obtained. It cuts with great facility and isa beautiful stone. Large 
quantities are shipped to Milwaukee, and the surrounding country. 

At Kuntz’ quarry, Manitowoc, a compact, fine-grained, crystalline 
dolomite of excellent quality has been mined to some exent, and even 
sawed and polished asa marble. While not suited to polishing, it is 
excellent for the coarser, ornamental purposes. In Cooperstown and 
elsewhere very fine dolomites await development. 

Gen. Q. A. Gilmore, in his work on Building Stone, gives the 
crushing strength of a two inch cube of bluish drab limestone, from 
Sturgeon Bay, as 86,000 pounds on bed, and 66,750 on edge, with the 
comment, “a remarkably solid, stable stone.” That of the white Jol- 
iet (Ill.) limestone, sometimes imported, he gives as ranging from 
45,000 to 67,000 on bed. In addition to the fine qualities of rock, the 
formation furnishes unlimited quantities of material suitable for 
rough-dressed, course work, and the heavier class of masonry. 

Flux. The limestone from Schoomaker’s quarry, west of Milwan- 
kee, is used successfully as a flux in the Bay View Iron Works, and 
the limestones from Trimbone’s and Druecker’s quarries have been 
also tested with favorable results. The pure, granular limestones in 
the towns of Cedarburg, Grafton and Germantown, may also be recom- 


mended. 


38 


GEOLOGY OF EASTERN WISCONSIN. 


FOSSILS OF THE NIAGARA GROUP. 


GENERA AND SPECIES. 


Author 
of 
Species. 


PLANTS. 
Buthotrephis, und. sp 


see e wee 


FORAMINIFERA. 


Receptaculites hemisphericus. . 
R.  infundibuliformis 


PETROSPONGIA. 
Stromatopora concentrica .... 


CORALS. 


Favosites favosus ...-.....+0.5 
Gothlandicus? (large cells). 
Niagarensis 


cells small, cheetetes-like . . 
. clavate form, 2 kinds cells . 
Astrocerium venustum 


ep CAORUMAIOE tha cece aroeg 
H. 


pyriformis ........ 
H.  spinoporus?.............. 
Syringopora compacta......... 
8S. Dalmani................. 
8. infundibula............... 
S. retiformis ..... .......... 
8, verticillata............ .. 


S. und. s 


Shumardi 


Zaphrentis, sp. res. Z. gigantea . 


Z.  turbinata 


WHC. Spi. ovisss sys awe aca, “LH 


| Mayville beds. 


Byron beds. 


| Lower Coral beds. 


Ha 


Hall 
Billings 
Billings 


EN! 


a 


x ¥! 


* 


HX EK KEK KET 


x: 
4 SSS 


| Upper Coral beds. 


| Waukesha beds. 


| Racine beds. 


* 


weal lll 


Ce a 


eX HR x! 


¥*e eR! 


| Guelph beds. 


| Not observed. 


* 


FP cos 


NIAGARA LIMESTONE. 


Fossits oF THE Niacara Group — continued. 


Author 
GENERA AND SPECIES. of 
Species. 


| Mayville beds. 

| Byron beds. 

| Lower Coral beds. 

| Upper Coral beds. 

| Waukesha beds. 
Racine beds. 


| Guelph beds. 


CORALS — (con.) 


* 
* 
* 


Aulacophyllum, und. sp....... 
Cyathaxonia Wisconsinensis . . 
Chonophyllum magnificum. . 

Chonophyllum Niagarense..... 
C. compound form .... .... 
Ch, ANG SP i cascoasedadcous: 
Cystiphyflam Americanum.... 
Cystiphyllum Niagarense ..... 
Cystiphyllum, und. sp....---- 
a pentagonus ...... 


* 
* 


CRINOIDEA. 


Platycrinus, und. sp........0.[eceese eee ecees Setetall Rana awe cihoiatesdlentete 
Stephanocrinus gemmiformis..| Hall......... brew leca'sinl awleiale gel eares 
Saccocrinus Christyi ..... «++ Halll 2:00 feraeei ig ace [aisle ol wees berets 
GS. semiradiatus sc ceciecccac[ecesasageacues rer er eee ee meee 
Macrostylocrinus striatus...... Hall os cesises ere ee 
Melocrinus Verneuili......... Troost ....... Lateral inva oat lata eble avai sons 
ae canal celatus...... Halls scsncees egal a datas wgtaed,| eeshanesl sede 

COYHULUS .. 06. e eee eee ee Halls sea ssa aa at ie aeanerfieasenta oreit I 

cornutus, var. excavatus ..| Hall......... ssotaiell ca avadibigraygil landed ae 

crassus Hall 


ornatus 


Lampterocrinus inflatus 
aaa occidentahs........ 

entangularis .... ...--- 
no locrinus rectus.........++ 
R. sculptilis.........---+--5 
Cyathocrinus Cora .......+++- 
Cyathocrinus pisiformis 
C. Waukoma ........-+000+ Hall 
Caryocrinus ornatus........-. 
Cryptodiscus .....--+.++++-+- 


ees 


ee 6 KK KKK KKK KKK RAK 


eee KRIS 


H. 
H. Winchelli.... ...--+..+. 


a 


Wis. Sur. — 25 


| Not observed. 


GEOLOGY OF EASTERN WISCONSIN. 


386 
Fosstis or THE Niagara Grour— continued. 
wo 2 ec D : i : 
Author fs a/e|¢ 3 3 f: 
GENERA AND SPECIES. of e|elielealel= le], es 
species. Be | cae Pee | ay | eB 
S =| a oO | aq a= 3° 
P/BIE| BS | esis 
Sielif#ilPlelel(ole 
CYSTIDEA — (con.) 
Echinocystites nodosus........ Hales ccnarw Rane 
Crinocystites ornatus ......... Pall sstasccocrted tee * 
ADS SPDs. rok cassette el SRVat acussant [ieee enya eR ac lel| se 
BRYOZOA. 
Lichenalia concentrica........ A es secscdiaxe * des 
Sagenella membranacea...... Fa se ccets-dcace # shes 
Fenestella elegans ........... Fallisievccsoas secs * ae 
Retépora,. und. 'Spisscixecisweleaevane va edac secon * siclats 
Polypora incepta...........-. nyt aaa ereeereoertes bana * 
Stetopora;, Sp. UN sss wrrdoewe les acing scecccencalione.s * 
Trematopora, sp. UNd.... 0. ec cfees cece eee scucleceafesecfece [es % 
BRACHIOPODA. 
Prom ats; Spe tides ex a x cial |aceees eed sseccaelllocarooells arses : one He eos llamas 
Dinobolus Comrade errr Te Pla Ds i tateceiens ce : aiad cc Pore Pee 
Monomerella prisca .......... Billings r ee sfesacig || OARS tae 
Trimerella grandis?.......... BO aeiaesea * ae © bissavs eats 
Orthis biloba .........0.0065 Linneus .....]....J.++. wich ae % | ae siliqaie 
QO. elegantilt.ecsaaisseecanal evar eeacieaasels sees “nig ecaiars PE awa 
O.  flabellula.................] Sowerby......) #* |. : * poe | * aclirawe 
QO. hybrida......... -| Dalman ..... Dl Sasoelbaenall ances | Berga oe eal) sia 
Oh TYR arerstancsatscattat arenes domains Fichwald.....f....J....{eeefeecelae] # ae leas 
Streptorhynchus subplanum onrad.......Jeeee * | % asiban sd 
Strophomena patenta......... Halll. is ceievsiase ne tasiallesesscgl|) OF See Teas 
BS. “prohunda essen ceesiaawas Conrad....... aa PO esoat | Pec 
8. rhomboidalis............. Wahlenberg..| * see | AE TL PR PRE Ws cae 
S. semifasciata ..........6. Hall esiiscascisrere: alles sian FE scacguat| acute 
Su SDs MEWir ah sina LeaamadaoullyMacewe cans cecalaes * aeellawe sl acave 
Strophodonta striata..... .... ELAM sie sence * BN scaalll cnaee 
Lepteena transversalis........ Wahl. ME Nene cliente 
Skenidium insignum?........ Hall sitiscecalsewells Bl cawtallay se 
Spiritera cudora............04 Hall os ssisiecs asi dialer cesinie || 
Des SUDDOSA irserayde ed cacoaieraslane Hall sic. seca s eel een eet 
SO LICL eiiemanioralnmerctesnrw sire Halll ic ss.n.s.0 a ae eee 
8. Niagarensis............. Hall ee stoi ac0 bes rises |! 7 
8. nobilis Barrande Soll es Bi saeises 
5. plicatella SOWELDY. aisie.n| ane sling eel vesclonanlewael OF Love, 
8S. plicatella, var. radiata.... Sowerby......J..../... x lok 
Ds SP UT isa ot fetaia.j soups te one Seeeas4| naw anes es a es * 
Meristella Hyale = Charionella 
Ten Gs ctavznsiccs’ccoreieia syonteverronses Billings.......]....].. co se ll) PERI caves 
Cyrtia myrtia.............08. Billings.......]... ¥en * 
Meristina cylindrica.......... % eal Leds 
IMB Ciia:sfecsui seats “Wes direracteoksne igi: Ee 
Mle. “anit Ay acoavs saduencen audccatevnnine x x 
Pentagonia, sp. und.......... x 
Nucleospira pisiformis........ * 
Retzia aprinis—=Atrypa and 
Rhynchonella aprinis....... * Se slatae alllds « E 
Retzia, sp. und............... wavelet ae 
Atrypa nodostriata............ * | x 


NIAGARA LIMESTONE. 


Fossits OF THE Nracara Group — continued. 


387 


GENERA AND SPECIES. 


Author 
of 
Species. 


Mayville beds. 


BRACHIOPODA — (con.) 


pisum 


oblongus.........-+e--6- 
pergibbosus 
ventricosus 
und. 
. news 
ypidula occidentalis......... 
multicostata 
Stricklandinia Galtensis? ..... 
8. multilirata 
S. undet. sp.....sccseeeeees 
GS. NeWSPi.cx veevceduee raw ss 
Leptoceelia planoconvexa -...- 
L.  plicatula 
Porambonites punctostriata ?= 
Orthis punctostriata 


LAMELLIBRANCHIATA. 


M. recta 
E. subundata 
Leptodomus Leidyi= 
Amphiccelia Leidyi......-- 
Leptodomus-undulatus 
Sohizedas? und. Sp. -seereee 
Cypricardinia arata 
Megalomus Canadensis 
Rensseleeria, n. sp 


GASTEROPODA. 


Platyceras Niagarense......- 
Platyostoma Niagarense 
Euomphalus macroliratus.... 
E. (Straparollus) mopsus ..- 
E. Racinensis 
Straparollus Hippolyte 
8. solarioides 
S. solarioides?....--++-+++++ 


McC 
Hall 


Straparollina, und. sp 


Linneus...... 


* 


| Byron beds. 


| Lower Coral beds 


| Upper Coral beds. 


hesney...|..--feeecleeeeleeeefeees 


ga eet es et 


| Waukesha beds. 


| Racine beds. 
| Guelph beds. 


* 


Hee EK 
* 


KR! 


HBR *K 


* 
x 


| Not observed. 


B88 GEOLOGY OF EASTERN WISCONSIN. 


Fossits oF THE Niagara Group — continued. 


a 2/2/o] . 
Author 2 \2 eie pele 
GENERA AND SPECIES. of e®/f/8SiS8/a/3 
Species. Alejsisel/ele 
E/s|'!] 8) 2-8 
f/ E/E) a) 213 
Sata |e ee |e 
GASTEROPODA — (con.) 
Xenophora, n. Sp... ....eeee iontaay ae wea yom ES mela lapse 
X.? trigonostoma........... Meek........ ia shsilleravdalicielsens grsesalletawe dl] OF 
Trochonema Fatua .......... Halll sis iecstsaces a 
Holopea elevata ............ Hal yees 5.03% | vent [eeealaeaalineatacceleoss 
Guelphensis........ 2... Billings...... Sear 
H.. Narmonia nase cscs sais Billings...... eed 
Cyclonema? elevatum........ Hall vesene ie 
magniventrum .......... TSPisies sweiee eellexed 
Oh PAMPlrice & cuccee ve veevee'es Hall saseie teats ba certs 
Pleurotomaria axion .... .... Hall asisveaneeus iets SNacaey [aia sail p aoe gif ecece a [idea 
P. Halei 
P. 
PR, 
Po 8 
P. 


M. 
M. 
M. 
M. 
M. 
M. macrospira........ ... Hall ais saaerieal genoa actuelane elses lexeclhe oc: 
M. Mylitta... ........0000, Bilhngs...... ssh 6! Geld fenced |eceneee [secoralltale e.c 
M.- tuwmitiformis ....... Jakoalt allies wisees dps, Bgyts fsserceallaasnardllmeenes lease eae 
Loxonema Leda ............. Hall cies gheie e d, , 

MaAgnuM............000. MS Biles eee. 
Bucania angusta............ Hal 

trigonostoma .......... H.& W...... * 
Metoptoma, sp. und......... [eceeeeeee es eee 
Trochoceras Gebhardi....... Hall 
ubulites ventricosus ......0. eee ee ce eeeaee 

CEPHALOPODA. 

‘Orthoceras abnorme.......... Hall aaecaics[ieidl na eal eacen' leds lone 6 
QO. alienum ................ ee * {olf o« 
O. annulatum Sowerby... ..]...-/....[....f..6) # 
O. Carltonense...............] n.sp......... eal eyes ar ecpeal| sranal aess foc. 
O. columnare .............. Halliccss secs s ie 5 ail Syerell a agelltesnve || 
O. crebescens............... Hal ics nese sccea-s E48 icecaafcmaellaniecal) OF 
O. HOY ee eixer sian wanes McChesney...].--.J....)....f.0--/000.1... 
QO. Laphami................ HAM ssises ce. tales] e.t Alaa Saini ce 
O. medulare ..............,. Hall.......... aside aslecaael anal ae 
O. Niagarense.............. Hall.......... ss uses eoo-cala avaiee Heagte alle wake 
Ormoceras, sp. res. OQ. verte- 

DIBIG: svniis 6 seats Geena secte a sole sites haul Sacnetans ms a 
Huronia annulata ........... Hall.......... * fo 
Discosorus conoideus...... ... Hall.......... siccipeerscs) OE oaceke 
Gomphoceras scrinium........ Halles ccscsiecy Jenalldeestee cal veel aye 
G. septoris?................ Halles wanacigeny seats listo aecvaselsceesclh Te 


| Guelph beds. 
| Not observed. 


a a ne 


FossiLs OF THE Niagara Group — continued. 


NIAGARA LIMESTONE. 


389 


GENERA AND SPECIES. 


Author 
of 
Species. 


Mayville beds. 
| Lower Coral beds. 


| Byron beds. 


CEPHALOPODA — (con.) 


ere arcticameratum. . 
brevicorne.........2.065 


.? rigidum 
(Oncoceras) Orcas. . 


aaseaaaaga 
e 
fa] 
is] 
é 
c 
B 


Phragmoceras labiatum. 
PB estor 


SD vs eeesereenreneres 
Gyroceras Hercules........-- 
Trochoceras costatum.......- 
T. Des Plainense.........-- 
Lituites Ortoni...... ....+6. 
Nautilus occidentalis ........ 


CRUSTACEA. 


Leperditia fonticola ......... 

Iilzenus armatus 
Barriensis ? 
CUNICULUS ... eee cece eens 
Daytonensis...-.+.++.+++ 
imperator...+-.+s.eeeee- 


bee e ener ence 


RRP ie 
5 
E 


n. ee samen sees 
Gatymene NG iagarensis 

Clintoni.....seeeseeeeee 
Pines TD. SPeveeeeeeceeers 
Dalmania vigilans.-.---.+-+- 
Ceraurus Niagarensis....-.-- 
Cc. n.sp 
Encrinurus Nereus-..----+++ 
E. omatus...+---+eseeeees 
LE. n.sp 
Lichas previceps pieehvare erie 
L. phlyctonodes... Beate 
Bronteus Acamas..---+++-+: 
B. Laphami......--.-s+++- 


Site cactiog Romingeri. .-- 


| Upper Coral beds. 


| Waukesha beds. 


| Racine beds. 


*) 


ek 
ae 


eX * KG 
. 


Hee RR HD TE 
a 


Se a 


Guelph beds. 


| Not observed. 


890 GEOLOGY OF EASTERN WISCONSIN. 


LOWER HELDERBERG LIMESTONE. 


Four miles northwest of the city of Milwaukee — Sec. 7, town of 
Wauwatosa —in the banks of Mud Creek, are two low exposures of a 
shaly limestone, that differs in Zthological character from both the 
Niagara limestone, upon which it rests, and the Hamilton cement 
stone, by which it is overlaid. The rock is a hard, brittle, light gray, 
magnesian limestone, distinguished -by numerous minute, angular 
cavities, that give to it a very peculiar, porous structure. It is thin. 
bedded and laminated, by virtue of which it splits very readily into 
flags and thin plates, which are, for the most part, too brittle, and too 
much subject to further splitting, to be serviceable as paving, but 
which are considered valuable for Macadamizing. A transverse frac- 
ture of some of the layers exhibits an alternation of gray and dark 
colored lamine, peculiarly characteristic of this formation. 

The rock is a nearly pure dolomite, as shown by the followiug an- 


alysis, by Mr. Bode: 


Carbonate Of lime: <:i4 os eud aaiee eed Heng Rea Beene ewes 54.569 
Carbonate of Magnesiaws s. csc 5256 cheeses eee sed dee ete daee aoa asa 43.410 
Gil1G 8) el cavascd Saavs oa Nica y lends dash eRe eee athe Bede seen tates des 1.494 
MLMINGs ceed AkGea Reel we ed dois eow re dea Dead wees aE nade 0.211 
Oxiderot rotiec i. eis eds, Se oh dee ad aa hentaeseaeanwiawies 0.316 

100.000 


The two quarries are less than half a mile apart, and lie on a near. 
ly east and west line. On this line, a little less than two miles to the 
east, along the Milwaukee river, a short distance above the Washing- 
ton street bridge, the Hamilton cement stone is found to rest upon a 
dark brown, ferruginous rock, that, to casual observation, bears little 
resemblance to that above described, but which, upon closer inspec- 
tion, is found to possess, in a large degree, the same peculiar porous 
and laminated structure, and to differ from it chiefly, in being a lit- 
tle less shaly and much more ferruginous. Its chemical composi- 
tion is shown by an analysis, by the above named chemist, to be as 
follows: 


Carbonatevof lime, 54.6 sescacieetaeedeces eeceacteaw 40ecagewaonrs 54.693 
Carbonate of magnesia......... cece e cee eeecceccenscctececaceves 41.818 
Silica: nines santas nsaewad len saiaetaen wis erdgemiacmonaeaees eens as 1.575 
MuUMINAS Gost saids Vaan ener seas Balan ates ep epelster eda cainehs tel ee ae etal 0.478 
Oxide of iron........ceeeeee cee sf aides i Siorarbiavanavarevtaternaueuas a wemiae's 1.486 


100.000 


LOWER HELDERBERG LIMESTONE. 391 


From this it appears that it differs from the rock upon Mud creek 
very slightly, except in its content of oxide of iron, which gives to it 
its dark brown color. There can be no doubt then that this is to be 
regarded as constituting the uppermost portion of the formation un- 
der consideration, which, therefore, immediately underlies the I.am- 
ilton strata. The exposure upon the Milwaukee river is very slight, 
and it is impossible to determine whether there is strict conformabil- 
ity between the Hamilton rock and that under consideration or not. 
It can only be said that if any unconformability exists, its amonnt is 
very slight, as the dip of the strata do not markedly differ. 

Extent. These are all the exposures of this rock at present known 
immediately adjacent to the Hamilton formation. Unfortunately al- 
most the whole of this region is thickly covered with drift, and ex- 
posures of rock are exceedingly rare. All the territory that can safe- 
ly be regarded as occupied by this shaly limestone will be found in- 
dicated by gray checks on the accompanying map. As hereafter 
stated, it is probable from drift evidences that there is a small patch 
on the north side of the Hamilton area, but its precise location is un- 
known. It might be presumed that the formation would occupy a 
belt surrounding the cement rock, a conjecture which has heretofore 
found expression. But the following facts forbid such an hypothesis. 
At Schwartzburg, a mile north of the outcrops on Mud creek, rock 
was reached in the excavation of a cellar, which presents all the litho- 
logical characteristics of the Niagara limestone, and contains Pen- 
tamerus ventricosus, & Niagara species. 

In the N. W. qr. of Sec. 10 and the N. E. qr. of Sec. 9, of the town 
of Granville, we find the most northwesterly known exposure of the 
overlying Hamilton formation, in the brow of a hill facing to the 
northwest. Only thirty-six paces down the gentle slope, from the Ham- 
ilton beds, a pit has been opened which discloses the Niagara lime- 
stone. The vertical distance between the top of the Niagara exposed, 
and the bottom of the quarry of Hamilton rock is about six feet. 
The intermediate slope is largely occupied with old pits, now filled, 
but in the material thrown from them, only Niagara and Hamilton 
rock was seen. In the gutter of the adjacent road, both the Hamil- 
ton and Niagara are shown, with a vertical distance of less than five 
feet between them, and in the abundant chipstone of the gutter, there 
was none of the shaly limestone under discussion. But it is a rock 
peculiarly liable to break up into chipstone, and is abundant in the 
drift near the known outcrops, and in the line of drift from them. 

‘ In view of all these facts, the shaly limestone must be regarded as 
absent at this point. The occurrence of the Niagara limestone along 


392 GEOLOGY OF EASTERN. WISCONSIN. 


the creek, a kalf a mile east, near the lower face of the Hamilton 
formation confirms this view. 

We find, however, on the north side of the Hamilton area, some of 
the shaly rock under discussion in the drift, from which it is probable 
that there is a conecaled area on that side. This harmonizes with the 
view taken in this report, viz.: that this shaly rock belongs to the 
Lower Helderberg formation, which is found in Michigan, and ab- 
sent in Iowa, according to the geologists of those states, and hence, 
must terminate in the interval, and it would seem that we have here 
the point of its disappearance. It is certain, at least, that no “ narrow 
circular rim”’ of the shaly limestone surrounds the Hamilton. 

Fossils are very rare in this rock, and I am not aware that any have 
previously been reported from it. A fair.specimen of Meristella 
nucleolata, an Orthis, resembling a young O. oblata, and an imper- 
fect specimen of Meristella or Pentamerus were the only reward of 
repeated and diligent search. 

About one mile above the village of Waubakee, in the town of 
Fredonia, Ozaukee county, in the bed of the Milwaukee river, and the 
vicinity, is a formation that deserves our consideration in this con- 
nection. On the north side of the river is a quarry in which the fol- 
luwing section is exposed: 


. Jight gray, thm bedded, shaly dolomite, resembling 
that above described as occurring at Mud creek, but 
less porous. The surfaces of some of the layers are 
covered with large numbers of a Leperditia, undistin- 
guishable from Leperditia alta... 1.10... c cece eee eens 2 ft. 


. A layer of hard dolomite, containing cavities, some 5 or 
6 inches in diameter, which are usually filled with large 
erystals of calcite. Leperditia occurs occasionally in 
THIS AV Ors sai ercatnses tradeee ovate Gaaver ease 10 in, 


. Alternating thin and thicker beds similar to No. 1 in 
lithological character, but some layers are marked with 
a dark, rusty coating. ........0.ccccee ee ce eeeseenes 2ft.2 in. 


Giallo toe, Oi aalscnangormuis an awaetbettl dy 1 ft. 244 in, 


. Moderately thick beds somewhat shaly, intermediate in 
character between the thinner and thicker beds above. . 1 ft. 


LOWER HELDERBERG LIMESTONE. 393 


The remains of Leperditia, found at this locality, are very abund- 
ant, literally covering the surface of some layers, and, to a greater or 
less extent, disseminated throngh the mass of some of the beds, but 
unfortunately the state of preservation is poor. A careful examina- 
tion and comparison of a large number of specimens leaves no doubt 
that the fossil is Leperditia alta, or a very closely related species. 

In the bed of the river a little above this locality, very thin beds of 
a softer, dark dolomite, colored by carbonaceous matter, are found. 
Some of the layers are marked by numerous black or dark brown car- 
bonaceous laminee, which give to the rock an appearance quite pecu- 
liar. This carbonaceous matter is evidently derived from the remains 
of plants, many indications of which are present, among them forms 
resembling Sphenothallus. In addition to these, two species of 
Orthis are found, one resembling Orthis oblata, and the other closely 
similar to Orthis subcarinata, but smaller. Pterinca aviculoidea, or 
a very closely allied, if not absolutely identical, species, an imperfect 
Orthoceras, and a doubtful Znocaulis, are also present. 

Farther up the stream, on the opposite side, a quarry has been 
opened which exhibits a more compact, close textured rock, and one 
intermediate in lithological character between these and the Niagara 
limestone. No fossils were found in it, and its relationship is uncer- 
tain. Its most striking peculiarity is the strong undulation of its 
strata, which allies it rather with the Niagara than with the forma- 
tion under consideration, whose beds have never been observed other- 
wise than as horizontal and perfectly plane. 

The composition of the formation at this point is shown in the 
following table of analyses by Mr. Bode; No. I being the rock asso- 
ciated with Leperditia; No. II being that in which the cavities filled 
with spar ocenr; and No. III being the dark fossiliferous rock from 
the river bed: 


I Il. Tl. 
Carbonate of lime......-.-. cece eee ee coos 53.233 56.552 52.786. 
Carbonate of magnesia.....---.++sseeeeeee 41.573 41.504 43.781 
Gilica ... 22. cece cece cere eect eee e et eneeees 2.905 1.287 3.094 
Alumina ........e0e scree cree tenet eeeeee 1.462 0.168 0.097 
Oxide of iron... see eee e eee e teeter teen eee 0.827 0.495 0.242 
Potala isa ceinapession ye euren.nwin dors oe ERS 100.000 100.006 100.000 


It will be observed that they are all essentially dolomites, with a small 
percentage of impurity, and that in compositton they do not essen- 
tially differ from the Mud creek rock. 

The location of this peculiar deposit adds interest to the problem 
of its age and relationship. A little nore than two miles to the 


304 GEOLOGY OF EASTERN WISCONSIN. 


southeast (center E. $ Sec. 30, Fredonia) is Smith’s quarry, where we 
tind a very soft, porous, granular, friable, cream colored dolomite, 
belonging, undoubtedly, tu the Niagara formation. At Newburg, 
three miles and a half to the northwest, occurs one of the more com- 
mon varieties of the Niagara limestone. To the south, similar Niag- 
ara rocks frequently outerop. To the northward, there is heavy drift 
for twenty miles. The deposit under consideration lies at a lower 
elevation than the rock at Newburg, and at about the same as that at 
Smith’s quarry. It is nine miles distant from the lake, and twenty- 
six miles distant from the deposit on Mud ereek. It is evident from 
these facts that the stratigraphical relations of the deposit contribute 
nothing but negative indications, and the question of its age and 
equivalency must rest upon its lithological character and organic con- 
tents. While it is evident that neither of these is entirely decisive, 
yet it is apparent that the weight of their testimony is in favor of re- 
ferring this formation to the base of the Lower Helderberg group. 
The same may be said of the formation near Milwaukee. The limited 
area of these deposits, and their intimate association with the Niagara 
limestone, taken in connection with the unusual changeableness of 
the latter formation, both as respects its lithological character, and 
organic contents, merits consideration however in this connection. 
On the accompanying maps, the two areas will be found represented 
by checks of the color of the Niagara formation, at once indicating 
their relationship to that formation, and their distinction from it. 

Economic Considerations. The rock near Waubakee has been 
burned for lime with fair success. It is not, however, to be recom- 
mended for that purpose, since, in the vicinity, dolomites of the 
Niagara formation of superior quality abound. Certain layers fur- 
nish excellent building material, and the thinner beds serve a tem- 
porary purpose as flagging, but their tendency to split is detrimental 
to their durability. The same remarks are true of the formation near 
Milwaukee. Both are very serviceable for the purposes of Macad- 
amizing, owing to their hardness, and, at the same time, the ease with 
which they are reduced to the proper form. 


‘ANUVOIO INAHWAO AAYMNVMTIN 


HAMILTON CEMENT ROCK. 395 


CHAPTER IX. 
DEVONIAN. 


HAMILTON CEMENT ROCK. 


The uppermost and newest of the indurated formations of Wiscon- 
sin, and the only representative of the Devonian age, is the Hamilton 
cement rock, near Milwaukee. It occupies a limited area, lying adja- 
cent to the lake, immediately north of the city, and rests in part upon 
the shaly limestone above described, and apparently upon the Niagara 
limestone in other portions. In general lithological characteristics, 
it consists of a bluish-gray or ash-colored, impure dolomite, which 
weathers, upon exposure, to a yellowish or buff color, owing to the 
oxidation of the iron which constitutes one of its ingredients. The 
impurities consist chiefly of silica and alumina. The rock is char- 
acterized in certain portions by the occasional] presence of cavities, in 
which occur crystals of iron pyrites and calcite, and, very rarely, zinc 
blende. Crystals of the two former minerals. are disseminated more 
or less through certain portions of the rock. In texture, it is some- 
what varying, being quite homogeneous in some layers, and quite ir- 
regular and lumpy in others, while the chemical composition changes 
much less markedly, though sufficiently to affect the hydraulic prop- 
erties of the rock. In degree of induration, it ranges from rather soft 
to moderately hard. The beds are usually thick, with the exception 
of some portions, which are somewhat shaly. The general aspect of 
the bedding and stratification is well shown in the accompanying 
chromo-lithograph. 

- The chemical composition of the typical portion is very fully indi- 
cated by the accompanying table of analyses of cement rocks, in which 
will be found eight analyses of the rock from the Milwaukee river, 
the selections and determinations being by different parties. 


896 GEOLOGY OF EASTERN WISCONSIN. 
ANALYSES OF CEMENT ROCKS. 

e/ 2] g $8 
ome: ae a | ae 
Authority o} 3 8 & | ig eS 
Kinp or Rock. for 4 £ ; % @ | ga (eee 
analysis. a | as} & a o | ia-A 

oO} E 7) 4a/ 6/8 
Milwaukee, No. 1........... Bode ..... 45 .54/32.46178.00)/17.56} 1.41] 3.03/22.00 
Milwaukee, No. 2........... Bode ...... 48 .29/29.19/77.48//17.56] 1.40) 2.24/21.20 
Milwaukee, Layers 2-6...... Bode ...... 47.55)/30.91/78.46)/13.74) 3.95) 3.85/21 .54 
Milwaukee, Layers 7-11..... Bode ...... 47.09/24.95)72.04/|18.77] 5.14) 4.05/27.96 
Milwaukee, Layers 2-11 ..... Bode ...... 45 .44/31.27/76.71/|15.65| 4.60] 3.04/23.29 
Milwaukee................. Doremus .. .|45.57/27.67/73.24//15.60} 12} .88/27.98 
Milwaukee, Wash. St. bridge; Bode...... 41 .34/34.88]76.221/16.99] 5.00) 1.79123.78 
Milwaukee, Wash. St. bridge} Bode ...... 40.05/35.82/75.87//17.00; 5.00] 1.80/23.80 
Milwaukee, average.........J..--..eeeeee 45.11}30.89]/76.00)|16.61] 4.09} 8.25124.00 
Rosendale, New York....... Gilmore. . . .|46.00/17.76/63.76]|27.70) 2.34) 6.20/36.24. 
Utica, Minois.......... 24. Gilmore... .|50.42/18. 67/69 .09|/21.60] 5.27] 4.04/30.91 
Utica, Ilinois...... ....... Reid ...... 58.84)15.38/64.221/25.20) 6.16} 4.40/35.76 
Alzon, New York.......... Gilmore ...|35.60}19.26/54.86//33.80] 3.96] 7.38/45.14 
Alzon, New York.......... Reid ...... 35.60/19. 26/54.86]/33.80] 3.96] 7.38)]45.14 
Sandusky, Ohio..... ....... Reid ...... 40.54/17. 98]58.52//19.66] 3.14} 5.36/40.26 
Points aux Roche, L.Champ’n; Reid ...... 53.30)22.60175.90//20.07] 1.70] 1.70123. 44 
Cumberland, Maryland...... Gilmore. .. 41.80] 4.10/45.90]/21.74/16.74]15.30156.78 
BISA seca erot siesta § Berthier .. ./65.70] 0.50/66.20/|18.00] 6.60] 8.80/33.40 
Bologne, France............ Drapies.... .[61.60] 0.00/61.60]]15.00] 4.80]15.60/35.40 
Vasey cP Vance iss comodieansell aosteenamyas 63.80} 1.50/65.30}/14.00) 5.70/15.00/34.70 
Theil, Pram @es<:sisraesiaayacqevrati Reid ...... 60.00} 1.32/61.32//18.20] 1.20/11.28/30.68 


Organic Remains. The Hamilton period marked-a new era in the 
history of the life of the Wisconsin formations. While multitudes 
of Protozoans, Radiates, Mollusks and Articulates lived in the Sil- 
urian seas, and left their remains embedded and embalmed in the 
accumulating sediments, whether of sandstone, shale or limestone, no 
fragment or trace of a Vertebrate has been found. The Hamilton 
period witnessed the introduction of this highest type of the animal 
kingdom into the Wisconsin series. In other portions of America, 
the remains of Vertebrates appear somewhat earlier, in strata wanting 
in our state, and, in the deposits of Europe, still earlier. The ver- 
tebrate remains of this formation are confined to the relics of fishes, 
and, unfortunately, these are fragmentary and imperfect. They have 
been submitted to the inspection of Dr. J. 8. Newberry, a most 
eminent authority in this department of paleontology, who finds them 
to be new and unknown species. They consist of fragments of the 
teeth of Chimeeroids and a plate of a Placoderm. Only one specimen 
is sufficiently well preserved to justify description, and being thus 
exceptional in character, may merit the partiality of delineation here. 
The following is the description of Prof. N. ewberry: 


HAMILTON CEMENT ROCK. 897 


Phynchodus excavatus. Newberry. 


Tooth small, when entire, perhaps two and a half inches long by 
one and a quarter inches deep; crown alone preserved. Of this, the 
external surface is marked vertically with vermicular furrows; supe- 
rior margin sinuous, terminating anteriorly in a prominent point; the 
superior surface irregularly excavated and roughened, showing two 
prominent points, or tubercles, one on the middle of the exterior 
margin, the other on the inner margin, and near the anterior ex- 
tremity. The inner surface of the tooth shows a prominent ridge, 
running up to the anterior point. This tooth is evidently fitted for 
trituration rather than cutting, and resembles, in its general form, JZ. 
Frangens of the Corniferous limestone. It is, however, much smaller 
‘and thinner, and the tubercles of the upper surface are differently 
situated from what they are in the tooth of that species. 

Locality and Formation. Hamilton Group. Brown Deer, Mil- 
waukee county, Wisconsin. 

In addition to the fish remains, there are the following inverte- 
brates: Of Bryozoans, a Fenestella and a tuberculated Zrematopora 
occurring in massive and frondose forms; of Corals, the ‘cast of the 
cup of a Cyathophyllum; of Brachiopoda, a new species of Lingula, 
and also one of Discina, Orthis impressa, and an undetermined 
Orthis, Strophodonta demissa, S. perplana, Chonetes coronata and a 
species closely resembling C. deftecta, a Productella, allied to P. 
spinulicosta, Spirifera mucronata, S. medialis, S. granulifera, 8. 
fornacula, 8. pinnata, a species allied to S. fornacula, but larger 
-and one near 8. angusta, Spiriferina zigzag, Cyrtina Hamiltonensis, 
Trematospira hirsuta, Atrypa reticularis, A. occidentalis, Lewor- 
hynchus, resembling LZ. Kelloggi, of Lamellibranchs, a Pteronites, 
Paleoneilo constricta, P. emaryinata, a species allied to P. plana, 
Modiomorpha concentrica, and an undetermined species; of Pter- 
opods, an Heculiomphalus, closely resembling Euomphalus lacus; of 
Cephalopods, two new species of Gomphoceras, and an Orthoceras; 
‘and of Crustaceans, Phacops rana. 

These show a preponderance of Hamilton forms, some of which are 
highly characteristic species, and occur in great abundance. With 
these are mingled a number of Cornifcrous species, representing a 
Jower horizon, and a few Chemung forms belonging to a higher 
series. 

Age. The foregoing fossils are entirely decisive as to the age of 
the formation, and place it in the early portion of the Hamilton 
period. This is entirelyin harmony with its stratigraphical relations 
and with the general geological structure of the interior of the conti- 


398 GEOLOGY OF EASTERN WISCONSIN. 


nent, since, eastward from Wisconsin, there intervenes between the 
Hamilton strata and the Niagara series, the lower Devonian and the 
uppermost Silurian formations; while to the westward, in northern 
Illinois and Iowa, the Hamilton beds rest directly upon the Niagara 
group. The intermediate formations thin out and disappear, and, as 
already indicated, the vanishing edge of the Lower Helderberg strata 
barely reaches the eastern margin of our state. The mingling of Cor- 
niferous species from below with Chemung forms from above is not 
age of the only an interesting fact in itself, but is one whose bearing 
upon the deposit is most significant and decisive, and establishes the 
correctness of its reference to the Hamilton period. 

Local Descriptions. The most extensive and important outcrop 
of this formation is found along the Milwaukee river, in the vicinity 
of Washington Street Bridge, extending above and below, in Secs. 
4 and 5, T. 7, R. 22 E. The rock nowhere rises to any considerable 
height above the river-bed, so that no extensive vertical section can 
be seen, and the frequent interruptions of the exposure, as traced 
along the river, prevent any trustworthy correlation of the strata. 
The lithologival characters of the rock at this point are essentially 
those before given as general characteristics, and this locality may be 
regarded as the typical one of the formation. A portion of the layers 
fuund west of the bridge are more shaly than the average rock of the 
formation, and tend to disintegrate somewhat more readily on expos- 
ure. <A stratum found below the bridge possesses a more granular 
character than the rest of the formation, but the chemical analyses 
that have been made of the several portions, indicate that these varia- 
tions are largely of a physical nature, and that the chemical com posi- 
tion is less varying. In the drift lying upon this rock, an abundance 
of black shale is present in thin, fragile, more or less rounded chips, 
indicating the near presence of the formation from which they are 
derived, and which may be conjectured to be the overlying black slate, 
so abundant in other regions. No exposures of this rock have, how- 
ever, been discovered in Wisconsin, but as this region is extensively 
covered with drift, it is not impossible that they exist. 

Nearly all the species of the foregoing list have been found at this 
locality, notwithstanding the limited extent of the exposure, and indi- 
eate a rich and abundant fauna. The working of the beds, which has 
been commenced since this collection was nade, and the importance 
and interest which now attaches to the formation will, doubtless, 
very much increase the number of species now given, and develop 
specimens which will more fully elucidate the structure of some that 
are now imperfectly represented. 


HAMILTON CEMENT ROCK. 899 


In section 11, town of Granville, a railroad cut just south of the 
flag station, known as Brown Deer, exhibits a few feet of this forma- 
tion. The original lithological characters are essentially those already 
described, but the rock of this locality has been more extensively 
weathered than that near Washington Street bridge, and presents a 
buff color, except in the interior of some of the heavier layers, and is 
also somewhat decomposed in certain portions. This is the typical 
locality of the Chimeroid fish, Rhynchodus excavatus, previously 
described, and with it are associated the leading forms of the general 
list above given, prominent among which are Orthis impressa, 
Strophodonta demissa, 8. perplana, Sperifera pinnata, S. medialis, 
Speriferina zigzag, Atrypa reticularis, Palwoneilo constricta, 
Modiomorpha concentrica, and others. It is stated that in the bed 
of the Milwaukee river opposite this point, the formation exists in 
place; but it was not accessible at the time of our investigations. 

In sections 9 and 10 of the same township, occurs the most 
northwesterly exposure of this formation now known. It occupies 
the brow of a hill, underlaid by limestone belonging to the Niagara 
formation. The rock is here a rather soft, granular, buff, impure 
dolomite, much stained with iron, doubtless due to the decomposition 
and oxidation of pyrites, originally disseminated through it. Orthis 
impressa, Strophodonta demissa, Spirifera pinnatu, Atrypa occi- 
dentulis, and A. reticularis, show the character of the fauna. 

Along the lake shore, on Whitefish Bay, the formation rises 
slightly above the water level in a very limited exposure. The strata 
at this point have a firmer texture, but more uneven structure, than 
at the previously named localities. The lines of deposition and bed- 
ding are irregular. Angular cavities of moderate size are not unfre- 
quent, some of which are filled with a semi-fluid, tar-like bitumen. 
An analysis of this rock by Professor Daniells shows it to have the 


‘following composition: 


Carbonate of Hime .....- cee cee eee e treet e reece ener eee eee eenne 49.12 
Carbonate of magnesia..... 0... sec e cece ect e eee r eee t nent eee e ee wee 38.76 
Sulphate of lime... ...-eeeeeee cee tee cere tent eee eet teen eee 0.07 
Phosphate of lime....--0---seesece scenes cette ene ee eset er eee e nes trace. 
Sulphur... 6... cece cece ee eee eect ee ene tere e eee e ees trace. 
Gas ocx aks <ntes GdaseemnuniGinns dha phe eA No oes ais Hamels 8.59 
Sesquioxides of iron and alumina ...-.. +++. e+ eeeeeeeeee eters etree 3.51 

100.05 


From this it will be seen to have much less silica and alumina than 
the beds on the Milwaukee river. 


400 GEOLOGY OF EASTERN WISCONSIN. 


The following species were collected at this point: Orthis im- 
pressa, Strophodonta demissa, S. perplana, Sperifera medualrs, S. 
pinnata, Atrypa reticularis, Palwoneilo constricta, P. emarginata, 
Modiomorpha concentrica, two new species of Gomphoceras, Pha- 
cops rand, and several imperfect forms belonging to the genera 
Cyathophyllum, Lingula, Spirifera, Palwonetlo, Modiomorpha and 
Eceuliomphatus, and the plate of a Placoderm fish. 

Economic Considerations. The credit of first calling attention to 
the hydraulic properties possessed by the rock of this formation be- 
longs to the late Dr. I. A. Lapham, who, some years since, directed 
attention to it as probably possessing the property of hydraulicity. 
In an article prepared for Walling’s Atlas of Wisconsin, under date 
of July, 1874, he called attention to the geological relation existing 
between this rock and the water-limestone of Louisville, Ky., with a 
suggestion as to its possessing the same useful qualities. The first 
investigations upon the part of the geological survey were made by 
the party under my charge, between the 5th and 12th of June, 1874, 
and specimens were sent to the chemist of the survey for analysis on 
the latter date, but owing to the crowded state of that department, 
analyses were not received until the following year. The investiga- 
tions of Dr. Wight upon the same subject in the year 1875 are fully 
stated in his Annual Report. The credit of demonstrating by actual 
tests, the unusual hydraulic excellence of the rock of this formation, 
is due to the gentlemen constituting the Milwaukee Cement Co., and 
to Mr. D. J. Whittemore, Chief Engineer of the C., M. & St. P. R. 
I. To these gentlemen I am under obligations for the following 
facts, relating to their interesting and important investigations: + 

The first series of experiments of Mr. Whittemore to determine 
the quality of this rock as a cement stone, and the strength and value 
of the product, extended continuously over nearly one year and a half, 
and embraced about 1,500 individual tests, and perhaps an equal num- 
ber has been made by him and other competent gentlemen since. 
These experiments were conducted according to standard methods, 
with excellent apparatus, and appear to have been characterized by 
impartiality in selection, and conscientious care in manipulation. The 
results obtained from the commercial cements with which comparison 
was made compare very favorably with those obtained by other com- 
petent experimenters upon the same products, which indicates that 
the selection was a fair one, and as the several samples were subjected 
to the same processes, the results possess much more value than if 


"See a paper read before the Fortnightly Club of Milwaukee, November 4, 1875, by 
Don J. Whittemore, of which the following is little more than an abstract. 


HAMILTON CEMENT ROCK. AOL 


the data; with which comparison is made, were compiled from trials 
made at various times, and under varying conditions and manipula- 
tion” The Milwaukee cement was prepared by calcination in cru- 
cibles with varying degrees of torrification, and, in the absence of 
experimental knowledge of the peculiarities of the rock, it cannot be 
supposed that the maximum of good results was secured. Mr. Whit- 
temore expresses the opinion that, with proper care, a better com- 
mercial article than the one used might be manufactured. 

The commercial cements were obtained as fresh as possible from 
the stock in the market, a selection being made from large quantities, 
and only those used, that, upon trial, were found to be of good qual- 
ity. To secure uniform fineness, only that portion of each product 
was used that passed through a sieve of 2,704 meshes to the square 
inch. 

The following table shows the tensile strength in pounds per square 
inch of mortars of clear cement, seven days old, the last six in water; 
aso of mortars composed of equal weights of cement and sand at 90- 
days, the last 89 in water: 


TENSILE STRENGTH, IN PouNpDs 
PER SQuaRE Incu, or Mortars 
COMPOSED OF 
Kinp or CEMENT. 
Equal weights of 
Clear cpa sev- ae ‘and sand, 
eu daye'o ninety days old. 
Commercial Cements — 
INGO. Lscsaieiea-ci-300 142 O04 a8 HAE eee 95 194 
Oy iasincic aig nablgie G80 EOE Sie OE SHAE EGS 77 185 
Nese gausad Gu, Baar cd sa eide BG Solecea PROS ATTN 388 1524 
Th siadh eb a lgtar 6 vewasg a SCavac cle: ae fe- dD ahaRDoueT oes 97 que 
By Au doula kann chad Ge masta 10744 
OT esl ccs deca anna Ns teh beatae Ba asen bua ea 13914 20414 
Be rad prick ide scatertile ae dope ask Sve ms ealost ae AA | N asaiseideenavhay Guavacorsys erat 
Q). cnc gue diacaiisied sie oes keh eae oat ears 36 140 
10} oss actiiesecepe enue cae sa meson 941g 18234 
Ve vacanunatnin mearecesael ears se 95 280 
1 Dh sual irbseisliigts hua-aie nly on widlateteccte steiaiok 9814 149 
TO cxsiatinewracen hissed soldier lea sou 90 157 
DA 20 metacenachiecte’ Guay ues abs WANA ERAT 4 196% 
2 diene Sodas AUT OPRRES Bal OWE Pe aa Stag Se 101 190 
bEkaA mneegiones AOE BE ORES EPEAT TIES 98 20234 
“Milwaukee Cémbiitcnccatacr cor eeer sews 96 290 


In the above table, the result for the Milwaukee cement was ob- 


1 Those who may wish to compare the results obtained by Mr. Whittemore with those 
of others will find the means of doing so in Gen. Q. A. Gilmore’s standard work on 
‘Limes, Hydraulic Cements and Mortars. 

Wis. Sur. —26 


402 GEOLOGY OF EASTERN WISCONSIN. 


tained from the average of separate tests of two samples taken from 
widely different parts of the outcrop on the Milwaukee river, and cal- 
cined, one four, and the other three hours, and from a mixture of 
these calcined for two and a half, three, three and a half, four, and four 
and a half hours, respectively. The results indicate a convenient lat- 
itude in calcination, which is an important consideration in securing 
a uniformly reliable commercial product. 

To ascertain the breaking stength of the cement, rectangular bars 
one inch square, in cross section, and four inches long, were prepared, 
from the several samples tested, in a precisely similar manner, and al- 
lowed to set under an end pressure of 32 pounds; when they were 
removed and kept one day in air and ninety-nine in water. They 
were then broken by resting them upon supports four inches apart 
and applying weight gradually at the center. The results are given in 
the following table: 


BREAKING STRENGTH OF CEMENT MORTARS. 


WHITTEMORE. YARDLEY. 


Kinp oF CEMENT. 
Cement 2 | Cement 1 | Cement 2 | Cement 1 
Sand 1]|Sand 2/;Sand 1]|Sand 2 
Commercial Cement, No. 1 54 OU le sehncar cig sai ap yeseiay gine 
HOO sscoe irate Ox 5-5 3. 59 BAVA. © ls cetsictwisvuieiaie |arnia aie aiee 9 
. do. swlOuns s Acs 9846 441g 64 82 
.-do. -do. ve 100 47 70 33 
do. ..do. 10 59 ASH lien exedtaratatartid| Weave, chat’ 
jase Oued Seated do... 11 107 56146 62 20 
Milwaukee Cement calcined 24g hours..| 11934 BOLE. | y wswadeene go eles eels 
Or cece naeaed dOsssceseces 3hours...| 12094 TOMA, || -wesewmawsslaces iwi 
OO is dar vacty Git erneaics 4 hours 11914 DIG |wwaewaw sas |siad eevee 
AOsscnsrns do. .mixture (before men- 
Hored vse ev eaveseeasae essesssn 188 DD  |sviivaswsaaleveseree os 
Milwaukee cement, average .--:4--++-- 124 69 


From the above, it will be seen that the average breaking strength 
of the Milwaukee cement is 16 per cent. higher than the best result 
obtained from the six commercial samples tested, when the propor- 
tions were two of cement to one of sand, and 22 per cent. when the 
proportions were one of cement to two of sand. The average of the 
Milwaukee cement exceeds the average of the commercial cements by 
56 per cent. That this difference is not due to inferiority in the com- 
mercial cements used by Mr. Whittemore appears from a comparison 
with the results of tests made by Edward Yardley, ©. E., reported in 
the transactions of the American Society of Civil Engineers for 1872, 
and given in the table above. Mr. Yardley’s specimens were of sim- 


HAMILTON CEMENT ROCKS. 403 


ilar form, composition and age, but were made plastic like mason’s 
mortar, while Mr. Whittemore’s were all made stiff. Making all due 
allowance for this, it still appears evident that Mr. Whittemore used 
a superior selection of commercial cements. 

For determining the crushing strength, cylinders of mortar having 
a base area of one square inch, and a height of one inch, were formed 
from the several cements, and kept under a pressure of 32 pounds 
until set, when they were kept in a dry room one day, and then im- 
mersed for 89 days in water, when they were crushed, several samples 
of each being used. The following table gives the results obtained: 


CRUSHING STRENGTH, 


In pounds per square inch, of cement mortars, 90 days old, the last 89 in water. 


oD 
Composition or Morranrs. see 
ees 1 oem | 
Sg 
Kinp oF CEMENT, ro) 2 & 
~~ 
4 8 ni a ai Ee 3 
ea} gs g g g a. | vd 
oO a 4 af 
(NOs disGeveess 2,775 | 1,980 884. 299 128 | 1,311 | 33 
NO» -2.ssaxecss 2 1,614 794 337 180 | 1,811 | 83 
No. Bisxes eee 2,028 | 1,661 | 1,071 417 233 | 1,721 43 
NO: Ais acs cues 3,302 | 2,767 | 1,536 802 524 | 2,893 | 70 
NO. Osasecerse 2,983 | 2,150 939 742 | - 472 | 2,153 | 54 
Commercial ~ No. 6......... 3,479 | 3.060 | 1,590 895 615 | 3,100 | 77 
: INO. “Tawwscows ae 4,742 | 3,475 | 1,737 843 625 | 3,205 | 80 
NOs. Sidainses ced 2,767 | 2,396 | 1,596 | 1,068 571 | 3,235 |] 80 
NOs Oeaticice< 3,789 | 3,156 | 1,900 95: 586 | 8,441 85 
NO. 10..scaie cys 3,247 | 2,981 | 2,075 | 1,208 750 | 4,030 | 100 
L Noe ies: aie s 5,019 | 3,572 | 2,180 | 1,192 681 | 4,003 | 100 
seb car cosa tnvovsiteenee Pte ai Soeceud ld tnaivauies 2.340 | 1,596 | 1,083 | 5,019 | 125 
‘ B 3,705 | 3,691 | 2,146 | 1,261 | 1,127 | 4,534 | 114 
Milwaukee @7777277°1727"] 3887 | 3'391 | 27478 | 13467 | 1,083 | 5,098 | 195 
B and C Mixture} 3,704 | 3,469 | 2,497 | 1,479 | 1,135 | 5,111 | 128 
Portland occ sais axiveduininsics 5,330 | 4,630 | 3,356 | 1,769 792 | 5,917 | 148 


By an inspection of the above table, it will be seen that in the 
streneth of the clear cement, the commercial articles Nos. 7 and 11 
surpass the Wisconsin product, but as the admixture of sand is in- 
creased, the relative superiority of the latter becomes very conspicu- 
ous. It appears that the larger the proportion of sand, the greater 
the relative value of the Milwaukee cement. Since cement is usually 
used with at least an equal quantity of sand, the columns in the above 
table that give the proportions of 1 to 1, 1 to 2, and 1 to 3, indicate 
the practical value of the products examined, and they therefore are 
combined in the sixth column of the table. The last column gives in 
a more convenient form the value of the several cements for the pro- 


404 GEOLOGY OF EASTERN WISCONSIN. 


portions indicated, the two best commercial cements being taken as a 
standard of comparison, and expressed by 100. It will be observed 
that the average of the tests of the Wisconsin product, exceeds the 
highest of the commercial articles by 23 per cent., and exceeds the 
average of the eleven, which represent the relative strength of the ce- 
ment in the Milwaukee market, by 54 per cent. The remarkable im- 
ported cement, known as Portland, was included in these tests, and the 
results are given in the table. As it is extensively used in Europe, 
and has been submitted to a great many trials, its character and value 
are well known to engineers and experts, and it therefore furnishes a 
valuable standard of comparison. Within the proportions named 
above, the Wisconsin cement surpasses the best of the commercial 
cements almost as much as it is surpassed by this unrivalled artificial 
European product. 

It remained to test the adhesive strength of this mortar, and for 
this purpose Mr. Whittemore joined common brick crosswise with 
mortar composed of equal parts of cement and sand, and kept them 
under a pressure of five pounds per square inch, until the mortar had 
set, when the brick were packed in damp sand for seventy days, and 
then were separated by tensile strain, with the following results: 


Commercial; cement NO. 1 axis doc ais ansisecrtided mann aiadulaaloaseolutvawien 3934 
a “ BD oie aah a,tin dacta Guise aod dyer nepaked SAEeMeeet 59 
e i OD adi ntgie ears data arena’ Secs glue slag alban gieilampatie 16 
es we OU: A eletinie ee nah oe Perey aeeatadeean état 2733 —~CO« 
“ BS UG dace ks celle h eA TN ao 4134 
eo ee Ye SU Gries aa ec tase asi ce. SSP e ADM AD. Sed RAMI ase asbls as 541g 
e “ Sts neha laa felene Ouuheoidseina sak algiem Cyuradana nial 4134 
‘ a OAD: 3 sxsioe in cnaadrnteiniteaersiahisriney a tae eerste Soe ales 66 
“ tiie, dca aeghecs essa ety ie Ia sO 6314 
Average of commercial cements ........- 0.00 cccecseecsecesecseeeness 451g 
Average of three products of Milwaukee cement..........00..0 ceeeeees 751g 
English Portland iss scak nena vena toaawes/ ghuie asa gua bs Peaeecaetaas 4716 


In many instances, the result only shows the cohesive strength of 
the brick, since after a strain of 60 pounds is reached, the brick is of- 
ten ruptured instead of the mortar. 

Sawn slabs of marble treated in a similar manner showed an adho- 
sive stréngth of 53} pounds, when joined 96 days. The rate of indu- 
ration was ascertained by crushing cylinders composed of equal parts 
of cement and sand, at the end of every five days up to ninety. The 
following series indicates the strength, in pounds, per square inch, 
attained, beginning at the age of five days and ending at ninety: 403, 
837, 1,178, 1,519, 1,953, 2,418, 2,635, 2,759, 2,867, 2,976, 3,068, 3,162, 
3,255, 3,882, 3,410, 3,487, 3,571, 3,658. 


‘HAMILTON CEMENT ROCK. 405 


Gen. Q. A. Gilmore, U.S. A., the highest authority upon this sub- 
ject in this country, gives as the average tensile strength of the Mil- 
waukee cement, at the end of seven days, 644 pounds to the square 
inch, and that of the standard brands of five of the Rosendale compa- 
nies at 47 pounds. He also informs me that the commercial product of 
the Milwaukee stone, used under his direction at Washington city, 
for making concrete, produced excellent work. Similar testimony is 
given by others who have used the cement. The excellence of the 
product may therefore be regarded as established. 

Four large kilns, with a mill and accessory works, have been already. 
constructed and put in successful operation. The extent of the deposit 
is abundantly sufficient for all anticipated wants, and its location is 
convenient and accessible. The description of so interesting and im- 
portant a resource forms a fitting close for our discussion of the geol- 
ogy of Eastern Wisconsin. 


H.HBennett,Photo. 


Tae Muwavnee Litto.k Excr Co 


Devils Lake from the SouthBluff, Kirks Bluff on the right +75 ft. high. 


PART IIL 


GHOLOGY 


OF 


CENTRAL WISCONSIN. 


BY ROLAND D. IRVING. 


INTRODUCTION. 


The following report covers a region having an area of about 10,000 
square miles, and is the result of something more than nine months, 
in all, of field work. The greater part of this was done in the seasons 
of 1874 and 1875, my work during the other years of the existence of 
the survey having been in the Lake Superior country, which will be 
treated of in a subsequent volume. 

The district now reported on, including the central counties of 
Wisconsin, is nearly one-fourth larger than the state. of New Jersey, 
whose third geological survey has been in progress from 1864 up to 
the present time, and has issued, besides numerous annual reports, a 
large volume of nine hundred pages, and an atlas of maps. Prof. 
Geikie, director of the geological survey of Scotland, has recently 
made the statement, in a public lecture, tuat the average annual 
amount of ground gone over by each geologist of that survey is about 
one hundred square miles, this amount of labor being performed by 
an average daily walk of ten to fifteen miles, in a year of two hundred 
days in the field. At the same rate, an examination of the Central 
Wisconsin district would require over one hundred years of continu- 
ous work. These statements are made in order that a fair judgment 
may be passed upon the results accomplished, as compared with those 
of the surveys of other states and countries, and in order that it may 
be understood that no claim is made of having made an exhaustive 
survey of the district reported upon. 

Geological mapping is accurate, ceteris paribus, exactly in pro- 
portion as the geographical maps used as a basis are accurate. One 
great advantage enjoyed by the surveys of Great Britain lies in the 
almost absolute accuracy of the celebrated Ordnance Maps of that 
country, which are drawn on a scale of six inches to the mile, and 
show every topographical feature, road, and house, with such faithful- 
ness that the geologist has little more to do than to mark upon them 
outcrops as fast as found. In the United States, the only maps hav- 
ing any genuine claim to accuracy are those of the coasts of the 
continent, and of the shores of the great lakes, made by the gov- 
ernment triangulation surveys, and even these are, for the most part, 
on too small a scale to be of much use in geological mapping. Nev- 
erthcless, in this regard, we have in Wisconsin a great advantage over 


410 GEOLOGY OF CENTRAL WISCONSIN. 


most of the older states of the Union, in the possession of the United 
States Linear Surveys, which have divided the whole state up into 
townships of thirty-six square miles, and these again into sections of one 
square mile each. Plats of each township are always to be obtained, 
drawn to a scale of two inches to the mile, and showing marshes, prai- 
ries, streams, and timber land; all of which are pretty closely correct 
where crossed by the section lines, though elsewhere only roughly ap- 
proximate. With these maps, a little trouble suflices to locate out- 
crops with considerable accuracy, and the task becomes still easier in 
the case of those few counties of which there are atlases showing the 
locations of roads and houses. Notwithstanding the size of the dis- 
trict, and the shortness of the field work, it is believed that the maps 
accompanying this report will compare favorably in closeness of detail 
with those made of any other states in the Union. 

The present report is the only comprehensive one ever made on the 
area included within the Central Wisconsin district, the greater part 
of which has, indeed, never before been geologically examined, al- 
though a number of weconnoissances along certain lines have been 
made in former years. About 1847, Dr. Randall, one of the corps of 
the United States survey of Wisconsin, lowa and Minnesota, under 
Dr. D. D. Owen, made a trip along Black river from the falls to the 
Fourth Principal Meridian. His observations occupy two or three 
pages in Dr. Owen’s final report,’ and are accompanied by one or two 
colored sections. In the same year, Dr. J. G. Norwood, another of Dr. 
Owen’s corps, made a canoe trip along the Wisconsin from its source 
to Sauk City. His observations, in the form of an itinerary, cover 
about fifteen pages* of the same volume, which includes also about 
twelve pages* by Dr. B. F. Shumard on the valley of the Wisconsin 
below Portage. In 1855, Dr. J. G. Percival, then state geologist, 
spent five months in making a general reconnoissance of the entire 
state, visiting all but twelve counties. His report on this reconnois- 
sance, printed after his death in May, 1856, covers about fifty pages, 
in which each formation is taken up in regular order. Whilst this 
report is tinctured somewhat with the older ideas, and some of its 
statements have been since proved erroneous, and although Dr. Per- 
cival did not have the advantages of the latest discoveries in the 
science, and of the light now to be obtained from the geological reports 
of adjacent states, nevertheless his general summary of the geology 
of the state, so far as my observation goes, is an exceedingly faithful 
one. The report was published only as a small pamphlet, and has 
never received the credit it deserved. How far the survey under Mr. 


1 Owen's Geological Survey of Wisconsin, Iowa and Minnesota, p. 151. 
2 Ibid, pp. 277-293.  * Ibid, pp. 510-522. 


INTRODUCTION. 411 


James Hall, in 1858-1861, extended into the Central Wisconsin dis- 
trict, I have no means of knowing, since no reports were ever pub- 
lished, except that on the lead region by Prof. Whitney. The large 
geological chart of Canada and the northern United States, issued by 
the Canadian Geological Survey, gives some quite accurate details 
with regard to the distribution of the Lower Silurian formations of 
Central Wisconsin, and as these were contributed by Mr. Hall, they 
would seem to indicate that a good deal of work was done by his sur- 
vey that was never published. 

Future surveys will, beyond doubt, make farther and more detailed 
observations than now submitted, points now in doubt will be cleared 
up, and new generalizations, now unthought of, will be made. 
Amongst those points that now appear especially to need further in- 
vestigation, may be mentioned the detailed structure of the Archean 
terranes of the northern part of the district, and the question as to the 
existence of two distinct formations within what is now called the 
the Potsdam sandstone series, the one resting upon the eroded surface 
of the other. The first of these can be fully attained only by an ex- 
haustive traversing of the unsettled regions on foot, the location of 
every outcrop, and the microscopic examination of all specimens. 
The Archean ranges of the Baraboo valley, too, deserve a more de- 
tailed study, and such a one as can only be given by the most thorough 
traversing on foot. 

The general arrangement of this report, by geological formations, 
seems to be the only logical one. A complete arrangement by coun- 
ties involves a great deal of repetition, and renders a report far less 
intelligible to those outside the state. Nevertheless, it has not been 
thought best to carry the geological arrangement too far, and the local 
details are, therefore, arranged geographically, so that information 
with regard to any particular locality may be the more readily found. 
Moreover, in giving details with regard to the several Silurian forma- 
tions, these have been grouped together, because in much of the dis- 
trict the areas occupied by them are so interwoven that any attempt 
to give the details with regard to each separately would result only in 
contusion. It isa matter of great regret, tome at least, that the 
small space necessarily assigned to this report has rendered it impos- 
sible to print all of the manuscript prepared. The pages thrown out 
include a detailed topographical and geological description, by town- 
ships, of most of the Silurian portion of the district, and the plan of 
the report is marred by the omission. An Appendix on Artesian 
Wells and a Chemical Appendix, in which are tabulated, with addi- 
tions, the analyses cited in the folowing pages, for the most part the 

work of Mr. E. T. Sweet, are also crowded out. 


412 GEOLOGY OF CENTRAL WISCONSIN. 


The parenthetical numbers of the detailed descriptions of this re- 
port are those of specimens representing the rocks described. These 
specimens will be distributed, according to law, to different institu- 
tions in the state, and will be much more valuable for being cited here. 

It remains to make acknowledgments for aid received in the pros- 
ecution of the field work, and in the preparation of this report. 

Mr. E. T. Sweet, M.8., a graduate of the State University, aided 
me in the field work throughout the season of 1874, and during much 
of that of 1875. Several of the towns in Dane county were mapped 
wholly by him, besides which he made many independent observations 
in other parts of Dane county, and in southeastern Columbia county 
Mr. Sweet also aided greatly in the chemical work, having been thus 
employed especially during the winter of 1875-6. With very few ex- 
ceptions all of the analyses given in this report are Mr. Sweet’s work, 
and full credit is given him here for them. 

The late James H. Eaton, Professor of Chemistry and Mineralogy 
at Beloit College, aided me in the fleld work during about two months 
in each season, his services being given for his expenses only. His 
faithful observations, more especially with regard to the Glacial Drift, 
have contributed much to the material of this report. It is no exag- 
geration to say that in Professor Eaton’s death the state has lost the 
best trained and most accomplished, and at the same time one of the 
most conscientious and painstaking of its scientists. 

In the latter part of 1875, Mr. G. C. Synon, B. 8., was my aid in 
the field work. Messrs. Oliver Matthews and W. A. Hover, of the 
Metallurgicat Department of the State University, have both given 
aid gratuitously in field work, and in making analyses. Analytical 
determinations have also been made gratuitously by Mr. A. ©. Pres- 
cott, in the University laboratory. Messrs. J. P. Paine, A. D. Con- 
over, and P. L. Norman have aided me in preparing the cuts and 
plates for this report. Mr. W. H. Canfield, of Baraboo, for many 
years a surveyor in Sauk county, furnished me with a map of that 
county, on which he had marked, from personal observation, the loca- 
tion of quartzite outerops, thus greatly lessening my own labor. I 
should also add that Mr. Canfield’s topographical map of Sauk county 
has been of great assistance in outlining the formations. The citizens 
of the region generally have aided me greatly. 

This report has been nearly all prepared, including illustrations, 
and the examination of between two and three thousand specimens, 
during the year ending June 1, 1877, for the most part whilst engaged 
in teaching several hours a day; and the task has not been a light one. 


Unrverstty oF Wisconsin, June 2, 1877. R. D. I. 


GEOLOGY OF CENTRAL WISCONSIN, 


CHAPTER. I. 
SURFACE FEATURES OF CENTRAL WISCONSIN. 


The region here designated as Central Wisconsin includes Colum- 
bia, Marquette, Waushara, Adams, Juneau, Wood, Marathon, Clark 
and Jackson counties; all of Dane and Sauk counties except the west- 
ern tier of towns in each; and also that portion of Green Lake county 
which lies north of the Fox river. The Atlas plates of Areas D, E, F, 
and H, apply in part or wholly to this region. 


RIVER SYSTEMS AND GENERAL SURFACE SLOPES. 


Disregarding the small areas in Clark and Jackson counties which 
drain into the Chippewa and Trempealeau rivers, the region may be 
said to include portions of four distinct drainage systems: those of 
the Wisconsin, Black and Rock rivers, which flow southward and 
westward to the Mississippi, and that of the Fox river, which flows 
northward and eastward to Lake Michigan, and is thus tributary to 
the Saint Lawrence. 

The directions and areas of these river systems are more or less 
directly influenced by the rock structure of the state. Extending into 
Wisconsin from the Upper Peninsula of Michigan, and forming the 
central nucleus of the northern half of Wisconsin, is a great mass of 
ancient crystalline rocks, which is bordered on all sides by newer and 
undisturbed formations, whose outcropping edges, on the south, east, 
and west, succeed one another in concentric bands. The central erys- 
talline mass, probably for the most part never covered by later forma- 
tions, includes the highest land in the state. It has a general slope 
to the southward, reaching its greatest elevation —1,000 feet above 


414 GEOLOGY OF CENTRAL WISCONSIN. 


Lakes Michigan and Superior — along its northern edge, within thirty 
miles of the latter lake. The waters which fall upon it are shed in 
four different directions: to the north, into Lake Superior; to the 
southeast, into Lake Michigan; to the south, into the Wisconsin — 
which ultimately reaches the Missis:ippi; and to the southwest directly 
into the Mississippi. The northward streams, which interlock on the 
summit of the divide with those flowing southeast, south, and south- 
west, and descend in a distance of thirty miles nearly a thousand 
feet, are entirely without the region at present under consideration, 
Of the streams flowing sonthwestward, only the Black river drains 
any considerable portion of the region, whilst the southeasterly streams 
are mostly outside of its limits. Some of the latter pass directly to 
Lake Michigan, whilst others concentrate into the stream known as 
the Wolf, which, after leaving the area of crystalline rocks, takes a 
southerly course until it meets the northward flowing Fox. The two, 
uniting, pass through Lake Winnebago northward to Green Bay. 
The systems of the upper Fox and of the Rock, though less immedi- 
ately under the influence of the Archeean watershed of the north part 
of the state, are still directly affected by the geology of the regions 
they drain, the waters of the upper Fox being shed to the east by the 
‘high sandstone and drift region of western Marquette and Waushara 
counties, and to the north by the high limestone belt which runs 
southwestwardly through Green Lake and Columbia, whilst the tribu- 
taries of the Rock river are shed southeastward by the same limestone 
belt. Although traced thus directly to other influences, the drainage 
areas and general surface slopes of the southern half of the state are 
still in some degree ultimately attributable to the position and shape 
of the Archxan nucleus. Whilst the southern region retains the gen- 
eral slope southward of the crystalline rocks in the north, it also shows 
the same eastward and westward slopes from a central north and south 
line. This seems without doubt to be due to the continuance, beneath 
the Paleozoic accumulations, of the Archsean mass with the same sur- 
face structure as on its exposed portions, 7. ¢, a central north and 
south crest line, itseif sloping southward, from which there are east- 
ward and westward slants. 

Of the whole area of the Central Wisconsin district, the Wisconsin 
drains about 160 townships, including the eastern part of Clark, nearly 
all of Marathon, a small part of eastern Jackson, nearly all of Wood 
and Portage, all of Juneau, nearly all of Adams, all of Sauk, about 
half of Columbia, and a few towns in northwestern Dane; the Black. 
river drains about 41 townships, including about half of Clark, nearly 
all of Jackson, and a small area in the western part of Wood; the 


RIVER SYSTEMS AND GENERAL SURFACE SLOPES. 415 


Fox drains about 49 townships, including the easternmost part of Mar- 
athon and Portage, almost all of Waushara, all of Marquette, south- 
eastern Adams, about four townships in northern Columbia, and all 
of Green Lake within the district; and the Rock drains about 31 
townships, including eastern and southwestern Columbia, and nearly 
all of Dane. 

Much the most important of these streams is the Wisconsin, which 
constitutes, with its valley, the main topographical feature of the 
region. The total length of this river, from its source to its mouth, 
is about 500 miles. Rising in Lac Vieux Desert, on the summit of 
the Archzean watershed, at an elevation of 951 feet above Lake Michi- 
‘gan, it pursues a general southerly course for 300 miles over the erys- 
talline rocks, and then, passing on to the sandstones which form its 
bed for the remainder of its course, continues to the southward for 
some eighty miles more. Turning then westward, it reaches the 
Mississippi within 40 miles of the south line of the state, at an eleva- 
tion of only 30 feet above Lake Michigan. Like all the other streams 
which run to the south, southeast, and southwest from the crystalline 
rocks, it has its quite distinct upper or crystalline rock portion, and 
its lower or sandstone portion. In the case of the Wisconsin, how- 
ever, we may conveniently regard the river as having three distinct 
sections: the first including all that part from the source to the last 
appearance of crystalline rocks in the bed of the stream, in the south- 
ern part of Wood county; the second, that part from this point to the 
Dalles, on the south line of Adams and Juneau counties; and the 
third, that portion from the Dalles to the mouth of the stream. The 
first of these divisions is broken constantly by rapids and falls, caused 
by the descent south of the surface of the Archean area, and by the 
obstructions produced by the inclined ledges of rock which cross the 
stream. The second and third sections are alike in being almost en- 
tirely without rapids or falls, and in the nature of the bed rock, but 
are separated by the contracted gorge known as the Dalles, which, 
acting in some sort as a dam, prevents any considerable rise in the 
river below, the water above not unfrequently rising as much as 50 
feet in flood seasons, whilst below the extreme fluctuation does not 
exceed 10 feet. The total lengths of the Archean, upper sandstone, 
and lower sandstone sections of the Wisconsin, are, respectively, 800, 
62 and 130 miles, the distance through the Dalles being about seven 
miles. 

For a description of the course of the river more in detail, we may 
begin with its entrance into the district in the northern part of Mara- 
thon county. From here, where the width according to the land 


416 GEOLOGY OF CENTRAL WISCONSIN. 


office plats is from 300 to 500 feet, the river pursues a general south. 
erly course through towns 29, 28, 27, 26, 25 and 24, of range 7 east, 
and towns 24 and 23, of range 8 east, in the southern part of Portage 
county. In this part of its course the Wisconsin flows through a 
densely timbered country, and has, except where it makes rapids, or 
passes through rock gorges, a narrow bottom land, which varies in 
width, is usually raised but a few feet above water level, and is wider 
on one side than on the other. Above this bottom, terraces can often 
be made out, with surfaces in some cases one or two miles in width. 
Above, again, the country surface rises steadily to the dividing ridges 
on each side, never showing the bluff edges so characteristic of the 
lower reaches of the river. Heavy rapids and falls are made at Wau- 
sau (Big Bull Falls), Mosinee (Little Bull Falls), Stevens Point, and 
on section 8, town 23, range 8 (Conant’s Rapids). All but the last 
named of these are increased in height by artificialdams. Two miles 
below the foot of Conant’s Rapids, just after receiving the Plover river 
on the east, the Wisconsin turns a right angle to the west, and enters 
upon the sparsely timbered sand plains through which it flows for a 
hundred miles. At the bend the river is quiet, with high banks of 
sand and a few low outcrops of gneiss at the water’s edge. From the 
bend the course is westward for about nine miles; then, after curving 
southward again, the long series of rapids soon begins which, with 
intervening stretches of still water, extend about 15 miles along the 
river to the last rapid at Point Bass, in southern Wood county. East 
of the river line, between the city of Grand Rapids and Point Bass, 
the country rises gradually, reaching altitudes of 100 feet above the 
river at points ten or fifteen miles distant. On the west the surface 
is an almost level plain, descending gradually as the river is receded 
from. At Point Bass the gneissic rocks disappear beneath the sand- 
stones which for some miles have formed the upper portions of the 
river banks, and now become in turn the bed rock; and the first 
division of the river’s course ends. The main tributaries which it 
has received down to this point are, on the left bank — the Big Eau 
Claire, three miles below Wausau; the Little Eau Claire, on the north 
side of Sec. 3, T. 25, R. 7 E., just south of the north line of Portage 
county; and the Big Plover, on Sec. 9, T. 28, R.5 E., just at the 
foot of Conant’s Rapids; on the right bank —the Placota, or Big Rib, 
about two miles below Wausau; the She-she-ga-ma-isk, or Big Eau 
Pleine, on Sec. 19, T. 26, R. 7 E., Marathon county; and the Little 
Eau Pleine, on Sec. 9, T. 25, R. 7, in Portage county. All of these 
streams are of considerable size, and drain large areas. They all 
make much southing in their courses, so that their lengths are much 


RIVER SYSTEMS AND GENERAL SURFACE SLOPES. ALT 


greater than the actual distances from the sources to the Wisconsin 
at the nearest points, and all of them have a very considerable descent, 
making many rapids and falls over the tilted edges of schistose and 
gneissic rocks, even down to within short distances of their junctions 
with the main river. The streams on the west side head on the high 
country along the line of the Fourth Principal Meridian, about 40 
miles west of the Wisconsin, and at elevations from 200 to 300 feet 
above their mouths; those on the east head on the divide between the 
Wisconsin and Wolf, about 20 miles east, at elevations not very much 
less. Reaching back, as these streams do, into a country largely tim- 
bered with pine, and having so large a descent, they are of great value 
for logging and milling purposes. 

The second section of the Wisconsin river begins at Point Bass, 
with a width of from 700 to 900 feet. The next sixty miles of its 
course, to the head of the Dalles, is a southerly stretch, with a wide 
bow to the westward, through sand plains, here and there timbered 
with dwarf oaks, and interspersed with marshes. These plains stretch 
away to the east and west for twenty miles from the river bottom, 
gradually rising in both directions. Scattered over them, at intervals 
of one to ten miles, are erosion peaks of sandstone from 50 to 300 feet 
in height, rising precipitously from the level ground. Some of these 
are near and on the bank of the river, which is also in places bordered 
by low mural exposures of the same sandstone. The river itself is 
constantly obstructed by shifting sandbars, resulting from the ancient 
disintegration of the sandstone, which in the vicinity everywhere 
forms the basement rock, but its course is not obstructed by rock 
rapids. As it nears the southern line of Adams and Juneau counties, 
the high ground that limits the sand plain on the west, curving south- 
eastward, finally reaches the edge of the stream, which, by its south- 
easterly course for the last twenty miles, has itself approached the high 
ground on the east. The two ridges thus closing in upon the river 
have caused it to cut for itself the deep and narrow gorge known as 
the Dalles. In the second section of its course, the Wisconsin re- 
ceives several important tributaries. Of those on the east, the princi- 
pal ones are Duck creek and Ten Mile creek in the southern part of 
Wood county; and the Little and Big Roche & Cris creeks, both in 
Adams county. The two former head in a large marsh 25 miles east 
of, and over 100 feet above, the main stream. The two latter head 
on the high dividing ridge on the west line of Waushara county, at 
elevations between 150 and 200 feet above their mouths. These 
streams do not pass through a timbered country, but have very valn- 
able water powers. Of those on the west, two are large and import- 

Wis. Sur. — 27 


418 GEOLOGY OF CENTRAL WISCONSIN. 


ant —the Yellow and Lemonweir rivers. Yellow river heads in 
township 25, in the adjoining corners of Wood, Jackson and Clark 
counties, and runs a general southerly course nearly parallel to the 
Wisconsin for over 70 miles, the two gradually approaching one an- 
other and joining in towship 17, range 4 east. The Yellow has its 
Archean and sandstone sections, the former exceedingly rocky and 
much broken by rapids and falls, the latter comparatively sluggish 
and without rock rapids. The upper portions of the river extend 
into the pine regions, and much logging is done in times of high 
water. The water powers are of great value. The Lemonweir is also 
alarge stream. Ileading ina timbered region in the southeast corner 
of Jackson county, it flows southward for some distance through 
Monroe, and entering Juneau on the middle of its west side, crosses 
it in a southeasterly direction, reaching the Wisconsin in section 24, 
township 15, range 5 east, having descended in its length of some 70 
miles about 200 feet. 

The “ Dalles ” of the Wisconsin, as already said, is a narrow pass- 
age cut by the river through the high grounds which, after bounding 
its valley on both sides for many miles, have now gradually approached 
and joined. The total length of the gorge is about seven and one- 
half miles. At the upper end, about two miles north of the south 
line of Juneau county, the river narrows suddenly from a width of 
over one-third of a mile to one of not more than 200 feet. Through- 
out the whole length of the passage the width does not ever much 
exceed this, whilst in one place it is only fifty feet. The water in the 
gorge is very deep, although immediately above it there are broad 
sand flats with scarcely enough water at low stages to float a canoe. 
The perpendicular sandstone walls are from fifteen to eighty feet in 
height, the country immediately on top of them being about 100 feet 
above the river. From this level, about midway in the passage, there 
is a rapid rise in both directions to the summit of the high country 
on each side. In several places branch gorges deviate from the main 
gorge, returning again to it; these are evidently old river channels 
and are now closed by sand. The streams entering the river in this 
portion of its course make similar cafions on a smaller scale. 

At the foot of the Dalles the Wisconsin enters upon the last see- 
tion of its course, and also upon the most remarkable bend in its 
whole length. From a nearly southerly course it now turns almost 
dune east, in which direction it continues with one or two subordinate 
turns southward for about seventeen miles, through low sand banks, 
as far as Portage. ere it bends abruptly south again, and, 
reaching its easternmost point at the mouth of the Baraboo, soon 


RIVER SYSTEMS AND GENERAL SURFACE SLOPES. 419 


swerves around into the final southwestward stretch to the Missis- 
sippi. The cause of this long détour to the east is sufficiently evi- 
dent. As the river leaves the Dalles it finds lying directly athwart 
its course the two bold quartzite ranges which extend east and west 
through Sauk county for upwards of twenty miles, and, crossing into 
Columbia, finally unite about eight miles east of the county line, ina 
sharp and bold, eastward projecting point, which rises 400 feet above 
the river bottom. Above Portage, where the Wisconsin forms the 
southern line of the town of Lewiston, the ground immediately north 
is lower than the water in the river, the heads of Neenah creek, a 
tributary of the Fox, rising within a short distance of its banks. In 
times of high water the Wisconsin overflows into these streams, and 
thus contributes much to a totally different river system. At Port- 
age the Fox, after flowing south of west for twenty miles, approaches 
the Wisconsin coming from the opposite direction. Where the two 
streams are nearest they are but two miles apart, and are separated by 
a low, sandy plain, the water in the Fox being five feet below that of 
the Wisconsin at ordinary stages. The greater part of this low ground 
is overflowed by the latter stream in times of high water, and to this 
is chiefly due the spring rise in the Fox. After doubling the eastern 
end of the quartzite ranges, as already said, the Wisconsin turns 
again to the west, being forced to this by impinging on the north 
side of a high belt of limestone country, which, after trending south- 
west across the eastern part of Columbia county, veers gradually to a 
westerly direction, lying to the south of the river along the rest of its 
course. Soon after striking this limestone region, the river valley 
assumes an altogether new character, which it retains to the mouth, 
having now a nearly level, for the most part treeless bottom, from 
three to six miles in width, ten to thirty feet in height, usually more 
on one side than on the other, and bounded on both sides by bold and 
often precipitous blufis, 100 to 350 feet in height, of sandstone capped 
with limestone. Immediately along the water’s edge is usually a 
narrow timbered strip — rising two to four feet above the river — which 
is overflowed at high water. The line of bluffs along the south side 
of the valley is the northern edge of the high limestone belt just 
mentioned, which reaches its greatest elevations ten to fifteen miles 
south of this edge. In front of the main bluff-face, especially in its 
eastern extension, are frequently to be seen bold and high isolated 
outliers of the limestone country. On the north bank the bluffs are 
at first the edges of similar large outlying masses, but further down 
they become more continuous, the river crossing over the northwest- 
ward trending outcrop line of the Lower Magnesian limestone. 


420 GEOLOGY OF CENTRAL WISCONSIN. 


In this last section of its course the Wisconsin is much obstructed 
by bars of shifting sand derived originally from the erosion of the 
great sandstone formation which underlies the whole region, and to 
whose existence the unusual amount of obstruction of this kind in 
the river is due. The peculiar instability of these sand bars, and 
their liability to form and disappear within a few hours, renders their 
control very difficult. In view of the enormous quantities of this al- 
ready disintegrated sand in the region drained by the river and its 
tributaries, many of which have their entire course through sand dis- 
tricts, the construction of a continuous canal along the Wisconsin 
river from Portage to its mouth, would appear to be the only way 
to utilize the natural highway from the lakes to the Mississippi 
which is offered by this and the Fox rivers. In the last section of its 
course the Wisconsin receives within the limits of our district only 
one streain of importance, the Baraboo, which enters the river 
near the easternmost point of its great bend. Heading in the adja- 
cent corners of Monroe, Vernon and Juneau counties,at an elevation 
of about 400 feet above its mouth, the Baraboo runs southeastward 
jnto Sauk county, where it breaks into the valley between the two 
east and west quartzite ranges already alluded to, through a narrow 
gorge in the northern range. Turning then eastward: it runs along 
the middle of the valley between the two ranges for about fifteen 
miles, and then, breaking again northward through the north range, 
follows its northern side east to the Wisconsin. The Baraboo is a 
stream of very considerable size, and yields a number of excellent 
water powers in the valley between the quartzite ranges, having a 
fall on this portion of its course of seventy feet. The tributaries on 
the south side of the Wisconsin, in this section of its course, are of 
little importance, owing to the nearness of the limestone divide. The 
most noteworthy is Duck creek, which with its branches drains a 
considerable area in the towns of Pacific, Springvale and Courtland, 
in Columbia county, cutting a long way back into the divide. 


RIVER SYSTEMS AND GENERAL SURFACE SLOPES. 421 


The following tabulation gives the altitude of the water surfave of 
the Wisconsin at prominent points from the source to the mouth: 


ALTITUDES OF 
WATER SURFACE 
Darr. Locauity. A AUTHORITY. 
ove 
‘en | Hake 
. Mich. 
Js new sane Lac Vieux Desert ... ...} 1532 951 | Reportof I. A.Lapham. 
nemisiniewe: anes Wausau, above Dam ....| 1204 623 | Railroad Survey. 
rortttstt tl) Knowlton. ....- yeh ; oe aa t Railroad Survey. 
eer ee Stevens Point.........../ 1065 484 | Railroad Survey. 
s Solas eae awe Conant’s Rapids (Sec. 8, 
2 died ay bean T. 23, R. 8).....-2...., 1049 468 | Railroad Survey. 
sist Gaeaeeses Grand Rapids Railroad 
Sapa tees Bridge s..2scsasesvese; LOOL? 420? | Railroad Survey. 
toys BEAT Kilboum City Railroad 
iaiie Sega wa Bridge .......... ..../ 814 233 | Railroad Survey. 
Aug. 27, 1867 | Portage ..........2606+- 792 211 | Warren’s River Survey. 
Sept. 9, 1867 | Merrimac.............-. 763 182 | Warren's River Survey. 
Sept. 17, 1867 | Sauk City .............. 746 165 | Warren's River Survey. 
Sept. 27, 1867 | Spring Green Bridge ....] 715 134 | Warren’s River Survey. 
Oct. 12, 1867 | Muscoda .........--.... 696 115 | Warren's River Survey. 
Nov. 6, 1867 | Mouth of River ......... 615 34 | Warren's River Survey. 


The average velocity of the river below Portage is remarkably uni- 
form and is just about two miles per hour.’ The daily discharge of 
of the river at Portage in times of extreme low water is about 
259,000,000 cubic feet.2 The average fall of the water surface 
of the river below Portage is 14 feet per mile. General Warrren, 
from whose report ® this statement is taken, very truly says that this 
rapid fall, were it not for the great amount of sand in the river-bed, 
would make the stream a series of pools and rock rapids; so that, 
whilst making a great obstruction, the sand really gives the river 
what navigability it possesses. 

In subsequent pages are given a number of geological sections 
across the valley of the Wisconsin below Portage. The profiles of 
these sections are reduced from the profiles given in the atlas of Gen. 
Warren’s report, and the geology has been added from my own ob- 
servations. 

Black river rises in townships 31 and 32, on the high drift-covered 
divide near the Fourth Principal Meridian, at elevations of over 800 
feet above Lake Michigan, runs first west into range 2, and then takes 


1 Maj. C. R. Sutter, in Chief of Engineer's Report, 1867, p. 353.” The same. 
3 Report on the Transportation Route along the Wisconsin and Fox River,’’ by Gen. 
G. K. Warren, U. 8. Engineers, Washington, 1876. 
) 


429 GEOLOGY OF CENTRAL WISCONSIN. 


a southerly course through Clark county as far as township 24, where it 
begins a southwesterly stretch towards the Mississippi, which it reaches 
in town 17, range 8, on the boundary line between Trempealeau and 
La Crosse counties. Its total length is about 150 miles, and total fall 
about 750 feet. Like the Wisconsin, it has its upper or Archean por- 
tion, broken constantly by chutes and rapids over gneiss and granite, 
and its lower or sandstone section without falls. The Archean sec- 
tion of the river extends to the town of Black River Falls, in town- 
ship 21, Jackson county, where the gneissoid granite and gneiss 
cause a long rapid and disappear tinally beneath the sandstones, 
which, however, extend for many miles northward of this point on the 
immediate banks of the stream, covering the crystalline rocks every- 
where except in the river bed. Towards its mouth the valley of 
Black river is bounded by limestone-capped bluffs like the lower por- 
tion of the valley of the Wisconsin. Like the Wisconsin, again, it 
has its upper waters in a pine covered region, is much used for log- 
ging, and affords numberless water powers by its rapid descent and 
frequent rock interruptions. Most of the branches of the upper Black 
run over crystalline rocks like the main stream, and have numerous 
rapids and falls. Some of them, however, as for instance the East 
Fork, reverse the ordinary conditions of the streams of the region, 
and have their upper portions in sandstone on the high divide near the 
Meridian in northeastern Jackson and eastern Clark county, whilst 
farther down they cut into the crystalline rocks, making the usual 
rapids and falls. 

The main Rock river only touches the southeastern corner of our 
district in the expansion known as Lake Koshkonong, but its branches 
drain nearly all of Dane and most of eastern Columbia. These 
branches are everywhere divided from the tributaries of the Wiscon- 
sin by the high belt of limestone country already described as run- 
ning southwestward through eastern Columbia, and then westward 
through northern Dane. In Dane county are three branches of 
Rock river, draining three distinct north and south basins. Central 
Dane is traversed by the Catfish, whose upper waters expand into 
several large lakes that lie in a series of N. E.—S. W. valleys appar- 
ently of glacial origin. Between two of these lies Madison, the cap- 
ital city of the state. In the western towns of Dane are the heads of 
Sugar river, whilst on the eastern side the drainage is into Kosh- 
konong creek, except on the extreme northeast, where it is eastward 
to the Crawfish, as is also the case with the eastern part of Columbia 
county. 

The Fox river, the fourth of the main rivers of the district, heads 


RIVER SYSTEMS AND GENERAL SURFACE SLOPES. 423 


in the northeastern part of Columbia county and the adjoining por- 
tions of Green Lake, on the west edge of the high limestone belt 
previously alluded to. Flowing at first southwest and then due west 
nearly parallel to the Duck creek branch of the Wisconsin, it ap- 
proaches the latter stream at Portage. When within two miles 
of the Wisconsin, separated from it and from Duck creek by only a 
low, sandy plain, it turns abruptly northward, and, with a sluggish 
current, continues on this course for twelve miles to the head of Lake 
Buffalo in the southern part of Marquette county. For some dis- 
tance below Portage the river has been shortened by cut-offs and 
slackened by a system of dams and locks. It has already been said 
that in the spring this portion of the Fox receives a large amount of 
water from the Wisconsin, much of which reaches it through a 
branch known as the Big Slough or Neenah creek, which, heading 
within a mile of the Wisconsin, in the town of Lewiston, reaches the 
Fox just south of the north line of Columbia county, in the town of 
Fort Winnebago. At the head of Lake Buffalo the Fox begins a wide 
curve which brings its direction finally around to due east. Lake 
Buffalo is merely an expansion of the river, grown up with grass and 
wild rice, except where the channel crosses it, and is thirteen and one- 
half miles long and half a mile wide. It runs through a sand plain, 
which is not many feet above its level. At the foot of the lake, near 
the village of Montello, a dam has been built which raises the lake-level. 
several feet. From the foot of Lake Buffalo the river for seven miles 
has an irregular, easterly course, with a somewhat rapid current, to 
the head of Lake Puckawa, which is eight and one-fourth miles in 
length and from one to two wide, and is in part grown up with reeds 
and wild rice. At the foot of the lake there are wide marshes 
through which the river leaves on the north side, and, after making a 
long, narrow bend to the west, begins its northeast stretch to Lake 
Winnebago, kecping along the western edge of the northern exten- 
sion of the same limestone ridge, to which we have already had occa- 
sion so many times to refer, until after it leaves the district. From 
Lake Puckawa to Berlin the river is wider and deeper, interrupted 
by but few sandbars, and runs for a considerable portion of the dis- 
tance between high banks. The main tributaries of the upper Fox 
enter from the north, and head in the high drift-covered region of 
southwestern Waushara and northwestern Marquette, at elevations of 
between 200 and 300 feet above their mouths. The principal ones 
are the Montello, Mechan and White rivers, each one of which 
branches many times towards its head. All of these are large, clear, 
rapid streams, but, running in sand and drift bottoms, are not broken 


124 GEOLOGY OF CENTRAL WISCONSIN. 


by rock rapids. They are in many places utilized for milling pur- 
poses. The eastern side of Waushara county is drained by similar 
streams, which reach the Fox through Lake Poygan,outside the lim- 
its of the district, in Fond du Lae county. The following figures 
with regard to the Fox are taken from the report of Major Charles 


Sutter, already referred to: 
Distance. Faun. 


Miles. Feet. 

Portage to head of Lake Buffalo ......-.+--seeeee seer rece 12 7.12 
Head of Lake Buffalo to foot of same....--+ seer rere trees 131 1.14 
Foot of Lake Buffalo to head of Lake Puckawa.....+- +++ 7 5.22 
Head of Lake Puckawa to foot of same ....--+seeere reese 84 ale? 
Foot of Lake Puckawa to Princeton .....-.+-ee seers e eer ees 12 3.35 
Princeton to Berlin bridge .....---seceeee cree eee tee eee 2014 8.82 
Portage to Berlin bridge... ...- ++ se eee sere eee e eee teens 73 25.32 


The Fox river, at the foot of Winnebago lock at Portage, is 203.1 
feet above Lake Michigan. 

The remarkable relations of the valleys of the upper Fox and 
lower Wisconsin, and the probable former drainage southward of 
the whole basin of the Fox and Wolf rivers, are alluded to on a sub- 
sequent page. 


SURFACE RELIEFS. 


With the exception of the sand region of Juneau and Adams coun- 
ties, and portions of the lower Wisconsin valley, no considerable part of 
the district can be designated as a plain, the surface being everywhere 
roughened by erosion or heaped up drift. The extremes of elevation 
are, however, only about 1,100 feet apart, being 1,263 feet for the Rib 
Hills near Wausau, and 134 feet for the Wisconsin river at Spring 
Green, both altitudes being referred to Lake Michigan. These are, 
moreover, at opposite ends of the district, the Rib Hill being itself an 
isolated ridge 600 feet above the general level. For the most part 
the region lies between 200 and 900 feet above Lake Michigan, whilst 
the changes of level in any one vicinity, except in such districts as 
that of the Sauk quartzite ranges, but rarely reach 300 feet. 

The general surface slopes and the extents of the hydrographic ba- 
sins have already been indicated. The watersheds need further re- 
mark, those separating the four great basins of the district especially 
meriting our attention. The high ground which sheds in different 
directions the waters of the Wisconsin and the Fox begins in town- 


SURFACE RELIEFS. 495 


ship 87, range 11 east, at an elevation of about 900 feet,! and trends 
southward through ranges eleven and ten to the north line of Portage 
county, where it veers into range nine, which it follows southward to 
township nineteen, Waushara county, with an elevation gradually 
lessening from 600 to 500 feet. Thus far the watershed has been be- 
tween the Wisconsin and the Wolf, the northern branch of the Fox. 
Its upper end, as far south as Portage county, is on the Archzan rocks, 
its height being augmented by drift, and its slopes in both directions 
gradual, although the streams are constantly broken by rock rapids. 
South of the north side of Portage county, the rock formation is the 
sandstone. Here also the elevation is increased by drift accumula. 
tions, which occur in a morainie condition, of great thickness, and 
spread over a wide extent of country east and west. The slopes in 
both directions are very gradual. South of township nineteen this 
divide, which is now between the Wisconsin and upper Fox, veers 
again slightly to the west, and, crossing the southern end of Adams 
county, is cut through by the Wisconsin itself at the Dalles, in town- 
ship fourteen, range six, having here an elevation of about 400 feet. 
South of here there is no proper divide between the Wisconsin and 
upper Fox, both traversing a flat country. 

The watershed between the Wisconsin and Black rivers follows 
nearly the line of the Fourth Principal Meridian from township 31, 
where it has an elevation of about 900 feet, to township 20, where the 
elevation is about 400 feet. As far south as township 45 this ridge 
is on Archean rocks, much covered by drift, whilst further south the 
drift soon runs out and the sandstone makes up the ridge. South of 
township 20, on nearly the same line, the high ground continues, be- 
coming the divide between the Kickapoo, Pine and Baraboo branches 
of the Wisconsin, and carrying limestone on the summit. 

The high limestone prairie belt, separating the systems of the Rock 
and Wisconsin, has already been several times spoken of. Beginning 
outside the district, it crosses Green Lake county in a 8. 8. W. direc- 
tion, enters Columbia on the north line of the towns of Scott and 
Randolph, crosses this county in a line gradually veering to the west, 
and, entering Dane in the towns of Dane and Vienna, turns due west, 
in which direction it continues to the Mississippi river, breaking 
down, however, on the line of Black Earth creek in the towns of Mid- 
dleton and Cross Plains. On the west this divide has an abrupt, ser- 
rated face, which increases in boldness and height as followed south- 
ward and westward, the watershed itself reaching altitudes of 400 feet 


1 Hereafter all altitudes, unless otherwise stated, are referred to Lake Michigan, which 
is taken at 578 feet above the sea. 


426 GEOLOGY OF CENTRAL WISCONSIN. 


above the adjacent Wisconsin. The eastward slope, on the other 
hand, is, in Columbia county, very gradual, owing to the general de- 
scent eastward of the strata. As the watershed turns westward the 
direction of the dip changes gradually to the south, its amount at the 
same time becoming lessened. As a result the slopes towards the 
Catfish valley are again somewhat more abrupt, but never become 
like those on the Wisconsin side of the divide. 

The western and northern face of this divide, as indicated, forms 
the eastern and southern side of the Wisconsin valley continuously, 
from the mouth of the river to the easternmost point of its great 
bend. Farther north, however, the ridge continues its northeasterly 
trend, leaving the Wisconsin entirely, and becoming now the eastern 
boundary of the valley of the upper lox river as far as Lake Winne- 
bago. This interesting relation, which is very instructive as to the 
past conditions of the drainage of these valleys, is finely brought out 
by the colored Atlas Map of Area E, on which the western edge of 
the main brown-colored (Lower Magnesian) area, together with the 
brown line (Mendota base) just west of it, show the position of the 
western face of the ridge under consideration. The map will suggest 
at once, what is in every way the truth, that the valleys of the upper 
Fox and of the lower Wisconsin are really one continuous valley, the 
valley of the upper Wisconsin being an entirely independent one. As 
already described, the Fox and Wisconsin at Portage traverse a sandy 
plain within two miles of one another, and without divide of any kind. 
A glance at the map will show that the Fox makes towards the Wis- 
consin exactly as do other small tributaries immediately to the 
south — and from which there is also no divide — then suddenly turn- 
ing at right angles, passes northward and eastward through a broad 
valley, out of all proportion to its size. The whole length of this val- 
ley bears testimony to the former presence of a great river. The 
identity of the two valleys is still further shown by the fact that they 
constitute one continuous channel of erosion through the same geo- 
logical formations. The lower Wisconsin is everywhere cut down 
through the Lower Magnesian limestone, which forms horizontal 
strata in the upper parts of the high ground on each side. The same 
formation constitutes the ridge all along the southeast side of the 
Fox river, and moreover was once spread over the whole country north 
of that stream, where it is now still found in a few ontliers on the 
very highest ground. The bottoms of both valleys are composed of 
the Potsdam sandstone. 

The natural inference from these facts is that Lake Winnebago, in- 
cluding the whole of the great basin of the Wolf, formerly drained 


SUBFACE RELIEFS. 427 


southward, forming a continuous river with the Wisconsin below 
Portage. This former drainage southward has been suggested by 
other writers, but most clearly by Gen. G. K. Warren, in his recent 
report on the Fox and Wisconsin rivers, in which he shows that the 
lower Fox, through which the entire basin of the upper Fox and 
Wolf now outlets, is a modern channel, induced to form by a lower 
position of the continent to the northward than it formerly had. The 
real identity of the valleys of the upper Fox and lower Wisconsin, 
now shown, seems to be a convincing proof of the theory. Moreover, 
in subsequent pages it is shown that the upper Wisconsin has also 
undergone a change of course, having at one time passed through the 
Baraboo quartzite ranges, in the gorge now partly occupied by 
Devil’s Lake, and reached the valley of the lower Wisconsin in the 
region of Sauk Prairie, more than 20 miles below the point at which 
the Fox and Wisconsin now approach each other. It is shown that 
this condition held until the Glacial Period, when, the gorge through 
the quartzite ranges becoming choked with drift, the Wisconsin was 
forced to find itself a new passage around the eastern point of those 
ranges. But this passage around the point of the quartzite ranges, 
and as far southwest as the former junction of the upper and lower 
Wisconsin, is just as ancient and as deeply eroded as the channel 
of the lower Wisconsin itself. It follows that even when the upper 
Wisconsin had its former course, there was still a great river oceupy- 
ing the valley immediately below Portage, and this could only have 
come from the region of the Wolf and upper Fox. 

Of the subordinate dividing ridges we need only mention here the 
quartzite ranges known as the “ Baraboo Bluffs;’’ all others will be 
described in the chapters on Jocal geology. The Baraboo ranges, 
however, constitute so striking a feature in the topography of the 
central palceozoic portion vf the state, and present so marked a con- 
trast in direction and outlines to all other relief-forms south of the 
main region of crystalline rocks, that they deserve especial mention. 
They are two bold east and west ridges — the southern much the bold- 
er and more continuous of the two—extending through Sauk and 
eastern Columbia county for twenty miles, and lying within the great 
bend of the Wisconsin river. Their cores and summits, in some 
places their entire slopes, are composed of tilted beds of quartzite, 
metamorphic conglomerate, and porphyry, whilst their flanks are for the 
most part made up of beds of horizontal sandstone, which, in lower 
places, sometimes surmounts and conceals the more ancient rocks. 
On the east and west the two ranges join, and thus nearly completely 
surround the lower ground between them. The eastern junction, 


428 GEOLOGY OF CENRTAL WISCONSIN. 


caused by divergence northward of the southern range, the northern 
retaining its E. W. direction, is a bold, sharp point, rising abruptly 
400 feet above the level valley of the Wisconsin. From this point 
westward the southern range is a continuous ridge of 400 to 700 feet 
elevation above the low ground on the south, and 600 to 900 feet 
above Lake Michigan, always bold on both sides, often precipitous, 
and rising at top into long rounded swells, which not infrequently 
show the bare, purplish, quartz rocks. The wide, level prairie lying 
south of the middle portion of this range, known as Sauk Prairie, 
makes it stand out all the more boldly. It is not, however, only near 
by that this range is noticeable. It is seen from elevated points forty 
miles to the north, where its rounded contours distinguish it from the 
horizontal rock elevations seen on each side of it. Even from points 
around Madison— which has between it and the Baraboo Blufts a 
high limestone divide—by the aid of a telescope, their rounded 
contours can be distinguished through low places in the divide. 
At their western ends the two quartzite ranges are a number of 
miles apart, but are joined by a cross ridge of nearly the same alti- 
tude, which has probably a quartzite core throughout. Except, how- 
ever, over a large rounded elevation about midway in its length, and in 
other places at its ends, this cross ridge shows only sandstone as the 
surface rock. On the east the cross ridge descends rapidly to the 
level of the Baraboo valley. On the west, the high ground descends 
only gradually, and soon showing the Lower Magnesian limestone as 
the surface formation, continues many miles westward. 

A remarkable feature of all of the paleozoic portion of central 
Wisconsin is the occurrence of isolated ridges and peaks, ris- 
ing from 100 to 300 feet abruptly, and often precipitously, from 
the low ground around them, having an area on top of from a frae- 
tion of an acre to a square mile, and composed of horizontally strati- 
fied sandstone, or of sandstone capped with limestone. Such outlying 
bluffs lie all along the face of the high limestone country of Columbia 
and Dane counties, and are generally there capped by the same lime- 
stone that forms the elevated land, of which they are themselves frag- 
ments. Others again, and these are nearly all entirely of sandstone, 
occur scattered widely over the central plain of Adams and Ju- 
neau counties, often covering but a small area, and showing bare rock 
from the base to the summit, which not infrequently is worn into 
jagged pinnacles and towers. 

The following tables give the altitudes of numerous points through- 
out the district, referred to Lake Michigan as zero. The railroad ele- 
vations were furnished me by the late Dr. I. A, Lapham, who ob- 


SURFACE RELIEFS. 499 


tained them directly from the profiles in the offices of the several com- 
panies. The list is very full, an altitude being given for almost every 
section line crossed, and of course the figures have a high degree ot 
accuracy. Except where otherwise stated, the railroad grade is al- 
ways meant. The remaining tables include a number of altitudes, de- 
termined by the aneroid barometer, which are, of course, approxima- 
tions only. These are selected from a list of many thousand, and 
. apply almost wholly to Dane, Columbia and Sauk counties, which 
have been chosen because in them the conditions of observation were 
more favorable, reference points having been accessible during near- 
ly every day’s work, and because, also, in this part of the district 
the mapping of the geological formations required that the observa- 
tions should be much more numerous, aud consequently more accu- 
yate, than elsewhere.! Numerous determinations of altitude were 
made in the other counties of the district, but, on account of the dis- 
tance from railroads or other standards, only a few deserve to be list- 
edhere. The generalaltitude of any portion of the district can be 
obtained from the chapters on local details. 


MADISON TO ELROY. 


Chicago & Northwestern Railway. 


Place. Altitude. Place. . Altitude. 
Fast Madison depot...-...+--++++++ ae ree bridge... eee 215 
Stati 5, voad crossings. «+. - 24 ¥s ee ation. ,4\ sur. Wis. riv., low wat. 
es aaa .. pencil ee deletes sass 273 sur, Wis. riv., high wat. 180 

“175, (summit)......---.ee eee 305| ‘* 1880, Merrimac depot........ 215 
‘962, (summit). .... 6.5 ee ee eee 325 e TAG Ob suerte siescetotinncs ee eet ets 250 
“977, deep cut, surtace......--- B55) ou 4493 i grade... -.. sess eee 221 
“oo surface Catfish marsh.... 255 *) Surface ens. eegecans’ 178 
Ole sete speunawdparniaacs 27 | a Bie ce das 293 
pede: 1600, | 
«400 285 >? top Devil's Nose. .... 378 
me , 5 is 1696, surface.......0.eeeeeee 464 
458, { A (7 CROONER ee 429 
“520, Waunakee ae 1783, Peas Lake, grade .. 
6s r ee ridge 
a se 1908, 1 surface 
667, 12. BO “© 1950, Baraboo depot 
‘* 787, Dane depot i i de Obictertaeteee ate Seas 
“© 900, yes 8 anon NPS es 
f creek 5 pleman’s depot.......seeee cere eees 
“1002, j a ae : a see ae wee 267 | Reedsburg depot... eeee cree 
“1039, Lodi depot...-------+++++- 267 | La Valle depot.....-..- 
Con 0 8) ee 319 | Wonewoc depot.......-.- 
: grade... .e. seer ee eee eee 265 | Union Center depot ste 
‘© 1200, { SULfACE,... ese eee eee ee 255 | Elroy depot.....:..e.es eee eeeeeeeee 
grade.. ss. essere eee ees 200] 2 tations 100 fect apart, beginning with East 
“1800, j surface 175 | Madigon depot as zero. 


1 The aneroid determinations of altitude listed here are believed to have a considera- 
ble degree of accuracy. In many cases the same point was visited on different days, 
from different directions; and in other cases a second barometer was read half-hourly at 
a fixed point, whilst observations were being made. In this Jatter way it seems possi- 
ble to attain great accuracy with the aneroid, especially if such suitable and reliable in- 
struments are used as those male by J. H. Steward, of London. These have a range of 


only 3.000 feet, and show a variation of 5 feet very distinctly. 


430 GEOLOGY OF CENTRAL WISCONSIN. 


ELROY TO MERRILLON. 


West Wisconsin Railway. 


Place. Altitude. Place. Altitude. 
Elroy depotisscssnsvssceuei eeu: eoe a 360 | Warren's Mills depot.....-.....+.++- 448 
Orange depot.... 00.06. ecccec eens 327 | Rudd’s Mills depot.......--... see eee 403 
Camp Douglas depot........... 6006 356 | Black River Falls depot.......-... .- 231 
Valley Junction depot..........+..4+ 354 | Wright's depot.......-..seesee eee 853 
Lowry’s depot.........scceecevceeee 389 | Green Bay Junction depot.-......... 356 


WATERLOO TO MADISON. 


Chicago, Milwaukee & St. Pawl Railway. 


Place. Altitude. Place. Altitude. 
Waterloo depot........-..eseeeeeee 241 | Sun Prairie depot....-.......e.eeeee 356 
W. line, Sec. 7, T. 8, R. 1B E........ 260 | W. line, Sec. 8, T. 8, R. 11 E........ 349 
W. line, Sec. 12, T. 8. R. 12 E....... 272 | W. line, Sec. 18, T. 8, R. 11 E....... 341 
W. line, Sec. 11, T. 8, R. 12 E....... 280 | S. line, Sec. 13, Tr 8, BR. 10E........ 853 
Marshal depotie. .< 0s sssscees ceagee< 286 | W. line, Sec. 24, T. 8, R. 10 E....... 855 
W. line, Sec. 10, T. 8, a 12. His sasans 286 | S. line, See. 23, T. 8, R. VO sccaisessaacns 322 
W. line, Sec. 4, 7. 8, Re 12 Bis seseees 278 | W. line, Sec. 26, T. 8, Re 10 Bee cciciess 321 
Deanville depot Veet hag ehe mms he SE VS 305 | W. line, Sec. 34. T. 8 Rr 10 Bre sscacnes O77 
W. line, Sec. 5, T. 8, R. 12 E........ 295 | 8. line, Sec. 33, T. 8, R. 10 E........ 270 
W. line, Sec. 6, T. 8, R. 12 E........ 377 | W. line, See. 5 T. 7, By 10 Bienes 286 
W. line, Sec. 1, T. 8, R. 11 E........ 815 | East Madison depot. i actshavel ida wieapaacnmees 268 
W. line, Sec. 2, T. 8, R. 11 E........ 374 | West Madison depot................ 275 
W. line, Sec. 3, T. 8, R. 11 B........ 393 | Lake Monona (8d Lake)............. 262 
W. line, Sec. 4, T. 8, R. 11 E........ 369 | Lake Mendota (4th Lake)............ 270 


EDGERTON TO BLACK EARTH. 


Chieago, Milwaukee & St. Paul Railway. 


Place. Altitude. Place. io eae 

Edgerton depot...........e cee eens 242 ~ line, N. E. qr. Sec. 33, T. 
W. line, 8. E. qr. Sec. 4, T. 12, R. 4 BE. 255 OBE fiaidiacdgna vin tiee aa eu bac aatemnce , 265 
W. line, N. Ww. qr. Sec. 4, T.12, R. 4 E. 262 w. The, Sec. 28, T.7, R. 10 B....... 265 
N. line. Sec. 5,1. 12, B.4 Ee... 268 | W. line, Sec. 99, Ts 7 Bel0 Biccuscs 265 
Mid. W. line, Sec, 32, T.5, R. 12 E... 275 | W. line, Sec. 30, T.. 7, Rie IO Baccus ss 270 
Mid. N. line, "Sec. 31, T.5, R.12 E.... 284] N. line, Sec. 86, T. 7, BR. 9 E......... 267 
E. line, 8. E. qr. Sec. 95, T. 5,R.1LE.. 297 | West Madison depot...-............ 275 
W. line, 8. E. qr. Sec. 25, T.5, R. 11 E. 285 | W. line, N. E. qr. Sec. 22, T. 7, R.9E. 291 
Ww. line, Sec. 25, T. 5, R. 11 E....... 285 | W. line, Sec. 22, 7.7, R.9E........ 291 
N. line, Sec. 26, 'T, Os. By LD Biseeee nes 272 | W. line, N. E. qr. Sec. 21,T.7,R.9E. 291 

. line, N. E. qr. Sec. 23, T.5, R. ‘ W. line, Sec. 16, T. 7, R. 9 E........ 299 
W. line, N. E. qr. Sec. 15, T.! W. line, Sec. 20, Ly 3,. Bi 9, Bis haa 326 
8. line, 8. E. qr. Sec. ‘4 T.5, W. line, N. E. qr. Sec. 19, T..7, RB. 9 E. 332 
Mid. W. line, See. 9, T. 5, R. 1 ees W. line, Sec. 18, T. 7, R. 9 E........ 340 
Stoughton de pet teinlgiosspatie-s aa lelecs'a'e ils N. line, Sec. 18, T. 7, R. 9 : 
S. line, Sec. 32, T. 6, R. 11 Middleton depot Sa Aditoe Miata dienn 
N. line, See 32, T. 6, R. 11 W. line, Sec. 11, T. 7, BR. 
N. line, Sec. 29, T. 6, R. 11 Ww. line, 8. E. qr. See. 10, T. 
N. line, See. 20, T.6, R. 11 W. line, Sec. 10, T. 7, R. 
Mid. W. line, Sec. 17,T. 6, W. line, Sec. 9, T. 7, R. 
N. line, Sec. 18, T.6, R. 11 W. line, Sce. 8, T. 7, R. 
W. line, Sec. 7, T, 6, R. 11 Ww. line, Sec. 7, T. 7, R. 
S. line, See. 1, 7. 6, R. 10 E Ww. line, Sec. 12, T..7, R. 
W. line, Sec. 1, T. 6, R. 10 W. line. Sec. 2, T. 7, R. 
W. line, 8. E. qr. Sec. 2, T.6, R. 10 £.. Cross Plains depot eH avers R era Dae ers 
McFarland depot... ....... mths W. line, Sec. 4, T. 7, 


R. 
Center Sec. 31, T. 8, R.7 


8. line, Sec. 34, T iheys areas 
« 10 Bavavesceays 276 | Black Earth depot inn easier e Ana 


W. line, Sec. 34, T. 


ee 
==] 
= 
a 
= 


bof 


SURFACE RELIEFS. 431 


CAMP DOUGLAS TO RANDOLPH. 


Chicago, Milwaukee & St. Paul Railway. 


Place. Altitude. Place. Altitude. 
Camp Douglas depot.............+5. 368 | Fox river crossing N. W. qr. Sec. 4, T. 
New Lisbon depot ........-...0e000- SLL |. V2) Ris 9 By sz os as eaten eee ae 244 211 
Mauston depot......... 2. eee ee eee ee 806 | E. line, Sec. 3, T. 12, R. 9 H.... 22... 224 
Kilbourn City depot.............2.6- 316 | E. line, Sec. 2, T. 12, R. 9 E......... 227 
Lewiston depot......0.-.e 2c. cee eee 231 | E. line, Sec. 1, T. 12, Ri 9 Reeavasscs 225 
W. line, Sec. 35, T. 13, a ne Mavsaae a « 229 | E. line, Sec. 6, T. 12, R.SH......... 205 
‘W. line, Sec. 6, T. 12, Ry 9 Beeocae . 243 | E. line, Sec. 5, T. 12, BR. 8 Hives eas 213 
Portage depot...... 2... cece eee ee 232 | E. line, Sec. 4, T.12). Re 8 Mieescsvss 232 
E. line, Sec. 6, T. 12, R. 9. E......--. 233 | Pardeeville depot Anand tes bee TIER 237 
Near center Sec. 5, T. 12, R.9B..... 236 | Cambria depot.........+...ece seen 284 
ae eee N. W. qr. Sec. 4, T. 12, wit Randolph depot ......... sc ee eee ee 378 


TOMAH TO WAUSAU. 


Wisconsin Valley Railroad. 


Place. Altitude. Place. Altitudes 
Tomah depot .... 0... cece cree eens 883 | N. line, Sec. 4, T. 23, R. 6 E.......- 560 
Valley Junction depot.....-....--++- 350 | N. line, Sec. 33, T. 24, R. 6 E....... 570 
N. line, Sec. 6, T.19, R. 2H. .....-- 379 | N. line, Sec. 27, T. 24, R.6 E....... 556 
N. line, Sec. 32, T. 20, R. 2E ee 379 | N. line, Sec. 92) T. 24, R. 6H. ...... 558 
Beaver Station.......22-.eceeeeeeee 379 | Crossing Mill er., 8. 22, T. 24,R.6H 543 
N. line, Sec. 22, T. 20, R. 2E. ...... 384 | N. line, Sec. 15, T, 24, B.6E. ...... 554 
N. line, Sec. 12, T. 20, R. 2E, ...... 386 | N. line, Sec. 10, T. 24, R.6 E. ...... 563 
N. line, Sec. 6, T. 20, R. 3 E........- 839 | Junction au depotees easy aseneeess 572 
N. line, Sec. 31, T. 21, R. 3 E. astvaieede 391 | N. line, Sec. 35, T. 25. R. 6 E. ...... 601 
N. line, Sec. 28, T. 21, BRAS Wicd vieneacs 395 | N. line, Sec. 25, T. 25, R. 6H. ...... 590 
Yellow river crossing, Sec. 14, T. 21, N. line, Sec. 24, T. 25, R. 6 E. .....- 576 

Roo le ictsere aeece ay euteen ata 401 | N. line, Sec. 13, T. 25,R. 6 E. ...... 566 
W. line, Sec. 13, T. 21, R. 3H. ..... 400 | N. line, Sec. 12, T. 25, R. 6 E. ...... 554 
W. line, Sec. 18, “IN. a1) RuvA Be sess 403 | Crossing Little Bau Pleine eanendeinieia 544 
W. line, Sec. 8, 21, Bod Be vianees 405 | N. line, Sec. 6, T. 25,R.7E......-. 554 
W. line, Sec. 9, T. 21, R. 4 E. ..-..- 408 | N. line, Sec. 32, T. 26,R.7E. wo... 553 
W. line, Sec, 10, T. 21, R.4E....... 409 grade........ 550 
W. line, Sec. 2, T. 21, R. 4 E. ...... 410 | Crossing Wisc. River + high water... 538 
W. line, Sec. 1, T. 21,R.4 4H. ......- 414 low water ... 523 
W. line, Sec. 6, T. 21,R.5E. ...... 419 | Knowlton depot .....--.+.-. eee eee 547 
W. line, Sec. 5, T. 21, R.5E. ....-.- 421 | N. line, Sec. 20, T. 26, R. 7K. ...... 561 
W. lime, Sec. 4, T. 21, R.5 EH. .....- 425 | N. line, Sec. 17, P26 RAT WW, askees 571 
W. line, Sec. 34, T. 22, R.5E. ..... 413 | N. line, Sec. 8, T. 26, R. 7H. ...... 579 
Port Edward station ........---++-- 888 | N. line, Sec. 5, T. 26, R. 7H. ....-. 578 
N. W. corner, Sec. 36, T. 22, R. > E. 897 | N. line, Sec. 32, T. 26, R. 7 K....... 558 
N.W. corner, Sec. 25, T. 25, B vp N. line, Sec. 28, T. 26, R.7E. .....- 575 

Bs. avicdhe wane ped Mar Wah PAR ee 426 | N. line, Sec. 21, T. 26, R. 7H. ..-.-- 586 
N. line, Sec. 24, T. 22,R.5 HE. ...-.. 433 | N. line, Sec. 15, T. 26, R. 7H. .....- 593 
Centralia depot’ cepatbacilecsssen nacre e SRS SEH ts 431 | N. lne, Sec. 2, T. 26, R. 7H. .....-- 606 
Crossing Green Bay R. R......---++- 442.1 N. line, Sec. 35, T. 28, R. 7 E.....-- 579 
N. line, Sec. 5, T. 22, R.6E........ 454 | N. line, Sec. 25, T. 28, R. 7K. ...--- 593 
N. line, Sec. 32, T. 2, Ru 6 Be. suse 458 | N. line, Sec. 19, T. 28, R. SE. ...--- 612 
N. line, Sec. 29, T. 23, R.6 EH. ...... 478 | N. line, Sec. 18, T. 28, R. 8 e Ss ruoiouerane 633 
N. line, Sec. 91; T. 23, B. 6B. ieee 507 | N. line, Sec. 7, T. 28, R. 8E...--.... 641 
N. line, Sec. 16, T. 23, R. 6 E....... 529 | N. line, cere PE 28, Het, anos ai 
Bl h de ot, Sec. 9, T. 23, R. 6 BOL ng wea smacuenesta bases : 

Hea ce ANY JERS US ONE 56g | Wausau {cep river above dam ....+-+-- 623 


432 GEOLOGY. OF CENTRAL WISCONSIN. 
AmuERsT TO MERRILLON. 
Green Bay and Minnesota Railway. 
Place. Altitude. Place. Altitude. 
Amherst depot .......eeeee eee e eee ee 553 | Crossing Yellow river, Dexterville .... 417 
W. line, Sec. 18, T. 23, R. 10 E...... 539 N.W. qr. N.E. qr. See. 21, T. 22. R.3 


ee yee Te 
OE. 54 


N. WW. qr. Sec. 22, T. 23, R. 9 EK... 
8. Bae 8 W. gz. Sec. 21, T. 23, RB. 


NH ge 8.18 gr, See. 90,1 2, 9H | 
ie Sinead: Wear Bea, Wt, aa. 


Wine, Sée. 19, T. 23, R. 9 E....... 
N. E. qr. 8. W. qr. Sec. 24, T. 23, RB. 
pH 


eee ee Mahe es et, SE epee te ee ater 
N. E. qr. 8. W. qr. Sec. 21, 
8E 


501 
497 


eo 33,7. 23, R.8 E., 
S. E. qr. 8.E. gr. Sec. 32, T. 23, R.8E., 
ae qr. N. H. qr. Sec. 5, T. 22, R. 7 


"s 
ee rv. Sec. 2, T. 22, R.6 E., 470 
S. E. qr. N1 qr. Sec. 10, T. 24 RB. 6 
NTs a ese ae reece aes 470 
N. E.qr.5. W. qr. Sec. 9, T. 22, R. 6E., 465 
Grand Rapids depot 
shen qr. 8. W. qr. Sec. 7, T. 22, R. 6 
H 


436 
wie iy Sa i888, 5, 438 
ae qr. N. E. qr. Sec. 16, T. 22, R. 


aie ce late alate adats alone ty tons tae ore btere ae 30 
Bn TE IG@ sens auvanacernmeaxtatoue Goeavcnsse eases 433 
8. E. qr. Sec. 15, T. 22, R.4E....... 433 


are qr. 8. W. qr. Sec. 16, T. 22, R. 
Hemlock ereek crossing ........ 20... 
“B.gr. N. EB. Sec. 247. 22 B. 3, B., at 


3/8. E.gr. NE. 


419 
qr. Sec. 20, T. 22, R.3E, 439 
, See 19 41 


He creek crosst 0 
‘00, 24,T. 22, R.2E., ae 


Scranton depot. ..........e eee eee 886 
ce creek crossing, Sec. 25, T. 22, 
Rib Ky syoreeaegstesseseeecs sess 882 


see ae ere ee 


385 


Creek crossing, N. W. qr. Sec. 25, T. 
22, R.1 W 


Near center, Rees 22, T. 22,R. 1 W... 402 
8. Tee N. E. qr. Sec. 21, T. 22, R. 


84 
78 Nines. E. oe Sec. 24, T. 22, R.2 W., 384 


8. E. qr. 8. E i. qr. Sec. 14, T. 22, RB. 3 
Wis derek wired asked ain weee Banwels 


Povecarweuty 


362 


el 


3 23 
te a ae 


Crossing Black river, } STARS s+ ++ +++ 


urface...... 255 


N.E.qr.N.E.qr.Sec.4, T.22, R.3 W., 338 
8.E.qr.8.E. r.Sec.22,T.23, R.3 W., 350 
S.E. qr.8. . qr. Sec. 20, T.23, R. 3 

WY saan tana chases sirinie greases coe ot M2 ees 388 
Hall s creek crossing, | a espa ns 
Merrilon depot.......e eee ce eee eee 356 


SURFACE RELIEFS. 433 


PORTAGE TO STEVENS POINT. 


Wisconsin Central Railroad Surveys. 


- Place. Altitude. Place. Altitude. 
Portage depot ............. ee 232 | N. line, Sec. 18, T. 18, R.8E....... 524 
N. line, 8. E. qr. Sec. 23, T. 13,R.9 E. 227] 8. line, Sec. 4 T.18,R.8E....... 524 
N. line, Sec. 21, T. 13, R. 9 E....... 223 | N. line, Sec 98) ie eo 519 
N. line, Sec. 16, T. 18, R. 9 E....... 220 | Hancock depot............ccceseeee 513 
N. line, Sec. 9, T. 13, R.9 E....... 276 | N. line, Sec. 10, T. 19, R. 8 E....... 520 
N. line, Sec. 4, T. 18, R.9E....... 225 | N. line, Sec. 11, 1.19, RB. 8E....... 529 
N. line, Sec. 32, T. 14, R.9E....... 228 | N. line, Sec. 2, 7.19, R.8E....... 538 
N. line, Sec. 29, T. 14, RB. 9E....... 227| N. line, Sec. 85, T. 20, R18 E......, 542 
N. line, Sec. 17 ee mine ansean ois 265 | N. line, Sec. 26, T. 20, R.8E....... 561 

3 > Vsurtace.......... 285 | N. line, Sec 24, T. 20,R 8E....... 561 
Ww. line, Sec. 8, T. 14, R.9E....... 230 | N. line, Sec. 13, T. 20, R. 8 E....... 532 
S. line, Sec. 30, T. 15, R.9E....... 218 | Plainfield depot’ sda heuahs Yura Ceaudeata: ate ¢ 532 
N. line, Sec. 30, T. 15, R. 9 E....... 218 | N. line, Sec. 1, T. 20, R.8E....... 518 
N. line, 8. E. qr. Sec. 19, T. 15, R. 9E. 225} N. line, Sec. 86, T. 21, R. 8 E....... 527 
N. line, Sec. 4, T. 15, R. SE....... 344 | N. line, Sec. 25, T. 21, R.8E....... 524 
N. line, Sec. 33, T. 16, R. 8 E....... 344 | N. line, Sec. 12, T. 21,R.8E....... 495 
NN. line, 8. E. qr. Sec. 21, 1.16, R. 8H. 338] N. line, Sec. 1, T. 21, RB. 8 E.. 494 
N. line, 8. E. qr. Sec. 16, T. 16, R. 8E. 344] N. line, Sec. 36, T. 22, tog Opeeermree 493 
N. line, 8. E. qr. Sec. 32, T.17.R.8E. 401] N. line, Sec. 25, 7. 22) B'S EBL... 11) 492 
a ae eee in ze ih ot siiaie usted Bo N. line, Sec. 24, T. 22, R.8E....... 494 
IN. line, Sec. ; Hy siaceent alates ade... 492 
N’ W. comer Séc. 18, 17, B-8 B.. 550 | N- Ear. N. W. or. Seo. 13, j omade -.. 482 
N. line, Sec. 17, T. 17, RB. 7 E....... 544 | W. line, N.W. gr. Sec. 12, T. 22, R. SE. 485 
N. line, Sec. 36, T. 18; Ri 7 Bs «26's sh2 534 | N. line, Sec. 2, T. 22, R.8E........ 496 
N. line, Sec. 25, T. 18, R. 7 E....... 516 | Plover depot. ........ec.eeceaeeeeee 496 
Middle E. line, Sec. 24, T. 18, R. 7 E. 514} Stevens Point depot................ 508 


STEVENS POINT TO THE NORTI LINE OF TOWNSHIP 29, 


Wisconsin Central Railway. 


Place. Altitude. Place. Altitude. 
Stevens Point depot....... aed oe W. line, See. 22, T. 25, R. apie ba 
Cutting N. E. qr. Sec. { grade.....-... grade. 

wes Toh, Re8 Be | puta meen 54g | W. line, Sec. 21, 1.214 | Be 865 

N. W. corner Sec. 31 1, T, 24, R. 8 H.. 511] W. line, Sec. 20, T. 25, R. 4 EL... 0... 626 
N. line, S. W. qr. Sec. 95, T. 24, R.7E. 511) W. line, Sec. 19, T. 25, R.4E....... 658 
S. line, 8. E. qr. Sec. 23, T. 24, R. 7E.. 513) W. line, Sec. 13, T. 25, R. 3 E....... 678 
W. line, Sec. 15, T. 24, R. 7 E....... 500 | W. line, Sec. 14, T. 25, R. 3 E....... 670 
‘W. line, Sec. 16, T. 24, R. 7E 526 | W. line, Sec. 15, T. 25, R. 3 E....... 680 
'W. line, Sec. 8, T. 24, R. 7 E...... 519 | W. line, Sec. 9, T. 25, R.3E... ... 693 
'W. line, Sec. 7, T. 24, R. 7E....... 522 | W. line, Sec. 8, T. 25, R.3E....... 716 
'W. line, Sec. 1. T. 24, R.6E....... 543 | N. W. corner Sec. 6, T. 25, R. 3 E 699 
W. line, Sec. 2, T. 24, R.6 E....... 563 | N. line, Sec. 26, T. 26, KR. 2 E....... 721 
‘W. line, Sec. 3, T. 24,R.6E....... 587 | N. line, Sec. 22, T. 26, R.2E....... 735 
W. line, Sec. 4, T. 24, R.64H....... 606 | N. line, Sec. 16, T. 26, R, 2E....... 721 
'W. line, Sec. 32, T. 25, R.6E....... 615! N. line, Sec. 8, T. 26,R.2E....... 731 
W. line, Sec. 31, T. 25, R. 6 E....... 615 | W. line, 8. W. qr. Sec. 18, T. 28, R. 2 E 768 
‘W. line, Sec. 36, T, 25, R. 5 E....... 612 | W. line, 8. W. qr. Sec. 7, T. 28, R. 2 FE. 789 
W. line, Sec. 35, T. 35, R.5E....... 623 | E. line, 8. E. gr. Sec. 1, T. 28,R.1E . 821 
W. line, Sec. 34, T. 25, R.5 BE... ... 608 | N. line, Sec. 35, T. 29, R. 1 E........ 830 
W. line, Sec. 28, T. 25, R.5 E....... 588 | N. line, Sec. 25, T. 29, R. 1 E........ 847 
W. line, Sec. 29, T. 25, R. 5 E.....-. 588 | N. line, Sec. 24, T. 29, R. 1 E........ 842 
W. line, Sec. 30, T. 25, R.5 E....... 583 | N. line, Sec. 13, T. 29, R. 1 E........ 838 
W. line, Sec. 25, T. 25, R. 4 E....... 631 | N. line, Sec. 12, T. 29, R. 1 E........ 866 
W. line, Sec. 26, T. 25, R. 4 E....... 639 | N. line, Sec. 1, T. 29, R.1 E... 855 


Wis. Sur. — 28 


434 


GEOLOGY OF CENTRAL WISCONSIN. 


BAROMETRICAL ALTITUDES.! 


Primrose. T. 5, R. 7 E. 


Mid. FE. hf. See. 3............ 0. eee 20 
Mid. 8. line 8. E. qr. Sec. 3........ 520 
NE. Cott. 806. Vaccciecassgaaasaes 375 
Mid. E. line N. E. qr. Sec. 7......- 510 
Mid. E. line 8. E. qr. Sec. 7.....-. 545 
Road at Grist Mill, N. W. qr. Sec. 8, 395 
Mid. E. line Sec. & ......- eee ee eee 5 
Stream crossing, 8. E. qr. Sec. 10.. 

N. W. cor. Sec. 11 «0-20.20... ‘ 
Ceriter: See. 1h. scscsccscee iced werent 
Stream crossing, E. hf. Sec. 11..... 330 
W. line N. E. qr. N. E. qr. Sec. 15. 410 
Mid. E. hf. Sec. 15....... 2... eee ee 390 
Di W.. COR: SOC. To. wwasunticawainates 480 
8. W. cor. Sec. 16..........--006- 430 
Center W. line Sec. 16............ 490 
Center W. line Sec. 17..........-. 445 


19 
Center W. line 8. W. qr. Sec. 20... 595 
Top of isolated blutf near mid. E. 


Aw ein 5.09 Sek javerhve sesh Gyeisca webs. on 385 
Center 8. W. qr. Sec. 26...... ... 570 
Center W. line 8. W. qr. Sec. 26... 560 
Center 8. E. qr. Sec. 27............ 580 
Center N. E. qr. Sec. 28.........-. 570 
Center Sec. 29.0.0... ccc c eee ees 540 


Stream at center 8. W. qr. Sec. 29.. 420 
Mid. N. line Sec. 35 0.0.0... eee 
Center Sec. 36 


N. W. cor. Sec. 86..........0 0000 530 |” 


Montrose. T.5, R. 8 E. 


Center Sec. 1. ........ Aaah aye Gae 430 
Mid, 8. line Sec. 1..... ee eee ee eee 470 
Ni He tor, ‘SeGe Lis ccuairattyneitecee 465 
NeW. 008. Bees Less coe sie saree ere 430 
Stream crossing, N. W. qr. Sec. 2.. 360 
Paoli Hotel, Sec. 2...........0.08, 315 

enter 5. W. qr. Sec 1l........... 310 
Mid. E. hf. 8. KE. gr. See. 14......¢ 405 


Aga k= eee erat ae 360 
Mid. E. line Sec. 22.........6. 00. 310 
Road, 8. line 8. W. qr. Sec. 23..... 300 
Road, E. line, N. E. qr. Sec. 23.... 380 
Mid. E. line Sec. 25............... 300 
Center 8. EK. qr. Sec. 25 .........4. 320 
8. W. cor. Sec. 25.......... inde eS 320 
8. W. cor. Sec. 26.0... cece eee 280 
Mid. W. line, Sec. 26............. 295 
Road, N. line N. W. qr. Sec. 26.... 300 
Center Sec. 80... .....cceceeeeeees 450 


Oregon. T. 5, R.9E. 


Railroad crossing, W. hf. Sec. 1.... 380 
Center: S60) 223i see a pee waveredins 


Mid. W. line Sec. 2............... 
Mid. W. line Sec. 8......-........ 
Center Sec. 4. . 22.0... .0 ccc r cece 
Center Sec. 5.......-..0005 
Mid. N. line See. 7....... 
Mid. W. line Sec. 7.. 
Mid. N. line See. 8........... Sse 
Center Sec. 8........0.cesceeev eee 
Center SeG.O'e seu: a.ociie aie ttenaaee 
N. E. cor. Sec. 9.0.22... 0 ccc eee e ee 
20 rods E of mid. of N. line Sec. 10.. 
Road under railroad, Oregon....... 852 
Mid. 8. line 8. E. qr. Sec. 12....... 357 
Road forks, near S. W. cor. Sec. 12. 380 
Mid. Eiht. See. 18.............005 407 
Mid. N. line Sec. 14............ » 455 
N. W. cor. Sec. 14.............008 490 
Mid. N. line Sec. 15............00. 425 
Center Sec. 15... ...ec ac cceeeeeee 460 
Ne W.. Core Sec. 15s viccieen vies ive vs 385 
Mid. E. bf. Sec. 16................ 460 
Center Sec. 16....... ...0.00 cee 440 
N. W. cor, Sec. 16.......:.008- ... 860 
Mid. W. line Sec. 16.............. 380 
Center Sec. 17......c.0ce cece eee . 895 
Mid. E. line Sec. 17........ 0... 0. ‘ 
Mid. N. line Sec. 17... 2.0.0.0... 
N. W.cor. Sec. 17s sass ins vncecwe 
Center Sec. 18......... ieee kina 
Mid. N. line Sec. 18.. ai : 


Mid. N. line Sec. 19............... 

N. W. cor. Sec. 20.......... eee ee 
Mid. W. line N. W 

Mid. K. ht. Sec. 21. .............. 
Mid. E. hf. Sec. 22..............0. 
Mid. N. line N. E. qr. Sec. 22...... 420 
Mid. N. line Sec: 23........ 00... 420 
Mann's quarry, N. E. qr. Sec. 24... 407 

Rutland, T. 5, R. 10 E. 

Mid. W. hf. Sec. 2............000% 295 
Mid. §. line 8. W. qr. Sec. 2....... 810 
Creek crossing, 8. E. qr. Sec. 15.... 255 
S. W. cor. Sec. 15... .... cece eee 290 
Mid. 8. line Sec. 16............... 295 


Road at mill, N. I. qr. Sec. 19..... 315 
Forks of road, $8. W. qr. Sec. 20.... 330 
Road at head of stream, 8. hf. Sec. 20 312 


Mad. E. line 8. E. qr. Sec. 20...... 350 
Mid. E. line Sec. 21.............., 290 
8. E. cor. See. Q1.........02 cee ee 290 
Mid. S. line 8. W. qr. Sec 22...... 330 
Dunkirk. T.5, R. 11 E. 
Mid. E. line See. 1........,... 02. 365 
Mid. W. line Sec. 1.. Seateeaes 410 
Mid. W. line Sec. 2...........0... 335 
Mid. W. line Sec. 3....... -.0 000, 280 
Railroad, N. line Sec. 5 .......2... 290 
Mid. N. line N. W. qr. Sec. 7...... 325 
N. EL cor. Sec. Tee cece eee eee e eee 305 


1T have been compelled, at the last minnte, to throw out several hundred of these altitudes, in 
order nut to excecd the limits assigned to this report, 


SURFACE RELIEFS. 435 


BaRoMEtTRicaL ALTITUDES — continued. 


Dunkirs. T. 5, R. 11 E.— (con.) 


Stoughton depot, BeOS eset ees 279 
N. B. cor, Sec. 8....-... cece cece ee 310 
N. Ey cor. See. 9..-..... cece cee 820 
Railroad, E. line, Sec. 9........... 278 
E. cor. Sec. 10...-.......0 0000 310 
Mid. W. line Sec. 11... .......... 335 
Mid. N. line See. 11............0.. 335 
Mid. W. line Sec. 12.............. 370 
Mid. N. line Sec. 12...........4.. 360 
N. E. cor. Sec. 12....-.... eee eee 325 
Mid. E. line Sec. 12............... 295 
N. W. cor. Sec. 18..........2. 0 0e 340 
Mid. E. line See. 13.. wagsaed 20D 
Mid. W. line Sec. 1 Rae 830 
Teailroad, 8. line See. 15........... 269 
Railroad, N. line Sec. 16.......... 273 
Mid. W. line Sec. 17... ........0.. 340 
Mid. N. line Sec. 18 ... «22.20... 280 
Mid. 8. hf. Sec. 19.........-..-6.. 310 
Forks of road, near mid. E. line Sec. 
Wivcoceaaie soee RES $508 Che OE ME 280 
Mid. E. line Sec. 21....... ....... 325 
Mid. W’. bf. Sé@;. 22.004 .seesn eee 310 
Center Sec. 23.2... 00. cece cree 310 
Mid. E. line N. E. qr. Sec. 24...... 240 
N. W. cor. Sec. 25. .... 2... eee eee 320 
Mid. W. hf. Sec. 28 .....-...-.... 290 
Mid. N. E. qr. Sec. 29........ -.. 290 
Mid. N. line Sec. 29 .............. 325 
Mid. N. line Sec. 30 .........-..-. 305 
Porter’s quarry, S. He Sec. 80...... 330 
Mid. N. line Sec. 81 ........-..00- 845 
Center Sec. 81....... cece cece eee ee 320 
Mid. N. line Sec. 82 .......-2..06- 290 
Mid. N. lime Sec. 83............-4. 300 
Crossing Catfish creek, N. line Sec. 34 215 
Mid. N. line Sec. 35 ...........-4- 265 
Mid. N. line Sec. 386..... ......-- 295 
N. E. cor. Sec. 36 ...--- eee eee ee 325 
Albion. T. 5, R. 12 E. 
Mid. W. line 8. W. qr. Sec. 6 ....- 365 
N.. Wi. C08 S66. Tesiweeice exe ssesae 325 
Mid. N. line N. W. qr. Sec. 7 ..... 330 
Humpbrey’s quarry, 8. E. qr. See. 10 ae 
Center Sec. 11... 02.2... cece eee eee 300 
N. W. cor. See. 13 «2... eee eee eee 290 
Surface of Rice lake...........++- 230 
Mid. N. line Sec. 14...........--- 250 
N. W. cor. Sec. 14.......2.00 eves 310 
Center Sec. 14 ....-.-.. eee eee eee 300 
Mid. S. hf. Sec. 14 ............--- 290 
Mid. S. hf. Sec. 18 ....-....0-.05- 260 
Mid. N. line Sec. 20 ........--.00- 280 
Mid. N. line N. W. ar. Sec. 20°.... 320 
N. E. cor. Sec. 20 ......- . eee eee 270 
Road forks, N. line Sec. 21........ 295 
Mid. E. line Sec. 21 ...-.-...--6+- 245, 
Mid.. E. ht: Sec. 22 wcsiwws vee vcanes 955 
Mid. E. hf. Sec. 28......-200 eee eee 270 


Surface Koshkonong lake, Sec. eae 200 
Mid. W. line 8. W. qr. Sec. 26 .... 270 
Center §. E. qr. Sec. 27..-.-+- ++ 265 
Mid. E. hf. Sec. 27 ..-.g- eee eeeee 260 
Mid. N. line Sec. 27 .......-- - eee 250 


Albion. T, 5, R. 12 E. — (con.) 


Ni W.cor; Sees 28u ewnaad caaieinuaes 280 
Mid. N. line Sec. 29 ...... 00. 00. 285 
Mid. N, ht. Sec. 29.........0c0 eee 295 
Center N. E. [r. See: 80s sserscivwa. 260 
Mid. W. line See. 81...........005 320 
Center Sec. 82 ...... 0... ccc e cee 315 
Mid. N. line Sec. 82 ........-..... 305 
Mid. E. line Sec. 84 ...... 2.0.00, 270 
Crossroads, near A tua Sec. 85..... 245 
BS: Ey cor. S66. Biss aaa acccisccne sae 255 
Road forks, E. i B66, 36 seccae: sce 285 


Stream crossing, N. W. qr. Sec. 36. 235 
Verona. T. 6, KR. 8 E 


Mid. N. line 'N. E. qr. § Bee: 2 caiasen 500 
Center S. line Sec, 3.1... 1. ee eee 430 
Head of stream, W. hf. Sec. 6..... 400 
N. E. cor. See. 6.0... 0... c eee ee eee 520 
Stream crossing, N. hf. Sec. 7 ..... 380 
Mid. E. ht, Sec. 7.-..-...0-ece eee 420 
Center Sec. 8.... 0.00. e eee e ences 450 
Mid. 8. line Sec. 10.............6- 450 
Ds He COP BEG, LQ scasinnicscae seuanievors 480 
S. E. cor. Sec. 18...-.... 0.00 ce eee 480 
Verona P. 0., Sec. 15. ........... 380 
Mid. §. line Sec. 17....-..-..-008. 865 
Center S66. 18 oe esis eae ernie atees aces 480 
S. W. cor. Sec. 23......-0.. ec eens 445 
Mid. 8. line See, 28... ........... 460 
By Hi COr: SOC, 23.0. once peak wae saa 500 
Mid. W. line Sec. 24...........0.. 463 
Center Sec. 24.........ccccneecees 490 
Mid. E. line Sec. 24............... 490 
NE cor. See. 24 6. acta von gece 460 
Mid. 8. line Sec. 24....... 22-0... 500 
Mid. N. 14 See. 25... «2... ee eee 520 
Center Sec. 26.......00ccceeseeene 520 
S. W... cor, Sec; 26: seccasecdiecces 460 
Mid. 8. line Sec. 26..........--.05 435 
Center Sec. 35......0. cece eee aoe 395 
Mid. 8. line Sec. 85..........55 66 880 
Fitchburg, T. 6, R. 9 E. 
Cross roads, E. hf. Sec. 1........-. 300 
Mid. S. hf. Sec. 1..........0 eee eee 380 
Mid. 8. lineSec. 1....-. 02... eee 407 
Stream crossing, center Sec. 2...... 260 
Mid. S. line Sec. 2........ 0... e eee 325 
Mid.S. lineS. E. qr. Sec. 2....... 320 
Center N. E. qr. Sec. 3.....----5-- 430 
Mid. 8. line S. E. qr. Sec. 6.......-. 395 
Top of bluff, N. W. gr. Sec. 7..-... 500 


Cross roads, 8. line S. W. qr. Sec. 8. aa 
S Bitor Sad, Wo ntyceenncwed vec 370 
Waldron’s quarry, S. line Sec. 16.. ee 
S. E. cor. Sec. 10......... 2.0. 


Center Sec. 22.......ecc cece eee eee 333 
Mid. S. line Sec. 12 ........---05- 295 
Mid. E. hf. Sec. 18.......-. .eeeee 355 
Mid. N.hf. See 13.....-.-....06. 825 
S. W. corner Sec. 14.....-.--.---- 393 
Mid. §. line Sec. 15... «ee eee eee 400 
S. W. cor. Sec. 15............0006- 425 
Mid. N. E. qr. S. E. qr. Sec. 16.... 480 
S. W. cor. Sec. 18..... .eeeee ween ATO 
Mid. W. line Sec. 19.....-++0-000- 490 


436 GEOLOGY OF CENTRAL WISCONSIN. 


BAROMETRICAL ALTITUDES — continued. 


Fitchburg. T. 6, R. 9 E. —(con.) Pleasant Springs. T. 6.R. 11 ie ee 

Cross roads, F. hf. Sec, 19.......+ 470| Mid. 8. line 8. B. qr. See. 6... 
Mid. E. line Sec. 19 ........200-- 440 Center S. line Sec. 8. on 
S. W. cor. See. 19...... 2. cs cece eee 490| §. E. cor. Sec. 8... 985 
Mad. S. line Sec. 19.2.0... .. eee eee 460| 8. E. cor. Sec. 9... : «. 829 
Centar Sec. 20.......- 2.0 ee ee eee 430| Mid. E. line Sec. 9.... 0-2. ...0ee 340 
Center'$60..2) cviuscnseeecedsceds 550] Quarry, N. E. qr. e E. qr. See. 410 
School House, E. hf. Sec. 21........ 470| Mid. N. hf. Sec. 11..... . 280 
Road, &. E. qr. 8. E. qr. Sec. 21.... 455] Center 8. E. qr. gee. ll. . 320 
Mid. EL Uf, Sees QQ.rcrseset aeeees 425| Mid. N. hf. Sec. 13......... .. 820 
Creek crossing, 8. E. r. Sec. 24.... 316| Mid. E. line, 8. E. qr. Sec. 13 ..... 325 
Mid. 8. ang E. qr. See, 24... 2 c00s 840) S..E. cor. Sec. 13..-...eeeeee wees 370 
8. E. E. gr. BOG. Qa. na cen owes 409| Mid. W. line N. W. ar. Sec. 13... 300 
Mid. Tne WN. W. qr. Sec. 26.... 460] S. W. cor. Sec, 14.2... eee eee 320 
Center Sec. 27... .ceeuceee ce vee 421 Mid. S. line See. 15........-.-. 005 290 
Center Sec. 28.......0. cece eens 367| Mid. W. line 8. W. qr. Sec. 15. .. 260 
Mid. E. hf. Sec. 29.......... re 480] Mid. 8. line Sec, 17............-5- 265 
Mid. W. hf. Sec. 29...........00.. 450| Center Sec. 22........... eee eee 268 
Center Sec. 30.... ce ceee cence reece 420| Mid. §&. line Sec. 22............005 840 
Mid. W. line Sec. 80........-.066- 480) §S. E. cor. Sec. 24.... ........00ee 400 
Mid. W. line a Ds ka aie wea acs 465 | Mid. E. line Sec. 25 .............. 3880 
Oak Hall, center Sec. 33........-66 354] Mid. W. line Sec. 81 ............. 805 
Mid. E. line Sec. 33...........--.. 3538} Center Sec. 81.......ceeeceeeeceee 300 
CentorSee: 84 .sisevisasuster.w0 ine oe ke 345 Center Sec. 32......6... eee ee eee 280 
Mid. W. hf. Sec. 36........... .-». 407| Mid. W. hf. Sec. 34 .......00-20- 308 
Center Sec. 36.... 0. ..e esse eeeee 885} Mid. N. hf. Sec. 84....... ....... 260 

Dunn. T.6, R. 10K. Mid. W. ht. Sec. 85 ........-..04. 340 
Road forks, E. line N. E. qr. Sec. 1. 280] Mid. E. line Sec. 36.............- 310 
Road forks, W. line N. W. qr. Sec. 1 290] 8. E. cor. Sec. 36........0.65 cee 300 
Mid. N. hf. Sec. 2............0..- 320 | Christiana. T. 6. R.12E. 

Creek Grossing center N. W. qr. Mid. W. line Sec. 2......... 0.066 290 

SOGs Maceatian ection Wis wtalaeecau 2551 Mid. BE. hf. See. 3..........2 000s 280 
Mid. “i! hE Sec, Gis. aves sees 315] N. W. cor. Sec. 6 ..... eee ee eee ee 315 
Mid. W. hf, Sec. 16..........-.05. 315| Mid. 8. line §, E. sft Sec. 6 ....aee 285 
Mid. W. line Sec. 16 ........0.. 6% 300) Stream Cooney . hf. Sec. 7... 275 
Creek crossing, 8. line 8. W. qr. Sec. Mid. 8. hf. Sec. 7.0.2... . cee eee 330 

1G asctinsa cate Senn Gali Waa eneeam 270 Mid. E. hf. Sec. 10 .............6- 320 
Conter See. 17.5 acs. sec eisaecce wee 265] Mid. W. hf. Sec. 11 .............. 280 
Center S. line Sec. 17.........2.6 290| Mid. E. line Sec. 11 ........-..04- 260 
Creek crossing, N. W. qr. Sec. 18.. 255| Mid. N. hf. Sec. 12.............0. 230 
SW. cor: See, 18. vascnecavincsae 270| Mid. E. hf. Sec. 12............0... 230 
Mid. E. line See. 19.........2-2-6- 330 Stream crossing, mid. W. line Sec.14 290 
Stream crossing. near center Sec. 20 316] §. E. cor. Sec. 15... .. cece eee eee 825 
8. W. cor. Sec. 20......... eee eee 340} Mid. S. line Sec. 15.............65 350 
Conter See: Ol cs.oncasoivedacdaaaan 325 | Mid. EK. line N. E. qr. Sec. 15...... 815 
Center S. line Sec. 21........6..2% 325] Mid. S. line Sec. 16............008 885 
Center S. line 8. W. qr. Sec. 21.... 860] 8S. W. cor. Sec. 16............... 400 
S. E. cor. Sec. 21.1.6... +. see ee eee 293 | Mid. §. line 8. E. qr. Sec, 17.....0 410 
Mid. E. line 8. E. qr. Sec. 21... ... 354] 8. W. cor. See. 17... 0... eee eee 355 
Mid. S. line Sec. 22.............8 285 | Center Sec. 18.............0 eee ee 315 
8. W. cor. Sec. 2B.......eceecseee 298| Mid. §8. line Sec. 18............... 340 
Mid. S. line Sec. 25.........00000e 275 | Stream, E. line S. E. r. See, 21.... 3815 
Mid. E. line Sec. 31 ........... 6 360} Mid. E. line 8. E. qr. Sec. 22...... 360 
Mid. 8. line Sec. Sat galelake ea avta eee 315 BS. Hy cor: Sec: 92. 0224.3 veean toe Bs 320 
Mid. §. line §. E. qr. Sec. 85.. .... 275 | Cross-roads, 8. line S. E. qr. Sec. 23. 310 
Mid. S. line 8. W. qr. Sec. 34...... 275] N. W. cor. Sec. 27...... cece eee ee 375 
Mid. 8. line 8. W. qr. Sec. 3o..... 295] Cross Plains. T. 7, R. 7 E. 

Pleasant Springs. T. 6. R.11 FE. Mid. E. line Sec. 1... ..0.0.-e-0eee 400 
Bend in road, 8. line 8. W. qr. Sec. 2 350 Cross Plains depot, Sec. 3... .....-- 274 
Mid. 5. line Sec. Secvewe ced eeesee 350| Topof bluff, N. line N. W. qr. Sec, 3. 420 
S.. Wor: See; Boeke oabve ees es 835 | Mid. S. line Sec. 3......2-. 00.000. 400 
Mid. W. line See. 3 Oeines Bee ES Re 400| Mid. EK. line N. E. qr. Sec. 7....... 345 
N. W. cor. Sec. 3 oe. eee eee ee eee 400] Center Sec. 10......... 0. cee eee eee 325 
Mid. S. line Sec. 4.00... -.e eee ee 880] Center 8. E. qr. Sec. 10.........4- 330 
Mid. W. hf. Sec. 4.......... eee eee 8251! Mid. E. line Sec, 11.............4 326 


SURFACE RELIEFS. 437 


BAROMETRICAL ALTITUDES — continued. 


Cross Plains. T.7, R.7 E.—(con.) 


é Middleton. i 7, R. 8 E.—(con.) 


Mid. E. line 8. E. qr. Sec. 12...... 83: Center Sec. 85 2.6... cece cee ee eee 448 
Mid. W. line . cor. Sec. 15... 480} Mid. E. tee 8. E. qr. Sec. 85....-. . 530 
Center 8. W. ar. Sec, 15........06. 490 | Mid. E. line Sec. 85.............8. 423 
Mid. 8. line S. W. qr. Sec. 15...... 400 | Center Sec. 86.... ...... cece eae 488 
Mid. N. hf. Sec. 17.......... 0000 825] Mid. E. hf. Sec. 86 ............005 458 
“Mid. W. line N. W. qr. Sec. 17.... 340} Madison. T. 7, RB. 9 E. 
Mid. E. line Sec. 19............... 500] Lake Mendota............ ....0. 270 
Mid. E. line N. E. qr. Sec. 19...... 480| Capitol Hill, 8. W. cor. Sec. 18.... 348 
Mid. E. line 8. E. qr. Sec. 19...... 595 | University Hill, 8. W. cor. Sec. 14. 372 
S. EL cor, See. 19 sé. s%..03 cscs gies 570 | Railroaa, 8. line Sec. 16 .......... 260 
Mid. S. line Sec. 20..........-.... 495| Mid. 8. line Sec. 18........ 2. . 882 
S. EB. cor. Sec. 21..... cee cee eee ee 490| Mid. 8S. line S. W. qr Sec. 19. 450 
Mid. W. hf. Sec. 22............... 390 Mid. 8. line Sec. 19 415 
Mid. W. line 8. W. qr. Sec. 27..... 405] 8. E. cor. Sec. 19..... 400 
Stream, center 8. E. qr. Sec. 33.... 405] Mid. S. line 8. W. qr. Sec. 20 360 
Middleton. T. 7, R. 8 E£. Mid. 8. line 8. E. qr. See. 20 . 435 
Road forks, E. hf. Sec. 2.......... 367| Mid. 8. line 8. W. qr. Sec. OL ensue 115 
Mid. W. line Sec. 2......0.008 see 367} Center N. W. qr. 8. E. qr. Sec. aL. 390 
Center Sec. 3.......00. cc cece eee ee 367| Lake Monona................ . 2 
Center Sec. 4......--0. 22 eee renee 447| Road, mid. S. line Sec. 26. 
Mid. W. line Sec. 4.............6. 407| Center S. W. qr. Sec. 28. 
Mid. E. hf. See. 5.......... 0 cce ee 421| 8S. lneS. W. qr. 8. ve a. See. 2. 
Mid. W. hf. Sec. 5 .........24.04. 507} Mid. W. line Sec. 31. 4 
Mid). Baht) Secs 6-5 sssie's velaw dis sine 547] Center Sec. 31...... : 
Mid. W. hf. Sec. 6 ....... ..-..-- 527| Mid. E. line Sec. 31 ......... . 448 
Mid. W. line 8. W. qr. Sec. 7 ....- 339| Mid. W. hf. of E. hf. of Sec. 32.... 488 
CenterSec: 9 i cscnescseeceecenas’ 852| Mid. §. hf. Sec. 33 . 320 
Center Sec. 10.... 365| Mid. E. line Sec. 34. 290 
Stream crossing, N. ‘hf. See. 11. Bol]  CenterSec.35...6..6 sescseaveens 300 
Road forks. E. hf. Sec. 12..... . 320 Blooming Grove. T.7, R.10E. 
Mid. E. line Sec. 13 . 345 | Mid. N. line N. W. aE. "Bec. 3...... 888 
Mid. S. line Sec. 13. - 415} Mid. B. hf. Sec. 4. 315 
Mid. 8. line Sec. 14. Hs 410| Mid. W. hf. Sec. 9.. 825 
S. W. cor Sec. 14............. . 390] Center Sec. 9 ..........6. 310 
Mid. §. line 8. E. qr. Sec. 15 . 380| Mid. W. hf. E. hf. Sec. 10... 390 
Mid. W. line Sec. 16........-- 553 | Mid. W. ht. W. hf. Sec. 11 .....-. 410 
Mid. W. hf. Sec. 17 2.0... . eee eee 453 Mid. W. hf. Sec. 11........... .. 455 
Mid. S. line Sec. 17.........------ 518 Mid. W. hf. Sec. 12.............05 400 
Center 8S. W. qr. Sec. 17 ...-.----- 555 | 4 mile W. of center of Sec. 12.... 380 
Mid. 8. line 8. W. gr. Sec. 17 ..... 518| Center N. E. qr. Sec. 15 .......... 40 
Mid. E. line N. E. qr. Sec. 18...... 353 | Center 8. lineS. E. qr. Sec. 15..... 290 
Center N. E. qr. Sec. 18 .......-6- 428 8. W. corner Sec. 15...........005 310 
20 rods south of last...........--- 541} Mid. W. hf. Sec. 16............ . 310 
Mid. N. hf. Sec. 20......-.--2.-5- 540] Mid. W. ht. E. hf. Sec. 20........ 820 
Mud. S. hf. Sec. 20.......-+2-ee eee 508} Mid. W. line Sec. 21 ..... ..-.... 330 
p. H. cor. Sec. 20.... 2. ceeeeeeee 508} Center 8. W. qr. Sec. 21.......... 290 
Mid. S. line Sec. 21........--40--5 538 Center S. E. qr. 8. E. qr. Sec. 21... 270 
Mid. S. line S. W. qr. Sec. 22...... 508} N. W. cor. Sec. 22 ....ce eee e eee 310 
Mid. S. line S. E. qr. Sec. 22... ... 478| Center 8. E. qr. Sec. 22.......+--- 290 
SEL cor. S€0. 23 00sec cer eeeeees 450 | Mid. W. line Sec. 26 .......--005- 290 
Mid. S. line Sec. 24........000. eee 425 ‘e mile E. of W. line Sec, 27.. .. 280 
Mid. S. line Sec. 27.....2...00000- 498 Wid. N. line Sec. 80..........60-- 300 
QW. cor. Sec. 27..-..20 2 cee 550] Mid. W. line N. E. qr. Sec. 30 .... 310 
QW. cor. Sec. 23. . ssesceeeeee 495| One-sixth mile E. N. W. cor. Sec. 35. 350 
Mid. S. line Sec. 29........-00-0-- 480 | Center Sec. 35 ...... cess we eeeee 340 
SW. cor. Sec. 29......0-. eee eee 535 | Cottage Grove. T. 7, R. 11 E. 
Mid. E. line Sec. 31 ....-....--- 6 540} Mid. N. line Secl ...........006- 320 
Mad. E. line N. E. qr. Sec. 31...... 600} Mid. BK. line Sec. 1.........00- eee 350 
SW. cor. Sec. 82.0... ee cece eee 560 | Center N. W. qr. Sec. 1 .....----- 295 
Center Sec. 84.2.2. ec ce cence eres 508| Mid. W. line S. W. qr. Sec. 2....- 365 
’ Mid. S. line Sec. 34 ...-..--- 0. eee 478 | Center S. W. qr. N. W. qr. Sec. 2. 275 
SE. cor. Sec. 84....0.. ceeeeeeeee 558] Mid. W. line S. E. qr. Sec. 3..-... 360 
Mid. S. line 8S. W. qr. Sec. 35..... 513] Mid. W. line N. E. qr. Sec. 4.. 320 
Mid. 8. line 8. E. qr. Sec. 35 .....- 433! Mid. W. lineS.W. qr. 8. W. qr. Sec. 55 35 


438 


GEOLOGY OF CENTRAL WISCONSIN. 


BAROMETRICAL ALTITUDES — continued. 


Cottage Grove. T. 7, R. 11 E.—(con.) 
Center Sec. 6 20... cece eee ee ee eee 330 
Mid. N. hf. Sec. 7... 2... eee 325 
Mid. E. line N. E. qr. Sec. 7 ....-- 345 
Mid. N. hf. Sec. 8.-.. .......006- 345 
Mid. E. line Sec. 8 ........02..05 315 
Mid. N. hf. Sec. 9 2... cece ee eee ee 320 
Mid. 8. hf. Sec. 9.2.6.2... eee 300 
Center N. W. qr. Sec. 10 ......46. 300 
Mid. N. hf. Sec. 10............0., 340 
Mid. E. line N. E. qr. Sec. 10..... 270 
Mid. 8. hf. Sec. 11........... 2... 300 
Mid. N. hf of N. E. qr. Sec. 11 .... 345 
Center of S. W. qr. Sec. 12....... 360 
44 mile 8. mid. K. line N. E. qr. 

DeCel Siesta nee sl honavel arate 275 
Mid. N. hf Sec. 18 .............. 275 
zs mile 8. W. of N. E. cor. of 

OG: dA oh! pawesaa exter asin es 320 
as mile E. of center of Sec. 14 . 330) 
I mile N. E. of 8. W. cor. Sec. 19... 280 
Mid. W. lineS. W. qr. Sec. 21..... 280 
Mid. N. line Sec. 21 .............. 260 
Ns Hs COM. SOG: Ob isaicsnteraie vadelsianes a 300 
Mid. 8. line 8. E. qr. Sec. 29....... 240 
Mid. 8. line Sec. 29... ........... 300 
Mid. 8. ht. 8. W. qr, Sec. 29...... 310 
Mid. W. line Sec. 29.............. 280 
¥y mile S. E.N. E. cor. Sec. 30.... 280 

. Mid. E. hf Sec. 82 ............00 255 
Mid. N. hf Sec. 33 ...... 0... 0... 350 

* 1S. By cor: Secs BBs esisis daar eed oxie 420 
Mid. K. line 8. E qr. Sec. 33...... 340 

Deerfield.. T. 7, R. 12 E. 

Mid. N. line See. 4... 2. eee 320 

w Mid. S. AE Secods. «kanes see veences 290 
Center 8. E. qr. 8. E. qr. See.5.... 335 
Mid. E. line Sec. 7.-.............. 325 
S. W. cor. S. E. qr. S. E. qr. Sec. 8. 285 
Mid. N. hf Sec. 9................ 325 
Mid. W. line S. E. qr. 8. E. qr. 

A, -IOOCHE Danvers s aheh wisivte sateen ek nce 280 
Mid. 8. hf See. 10................ 265 

| Mid. 8. hf See. 11.0.0... 0. 0200., 275 
Mid. W. ht Sec. 12.... 0 0.2.0.2, 290 
Center 8. W. qr. 8. W. qr. Sec. 12. 310 

. Mid. 8. hf See. 12... 300 
8. E. corner Sec. lv... oe... 270 
Mid. E. line See. 13.............. 265 
Mid. S. line See. 13...... 0.0.0... 250 
Crossroads, N. W. qr Sec. 14 ..... 285 

oad corners KE. line N. E. qr. Sec 

WB cris cere wh pen deena cana eae 295 
Center 8. E. qr. Sec. 23........... 325 
Mid. W. hf Sec. 25.........5...., 280 
Mid. W. line N. W. qr. See. 25.... 270 
Road corners, 8. E. qr. Sec. 26..... 260 
Mid. E. hf Sec. 28........ 000... 280 
Mid. 8. line 8. E. qr. Sec. 29 ...... 360 
S. E. cor. Sec. 81.... 0... .cec cece 320 
Center 8. E. qr. Sec. 32........... 300 
Center N. W. qr. Sec. 33.......... 365 
S. E. cor. Sec. 83.......0 00.00.00. 305 
8. E. cor. Sec. 34. 6. 0 ......c. ee 805 
Mid. S. line 8. E. qr. See. 35....... 290 


Deerfield. T. 7, R. 12 E.— (con.) 


Mid. 8. line Sec. 36.........- ..6 300 
Berry. T.8, R. 7 E. 
Mid. S. ine 8. E. qr. See. 3.2.2... 340 
8. W. cor. Sec. 3.2.2.0... eee eee 330 
Mid. W. line Sec. 5.... 0. eee. eee 340 
Mid. 8. line Sec. 5......-....-.4.. 330 
Center'Sec.. 7 s+ ne mec niece wetaae’s 280 
Roadforks, N. W. qr. Sec. 8....... 280 
Roadtforks, N. W. qr. Sec. 9....... 310 
Mid. S. line Sec. 9 ....-...-e. ee 450 
Mid. S. line 8. E. qr. Sec. 10....... 40 
Center 8. E. qr. Sec. 10........... 365 
Mid. 8. line 8. W. qr. Sec. 18...... 440 
Mid. E. line 8. W. qr. Sec. 18...... 515 
Be W. cor: Seey 14 haues ounemeeeicar 540 
Road forks, N. E. qr. Sec. 15...... 385 
8. Wescott: See. 15 io aaecdanseunwws 370 
Center N. W. qr, Sec. 15.......... 380 
Center 8. E. qr. Sec. 16............ 850 
Center Sec. 16..........2c.ce eee 435 
Mid. N. hf. Sec. 16............08. 475 
Mid, 8. line 8. W. qr. Sec. 16...... 300 
Center N. E. qr. Sec. 17.........5. 500 
Mid. N. hf. See. 17........... 04. 465 
Mid. N. hf. Sec. 18.............-. 445 
. Mid. W. line Sec. 18.............. 440 
N. W. cor. Sec, 21.......... wenn BIO 
Mid. W. line See. 21.............. 310 
Mid. E. line N. E. qr. Sec. 21...... 450 
Mid. E. line Sec. 21............... 540 
Mid. 8. line S. W. qr. Sec. ¥2...... 350 
Mid. E. line See. 22............... 400 
Mid. N. hf. Sec. 23 ............... 450 
Road corners, N. EB. qr. Sec. 23.... 510 
Mid. E. line 8. E. qr. Sec. 24...... 415 
S. E. corner Sec. 24............004 360 
Mid. E. hf. Sec. 25............0.... 340 
Mid. W. line Sec. 25.............. 400 
Center Sec. 27....... 000. e ee eee 335 
Mid. 8. hf. Sec. 27.............004 345 
Road-forks 8. E. qr. Sec. 27....... 44) 
Road corners 8. W. qr. Sec. 27..... 330 
Center 8. E. gr. Sec. 29....... 0... 480 
Center N. E. qr. Sec. 29........... 490 


Mid. E. hf. Sec. 29 


Mid. S. line 8. W. qr. Sec. 2 ie 
Mid. 8. line Sec. 8 350 
Mid. 8. hf. of N. hf. Sec. 4........ 410 
Center Se. 4. 2.2... eee cee 480 
Road-forks W. line Sec. 5......... 410 
Road-forks 8. W. qr. Sec. 8 ....... 520 
Mid. EK. hf. N. W. qr. Sec. 8 ...... 480 
Road corners N. BE. qr. Sec. 9...... 350 
Mad. W. line 8. W. qr. Sec. 10 .... 340 


SURFACE RELIEFS. 439 


BAROMETRICAL ALTITUDES — continued. 


Springfield. T. 8, R. 8 E.—(con.) Burke. T. 8, R.10E. — (con.) 
Center N. W. qr. Sec. 12.......... 380) 1-8mile ls 6. ccc. cases eee cases 392 
Mid. W. hf. Sec. 15........-...-5. 395 | 8. E. corner Sec. 8..........20000- 832 
Mid. S. line Sec. 15....-.....-0.-65 400 | Mid. 8. line Sec. 9.............0.. 334 
S. W. cor. Sec. 15.....-- 2. eee eee 450 S. EB. cor. See. 9 wee eee eee eae 804 
Mid. 8. line S. W. qr. Sev. 16...... 520| Mid. 8. line Sec. 10 .............. 380 
Mid. E. hf. See. 17 «2.2.0... eee ee 520 S. E. cor. Sec. 10 22.0... sees 380 
Mid. W. line Sec. 17........ 2... 450] School, N. W. cor. Sec. 13......... 332 
Mid. W. line N. W. qr. Sec. 17.... 450] Center Sec. 12.............0..008- 327 
S.part N.E.qr.Sec.18..........6 402| Mid. 8. ht. Sec. 14.............088 372 
S.part S.E.qr.Sec-18 ..........-. 880) 8. W. cor. Sec. 17........ cee eee 277 
Road corners §.W.qr.Sec.19...... 375] Mid. N. hf. Sec. 19............... 292 
Center Sec.19.......-.. 2. cee ee eee 380] Mid. 8. line Sec. 19........... ... 827 
eet N. line S.W. qr.8. W.qr.Sec. Mid. E. line Sec. 21 .............. 314 

base vaavayenasectdats aie ueceuuna eantae 450 i Sec. 21 ...... 854 

Gane S60. 2 Liiacue ne nkaaneecwass 480 | Center Sec. 22 .... 00 cee eee ese ee 390 
Mid. W.hf.Sec.21................ 450| Mid. §. line Sec. 22 .....--+-0+ + 340 
Center N. W. qr. Sec. 21....-...-. 480] Ruilroad, E. line N. E. qr. Sec. 23.. 355 
Mid. W. hf. E. hf. Sec 22 ........ 870] Quarr N. W. gr. Sec. 27......00 825 
Center Sec. 22 .. 0... ec cece eee 429] Mid. rw. line Sec. 28....... 2.000. 308 
8. E. corner Sec. 22 ........-..-- 390] Center Sec. 29.2... . cece eee ee eee 280 
Mid W. hf. Sec. 23 ..........-46. 450) Center Sec. 30... wee. ee ee ee Joes 802 
Mid S. line, Sec. 24 ......-..0.0.. 350] Mid. 8. line Sec. 80 .........-..0.. 302 
Mid. W. line, Sec. 25...........-- 390 | Center Sec. 81............ ce eeeee 392 
Mid. E. hf. E. hf. Sec. 26.......... 430.| Crossroads N. W_ qr. Sec. 33....... 815 
Mid W. line Sec. 26 ........-..4.- 390| Mid. E. line N. E. qr. Sec. 33...... 274 
Center Sees 27 x sis sais aise rcnssreinielniatens 880 | Mid. W. hf. Sec. 35 .......... ... 420 
Mid W. line, Sec. 27 ......------- 420| Quarry, N. E. qr. N. W. qr. Sec. 35 462 
S. W. cor. Sec. 27.2666 cece eee 380 | Sun Prairie. T. 8, R. 11 E. 
S. line 8S. W. qr. S. W. qr. Sec. 28. 450} Mid. W. linc 8. W. qr. Sec. Lec... 315 
Center N. W. qr. Sec. 31.........- 525] 8. E. cor. Sec. 13.2... ee ee eee eee 330 
Mid. W. hf. E. hf. See. 3l. . 500} Mid. 8. lime 8. E. qr. Sec. 18....... 350 
Center S. W. qr. N. E. qr. Sec. 31. 560| Center Sec, 24.........ceececceeee 350 
Center S. W. qr. Sec. aL 450 | Medina. T.8, R. 12 E. 
Mid. E. line, Sec. 33 . mie OF Mid. W. line Sec. 1............4.. 290 
Mid. S. E. qr. Sec. Bi nee set 8. W. cor. Sec. 1.....--.- 2. wee 250 

Westport. T. 8, R. 9, E. Mid. 8. line 8S. W. qr. Sec. 2....... 260 
Mid. E. hf. 8. E. ar. Sec. 1 . 800] Mid. 8. line Sec, 3.......... eee ee 315 
Center S. E. qr. Sec. 2. 350] S. W. cor Sec. 3.... .- B15 
Waunakee depot ........-- 341| Mid. N. line Sec. 4.. 300 
Mid S. line 8. E. qr. Sec. 6 - .. 33) Stream, W. line Sec. 4 280 
S. E. cor. Sec. 7...---6- .. 390 Mid. E. line See. 7...... 320 
Mid. S. line Sec. 11 .-..-..- .. 403| 8. E. cor. Sec. 7.. 820 
S. E. cor. Sec. LL... cee eee eee eee 403] Mid. E. line Sec. sa 255 
Mid. N. hf. Sec. 12......... 2... 320] N. W. cor. Sec. 13.. 295 
S. W. See. 17... eee eee eee eee 325 | Mid. W. line Sec. iB. 255 
Stream crossing, E. hf. Sec. 19..... 290| 5. W. cor. Sec. 18. 270 
Bluff-top N. hf. Sec. 19........-.. 400| Mid. 8. line Sec. 14. . 805 
Mid. S. line 8. E. qr. Sec. 19 ...... 295] Mid. E. hf. Sec. 15.... ... 260 
Mid. E. line Sec. 19 .......-----0- 325 | Marshall, Sec. 15...........-- cee 290 
Roadforks, N. E. qr. Sec. 22 ...... 277| Center 8. W. qr. Sec. 16..-...-..- 280 
Mid. N. hf. Sec. 23 ......... -+--- 371 | Mid. W. line N. W. qr. Sec. 16.... 295 
Quarry, N. line S. W. qr. Sec. 25... 894] Center See 1 Tanteeecuaoaees .. 300 
Mid. S. line Sec. 25 .....-e eee eee 290 | S. W.cor. Sec. 18........-.5 és 
Center Sec. 26...-...-.eeee ee eeeee ,340| 8. E. cor, Sec, 20...-.--.-- 
Mid. E. line S. E. qr. Sec. 36 ..---. 310| Mid. E. ling Sec. 22 

Burke. T.8, R. 10 E. S. E. cor. Sec, 22.......-6- eee Pe 
Mid. E. line Sec. 1... ... eee eee eee 400] Mid. S. hf. Sec. 28.......65. 00.08% 
Mid. N. line, Sec. 3 ...--- eee ee ee 296 | Mid. S. line Sec. 23... .--..e eee 360 
Quarry, 8. W. qr. 8. W. qr. Sec. 2. 460] Mid. N. hf. Sec. 24... ..+..0- sees 320 
Creek, N. line N. W. qr. Sec. 3.... 285] Mid. 8. line 8. E. qr. Sec. pd eee 300 
N. W. cor. Sec. 4 wee cece ee ee ee eee 307| Mid. S. line Sec. 25.......--. eee 365 
N. W. cor. Sec. 5... eee ee ee eeeee 295 S. W. cor. Sec. 25...... 0c cece ee ees 315 
N. W. cor. Sec. 6... cceee ce eeeee 982| Mid. N. hf. Sec. 26......20.-66- . 420 
Mid. S. line Sec. 8 .-. «-4--e wee B02] Mid. S. line Sec. 26.....--.--- eee 390 


440 GEOLOGY OF CENTRAL WISCONSIN. 


BaROMETRICAL ALTITUDES — continued. 
‘Medina. T. 8, R. 12 E. — (con.) Roxbury. TT. 9, R. 7 E. — (con.) 


S. line 8. W. qr. 8. E. qr. Sec. 10 .. 285 
Mid. E. linc N. E. qr. Bee. Tsiss ders 
Mid. N. hf. Sec. 11 ..... 

N. W. cor. Sec. 12.. 
Mid. Nie hf. Se¢:.12s cccce wre svies s 340 
Center N. E. qr. 8. W. qr. Sec. 12.. 500 
Center N. W. qr. 8. E. qr. Sec. 12.. ae 


Mid. E. line N. KE. qr. Sec. 27...... 320| Mid. W. line N. W. qr. Sec. 29... 815 
Stream, N. W. qr. oe 27 .....--. 290] Center. E. qr. Sec. 30 2... eee eee 490 
Mid. E. hf, Sec. 29......- .. 810] Center N. E. qr. N. E. qr. Sec.31... 390 
Mid. S. line Sec. 29. .. 315 Center S. E. qr. Sec. 31... «. 0.6. 255 
Center Sec, 382.....- 290! Center E. line 8. E. qr. Sec. 31..... 265 
Mid. 8. line Sec. 32. BY vent 8. hE See, 82. ccc eeecee. a 
enter Sec. 33...... 33 MTU Gs Nia cies pectoris goes de See RO 340 
Mid W. hf, Sec. 33 300} Mid. EB. linc 8. E. qr. Sec. 32...... 375 
Mid. ‘N. hf. Sec. 33. 340| Mid. W. hf. Sec. 83.............6 385 
Mid. 8. hf. Sec. 33..... 340| Mid. E. hf. See. 33.............0-- 505 
Center N. W. qr. ee 36. 305 | Mid. E. line Sec. 83..........6..- 400 
Roxbary. T.9,R.7E Center 8. E. qr. Sec. 34........... 380 
8. W. cor. See. 3. Mid. E. line Sec. 86.....0..-...06. 600 
8. W. cor. Sec. 4....... Dane. T.9, R. 8 E. 

Bluff near center Sec. 5. Mid. 8. line 8. W. qr. Sec. 2....... 320 
Center 8. E. qr. Sec. 5.. Mid. W. line, Be Qe Vi gene gees 875 
Road crossing, mid. 8. | N. W. cor. Sec. 2......cc cece eee 300 
BC. ONG £46-64 ot Se SES G HY eES alias Center N. hf Sec. 4 ...........0.. 280 
Center N. E. qr. 8. E. qr. Sec. 6 i AMUC Woe. cirite sn, osc sg 6 Mes eg ies 500 
Mid. E. line Sec. 7.....--..-  «- id. W. line N. ae qr Sec. 4..... 520 
Mid. 8. line Sec. 7 Mid. E. line Sec. 7........ 2-408. 355 
Mid. 8. line 8. E. qr. Sec. 7. S. By cordbecs fects < eeen ope ass 410 
Mid. S. line S. E. qr. N. E qr. Sec.7 300} Cross roads, N.W. qr. 8. E. qr. Sec. 7, re 

Center 8. E. qr. N. W. qr. Beat 8... 450}. Genter §. W. gr: See; Teces 2s ves 
S. E. cor. Sec. 8.0.0.0... 00 . 820 ip mile Niscsniedewacaesea yeas 5009 
N.E. qr. 8. E. qr. Sec. 9 350 id. 8. line Sec. 7... 540 
S. W. cor. Sec. 10.... 2.0... . 840] Center Sec. 9...... . 880 
Forks of road, 8. E. qr. Sec. 10..... 830) Center Sec. 11..-... .. 420 
Mid. E. line 8. E. qr. Sec. 10.....- 305 | §. HE. cor, See. 11 ........ - 610 
S. line 8. E. qr. 8. W. qr. Sec. 10.. 340] Center N. HE. qr. Sec. 12.. . 400 
Mid. E. line Sec. 12...... » 600 


Dane Station, Sec. 13.. 
Mid. W. line Sec. 15... 


8. W. cor. Sec. 15..-.... : 550 


Center 8. W. qr. Sec. 17...... 
Mid. 8. line 8. W. qr. Sec. 17. 
Center Sec. 19....... 


Mid. E. line Sec. 12 Center Sec. 20....... . 450 
8. W. cor. Sec. 12. OM ess Mid. 8. line Sec. 20 ... - 500 
1; He COr SOC. 12 scameceials vee eet y.< 8. E. cor. Sec. 20............ - 560 
Mid. N. line N. W. a, ae He scene 430} Mid. 8. line 8, W. qr. Sec. 23. « 445 
Mid. 8. hf. Sec. 13.. - 870} Mid. 8. line 8. E. qr.Sec. 23. . 560 
Mid. W. hf. Sec. 13.. 380 | Mid. W. line Sec. 27....... . 560 
Mid. 8. line Sec. 13.. - 400] Center N. W. qr. Sec. 80....... . 590 
Center N. E. qr. Sec. 14. ... 271| Mid. W. line 8. W. qr. Sec. 31 .... 560 
Mid. 58. line See. 16.......... --. 270] Center 8. KE. qr. Sec. 83........ .. 480 
Mid. 8. line 8. W. qr. Sec. 16...... 270] Vienna. T. 9, R. 9 E.— 

Mid. 8. line 8. E. ae Sec. 17.. . 255| Mid. W.hf. Sec. 7.......0e005 .- 540 
S. W. cor. Sec. 17 .........-. - 255} Mid. W. line Sec. 7.... ......000, 500 
Mid. FE. line N. th qr. Sec. 19. 215| Mid. EB. ht. Sec. 7.......... ce eee ee 530 
Mid. N. hf. 8. hf. Sec. 20..... 205] Mid. W. hf. Sec. 8..............0. 470 
Mid. 8. line 8. W. qr. Sec. 21. .-. 875] Center Soe. 8...........0 08 pies Sib OG 500 
Mid. E. line See. 22........ ..-. 805] Mid. S. hf, Sec. 8..............006 440 
Mid. N. W. ar. Sec. 23 . - 805) 8, W. cor, Sec, 15... 6... eee 480 
Mid. E. line N. E. qr. See. 23. 410| Knob, 8. hf. Sce. 20........0.06-., 520 
Mid. N. line N. W. qr. See. 24 425] Mid. in line Sec. 21...... sss. se 490 
Mid. E. line Sec, 24 530 | Mid. W. line Sec. 27... ......08.. 540 
Mid. E. line Sec. 25 500 | Windsor. T. 9, R. 10 E. 

S. E. cor. Sec. 25.. - 550] Mid. S. line 8S. W. qr. Sec. 1....... 416 
8. W. cor. Sec. 25 . 390| Mid. 5. line 8. E. qr. Sec. 2........ 426 
Aldens Corner, Sec. Deine 865} Mid. 8. line See. 2........ aes 426 
Mid. W. line 8. W. qr. Sec. 27 - 805 a We, CON sy BOCs Dien gd aia s aiaees fetis sed 416 
Mid. W. line, Sec. 28.............. 290} Mid. 8. line, 8. hie qr. Sec. 8....... 396 
Mid. W. line N. W. qr. Sec, 28.... 280] Mid. S. line S. . qr. Sec. 4.......4 436 


SURFACE RELIEFS. 


BaROMETRICAL ALTITUDES — continued. 


Windsor. T. 9, R. 10 E.— (con.) 


Mid. S. line Sec. 4.............08. 416 
Center N. W. qr. Sec. 10....... .. 406 
Center N. W. qr. 8. E. qr. Sec. 10.. 396 
8. W. corner Sec. 10............05 376 
Mid. E. hf. Sec. 11..-.......0.0008 411 
Mid. 8. line See. 11............... 416 
SE, cor, See: Wiss scien cate casos 416 
Center N. W. qr. Sec. 18.......... 396 
Mid. W. line S. W. qr. Sec. 13..... 416 
Quarry, 8. E. qr. Sec. 14.......... 466 
Forks of road, 8. E. cor. Sec. 14.... 426 
Ne We-gt: See. 16: 55 sicsccssecd nce 876 
Mid. W. line N. W. qr. Sec. 16.... 386 
S. W. cor. Sec. 16..... gabe Beee pradesh 386 


Mid. W. line N. W. ar. Sec. 21.... 401 
Mid. W. line 8. W. qr. Sec. 21..... 405 


Mid. E. line Sec. 28...........00.- 416 
S. E.. Cots, S66): 28.. sac snacie sna ae 376 
Mid. W. line Sec. 25.............. 396 
S. W Cor. S86. 25 os eacaeowe tacos 386 
Mid. S. linc 8. E. qr. Sec. 25....... 346 
Mid. N. line Sec. 25 ......... 00 ee 356 
8. E. cor. Sec. 25.2... cee eee eee 356 
Mid. 8. line Sec. 26............... 306 
Mid. 8. line 8. E. qr. Sec. 27....... 336 
Mid. W. hf. Sec. 27..........0eeee 386 
Center N. W. qr. Sec. 28.........- 396 
Mid. E. hf. Sec. 28........ 2.00 411 
Mid. W. line Sec, 28.............. 366 
Conler S66: 29 onic: sx 5.5 eles ai 326 
Forks of road, N. W. qr. Sec. 34.... 311 
Center N. W. qr. Sec. 35.......... 336 
Bristol. T.9, R. 11 E. 

Mid. S. line 8. W. qr. Sec. 1....... 366 
S. W. cor. Sec. 1... eee eee eee ee 346 
Mid. 8. line 8. E. qr. Sec. 2........ 376 
Mid. S. line Sec. 3............0008- 376° 
Mid. W. line Sec. 3..........-6-.. 356 
Mid. 8. line Sec. 4..............26- 376 
Mid. EK. hf. Sec. 5 ........... 0000. 371 
Mid. S. line See.5...... ee cece eee 366 
Mid. 8. line 8. W. qr. Sec. 5...... 366 
Mid. §. line S. E. qr. Sec. 6 ....... 386 
Mid. E. hf. Sec. 7 .........-00005- 366 
Mid. 8. line S. E. qr. Sec. 7-......- 356 
N. W. cor. Sec. 9 oe. cece eee eee 366 
Center 8. E. qr. Sec. 9.......0000- 376 
Center N. E. gr. Sec. 9.....-...++- 366 
Mid. 8. line 8. W. gr. S. W. qr. 

SOC 10 sce ne io ees oe xe eee 376 
Mid. E. line Sec. 10..........++-.. 376 
Mid. E. line N. E. qr. Sec. 11...... 376 
8. Ev cor, Seé. 12 e.scdsaseriseveees 366 
Center Sec. 13..........2eeeeeeeee 371 
Mid. E. hf. Soc. 16 ........-.. 000 371 
Mid. E. hf. Sec. 17 «0... -- eee eee 416 
Mid. 8. line See. 17 .........-.--- 406 
Mad. S. line S. E. gr. Sec. 18..-.... 386 
N. W. cor. Sec. 20 0... 2. cece ee aee 396 
Center N. E. qr. Scc. 20 .......--- 381 
S. W. cor. Sec. 20... .ccesvccrcnuce 406 
4 mile south ......-- ids wicigatene, 406 
Mid. E. line §. E. qr. Sec. 21 . 366 


S. E. cor. Sec. 21......6- 066 


Bristol. T. 9, R. 11 E.— (con.) 
Mid. 8. hf. Sec. 22.......0.0006.. 


8. W. cor. Sec. 25 ..........0008 
Center Sec. 26........ .....0 eee 
Mid. W. hf. Sec. 26 ............ 
Mid. W. line Sec 26 ........... 
N. W. cor. Sec. 27...........04, 
Bu W.. Cor. Sees, OT sides Sasieareein sats 
Mid. E. hf. Sec. 29 ...........0. 
Mid. 8. line S. W. qr. Sec. 29 ... 
8. W. cor. See. 29.0... 0... eee 
8. W. cor. Sec. 30....... ..0 005 
Mid. E. line N. E. yr. See. 31.... 
S. E. cor. Sec. 81 0... ... 0. ee eee 
Mid. E. hf. Sec, 82 ............. 
8. E. cor, Sec. 84........8 vgs tek 
Mid. E. line Sec. 34 ............ 
N. W. cor. Sec. 85..........005 

Mid. F. line Sec. 35 ............ 
York. T.9, R. 12E. 
Mid. W. hne S. W. qr. See. 1... 
Mid. 8. line 8. W. qr. Sec. 1.2 .. 
8S. W. cor. Sec. 1... ee. e eee 


S. W. cor. Sce.'4 .. 0. cee eee 
Mid. W. line 8. W. qr. Sec. 4... 
Center Sec. 5... ... sec ee cece 


Center Sec. 7.......65 cece sees 


Mid. 8. line 8. E. qr. Sec. 8 ..... 
S. E. cor. Sec. 9.. 1... ce eee eee 


Mid. N. line Sec. 11.........-.. 
Mid. E. line See. 11 ............ 
Mid. 8. line S. E. qr. Sec. 12..... 
S. E. cor. Sec. 12........ ec a eee 
B. HecGor; Secs, [Bead os eaivaeiaue ae 
8. W. cor. Sec, 15.0.2... eee eee 
Mid. W. line Sec. 16............ 
Center Sec. 17......- .eeeeee oe 
IN. BCors Sets 19) sescan wsercauseers 
Center See. 19.... 6... eee eee eee 
SE: cor: See: 200225 sso sae 
Mid. E. line N. E. qr. Sec. 21.... 
S. E. cor. Sec. 21........2..0088 
Mid. 8. line Sec. 21............. 
Center Sec. 22..... 0... 0. eee eee 
Mid. S. line Sec. 22...........-. 
Mid. S. line 8. E. qr. Sec. 23..... 
S. E. cor. Sec. 24......002.008 © 
S. E. cor. Sec. 25 ......5.66. see 
Mid. S. line See. 25%... 0... ee eee 
Mid. N. line Sec. 26 ............ 


-. 376 


441 


-. 360 


-. 320 


GEOLOGY OF CENTRAL WISCONSIN. 


BAROMETRICAL ALTITUDES — continued. 


449 

York. T. 9, R. 12 E.— (con.) 
S. W. cor. Sec. 26 «22... eee ewes 355 
Mid. S. line Sec. 26.........-2.06- 375 
Mid. W. line Sec. 27......... .60- 390 
Mid. E. line Sec. 34 ......-..-.55. 355 
8..E. Cor Se. 84. 0000 csc ceeecaese 325 
Mid. E. line Sec. 36 ........- - 26. 330 


West Point. T. 10, R. 7 E. 
Gibraltar Blutt, Mid. E. line Sec. 15 635 
Marsh at foot of same, E. hf. Sec. 13 230 
Cemetery, 8. KE. qr. 8. E. qr. Sec. 14 370 


Mid. §. line 8. E. qr. See. 15 270 
8. W. cor. Sec. 14.........- .. 290 
Mid. 8. line Sec. 15.............5- 280 
8. line 8. E. gr. Sec. 16 ....---2 6 290 
Mid. 8. line Sec. 16..............- 280 
Ge in road, N. line N. E. qr. Sec. “i 
ose as a aie ee ee ee ee ee 9) 
Top of limestone bluff, N. E. qr. 

DOC Osa acco cmtgoa garhing va gechs 485 
De He Or, Se OL cae sie eeaisne 320 
Mid. §. line 8. E. qr. sec. 22....... 280 
Mid. E. line Sec. 22 ............-. 325 
Mid. S,. Jie sS6e;, Bab a ards ne ceiesaiece 420 
Center 8. E. qr. Sec, 25..........4. 400 
Mid...H, Wt. Bee. 27.3 ccc s ees aed 270 
Center 5. E. qr. Sec, 27 ...... eee 310 
B.. EB. Cor, See. Ql cesccee sees eee 275 
Center 8. W. qr. Sec. 27.........6- 310 
Mid. 8. line $. W. qr. S. W. qr. 

BEG WT ens Maiouaite tage gears dee eens 340 
Mid. E. line Sec. 28........ ....0- 330 
Be. Wee COrt SOG. 2B cca sats ctateathcschtes 290 
Mid. §. line 8. W. qr. Sec. 29 ..... 280 
Road, 8. EK. qr. Sec. 31............ 290 
Mid. W. ht. N. E. qr. Sec. 33 ..... 370 
Crossroads, N. ht. Sec. 36.......... 345 

Lodi (and West Point in part). T. 10, 
R. 8 E. 
Bluff-top, 8. W. qr. Sec. 7........ 520 
Road-corners, N. W. qr. Sec. 14... 330 
Mid. 8. line 8. W. qr. Sec. 14.....- 420 
Mid. N. hf. Sec. 14........ .. 415 
Center N. W. qr. Sec. 15...... .. 840 
Center N. W. qr. Sec. 16.. 0.22... 315 
Mid. E. line Sec. 19..........2.... 310 
Mid. W. ht. Sec, 20 .....-......05 250 
1g mile 8. of Cent. of Sec. 20........ 240 
Bi W. e:COrt SSC: 20 casisage ewisiacsemuecete 440 
Center N. W. qr. Sec. 23.......... 360 
Mid. i. line N. E. qr. Sec. 23...... 460 
Mid. 8. line 8. W. qr. Sec. 28...... 340 
Blutf-top, 8. E. qr. Sec. 23......... 560 
Bluff-top, N. W. qr. Sec. 24....... 560 
Center Sec. 26 ......-..- eee ee eee 250 
Center 8. E. qr. Sec. 27.......... 330 
Center 8. W. qr. Sec. 28........... 470 
Mid. W. line 8. W. qr. Sec. 28.... 420 
Mid. W. line Sec, 29..... D aepactepdis 360 
Bloff-top, mid. N. hf. See. 31...... 475 
Mid. FE. line Sec. 31.............-. 350 
Mid. E. line See. 32... .....-.44.. 380 


Arlington. T. 10, R.8 E. ; 
Creek crossing, N. E. qr. Sec. 1.... 300 
Eluff-top, 8. E. cor. Sec. 2......... 445 


Arlington. T. 10, T. 8 E.— (con.) 


Si Wee Cor Bees secs sig arsenite sesiers wd 380 
Center See. Bee gaa wisest ce 305 
Creek crossing, 8. E. qr. Sec. 3..... 270 
Mid. 8. line 8S. W. qr. Sec. 4....... 375 
S. We COR: SOC sic ose weieesre'p saieahy a 355 
Ge Wi COR? eG bi osieine Giga eau 870 
Mid. W. line Sec. 5...........0005 340 
S. line 8. W. qr. Sec. 7 ....-.-.05- 525 
8. He COn: S06. Tessas. sx edepenas 425 
§. Ee cot. Sec: Be unceeeeescseseees 465 
Mid. FE. line Sec. 8 ........- heiepatae 440 
Mid. E. line See. 10..........00 0 520 
S. Ex cor, S66. 10. 22. cenccerccenes 480 
Mid. N. line N. W. qr. Sec. 13 .... 440 
Mid. 8. line 8. E. qr. Sec. 18 ...... 460 
Axlington station, Sec. 13 ......... 460 
8. W.. cor, Sec. 14sec ccnccceesoees 470 
8. W. cor. Sec. 15.2.2... 2. eee eee 500 
Mid. S. line See. 16.............-. 460 
S. W. cor. Sec. 16..........02006- 440 
S. W. cor. Sec. 17.2... eee eee eee 490 
Mid. W. line Sec. 17...... ... ... 460 
Center Sec. 19...-.-....0-. ee eeees 540 
8. EB. cor. Sec. 19. ..ccetccusecees 460 
Knob, 8. line 8. E. qr. Sec. 21..... 525 
Mid. E. line 8. E. qr. Sec. 21...... 500 
Bluff-top, 8. W. qr. Sec. 27.....-.- 520 
Bluff-top, N. W. qr. See. 28....... 525 
Bluff-top, W. line 8S. W. qr. Sec. 28. 520 
Mid. W. line See. 28.............- 420 
S. W.. cor. See. 09). ces ccda wees 480 
Bluft-top, N. E. qr. Sec. 34... .... 520 
Columbus. T. 10, R. 12 E. 
Mid. 8. line Sec. 7......--..-.000 300 
Stream, 8. line 8. E. qr. Sec. 8....-. 275 
Mid. N. line Sec. 9.............55. 310 
Ny iis COPS SOGi:9 a ccsassarmvedeninouesd wales 885 
N. E. cor. See. 16........... 00000 285 
N. W. cor. Sec. 17...-.....0000 ee 295 
Mid. N. line Sec. 17............04. 285 
W. line N. W. qr. Sec. 19......... 365 
Mid. E. line Sec. 20.........-00055 825 
N. E. cor. Sec. 20...........0.008- 305 
Mid. E. hf. Sec. 21..........0.00-- 285 
Stream crossing, N. W. qr. Sec. 28. 300 
Mid. N. hf. See. 382.........6 tee. 895 
Mid. E. hf. Sec. 33........... 0.006 395 


Dekorra. T.11N., R. 38 E. 


Mid. E. hf. Sec. 23 
Mid. E. line See. 23.... 


Dekorra. T. 11, R. 9 E. 


Mid. W. line 8. W. qr. Sec. 11 .... 280 


Cross-roads, W. hf. Sec. 14........ 335 
Mid. W. line Svc, 17......2.. 000 340 
S. W. cor. Sec. 17... 0.2... ee ee eee 370 
8. W. cor. Sec. 20 ....... ee ee eee 220 
Mid. 8. line S. E. qr. Sec. 16....... 880 
Cemetery, W. ht. Sec. 23.......... 810 
Mid. W. hf. Sec. 28............4.4. 320 
Stream crossing, N. E. qr. Sec. 30.. 220 
Mid. E. line N. E. qr. Sec. 80...... 240 
Mid. 8. hf. See. 83....... 0.0 eee ee 270 
Poynette depot.......... cee eee, 264 


SURFACE RELIEFS. 443 


BAROMETRICAL ALTITUDES — continued. 


Lowville. T.11N., R. 10 E. Fountain Prairie. T. 11, R. 12 E.—(con.) 
8. E. cor, See. Le...s eee eee eee eee 360; Mid. S. hf. of N. hf. Sec. 7........ 370 
Mid. 8. line 8. W. qr. Sec. 2....... 330 | Mid. W. line 8. W. qr. Sec. 8..... 370 
Mid. 8. line S. W. qr. Sec. 3....... 320} Mid. 8. line 8. W. qr. Sec. 8 ...... 360 
Bluff 4th mile north.............. 425 | Mid. 8. line 8. W. qr. Sec. 9 ...... 350 
Ravine, 8. W. cor. Sec. 4.......... 260} Mid 8. line, Sec. 9................ 330 
Se Ws Cor: See. 5 aces veavece #sc0hs 320] Stream, S. line 8. W. qr. Sec. 10... 300 
Mid. S. line 8. W. qr. See. 6....... 800} Mid. 8. line Sec. 10.. ..... 0.0... 330 
Mid. BE. hf. Sec. 8.00.0... eee eee 280] Mid. W. hf. Sec. 11............... 360 
ae 8. E. qr. Sec. 9.......... 400 | Stream crossing, N. hf. Sec. 14 .... 320 
Mid. 8. line 8. W. qr. Sec. 9....... 330 | Center N. E. gr. Sec. 13 .......... 314 
Mid. 8. line Sec. 10............... 350] Mid. W. line Sec. 28.............. 350 
8. W. cor. Sec. 11... 2... ee ee eee 350} Mid. E. hf. Sec. 29 ............... 360 
Bu B. cor. See, 1 aie os aciewecerecuce ne 370 | Stream, 8. E. cor. Sec. 30......... 295 
8. E. COE SOC TY. cue edinseteeiesnsis ness 370 mile south....... .........24. 840 
Mid. W. line Sec. 13........-...-. 350 S. E. cor. Sec. 81........0.. 0 eee 310 
Mid. S. W. qr. Sec. 17......-...-. 310] Mid. 8. line 8. E. qr. Sec. 82...... 335 
Mid. W. hf. Sec. 18............6-- 290] Mid. 8. line Sec. 33 ........... 0. 295 
Mid. E. line Sec. 19 ........ ..-.. 340] Mid. S. line Sec. 34........... 00. 280 
Mid. E. hf. See. 20................ 360] 8. E. corner Sec. 36 ..-.. 0. ee eee 252 
Mid. 8. line 8. E. qr. Sec. 20....... 420 | Caledonia. T. 11, R. 8 E. 

Knob, S. line S. E. qr. Sec. 23..... 460 | Mid. N. W. qr. Sec. 3 ............ 360 
S. E. cor. Sec. 23...-.. 0.00. ee eee 400} Mid. 8. line Sec. 7............... 480 
Mid. 8. line Sec. 24.............4. 400} Mid. 8. ht. Sec. 8............. 510 
Mid. W. line N. W. qr. Sec. 28.... 400] Center S. E. qr. Sec. 8........ 395 
Cent. N. E. qr. Sec. 29..... BA dasa 420| Center 8. E. qr. See. 9............ 520 
Bluff top, 8. E. qr. Sec. 31 ........ 410| Mid.S. line Sec 16............... 485 
Mid. E. line Sec. 81..........-..-- 350] Mid. W. line, Sec. i6............. 885 
Mid. E. hf. Sec. 32 ..............- 400} Mid. W. line N. W. qr. Sec. 21.... 330 

Otsego. T. 11, R. 11 E. Mid. W. line Sec. 21.............. 875 
Mid. W. hf. Sec. 1 ......-....000. 345 | Caledonia. T. 12, R.8 E. i 
Mid. W. line Sec. 1..........-.... 875 | Church, N.W.qr.N.W.qr.Sec.21. 280 
Conta Ses Qa weciciecs geea- dewartes 345 1g mile south ....... ...2 esse eee 420 
Mid. E. bf. Sec. 3.............08% 330] Mid. 8. line 8. W. qr. Sec. 22...... 500 
Mid. W. line Sec. 8............--- 350] Mid. N. hf. Sec. 25............... 205 
Cent: Sees 4 sinus sseaa yes geese ess 3875 | Cent. N. W. qr. Sec. 25........... 340 
Cent. Sec. 5... ..-- 840] Road, W. line N. W. qr. Sec. 25... 505 
Mid. W. line Sec. 5 . 360] Mid. E. hf. Sec. 26..............0. 560 
Mid. W. iine Sec. 7 .. 420] Center Sec. 26.......-. 2.000 cece ee 560 
Mid. E. line Sec. 11 .. 865] S. E. qr. N. E. qr. Sec. 26.. ...... 620 
Doylestown, Sec. 12 .- 860] Center Sec. 27 ....2.. cee ee ee eee 510 
8. W. cor. See. 15.. . .-.+. 880] Stream crossing, 8. W. qr. Sec. 27. 480 
S. W. cor. Sec. 16......... 22 eee ee 390| Mid. 8. line 8. KE. qr. Sec. 27 ...... 610 
Mid. S. line Sec. 17. .. 365] Center 8. E. qr. Sec. 28 ........... 470 
&. W. cor. Sec. 17.. . 880] S. W. cor. Sec. 28......-0.66- : 


Mid. S. line Sec. 19. .. 340] Mid.S. lineSec.29 ..... 
8. E. cor. Sec. 19... .. 850] 8. W. cor. Sec. 29. .- Ae 
Mid. S. line Sec. 20..... .. 899] Mid. N. hf. Sec. 29...-.......... : 

Cent. 8. W. qr. Sec. .. 860} Mid. W. line N, W. qr. Sec. 29. .. 505 


Mid. N. hf. Sec. 22... . 865) Center N. W. a Sec. 80.......... 505 
Otsego, Sec. 22....+.--.-+5-- .. 855] Mid. W. line N. W. qr. Sec, 30.... 540 
Stream, E. line N. E. qr. Sec. 23... 345] Bluff top, 8. E. qr. Sec. 34........- 760 
Mid. E. line Sec. 23 ........ .. 865] Mid. S. line 8. W.qr. Sec. 35...... 310 
Mid. E. line S. E. qr. Sec. 23 ‘ Caledonia. T. 12, R. 9 E. 
Mid. E. bf. Sec. 32........-. oy Bridge, Sec. 7... ..+-seseeeee eens 220 
Mid. E. line Sec. 32.........+--6+- 35 | Wyocena. T. 12, R.10E. 
Le6t, 650, ep kexnecatemaeneees s i ailroad, W. line Sec. 1........5.. 935 
Cent: See. 84s. cnics-nait ardenatnin eau 365] Mid. W. line Sec. 10.. 2 
Mid. W. hf. Sec. 35 ....-..-- eee 855] §. W. cor. Sec. 10.... 
Mid. E. line Sec. 35 .........-00-- 890} Center Sec. 12....... 

Fountain Prairie. T. 11, R. 12 E. Stream, S. line Sec. 12 
Marsh, W. hf. Sec. 2....----.++55 312 Center Sec. TB vcacucenss 
Cent. N. W. qr. Sec. 2.....-...++- 370| Mid. W. line Sec, 18.. 
Mid. S. line S. W. qr. See. 6.....-- 400} Stream, center Sec. 14 


Mid. 8. line See. 6.0... ee eee ences 840! Center Sec. 15..........e eee e eee 


d44 


GEOLOGY OF CENTRAL WISCONSIN. 


BAROMETRICAL ALTITUDES — continued. 


Wyocena._ T. 12, R. 10 E. —(con.) 


Mid. W. line Sec. 15.....-- 6. ee ees 93) 

Wyocena depot....-.s+-seeereeee 240 
Center Sec. 23 occ cece es cee ee eee 280 
Mid. W. line Sec. 28...-..++++5 ++ 310 
Mid. E. bf. Sec. 29... 6. eee ee eee 275 
S. W. cor. Sec. 29.6.6 ce eee eee eee 320 
Mid. E. hf. Sec. 381 ......6-- sees 280 
Mid. W. hf, Sec. 31... eee e eee 235 
Mid. W. line N. a tee 36.... 290 

Springvale. T. 12, R. J. 
[One fourth mile N. of cent. of Sec. 1 285 
Mid. E. line Sec. 1... wees e eee 240 
Mid. W. line N. W. qr. Sec. 2..--- 280 
Mid. N. hf. Sec. 3.... -. eee eee eee 290 
Mid. W. line Sec. 4...-.....--00005 235 
Railroad, W. line Sec. 5 ....--...- 240 
S. W. cor. SéC. Dees crecceeeeee ees 230 
Mid. E. hf. Sec. 7.2.2... .. cece eee 235 
Center Sec. T scsaccceceetcetane 230 
Center Sec. 15... ... eee cece were ee 360 
Mid. W. line Sec. 15..........-0-- 360 
Bluff top, N. E. qr. Sec. 16 ....... 370 
Mid. E. hf. Sec. 17.22... sees eee ee 300 
Stream crossing, N. hf. Sec. 18 .... 222 
Stream crossing, N. hf. Sec. 22... 266 
Mid. S. hf. Sec. 22..... stivbstdaitave tals 320 
Mid. N. hf. Sec. 27.2.2... eee eee ee 270 
Road, W. line N. W. qr. Sec. 27... 260 
Mid. §. line S. E. qr. Sec. 28...... 280 
Mid. §S. line Sec. 28..-....00. eens 300 
S. W. cor. Sec. 28.......0. ee eee 290 
Mid. S. hf. Sec. 29......+.. eee ene 250 
8. W.cor. Sec. 29... cece eee eee 300 
Mid. 8. line 8. W. qr. Sec. 29...... 280 
Courtland. T. 12, R. 12 E. 

Randolph depot, Sec. 1 ........-.. 378 
S. E. cor, Sec. Lee. eee eee eee eee 360 
Mid. N. hf. See,.2.... ....e cece 365 
Center Sec, 2. sisins sone sveie nance gincnis 355 
Mid. W. line Sec. 2.........000... 375 
Mid. W. hf. See. 3... 6. eee ee eee 355 


Mid. N. line N. W. qr. See. 3... 


Mid. N. line N. E. qr. Sec. 4...... 355 
Mid. N, line N. W. qr. Sec. 4..... 825 
Mid. 8. line 8. W. qr. Sec. 5..... . 395 
Cambria depot, Sec. 6..........6. 284 
Mid. W. hf. Sec. 8... 02. 2. eee. 380 
BS. W ar. See, Bes sae sccssee dines 390 
Center N. W. qr. Sec. 11.......... 402 
Mid. Wife, See. Ve wicqsua cease 390 
S: Woicor, Sec, lacetces kee esa es 3883 
S. Wi Cor. See: [Bsc eceesse eee ge se 377 
Mid. S. line Sec. 14............ 08 364 
Mid. W. line 8. W. qr. Sec. 14.... 880 
Mid. E. line N. E. qr. Sec. 13...... 367 
Mid. W. hf. Sec. 17...........0006 410 
Center Sec. 19.........ceeeree vee 430 
Mid. 8. hf. Sec. 19...........0.0.. 350 
Mid. W. hf. Sec. 20............... 390 
Mid. N. hf. Sec. 23.............065 360 
Stream crossing, N. hf. Sec. 26..... 335 
Mid... bt. See, 265,25 sesseee: wads 357 
Mid. N. hf. Sec. 30.... ........... 400 
Mid. 8. line Sec. 80..........0.08- 360 


Courtland. T. 12, R. 12 E.— (con.) 


Mid. 8. hf. Sec. 31............008. 360 

Mid. N. hf. Sec. 85 0... 0 eee ee eee 869 

Mid. S. line Sec. 385....-...ceeseee 370 
Lewiston. T. 13, R. 7 E. 

Lewiston depot, Sec. 26............ 231 


Lewiston. T. 13, R.8 E. 


Mid. N. hf of 8. W. qr. Sec. 14..... 250 
Center 8. W. qr. Sec. 23........... 220 
Mid. W. line Sec. 25...........05. 240 
Mid. N. hf. Sec. 386...... ... 20. 230 
Center 8. E. qr. Sec. 86............ 245 
Fort Winnebago. T. 13, R. 9 E. 
Mid. W. hf. Sec. 16.............8 230 
Mid. W. line 8. W. qr. Sec. 16..... 260 
S. W. cor. Sec. 16.............4.. 280 
Center 8. E. qr. Sec. 19 ........... 300 
Mid. 8. line 8. E. qr. Nec. 19...... 250 
Mid. 8. line Sec. 20....... ieiesss ae 260 
Mid. W. line Sec. 21.............. 240 
Cougliin’s quarry, E. hf. Sec. 20... 350 
Center N. E. qr. Sec. 80.......... 240 
Mid. E. hf Sec. 81..............0. 390 
Mid. N. hf. Sec. 86.......-.....06. 265 
Bluff-top, N. W. gr. Sec. 36........ 390 
Marcellon. T. 13, R. 10 E. 
Ne Hs cons SeC:: Ls aaiesar sa veel *. 260 
Mid. N. line N. E. qr. Sec. 1....... 320 
Ns Ws cor: See. Vs sos icweesasrea's ave 260 
Mid. W. line Sec. 1............... 300 
Mid. W. line N. W. qr. Sec. 12..... 820 
Mid. 8. line N. W. qr. Sec. 12..... 290 
Mid. W. line N. W. yr. Sec. 13.... 270 
Center 8. E. qr. N. E. qr. See. 14... 285 
Center N. W. qr. S. E. qr. Sec. 14.. 295 
Mid. 8. hf. 8. W. qr. See. 14....... 290 
4 mile E. 8. W. cor. Sec. 14...... 270 
Center Sec. 16......... ec ce ee eeeee 3870 
Mid. 8. hf. Sec. 16........... eee 340 
Mid. 8. line 8. E. qr. Sec. 16....... 350 
Mid. §. line Sec. 16......0........ 850 
Mid. E. line N. E. qr. Sec. Z1...... 355 
Mid. E. line Sec. 21............... 805 
Center 8. BE. qr. S. E. qr. Sec. 21.... 335 
Center 8. E. qr. N. E. qr. Sec. 22... 320 
B.. W.Cor See: 23) wee weagae avy 350 
Mid. 8. line 8. W. qr. Sec 23 ...... 360 
Mid. 8. line Sec. 23............... 350 
Mid. 8. line Sec. 24.............- 300 
Mid. 8. line 8. EB gr. Sec. 24....... 290 
Mid. EK. line N. W. qv. Sec. 25..... 350 
Center N. W_ qr. N. E. qr. Sec. 28. 260 
Scott. T. 13, R. 11 E. 
if mile E. N. W. cor. Sec. 2....... 390 
id. N. line Sec. 2.......... 000. 360 
Mid. .N. lf. Sec, Qiscsssseccev seca 360 
Mid. N. line N, E. qr. Sec. 3...... 300 
N. W.cor. Sec. 8. 0... cee. eee eee 280 
Mid. N. line N. W. qr. of N. E. qr. 
SoCs An mititine gees Week om aeecee 280 
Mad. N. line N. W. qr. Sec. 4...... 260 
Mid. N, line N. E. qr. Sec. 5....... 320 
‘ mile EK. N. W. cor. Sec. 5....... 260 
id. N. line N. E. qr. Sec. 6....... 280 
Mid. N. hf. of N. hf. Sec. 11...... 380 


SURFACE RELIEFS. 445 


BAROMETRICAL ALTITUDES — contiuued. 


Scott. T. 13, R. 11 E.— (con.) Banilolnh, T. 13, R. 12 E. —(con.) 
Mid. 8. line, Sec. 11 ............. 340} Mid. W. line N. W. qr. Sec. 31.... 350 
Mid. N. hf. Sec. 14..........6-005 885]} 8. W. cor. Sec. B1....... cece eee ee 240 
Mid. N. hf. 8. hf. Sec. 14........... 840] 8. E. cor. Sec. 81.2.0... . cece eee 260 
Mid. S. line Sec. 14........... 04. 320| Center 8. W. qr. N. W. qr. Sec. 32, 890 
Mid. N. line 8. E. gr. 8. W. qr. Sec. Mid. 8. hf. N. W. qr. Sec. 82...... 882 
vee eestes os sao aaesnenenws 870| 8. E. cor. Sec. 86 2.2... ee eee eee ee 360 
zs mi. north 8. E. cor. Sec. 19..... 230| Spring Green. T.8, R. 4 E. 
Mid. &. line Sec. 19........... 04. 270) Bluff, N. W. qr. Sec. 8, base ...... 144 
Mid. N. hf. N. hf. Sec. 23......... 290} Bluff, N. W. qr. Sec. 3, top ....... 374 
Mid. S. line Sec. 25..........0.08 370] Bluff, N. W. qr. Sec. 5, base ... 200 
4 mi. north center Sec. 26.......-. 380] Bluff, N. W. qr. Sec. 5, summit ... 465 
qs mi. south N. W. cor. Sec. 29.... 230] Spring Green depot, Sec. 7........ 144 
Mid. W. line Sec. 29.............. 240| Spring Green. T.9, R.4E, 
S. W. cor. Sec. 29 .....022 cece eee 825 Blutf top, N. E. qr. Sec. 28... .... 430 
Mid. E. line Sec. 81 ............6- 400) §. E. qr. N. W. qr. Sec. 30........ 460 
4 mi. north 8. E. cor. Sec. 31..... 375| Road, N. W. qr. Sec. 31.......... 360 
1 mi. east S. W. cor. Sec. 32......- 350} Bluff, 8. E. qr. Sec. 32............ 320 
SD con, Ree, Scr sc on eantucse's 440| Stream, 8. W. qc. N. W. gr. See. 34 140 
Mid. S. line S. E. qr. Sec. 33...... 380| Troy. T.8, R. 4 E. 
Mid. 8. line 8. W. qr. Sec. 34 ..... 275| Bluff baye, Sec. 1...............6- 170 
S. E. cor. Sec. 84...-... 0c cece eee 400| Bluff top, Sec. 1...............06. 420 
Mid. 8. line Sec. 35... eee ee es 420) IN. W.. cor. Sec. 2.5 sercecics sissaiees 130 
S. E. cor. Sec. 35... .0c. cee we eee 425| Troy. T. 9, R. 4 E. 
Mid. S. line Sec, 36...........0--- 420} Road, N. W. ur. Sec. 24 ........4. 185 
GiB. cor: Sec. 86.56 eerie wets tins 400| Blutf top, N. W. qr. Sec. 24....... 3875 
Randolph. T. 13, R. 12 E. Mid. N. hf. Sec, 25.......... 004. 270 
N. W. cor. Sec. 1.2... eee eee eee 415] Mid. W. hf. See. 25..........0.0. 440 
Center S. E. qr. Sec. L......eeeeee 320] Mid. W. line Sec. 25 ...........4. 270 
Mid. N. line Sec. 2....-------. 06 420| Stream ceoering, 8. W. qr. Sec. 35 . 134 
N. W. cor. Sec. 2...0.e eee eee eee 250| Bluff top, 8. W. qr. N. E. qr. Sec. 35, 870 
Mid. W. line Sec. 2 .......--0--5- 370| Troy. T. 9, R.5 E. 
Mid. N. hf. 8. hf. Sec. 5. .....---- 350} Mid. N. line Sec. 8.........-..06, 180 
Mid. 8. line Sec. 5 «6... eee eee wee 340| N. E. cor. Sec. 8............0006- 160 
Mid. W. line Sec. 6..........00008 320 Road, 8. W. qr. 8. W. qr. Sec. 11.. 830 
S. W. cor. Sec. 6....2..06 ce eeeee 850] Bluff base, N..W. gr. N. W. qr. Sec. 
Mid. S. line, Sec. 7......-.-00- eee 420 As Saree iakteee Cacao chet thee detrei: 210 
Mid. W. line 8. W. qr. Sec. 7 ...-- 320] Bloff top, N.W. gr. N.W. qr. Sec. 14, 500 
Mid. N. hf. Sec. 8...-......6 cee 350| Road, 8. E. qr. 8. W. qr. Sec. 17... 170 
Mid. S. line Sec. 8...........---- 360] Bluff top, 8. Ek. gr. 8. W. qr. Sec. 17, 250 
Mid. E. line Sec. 9 ........- 66-05 365] Center Sec. 17.......... 2. cee ee eee 170 
Mid. E. line Sec. 1].......--.2-.065 395 N. line N. W. qr. Sec. 19........ 170 
Center Sec. 12 .....2 cee erect ceee 395 N. W. cor. Sec. 24.......-. eee eee 370 
S. W. cor. Sec. 15.......- 2 seh ndieiaes 390 Mid. S. hf. 8. hf. See. 385......... 190 
Mid. W. line Sec. 15.. ..-..-.-00- 356| Bluff base, N. hf. Sec. 35.......... 190 
Mid. N. hf. N. hf. Sec. 16.......-- 356 | Bluff top, N. hf. Sec. 35. ......... 410 
. Mid. N. hf. S. hf. Sec. 16 ..... -.. 432 | Prairie du Sac. T. 9, R. 6 E. 
. Mid. S. line Sec. 16....... «eee 409 Sauk City, Sec. 12 ........ 2. eee 210 
. Center S. E. qr. Sec. 17......--+-++ 400| Bluff base, N. W. qr. Sec. 17. .... 180 
Center N. W. qr. Sec. 17...---.++- 865| Bluff top, N. W.qr. Sec.17. ...... 490 
Mid. W. line 8. W. qr. Sec. 18..... 880} Bluff base, 8. W. qr. Sec. 21....... 166 
| Mid. W. line N. W. ar. Sec. 19.... 400] Bluff top, 8. W. qr. Sec. 21........ 486 
Mid. N. hf N. hf. Sec. 20......... 400 | Prairie du Sac. ‘I’. 10, R. 6 E. 
Center 8S. W. qr. Sec. 20 ....- -.-- 400} Mid. KH, hf. Sec. 25.... 2.1... eee 250 
. Mid. E. line S. E. qr. Sec. 21...... 386| Center Sec. 26......60.-. ese eer ees 250 
Mid. N. hf. N. hf. Sec. 24 ........- 350] _ Mid. W. line Sec. 27.......+++.065 220 
Center 8. W. qr. 8. E. qr. Sec. 24.. 330) Franklin. T. 9, R. 9 E. 
Center N. E. qr. Sec. 25....-++..66 850] Mid. 8. line Sec. 2......--.--0000 195 
Mid. W. line Sec. 25....-. «+ sae Road, 8. E. qr. Sec. 9.....-- . eee 220 
Mid. W. line Sec. 27.......-+ ae Road, N. E. qr. Sec. 18......-.4-- 250 
Center Sec. 28... ..0+-seeeeeeeeeee : Road, 8. W. qr. Sec. 18......-.--. 320 
S. E. cor. Sec. 28....-. sees eee Road, N.. W. qr. Sec. 19....-..+-. 465 
Center 8. E. qr. N. W. qr. Sec. 29.. 360] _ Mid. W. hf. Sec. 19 ........--. eee 490 
N. W. cor. Sec. 80... -.. 2c eee ee ee 440| Franklin. T. 10, R.4 E. 


¥ mile N.S. W. cor. Sec. 30...... 400! Summit, KE. line Sec. 21........... 380 


‘ 


446 GEOLOGY OF CENTRAL WISCONSIN. f 


BAROMETRICAL ALTITUDES — continued. 


Frankliin. T. 10, R. 4 E. —(con.) Freedom. T. 11, 8. 5 E. — (con.) i 
Mid. S. line Sec. 29 ......- eee eee 950} S.dnf Sec. 28). caer were cnwsievene ee 700 
Honey Creek. TT. 10, R. 4 E. Near S. E. cor. Sec. 23............ 830 
Center See. Tossa ces see eee thie ee 530] Mid. E. line Sec. 26 ...... ....... 830 
Mid. N. line Sec. 1 ....-.----- +05 570 | Baraboo. T. 11, R. 6 E. 
Bluff-base, Sec. 12...-......-- eee 205 Baraboo depot, Sec. 2.......-..065 280 
Bluff-top, Sec. 12.......0 essere ee 480 | Mid. 8. line 8. E. qr. Sec. 11 ...... 325 
Bluff-top, N. W. qr. Sec. 18......- 300} Mid. E. hf. Sec. 23 ..-.-....-. see 635 
Bluff-top, N. E. qr. Sec. 14......-- 290] Railroad at Cliff House, Sec. 24.... 386 
Bluff-top, Sec. 35. ... 00 eee e eee ees 462| Bhluff-top, 8. E. qr. Sec. 24......... 805 
Center Sec. 36........ceeeceeeeeee 250] Bluff-base, 5. E. qr. Sec. 24....... 390 
Honey Creek. T. 10, R. 5 E. Cliff-top, mid. W. line Sec. 24 ..... 850 
S. E. qr. Sec, 2.02... ere ccet seers 610 | Baraboo. T. 12, R. 6 E. 
Goes 8, N. W. ar. Sec. 31 ..-++- 200} Mid. W. hf Sec. 25... 0 -...... eee 430 
Sumpter. T. 10, R.6E Mid. E. line Sec. 25............ 64 380 
Mid. 8. line ots 10 vss dase eae 240| 8S. W. qr. 8. E. qr. Sec. 27........ 420 
Center Sec. 15....... 0. eee e eee ees 250) S. W. qr. 8. E. qr. See. 28.6.2... 310 
Stream crossing, W. hf. Sec. 15.... 230] N. E. cor. Sec. 35 1.00.0... ee ee eee 400 
Bluff-top, W. hf. Sec. 15.......... 415| Mid. N. lne N. W. an aoe 36....- 370 
Sumpter. T. 11, R. 6 E. Greenfield. T. 11, R.7 
Mid. N. line Sec. 26.........+.44- 550/ Summit, 8. W. qr. Sec. - kha hoe a 
Road, N. E. qr. S. E. qr. Sec. 26... 575] Mid. Ww. line Sec. 1....-...-.--4-- 
Road, 8. KE. qr. 8. E. qr. Sec. 26... 625] Mid. W. line N. W. qr. Sec. 1 
Center N. W. qr. Sec. 27....-+.--- 600] Near Mid..S. hf Sec. 5 ..........4. 
Center ae Bde eesege Sasetstace ee 280] Center S. E. hf Sec. 5.1.2.0... eee 
. Road, N. E. qr. N. E. qr. Sec. 35.. 480] Road-forks, N. line N. W. qr. Sec. 7 270 
Mid. 8. line S. E. qr. Sec, 35...-.-. 320} Near center N. hf Sec. 14........ 740 
Morena: T. 11,8. 7E. Near center Sec. 15........000.006 850 
Ridge, 8. W. qr. 8. E. qr. Sec. 19.. 471} Near Mid. W. line Sec. 15 ........ 900 
Center N. W. qr. Sec. 25 .......-- 580! Road, 8. bt N. E. qr. Sec. 16 ...... 845 
Mid. N. line N. W. qr. Sec. 26 ..... 295| W. line Sec. 16 .....eceecceesecee 750 
8. hf. N. W. qr. Sec. 28.-......--. 280} 14 mile 8. center Sec. 16 ..-.....-- 600 
Mid. 8. E. qr. N. E. qr. Sec. 28.... 260] Mid. W. hi See. 17.........- 0.00 610 
Road, N. hf. 8. E. qr. Sec. 381 ....- 285 | Greenfield. ‘T. 12, R. 7 E. 
Mid. N. hf. Sec. 32...--... 6. ee eee 290} Quarry, center Sec. 25 .........066 410 
Under bridge, i E. qr. See. 32.... 270 DO:r0dS: N wnwsn. eicdneeh Aeeee ene 425 
Westfield. ‘I’. 11, R. 4, E. Road, N. line N. E. qr. Sec. 26 .... 215 
Mid. E. line Sec. 1...°.... A Ki 497| Blutt, top N. line N. E. qr. Sec. 26. 51S 
Center SeG. L sscrcsesceciesstes ss 500| Mid. W. line Sec.-27 ........ee 00s 825 
Mid. N. line Sec. 1 .....--- 21-2 eee 500 | Mid. W. line Sec. 29........-..5- 405 
De Wi COL: DOG: Qewzcurspexseane ss 530} Mid. E. hf Sec, 80 ...0.....--. 0s 475 
Blutt-to Ps center Sec. 3.1... ecw eee 471 Center Sec. 30 ..... eee eee eee eee 405 
Center Sec. 11.... 2.2.0.0... eee 610| Mid. L. ht Sec. 82 ..............6. 345 
Mid. 8. ine See: Ts cceveeaees seas 660 | Mid. W. hf Seo. *: Ds ccascetinia weats Sa 275 
Center N. W. qr. Sec. I1........-. 560 | Center Sec. 33.......... eee ee ee eee 270 
N. W. cor. Sec. 11 .....6. 2... 510} N. W. cor. Sec. 86......... cece eee 350 
Mad. S. hf. See. 12..........-..0. 627| N.E. cor. Sec. 36......-60.ee eee ee 365 
Se creue: E. ht. Sec, 18...... 477| Stream-crossing, N. W. qr. Sec. 36. 345 
W. bf. 8. W. a ee 18 S. W. cor. Sec. 86 1... wee ee ee eee 465 
Center Sec. IB... eee ee . 5380] Reedsburg. T. 12, R. 4 E. 
Center Sec. 14. 2.2... 20. ee eee : wae -crossing, 8. "line Sec. 1....... 285 
Logansville, Sec. 17 .........-.8- 5 d. 8. line Sec. 2.0... cece eee 320 
Center N. W. qr. Sec. 17 ......... 351 g W. COT SECs Daeconsewiererd> ais oie sue 330 
Center 8. W. qr. Sec. 17 .......... 361) Reedsburg depot, Sec. 10.......... 296 
Bluff, N. line Sec. 17............. 471) Maid. E. line Sec. 17 ........--.66- 320 
S. W. cor. Sec. 25.0... . eee scenes 540} E. hf 8S. E. qr. See, Wiiwswras seus 340 
Mid. 8. line Sec. 26... .....---0. 520) Mid.S8. line Sec. 20..........0.-6% 500 
Mid. KE. line N. W. qr. Sec. 29..... 401} Mid. W. line Sec. 22....... 0.0.00 451 
8. E. qr. 8. BE. qr. See. 35 6.0... 400 | Mid. N. line 8. E. qr. See, 25.2... » 8as 
Center 8. W. qr. Sec. 86.......... 580 | Center Sec. 25 0... ec ee eee eee ee 802 
Freedom. T. 11, R.5 E. Mid. 8. line Sec. 25............... 307 
Bridge, E. hf. Sec. 2.........-.08- 268) Mid. 8. line 8. W. qr. Sec. 26..... 280 
Bloom's Station, Sec. 2............ 280 | Mid. W. hf Sec. 29.......... 0.006 5AQ 
Mid. N. line N. W. qr. Sec. 5...... 437] Quarry, 8. W. qr. Sec. 29......... 530 
Mid. W. line Sec. 14.............. 340| 8S. EK. cor. Sec, 29....... Sia tense a 380 


RELATIONS OF THE TOPOGRAPHY TO THE. GEOLOGY. 447 


BaRoMEtRican ALTITUDES — continued. 


Reedsburg. T. 12, R. 4 E. —(con.) Juneau County — (con.) 
Center Sec. 30.........cccece eevee 580 T.17, R. 25. 
S W. cor. Sec. 80 ...... ccc cece eee 560 Target bluff, Sec. 28, GOP iitodie isease es 476 
Cross roads, N. hf Sec. 30 ...-..... 335 Target bluff, Sec. 28, base ........ 856 
id. W. line Sec. 80.............. 580 T. 18, R. 3 E. 
Mid. N. line N. W. qr. Sec. 31.... 500] Foot of bluff, Necedah ............ 340 
Creek crossing, Sec. 35 .......0.006 280} Top of bluff, Necedah ............ 510 
Mid. 8. hf Sec. 86 .............00. 467 T.18, R. 4 E. 
Mid. S. line Sec. 86.............0. 517)  Petenwell peak, Sec. 9, top ..... 530? 
Center Sec. 86.0.0... 2. cece eee e ee 460 | Adams County. 
Excelsior. T. 12, R.5 E. T. 14,R.6E. 
Mid. N, hf See. Qos ener senza: 290} §S. E. qr. Sec. 21, Eleph. back, top. 550 
Mid. 8. line S. W. qr. Sec. 3....... 325 | Wis. river hf. mile west, Sec. 21.... 240 
Mid. 8. line 8S. W. qr. Sec. 4...... 365 T. 17, R. 6E. 
S. W. cor. Sec. 5 oe... eee eee eee 320| Friendship mound, Sec. 6, top..... 750. 
Bluff top, Mid. KE. hf E. hf Sec. 5... 575| Bridge at foot, Sec. 6 ............ 440 
Center Sec. 28.............eee eee 900 T. 7. R. 7 E. 
Bluff top N. E. qr. N. W. qr. Sec. N. E. qr. Sec. 3. Pilot knob, base.. 540 
iL payee eee eave sisson ewuia aoe soe 007 | __N.E. qr. Sec. 3, Pilot knop, top... 705 
Ableman’s depot, Sec. 33.....,.... 297 | Marquette County 
Fairfield. T. 12, R. 7 E. T. 14, R. 8 E. 
Mid. 8S. line Sec. 17...... 0.0.2... 315] E. line Sec. 12...............0000. 235 
Center 8. E. qr. Sec. 17.......... 230 T. 14, BR. 9 E. 
Mid. W. line 8. W. qr. Sec. 19 .... 335 | Merrils’ S. E. qr. N. E. qr. See. 7 .. 196 
Center 8. W. qr. Sec. 20 .......-.. 340 T. 14, R. 10 EK. 
Center N. W. qr. Sec. 20.. ....... 350 Observ. hill, S. E. qr., Sec. 7 base .. 240 
Road, mid. E. hf Sec. 22.......... 226)  Observ. hill, 8. E. qr., Sec. 7 top... 490 
Bluff top, 4g mile S........ 22... 450 T.17,R. 8 E. 
Bluff top, E. line §. E. qr. Sec. 22. 590| N. W. qr. Sec. 7, lime bluffs. top .. 730 
Bridge, center Sec. 23............. 225| N. W. qr. Sec. 7, lime bluffs, base.. 570 
Winfield. T. 13, R. 4 E. Portage County. 
Si. W. qr: See: 24 5...4 05 cvins weercess 372 T. 21, R. 8 E. 
8. Hi.cor: Secs 24) s+nus oeceseccavs 468 Mosquito bluff, Sec. 28, top........ 630 
Wo HE: SO6.:27 sv sis 5 xs ashe oeeniore Bie 413 Mosquito bluff, Sec. 23, base ...... 520 
S. He. Cor Deel, 27 ss sana cee 286 | Marathon County. 
Mid. W. line 8. W. qr. Sec. 33 .... 807 T. 28, R. 7K. 

Center See. 35.2.0. cece ee eee eee 408} Top Rib hill, W. end, W. hf. Sec. 8 1263 
Dellona. T 13, R.5 E. Top Rib hill, E. end, W. hf. See. 9 1143 
Mid. N. hf. Sec. 5... eee eee eee 300 Lower Mosinee hill, center Sec. 27, _ 
Center N. W. qr. Sec.19.......... 390 HOD. sacsairal ws claielew inane seiatin 880 

Juneau County. Lower Mosinee hill, river at foot .. 600 
T. 14, R.2E. Upper Mosinee hill, N. E. qr. Sec. 
Mid. 8. line Sec.6...... Saat esiglarets 430 27, top ..--... pseu den atartietes otc te 1030 
Mid. E. hf. Sec. 7 .....---.6. wee 310 | Upper Mosinee hill, river at foot.. 600 
Mid. W. hf. W. hf. Sec. 24 ....... 550 T. 29, R. 7 E. 
T. 14, R.5 E. Mid. N. line Sec. 1... 0... eee 890 
High crest, Sec. 28 20... ee eee eee 700 | Wausau depot, Sec. 86......... J++ 643° 
T. 15, R.3 E. Jackson County. 
Mid. 8. line 8. E. qr. Sec. 7........ 360 T. 21, R.4 W. 
Bluff Sec. 13, base.........2.. 066 300} Isolated bluff, Sec. 23, base........ 230 
Bluff Sec. 18, top .......0.. Rakes 500! Isolated bluff, Sec. 23, top...... see 489 


RELATIONS OF THE TOPOGRAPHY TO THE GEOLOGY OF THE REGION. 


The topography of all countries is chiefly dependent upon the na- 
ture of the geological formations immediately underlying the surface. 
This is markedly soin Central Wisconsin. The rock systems of this 
portion of the state are altogether Archzean and Lower Silurian; the 
former consisting of gneisses, granites and schists, with other erys- 
talline rocks, the latter of a series of alternating sandstones and lime-’ 


448 GEOLOGY OF CENTRAL WISCONSIN. 


stones, in nearly horizontal beds. These include, in ascending or- 
der, the Potsdam, or Lower sandstone, the Mendota limestone, the 
Madison sandstone, the Lower Magnesian limestone, the St. Peters 
sandstone, the Trenton limestone, and the Galena limestone. The 
last named covers but a very small portion of our district. The 
Archean rocks lie in a great central mass in the northern part of the 
state, the Silurian formations encircling this mass in imbricating or- 
der, and, coming to the surface in a series of receding concentric 
bands, together forming the southern, eastern and western parts of 
the state. The surface features of the Archeean and Silurian regions 
differ much. In the Archean area we have unquestionable proof, in 
the crumpled condition of the rocks, of its former mountainous char- 
acter. Denudation has gradually, in the great lapse of time during 
which these beds have been exposed, stripped it entirely of these char- 
acteristics, leaving it now merely a high, and, in general, a gently undu- 
lating area, broken only very occasionally by small isolated ridges or 
peaks of quartzose rocks, which have remained standing by virtue 
of their superior hardness and power of resisting chemical action. In 
minor detail, however, the Archean area is much roughened by low 
' ridges whose sides frequently show outcropping ledges of tilted rock. 
In the Silurian area, on the other hand, the original condition must 
have been a nearly level one, and denudation has worked here in an op- 
posite direction, removing great portions of the horizontal beds, goug- 
ing them everywhere into valleys, and producing thus narrow ridges 
and bold isolated blufts. The horizontality of the Silurian strata, which 
is more nearly exact in central Wisconsin than elsewhere in the state, 
together with their alternately hard and soft characters, has resulted 
in producing a peculiar, abruptly roughened surface — narrow valleys 
with abrupt, bluffy sides, and irregular table-like outliers. 

These peculiarities of topography, resulting from the different ef- 
fects of the eroding agencies on the different kinds of rocks, have, 
however, in a large portion of the region, been much modified and 
obscured by other causes. I refer to those causes which gave rise 
to the glacial drift. The southwestern quarter of the state of Wis- 
consin is without trace of the glacial depositions, whilst all of the 
rest of the state is characterized by the presence of unusually large 
quantities of these materials. The line of demarkation, moreover, 
between the drift-bearing and driftless areas, is a sharp and easily 
traced one. Entering the state from the south on the southern line 
of Green county, the drift limit traverses this county centrally from 
south to north, and continues northward through western Dane and 
central Sauk; then, curving eastward across the southern end of Adams, 


VEGETATION AND SOILS. 449 


- it follows along the eastern line of that county, passes into Portage, 
curves westward, and crossing the Wisconsin river again, continues 
in a nearly westward direction across Wood, Clark, J ackson, Trem- 
pealeau and Buffalo counties, to about the foot of Lake Pepin, on the 
Mississippi. The driftless region is thus nearly altogether within the 
Silurian area. North and east of the drift limit the general contours 
are usually flowing, the valleys frequently wide and ill defined, the 
rock exposures not frequent, and the outliers not many in number, be- 
ing usually of large size and without jagged edges or peaks. On the 
other side of this line the topography is strikingly different; the 
changes of level are abrupt, the valleys narrow, with steep and high 
sides, the rock exposures frequent, and the outliers often of very small 
dimensions horizontally, though of very considerable height, and of- 
ten showing precipitous sides with jagged, peak-iike summits, even 
when of soft sandstone. The drift forces have contributed to this re- 
sult in two ways; (1) by planing down the irregularities resulting 
from subaerial erosions, and (2) by the deposition of great quantities 
of clay, sand and gravel. The peculiar mode of deposition of this 
material has, however, itself, in much of the region, produced a pe- 
culiar irregularity of surface, leaving it covered with ridges of low 
rounded knobs, and intervening rounded depressions, which are fre- 
quently filled by small ponds or lakes. It is also true that the change 
of topography noted in passing from the driftless to the drift-bearing 
area is not exclusively due to the former presence or absence of the 
glacial forces, but is in some measure owing to the fact that for a 
long distance the drift limit is nearly on the line of a change from a 
horizontal position of the strata to a gradually increasing eastward 
slope. 

A much closer connection can be traced between the variations in 
surface features and the changes in the formations, which will receive 
attention hereafter. 


VEGETATION AND SOILS. 


These are noticed here only in their most general relations; the 
soils only in reference to their connection with the underlying geo- 
logical formations. 

The three different kinds of surface in the district, as to vegetation, 
are the prairies, marshes and timber land. The prairves, or tree- 
less areas, are restricted to the Silurian region, and are chiefly charac- 
teristic, in central Wisconsin at least, of limestone districts, though 


oceurring also on the sandstone formations. In many places regions 
Wis. Sur. — 29 


459 GEOLOGY OF CENTRAL WISCONSIN. 


once prairie have been invaded by a timber growth, which has come 
in since the settlement of the country, having been in former times 
checked by the annual prairie fires. Very large areas in Adams 
county, for instance, which are now covered with a thick growth of 
small oaks, are said to have been open prairies at the time of the first 
settlements. The prairie areas are by no means always flat; indeed, 
the flat prairies are the exception, and have chiefly been noticed along 
the bottom land of the Wisconsin river. The ordinary prairie, how- 
ever, as in northern Dane and eastern Columbia county, is very roll- 
ing, commonly showing abrupt changes of level, even up to fifty or 
a hundred feet. These changes in level are, in places, due to heaped 
ap drift, but more commonly to unequal denudation of the rocky 
strata. In many cases, as, for instance, in the town of West Point, 
Columbia county, the prairie area includes both lowland and bold 
outlying bluffs, as much as two hundred or even three hundred feet 
in height. The Central Wisconsin prairies are, with one notable ex- 
ception, of small size, occupying at most not more than two or three 
sections. The exception is the limestone prairie belt which occupies 
large portions of the towns of Springficld, Westport, Dane, Vienna, 
Windsor and Bristol, in northern Dane county; and of West Point, 
Lodi, Arlington, Leeds, Hampden and Lowville, in Columbia county. 
The same belt, though somewhat broken in the towns of Otsego and 
Courtland, continues to the northeast and passes into Green Lake 
county. This large prairie area is for the most part on high land, 
oceupying the summit of the watershed between the Wisconsin and 
Rock rivers. It is nearly always underlaid by the Lower Magnesian 
limestone, whose irregular upper surface contributes much to the 
rolling character of the prairie. 

The marshes are widely scattered, occurring over both the Archean 
and Silurian areas, though more numerously in the former. As a 
general rule they are small, but in some cases are of very considerable 
size, as, for instance, those extending along Duck creek and the up- 
per Fox river east of Portage, which are many miles in length, and the 
great marsh south of Plover, in Portage county, which covers the 
greater part of four townships. Many of these marshes, as, for in- 
stance, the Plover marsh just alluded to, are underlaid by a valuable 
quality of peat. 

With regard to timber, it may be said that all of the counties of 
Dane, Columbia, Sank (except on the quartzite blufts), Juneau, 
Adams, Marquette and Waushara (except on the east), are covered 
by a prevailing growth of small oaks; whilst Marathon, Portage, 
eastern Waushara, most of Wood, Clark, and much of Jackson, are 


VEGETATION AND SOILS. 451 


heavily timbered with pine interspersed with hardwood on the more 
elevated lands. The Archwan region is generally heavily timbered, 
north Wisconsin being one of the great lumbering districts of the 
continent. 

Geologically, we may distinguish the drift, the purely sandstone, 
the purely limestone, and the crystalline rock soils. The last three 
terms are meant to apply to such soils as result exclusively from the 
disintegration of the underlying rocky formations. Inasmuch as these 
formations are not always perfectly pure limestone or sandstone, their 
disintegration gives other ingredients to the soil than lime or sand. 
The drift soils are either bad or good as the material is more largely 
sandy, or shows a predominating admixture of clayey and calcareous 
substances; those resulting solely from the disintegration of the sand- 
stone, of the poorest quality; whilst the limestone soils are usually 
the best in the region. The crystalline rock soils are often good, but 
as the region of crystalline rocks is nearly everywhere invaded by the 
drift, its soils are commonly dependent upon the nature of the drift, 
rather than upon that of the subjacent rock. Insome portions of the 
Archean region, where either the drift is not present in very large 
quantity, and the felspathic rocks have disintegrated into a good 
clayey soil, as in the high land in the western part of Marathon 
county, or where the drift is itself of a non-arenaceous character, as in 
much of Olark county, and in many places along the line of the Wis- 
consin Central Railroad, excellent lands for farming are made by 
clearing the heavy growths of hardwood timber. Where the drift is 
more sandy, as in a large region about the headwaters of the Wiscon- 
sin river, the land is worthless for agricultural purposes, though 
frequently covered with a valuable growth of pine. Through the 
sandy nature of the drift materials the sand region of central Wiscon- 
sin extends in places far beyond the district occupied by the Potsdam 
sandstone. In all of the region in which the last named rock is the sur- 
face formation, and where tne drift is either absent, or present in 
small quantities only, or is altogether sandy in nature, as in most of 
Adams, Juneau, Sauk, Jackson, Marquette, and Waushara counties, 
in much of Columbia, and in places all along the valley of the Lower 
Wisconsin, the soil is generally a loose sand, and the land of the 
poorest quality. Where the drift overlies the sandstone and con- 
tributes clayey or calcareous matter, asin the southern part of Adams 
county, or the eastern part of Waushara, the land is often good. In 
other cases, a good soil within the Potsdam area and where the drift 
is absent seems to have resulted from the filling of valleys with fine 
stream detritus, as along the valley of the Wisconsin; or from the 


459 GEOLOGY OF CENTRAL WISCONSIN. 


a 


nearness to the surface of certain clayey layers included within the 
sandstone, as in the town of Reedsburg, Sauk county; or from the 
presence of: considerable dolomitie material in the sandstone, as in 
the town of Honey Creek, Sauk county. All of these, are, however, 
but exceptions to the general rule, that, for the most part, the Pots- 
dam area, on both sides of the drift limit, is a barren sandy region. 

Above the lowest sandstone, we find, first, a layer thirty feet in 
thickness of clayey or sandy dolomitic limestone, to which I have 
given the name of Mendota limestone. Where it is the surface 
rock, as in portions of the towns of Scott and Marcellon, Co- 
lumbia county, a good clay soil usually results. Next above the 
Mendota is again a layer of sandstone, which I will designate as the 
Madison sandstone, having a thickness of 30 to 40 feet. Where it is 
the surface rock, as in a large part of the town of Otsego, Columbia 
county, the soil is a loose sand, and of little value. These rapid al- 
ternations explain the change of soil noticed with a slight change of 
elevation in many places along the borders of the areas occupied by 
the Lower Magnesian limestone, which is the next formation in 
order. 

The Lower Magnesian is a great mass of dolomitic limestone, 80 
to 200 feet in thickness, often carrying much silicious and clayey 
matter in its composition. The country occupied by it is hence 
nearly always one of most excellent soils. Such is the soil of the high 
prairie belt of northern Dane and eastern Columbia. These prairies 
are often much covered with drift, which occasionally lends a sandy 
character to the soil, but not frequently, since the drift of this partie- 
ular district itself is commonly calvareous and clayey. 

The next rock above the Lower Magnesian, the St. Peters sand- 
stone, but rarely forms the surface rock, being generally concealed, 
when present, by overlylng beds, and showing only on hill-sides and 
steep slopes. Where, however, it comes to the surface, as in the val- 
ley of Sugar river in western Dane county, and the drift is absent, 
the same sandy soil is observed as that produced by the disintegra- 
tion of the Lower sandstone. 

The Trenton limestone soils are usually of excellent quality, and 
frequently somewhat more argillaceous and less dolomitic than those 
from the Lower Magnesian. The Galena is so unimportant a forma- 
tion inCentral Wisconsin that it need not be especially alluded to in 
this connection. 


PLATE, XVI 


MAP OF 
CENTRAL WISCONSIN 
showing the~ 
HYDROGRAPHIC BASINS and the principal TOPOGRAPHICAL SUBDIVISIONS 
R.D. ving, 1876. 


i. / 


Seale, +iniles= Vind 


Litt of Hydrographic Basins 


ghana drat Northern and Eastern Limits of 
DriftlessArca 


LT Phe trystethine rook District. 


ae The Sandstone District 


but The taeestore List rict 


Tay Manwac ity Lorin & baer Co 


TOPOGRAPHICAL SUBDIVISIONS. 453 


TOPOGRAPHICAL SUBDIVISIONS — RESUME. 


The foregoing details, with regard to the surface slopes, river 
systems, surface relicfs, prairies, marshes, timber, etc., of central 
Wisconsin, will serve to render intelligible to the reader a very 
brief summary of the topographical features of the whole dis- 
trict. 

First, then, we find on the north, occupying all of Marathon and 
most of Portage, Wood, and Clark counties, a comparatively elevated 
region of crystalline rocks, which descends gradually from an 
altitude of 900 feet on the north, to one of 400 to 500 feet on the 
south. In general, this section has a gently undulating surface, 
which is, however, often broken in minor detail by low, abrupt ridges 
with outcropping tilted rock ledges, and is dotted occasionally with 
high points of quartzose rocks. The whole area is densely covered 
with a forest of pine interspersed with marshes, and hardwood ridges, 
which when cleared yield excellent land. It is traversed from north 
to south by two large rivers, the Wisconsin on the east, and the 
Black on the west, which, as also their numerous branches, are 
rapid streams, broken constantly by chutes and water falls over tilted 
rock ledges; and is covered everywhere with accummulations of drift 
material, which are, however, much greater in some places than in 
others. 

Proceeding now further southward we come next upon the great 
central sandstone region of the state. This covers all of Jackson, 
Juneau, Adams, Marquette and Waushara counties, southern Wood, 
Portage and Clark, northern and western Columbia, and most of 
Sauk. It extends east and west about eighty miles, north and south 
about one hundred, and: really includes several subordinate areas, 
which are, in some respects, topographically distinct, but all of which 
have in common the basement rock of sandstone, and, for the most 
part, the sandy soil. For the greater part of its area, the sandstone 
district is out of the heavy timber, which, however, invades it in east- 
ern Waushara, in southern Portage and Wood, and in eastern Jack- 
son. For the rest of the district, the prevailing growth, except on 
the high Archean bluffs of Sauk, is of small oaks. 

Of the subordinate areas, we note first on the east a district (1), 
including Waushara, southern Portage, those portions of Marquette 
and Green Lake which lie north of the Fox river, and southern 
Adams, which is everywhere heavily covered with glacial drift, to 
whose irregular morainic method of deposition is to be attributed a 
peculiar roughened surface, dotted in places with small lakes that oc- 


454 GEOLOGY OF CENTRAL WISCONSIN. 


cupy the drift depressions. The streams of this region are numerous, 
large, rapid, and extraordinarily clear, but without rock rapids. Rock 
bluffs are not frequent, and those that occur are without the castel- 
lated appearance so characteristic of the more western outliers. The 
whole of the area descends from its highest parts in northwestern 
Waushara, where the altitude is about 540 feet, in a southeasterly 
direction towards the Fox river, whose altitude at Portage is 200 
feet, and at Berlin 175 feet. The soil of this district is for the most 
part sandy. In central Waushara, however, good land occurs on 
limestone and crystalline rock drift, whilst in eastern Waushara the 
stratified drift clays yield an excellent soil. West of the high 
ground along the line of Adams and Waushara counties, we 
come upon an altogether different region, (2) the next of our sub- 
ordinate divisions. This is the central sand plain of Adams and 
Juneau counties, which is traversed from north to south by the Wis- 
consin river. Here we find no drift at all, a generally flat surface, 
rising gradually from the river in each direction, and dotted by nu- 
merous lofty and jagged peaks of sandstone, large and clear streams, 
and a prevailing growth of small oaks, interrupted by a few prairies 
and marshes, and mingling with small pine towards the north. 
Crossing now the divide on the northwest corner of Juneau county, 
we find ourselves in the sandstone portion of the Black river valley, (3) 
which resembles, for short distances from the river, in its general 
sandy, plain-like character, and gigantic, castellated outliers, the re- 
gion last described. As we pass westward, however, from Black 
river, or southward along its course, we find ourselves in a region of 
narrow but deeply eroded valleys and of steep hills. Returning now 
to the central plain of Juneau county, and proceeding towards its south- 
west corner, we cross, in the towns of Summit, Wonewoc, Plymouth and 
Lindina, a high, narrow, and deeply indented watershed, and find our- 
selves in the upper part of the Baraboo river valley, (4) which we may 
regard as another of the subordinate districts of the central sandstone 
region. The upper part of this valley shows the usual characters of 
the valleys of the driftless part of the state, being narrow, with abrupt 
sides, which are often of precipitous sandstone. The tributary 
streams have similar, but narrower and steeper valleys. On either 
side the country rises rapidly, and shows frequently excellent land. 
As the river is followed into Sauk county, its valley widens, but the 
same deeply indented divides are observed; that on the south, in the 
towns of Westfield and Reedsburg, rising into the horizon of the 
Lower Magnesian limestone, so that large patches of good limestone 
country occur here. In central Sauk county the Baraboo traverses 


TOPOGRAPHICAL SUBDIVISIONS. 455 


the length of the valley between the two quartzite ranges, whose top- 
ography has already been sufficiently indicated. About midway in 
the east and west length of this valley the western limit of the gla- 
cial drift is met with, which is here in a morainic condition. Cross- 
ing now to that portion of Sauk county which lies to the south of the 
limestone-capped divide in the towns of Westfield and Franklin, and 
of the southern quartzite range, we reach a part of the valley of the 
Wisconsin itself, which may be designated as the Honey Creek dis- 
trict (5). On the west side of this triangular area we find deeply 
eroded valleys with limestone-capped separating ridges; further 
south and east towards the river, numerous outliers and peculiar nar- 
row ridges are seen; further east still these cease suddenly, and on 
the wide prairie in the towns of Prairie du Sac and Sumpter, morainic 
drift begins as suddenly again. Along the Wisconsin in the south- 
west corner of this area, the limestone-capped bluffs of an immense 
outlier bound the river bottom for a number of miles. We have yet 
to consider the last of these subordinate areas, (6) which includes 
that portion of Marquette county south of the Fox river, and the 
northern, central and western towns of Columbia county, being lim- 
ited on the east and south by the western face of the limestone divide 
between the Wisconsin and [tock rivers. This isan area in general 
level, having an elevation of about 250 feet, with many bold lime- 
stone outliers. It is drift covered, showing numerous large bowlders, 
has everywhere a sandy soil, and a somewhat sparse growth of small 
oaks. 

The third and last of the great topographical subdivisions of Cen- 
tral Wisconsin we may designate as the limestone district, since in 
it one or other of the Silurian limestones is almost always the surface 
rock. It includes eastern and southern Columbia, and all of Dane, is 
characterized nearly everywhere by an excellent soil, includes the 
largest prairie areas of central Wisconsin, shows a prevailing growth 
of oak, and has a rolling and diversified surface. The drift materials 
are everywhere present, except in the southwestern towns of Dane, 
which show the usual abrupt topography of the driftfess area. On 
the northern side of this district, in the towns of Scott, Randolph, Court- 
land, Otsego, Lowville, Hampden, Leeds and Arlington, in Columbia 
county, and of Vienna, Westport, Dane, Springfield and Middleton, 
in Dane county, there is a nearly continuous belt of high rolling prai. 
rie from about 400 to 600 feet in altitude. The underlying rock on 
this prairie is limestone, and the soil of the very best quality. From 
the east and south flanks of this high land the country descends 
rapidly, and is watered by the various head streams of Rock river. 


456 GEOLOGY OF CENTRAL WISCONSIN. 


In western Dane, the descent is almost entirely towards the south, 
but in the center of the county the dip of the strata begins to veer 
eastward, and the surface slope corresponds. On the west side of this 
county, again, in the valley of Sugar river, the topography is more 
abrupt than elsewhere, owing to the entire absence of the drift ma- 
terials; in the center we find the broad southeast valley of the Catfish, 
With its chain of jakes lying in N. E.-§. W. valleys, and its morainic 
glacial drift; whilst further east still we find a more nearly level 
drift-covered region, sloping gradually eastward. 


GENERAL GEOLOGICAL STRUCTURE. ABT 


CHAPTER II. 


GENERAL GEOLOGICAL STRUCTURE OF CENTRAL 
WISCONSIN. 


The region of country included within the boundaries of the state 
vf Wisconsin is quite simple as to the grand features of its rock 
structure, and may be briefly described as consisting of a great nucle- 
us of ancient crystalline rocks, encircling which, but more especially 
on the east, south, and west, are succeeding bands of limestone and 
sandstone, belonging to the Silurian series. 

Forming most of the northern half of the state is a great mass of 
erystalline rocks — granites, gneisses, chloritic micaceous and horn- 
blendic schists being the predominating kinds—which are folded 
and eroded so as to offer the greatest obstacles to their detailed study, 
and which appear, for the most part, to be referable to the Laurentian 
division of the Archean. 

On the northern edge of this central nucleus, just south of Lake 
Superior, in Bayfield and Ashland counties, is a narrow belt of quartz- 
ites, magnetic and specular iron ores, diorites, taleose chloritic and 
black slates, ete., which overlie unconformably the gneisses of the 
Laurentian immediately to the south. This fact, taken together with 
their nature and relations to the newer adjoining formations, would 
seem to throw these beds, without any doubt, into the same catagory 
with the Iron Bearing series of Michigan, and the Huronian system 
of Canada. Similar rocks, with similar relations to the surrounding 
formations, exist in Oconto county, on the northeast border of the 
state, from where they stretch far into the Upper Peninsula of Michi- 
gan, and include the famous iron regions of Marquette and the Me- 
nomonee. On the south side of the Laurentian core, on Black river, 
in Jackson county, are again similar rocks, whose Hnuronian age is 
not. so clearly made out. Still farther south, and within the area of 
the Silurian formations, are projecting portions of the here buried 
Archean. These isolated masses are made up chiefly of quartzites 
and dark-colored quartz-porphyries, and are scattered widely over 
Marquette, Waushara, Green Lake, Columbia and Sauk counties, pre- 
serving in their positions a sort of rough parallelism to the southern 


458 GEOLOGY OF CENTRAL WISCONSIN. 


and eastern borders of the main Archean mass. There is no proof 
at hand that the rocks of these patches are unconformably super- 
posed upon Laurentian strata, but the contrast between them and the 
Laurentian gneisses and schists, their resemblance to Huronian rocks 
elsewhere, and more especially the parallelism just referred to, strong- 
ly suggest the possibility of their forming part of a continuous band 
of Huronian, of which the Lake Superior and Oconto areas are other 
portions, encircling the Laurentian core, after the manner of the later 
and undisturbed Silurian accumulations. Regarding the Black river 
ferruginous schists, and the associated gneisses as Huronian, a continua- 
tion of the same belt, completing the circuit, may possibly exist in 
the northwestward trending gneissic and hornblendic beds of the low- 
er Chippewa,! the arenaceous and conglomeratic quartzite of the hills 
in T. 32, R. 7 W., near the Chippewa river,’ and the quartzite and 
associated pipestone of Rice Lake, in Barron county? This idea of 
a continuous Huronian belt encircling a Laurentian core is thrown 
out as a suggestion only, a generalization towards which the facts in 
my possession at this writing would seem to point. At present all 
that we can affirm with any degree of certainty of the great crystal- 
line rock area of northern Wisconsin is that most of its rocks are 
Laurentian, that on its northern and northeastern edges are some un- 
doubted Huronian beds, and that on its southern and southwestern 
borders are again rocks between whose Laurentian and Huronian age 
there remains some question, although they quite probably are to be 
assigned to the latter period. 

From its northeastern corner the Wisconsin Archean nucleus, in- 
cluding now both Huronian and Laurentian rocks, sends a long pro- 
jection across the Upper Peninsula of Michigan to the shores of Lake 
Superior, possibly connecting, beneath the lake, with the great Cana- 
dian Archean area. Thus, from the earliest Paleozoic times, the rock 
depositions skirting the Archeean of Wisconsin on the east, south and 
west, must have gone on independently of those on its northern side. 

The outcrops of the undisturbed and unaltered Silurian formations, 
which succeed one another in receding concentric bands on the east- 
ern, southern and western sides of the Archean of Wisconsin, are the 
direct continuations of the outcrop bands of a series of strata, which, 
after following the southern side of the Canadian Archean westward 
through New York and Canada, make a great curve to the northward 
across the peninsula between Lakes Huron and Erie, and also across 


'K. T. Sweet, manuscript report and also Transactions Wis. Acad. Sci, Vol. IIT. 
2h. T. Sweet, Loc. cit. 
30wen’s Geological Survey of Iowa, Wisconsin and Minnesota. 


GENERAL GEOLOGICAL STRUCTURE. 459 


the Upper Peninsula of Michigan, and enter Wisconsin on its north- 
eastern corner with a sharp southwestward trend, having thus accom- 
modated themselves to the southern line of the ancient Archean con- 
tinent. On crossing into Wisconsin, these formations dip quite rap- 
idly to the eastward, and their southward trending outcrops succeed 
one another in comparatively narrow bands. As they are traced 
southward, however, these outcrops curve gradually westward, the 
eastward dip at the same time lessening, and the exposed portion of 
each formation becoming wider. Along the central north and south 
axis of the state, the eastward dip has entirely disappeared, each form- 
ation is the surface rock over a wide extent of country, and the bound- 
ing line of each makes a wide bow to the southward before the return 
northwestward. parallel to the western side of the Archean area. 
Thus it follows that in the Central Wisconsin district are to be ob- 
served a smaller number of the Silurian formations than occur further 
eastward and westward in the state. . 

The latest one of the Silurian formations of Central Wisconsin is 
of the age of the Trenton limestone of New York. Elsewhere in 
the state, the Upper Silurian is represented by immense thicknesses of 
limestone, and over a small area near Milwaukee, even Devonian beds 
are to be scen. The exact extent to which the original areas of these 
various formations exceeded their present ones, it is quite difficult to 
arrive at, so great has been the amount of denudation. 

After the close of the Silurian—for much of Central Wisconsin 
probably after the close of the Lower Silurian —no farther deposi- 
tions of any kind were made until the time of the Glaciai Drift, 
when immense masses of gravel and boulders, as also stratified sands 
and clays, were largely deposited. During all of the intervening 
time the region must have been out of water and exposed only to the 
ordinary suberial eroding agencies. Thus we see how it is that we 
find here proofs of a denudation unusually great for non-mountainous 
regions. 

The following table shows at a glance the several formations that 
enter into the structure of the Central Wisconsin district, with their 


geological relations :— 


460 


GEOLOGY OF CENTRAL WISCONSIN. 


Recent — Peat beds; bog iron ores. 


QUATERNARY. { Champlain — Lacustrine clays, over 200 feet thick. 


Lower 
SILURIAN. 


ARCHHAN. 


Glacial — “ Drift’’; including bowlders, till, sand, gravel, ete. 


Trenton limestone; alternating limestones and 


c Galena limestone; dolomite, 300 to 350 fect. 
Trenton. 
dolomites; in all 100 to 120 feet. 


St. Peters sandstone; 15 to 120 feet. 
Canadian. Lower Magnesian limestone; dolomite, 50 to 


125 feet. 

C Madison sandstone beds, 35 

Beds of pas- to 50 feet. 
sage. Mendota limestone beds, 80 

to 45 feet. 
( Including possibly two dis- 
Primordial. tinct formations, the one 
lying upon the eroded sur- 
Lower or Pots- face of the other; in all 800 


dam sandstone. to 1000 feet thick, but vary- 
ing much on account of the 
irregular surface of the un- 
derlying rocks. 


\ \ \ 


iron ores, gneiss (?); many thousand feet 
thick, 


( Quartzites, schists, quartz-porphyries, silicious 
Huronian. 
Gneiss, granite, schist, diorite, quartzite, ete.; 


Laurentian. { no crystalline limestone; many thousand feet 
thick. 


\ 


THE ARCHAAN, ROCKS. 461 


CHAPTER IIL 


THE ARCHAAN ROCKS. 


THE MAIN ARCHAHAN AREA. 


I. In General. 


The crystalline rocks of the Central Wisconsin district may be con- 
veniently separated into two groups, for the purposes of description; 
those of the main Archean body constituting one of these, and those 
which occur in isolated protruding patches within the region of the 
Silurian sediments, the other. The two are of course but parts of the 
same grand mass, which everywhere underlies the undisturbed Silu- 
rian beds, a fact proven, not merely by geognostical theory, nor the 
evident passage of the crystalline rocks beneath the Silurian, but also 
by the numerous Artesian borings which have penetrated through the 
horizontal strata into the underlying Archean, at points widely scat- 
tered over the state. At present, however, we have to do only with 
those of the crystalline rocks that appear at the surface. 

The area occupied by the rocks of the main Archean mass, so far as the 
district at present under consideration is concerned, covers all of Mara- 
thon, most of Wood, and much of Clark, Jackson and Portage counties. 

The line of junction betweeri the Archean area and that of the 
next formation to the south, the Potsdam, or Lower, sandstone, is 
exceedingly irregular, and often quite difficult to trace. The sand- 
stone is frequently found stretching far northward along the water- 
sheds between the southward fléwing streams, whilst the gneissic and 
other crystalline rocks are to be observed stretching as far south along 
the stream valleys, the areas of the two formations thus dovetailing 
into one another. Thus the Wisconsin and the Black rivers make 
rapids over tilted gneissic strata for many miles south of their first 
entrance upon the sandstone region, and as their courses are followed 
downwards the exposures of these rocks are to be found more and 
more closely restricted to the stream limits, until they finally occur 
in the river beds only, the sandstone overlying them in the banks. 
A more definite idea of the position of the boundary line between the 
sandstone and Archean areas may be obtained from the general geo- 
logical map of the state (Atlas Plate I), and also from Plate XV of 


462 GEOLOGY OF CENTRAL WISCONSIN 


the Atlas, which give the boundary, for the region examined by the 
writer, with as great accuracy as present knowledge will permit. 

The unconformability between the tilted crystalline rocks and the 
horizontal sandstones is frequently to be observed along the boundary 
line between the areas of the two formations, and especially where 

the streams have cut 


oe through the  sand- 
Sandstone : stones into the un- 
derlying Archean 

Inanumber of places, 


as to which details 
are given in sub- 
sequent pages, the 
exact junction of the 
two formations can 
be seen. In one 
place on Black river 
it is even possible to 
obtain hand speci- 
mens showing both 
formations, and their 
respective bedding 
and lamination lines. 


ms a 

SKETCOM OF A SPECIMEN FROM NEAR Buack RIVER FA.tsg, suow- af] 1g. 1 is taken from 
ING THE EXACT JUNCTION OF THE POTSDAM SANDSTONE AND AR- 
CHAN scuists; half the original size. 


one of these hand 
specimens. 

The general topographical features of the crystalline rock dis- 
trict have already been indicated. It is an elevated area with an 
altitude of from 500 to 900 feet, and highest on the north. In gen- 
eral, it may be said to have a surface of gradual, though considerable, 
changes in elevation. Looked at more minutely, however, the surface . 
is observed to be broken up frequently by low and narrow, but quite 
steep, ridges, often with rock exposures at top. The whole region is 
densely timbered, chiefly by pine. These pine trees, on account of 
the small depth of their roots, are easily and frequently prostrated by 
the wind, often over many square miles at once. Such windfalls, 
when burnt over and grown up with a small second growth, combine 
with the steep rocky ridges and the numerous small intervening 
marshes, to render traveling in this region to the last degree difficult. 
On the higher swells of the country, however, the pine is often re- 
placed by hard wood, maple especially. In such parts, traveling is 
easier, and excellent farms are obtained by clearing. The soil in these 


THE ARCILEAN ROCKS. 463 


cases sometimes evidently results for the most part from a direct disin- 
tegration of the felspathic rocks in place, but sometimes also from a 
disintegration of similar rocks in the drift. The descent of the re- 
gion southward has caused the river valleys and smaller watercourses 
to be cut deeply into the rocks, which are hence best exposed along 
streams. As already said, however, exposures occur also somewhat 
widely scattered away from the streams. Some large areas, as, for 
instance, the country along the Fourth Principal Meridian, from 
town 30 to town 42, are without rock exposures, the drift covering 
being especially heavy. 

~ By far the most common one of the crystalline rocks in this area 
is gneiss; next in order of abundance are granitoid gneiss, granite, 
syenite, hornblende rocks, chloritie schists, mica-schists, quartz-schists, 
quartzite and felsitic rocks. In one small district on Black river in 
Jackson county are large exposures of silico-ferruginous schists (iron 
ores), associated with silico-magnesian (talcose) schists. All of these 
general kinds include many varieties, which are noted in the follow- 
ing detailed descriptions. The granitoid and gneissoid kinds have 
most commonly a moderately coarse character. 

The original bedded condition of the whole series is rendered suf- 
ficiently evident, not only by a prevailing gneissoid and schistose 
character, but also by the existence of distinct bedding planes 
and lamination lines, which, though often obscured by cross-jointing, 
especially in the granitoid kinds, can nevertheless, in general, be 
readily made out. That the processes of metamorphism and disturb- 
ance have been carried almost to their last extremes is shown by the 
highly crystalline character of the rocks, the grading of the gneiss 
into granite, the greatly contorted condition of the gneiss laminee,! 
and the close folding of the whole series. In some places, portions 
of the arches are left; but in general erosion has removed or ob- 
seured all the crowns, and has made of what must once have been a 
lofty mountainous region, one in which the variations from a general 
level are only those of insignificant ridges, and comparatively shallow, 
eroded watercourses. 

Whilst the bedding of the whole series is thus evident, distinctly 
intrusive granite occurs, its nature being indicated by the way in 
which it joins and penetrates the bedded rocks. This extravasated 
granite is usually of a pinkish to reddish color, often very bright 
red, and occurs in very large masses. 

A tendency to weather characterizes most of the gneisses and other 

1 Most beautifully exhibited on Black river, just below the crossing of the Green Bay 
Railrcad. - 


464 GEOLOGY OF CENTRAL WISCONSIN. 


felspathie rocks, and also those that are largely hornblendic. The alter- 
ation usually extends but a small distance into the body of the rock, 
which can generally be observed in its trne unaltered character by re- 
moving the surface crust. In some localities, however — and these are 
altogether without the drift area, or at least where the drift materials 
are scanty — the whole exposed portion of the rock is so disintegrated 
as to crumble to dust under a blow of the hammer, or is completely al- 
tered, by removal of alkaline ingredients and absorption of water, to a 
clayey mass, which, when the original rock was non-ferruginous, or 
when the iron oxides have been also completely removed, is a mixture 
of pure kaolinite and quartz grains, and is of considerable commercial 
value. The almost entire restriction, so far as known, of this kaolin- 
ized rock to those districts where there is nothing to indicate the 
former presence of the glacial agencies, is a fact of very considerable 
interest. Its absence everywhere where the drift occurs may indicate 
that it has been removed by the drift forces. It is true, however, 
that the kaolin district coincides with one in which there is generally 
more or less of a sandstone covering to the crystalline rocks, and that 
many of the kaolin occurrences are beneath a few layers at least of 
sandstone. It may then be that the surface waters, percolating 
through the porous sandstone — in ancient times much thicker than 
now — have formed natural watercourses along the junction between 
it and the less easily penetrable crystalline rocks, and have thus ex- 
erted an unusual disintegrating action; whilst the sandstone itself 
has subsequently acted as a preserver of the kaolinized rock from the 
ordinary eroding agencies. ; 

No one system of strikes prevails over the whole region, but yet 
for long distances a marked parallelism can be observed in the courses 
of the outcrops of the various layers. Thus along the Wisconsin 
from its southernmost exposures of crystalline rocks, at Point Bass, 
in Wood county, as far north as Wausau, in Marathon county, the 
strikes are, for the most part, east of north, whilst the dips, though 
of course far less constant in amount and direction, are more com- 
monly north than south. On Black river, again, for the whole dis- 
tance examined, the strikes are just as markedly northwest, and on 
Yellow river more commonly west, than east of north. Whilst no 
general system of strikes can be laid down for the whole region, and 
no further generalizations can be drawn from the observations made 
in the Central Wisconsin district, it is nevertheless very probable that 
by comparing the results of different observers on the strike direc- 
tions for the whole Archean region of the state, some quite import- 
ant conclusions may yet be reached. At the time of writing investiga- 


THE ARCHAAN ROCKS. 465 


tions on this region are still in progress, and such generalizations 
would now be premature. Attention may be drawn, however, to the 
fact that the general directions of the strikes preserve a sort of paral- 
lelism to the sides of the somewhat irregularly shaped Archean area. 
Thus, on the Wisconsin, Wolf,’ Peshtigo? and Oconto,’ the strikes 
are northeastward, coinciding with the long boundary line on the 
southeast side; on the Black, Yellow, and lower Chippewa, the di- 
rections are northwestward, corresponding in general to the south- 
western boundary line; on the upper Chippewa, and in the Penokee 
region, the strikes are generally north of east, corresponding with the 
Lake Superior side of the Archean area. Whether this correspond- 
ence has any significance or not, remains to be seen. It is quite pos- 
sible that the northwestward strikes of the Black, Yellow and lower 
Chippewa indicate the existence of a continuous band of Huronian 
(including then gneissic rocks and granites) which, curving around to 
the north and northeast, includes the quartzites of Rice lake, in Bar- 
ron county, and joins finally with the Iron Range series of Ashland 
county. The remaining northeastward strikes, on this view, would 
be those of the original Laurentian nucleus. 

It has already been said that most of the rocks of the main Archzean 
area are referred to the Laurentian. This is done partly because of 
their general lithological characters, but more especially because 
they are found near Lake Superior, and also near the Michigan bound- 
ary, in Oconto county, underlying unconformably other metamorphic 
beds, chiefly of a slaty character, which, from their relations both to 
the Copper-bearing series and Silurian sandstones of Lake Superior, 
and to the Potsdam sandstone of Central Wisconsin, quite evidently 
occupy the horizon of the Canadian Huronian. When these relations 
are taken into account with their great resemblance in lithological 
characters to the typical Canadian formations, from which they are 
but little removed, and with which they are indeed quite probably 
continuous underneath the waters of Lake Superior, the reference of 
the two Wisconsin series of crystalline rocks to the Laurentian and 
Huronian seems unavoidable. 

The undoubted Huronian beds of Wisconsin lie entirely without 
the district which is the object of the present report. Those lying 
within the district, on Black and Yellow rivers, already alluded to as 
doubtfully Huronian, are as yet too doubtfully so to merit further at- 
tention in this place. 

The only materials of economic importance yet known to occur 
in the Archean of Central Wisconsin are kaolin or rotted rock, and 


1 Manuscript report, E. T. Sweet. 2 Oral communication, T. C. Chamberlin. 


Wis. Sur. —30 


466 GEOLOGY OF CENTRAL WISCONSIN. 


building stones, especially ornamental building granite. Beds large- 
ly charged with the specular and magnetic oxides of iron occur on 
Black river, but, so far as known, contain too little iron to be sed as 
ores of that metal. Judging from the character of the rocks of this 
age in Canada, a great variety of materials of economic importance 
might reasonably be expected, including the precious metals, lead, 
copper and iron ores, all of which are found and profitably worked in 
the Canadian Archean. Small traces of precious metals have been 
found in quartz from Clark county. Details as to the kaolins of the 
Black, Yellow and Wisconsin rivers, and as to the ornamental granites 
of Yellow river and other places, are given on subsequent pages. 
Both of these materials are obtainable in large quantity, and are des- 
tined to become important factors in the industries of the state. The 
red granites are quite extraordinary in their fine qualities, and are 
hardly to be equaled by any in the country. 


II. Local Details. 


The various rock exposures belonging to the main Archean area 
which have been examined by the writer, are chiefly in the vicinities 
of the three main streams, the Wisconsin, Yellow and Black, and 
their tributaries. A corresponding grouping of the detailed descrip. 
tions is here adopted, the valley of each stream being followed up 
wards from its southernmost crystalline-rock exposure. 


Urrer Wisconsin VALLEY. 


At Whitney’s Rapids, near Point Bass, on the 8. W. qr. of Sec. 10, and the N. W. 
ee 8 qr. of Sec. 15, T. 21, R. 5 E., oceur the southernmost exposures 
ioe of crystalline rocks on the Wisconsin river. They are here con- 
| MY) fined entirely to the river bed, the horizontal Potsdam sandstone 
Bh My) overlying them in the banks. The following sketch map serves 
i #/ | to show the occurrence of the various outcrops at this point. 

The southernmost exposure seen, and this only at unusually low 
stages of the water, is a low rounded one of quartzose gneiss (869), 
a few square yards in area, in the river bed at the point E of the 
map. Ten paces up the stream from here is a similar exposure 
of a greenish-black, pyritiferous, homblendic rock (870), traversed 
by pinkish felspathic veins, and striking N. 50° E.,!with a nearly 
vertical dip. Continuing northward along the bed of the stream, 
-| between the western shore and the island D, we find occasional 
exposures of decomposing gneiss, which is, for the most part, 
concealed by water and river gravel. At about eighty paces, a 
section across the stream was taken, on the line C D of the may, 
NiMH EF ane et deen aelais wt a) one ee Se 

Wace eRe : erlaid by 2 to 6 inches of 
sandstone, the lowest layer of which, about 2 inches thick. is 


highly charged with pyrite, which, in places, excludes the sand 
All bearings are referred to the true meridian, 


Scale, 1 mile to the inch. 


THE ARCHZAN ROCKS. 


entirely. The upper sand- 
stone layers are coarse and 
brownish-colored, and lie in 
ti large, flat slabs, giving the 
‘a. river bed, for many rods, 
the appearance of a paved 
street. 2 
On the line A B of the 
map, a section was meas- 
ured across the stream, 
which is shown in Fig. 4. 
At the southeast end of this 
section a vertical cliff ‘of 
heavily bedded sandstone, 
35 feet high, forms most 
of the river bank. Be- 
neath the sandstone, 


Sian WwW. 


Srction Across SipE CHANNEL oF WISCONSIN River, Near Point Bass, Woop County. 


of Wisconsin River JO paces 


KS gneiss shows for about 5 
os N feet down to the water's 
g edge. Its upper portions 
ey are altered to a soft kaolin, 


about 2 feet in thickness. 
Immediately at the foot of 
the cliff runs the main 
channel of the river, here 
about 400 feet in width. 
Beyond it to the northwest, 
a series of low outcrops of 
gneiss alternate with nar- 
row water. channels across 
the remainder of the river 
bed. The first exposure 
beyond the main channel 


Led of side channed 
Sandstone laver 2° 


Decomposing gnezssic 


A 
5 


NA 


Sol : 


x 
My = iS was not reached. The next 
PE SN : ese) 
Ssyes showed a coarse - grained, 
SR g N pink- white-and-hlack-mot- 
AD tled, quartzose, gneissoid 


granite (864), striking N. 42° E., and dipping north- 
westward 70°, with marked bedding planes. A second 
set of joimts, much less marked, strikes N. 50° W., 
and dips 80°N. E. The quartz of this rock is hyaline, 
and in fine grains aggregated into large blotches; the 
mica is blackish and fine-grained, and aggregated along 
certain lines; and the felspar is both white and pink, in 
large facets. The weathered surface is brownish and dull, 
with a white undercrust, and deeply pitted from kaoliniza- 
uon of the felspar. Quartz veins, a few inches in width, 
traverse the exposure in an east and west direction, stand- 
‘ing vertically. 

The next exposure to the northwest on the line of the 
section is 71 feet wide and of the same rock (865) as the 
last, with rather more felspar, and showmg the same 


“SINDOO GOOM ‘SSVG INIOG UVIN UTATNY NISNOOSIM FHL ssowoy NOTLOAg 


wen buryitjys ss2z2ug 


24 svds]27, 


224 ZPLDIGD U2 


MW OL Suddip pup 


TW J/?]9 au ORS puDe 


s3 
a 

TSS 
SSS 

Y Ys 
ES 
xe x s 
g iy y 

~ 


467 


y OL 


468 GEOLOGY OF CENTRAL WISCONSIN. 


bedding. A red felspathic vein was noted, 2 inches wide, dipping 70° N., and also the 
same east and west quartz veins as before. Towards the northwest end of this ex- 
posure the gneiss is quite thoroughly decomposed into a crumbling, earthy-textured, 
brown- and white-blotched material, showing still a few mica flakes and quartz granules 
in the interior, and containing 4.96 per cent. of water. The same partly kaolinized 
rock is found all along the section until the west bank of the river is reached, showing, 
however, still quite plainly the lamination and bedding planes of the unaltered rock, the 
dip and strike remaining the same. At the foot of the west bank, which is about 20 
feet in height, unaltered quartzose granite shows, with north and south quartz veins 14 
inch thick. Above this, and some few feet above the water level, fine, white, soft kaolin 
shows in a little swamp, and above this again are scen a few thin layers of the sand- 
stone. 

On the N. W. qr. Sec. 10 are openings in the river bank, here some 20 feet in height, 
showing a considerable quantity of white kaolin. The various exposures are at ditfer- 
ent levels, and may indicate a thickness of as much as 15 feet in some places, but as the 
clay is merely an alteration of the gneissic rock in place, it forms no continuous bed, 
the less altered portions of the rock occasionally rising entirely through it. At the 
principal opening 22 inches of soft, bluish-white clay were noticed. The following are 
analyses of samples from this place: 


861. 862. 
aa co oF 
A B A B 
Pitas, saceevaeatnyeseeeueeens 1.25 2.81 1.51 1.54 
Sod diandeetcuars asia Agen s Soe .08 trace -81 22, 
PON: aia asualec cages See peace 2.88 sae dead eees 
Weaater ssnnawknec ee aeoewe 8.69 


861 A is the raw kaolin from the lower part of the exposure; 861 B is the fine or ka- 
olinite portion of 861 A, separated by levigation. Nos. 862 A and 862 B are, in like 
manner, raw and washed clay from the upper part of the same opening. The amounts 
of alkalies are considerable, and no lessening in their percentages appears to be effected 
by levigation. The state of oxidation of the iron was not determined, but it would ap- 
pear to be chiefly in the protoxide state, judging from the color of the clay. These facts 
would indicate a less thorough kaolinization here than at other places in the vicinity. 
Immediately above the kaolin openings are two feet of coarse, brownish, friable sand- 
stone, whilst below it, down to the water's edge, gneiss in decreasing stages of decom- 
position is seen. At the foot of the bank is a low exposure of unaltered, fine-grained, 
light-colored gneissoid granite (868). The three ingredients of the rock are all distinctly 
visible, the felspar being both pink and white, the latter without apparent striations; 
the quartz is abundant, in hyaline grains; the mica is aggregated into layers and pro- 
duces a greasy feeling on some surfaces of lamination. 

At the foot of the rapids, on the west side of the Wisconsin, just above Port Edward, 
on Sec. 25, T. 22, R.5 E., a rather coarse grained, mottled, red-weatherig gneissoid 
granite (879) is exposed. A distinct parallel grain is perceptible, with corresponding 
bedding joints, which strike N. 45° E. and dip 50° N. W. Other joints, which make 
large smooth faces, strike N.75° KE. About 50 feet further up stream is exposed a coarse- 
grained, pinkish, highly felspathic rock, which shows a very distinct, sometimes con- 
torted, lamination, trending in the same N. 45° H. direction as before. In this rock 
the mica is nearly excluded by the felspar and quartz, which themselves are largely 
separated into distinct bands. In places much pyrite is present. Fifty feet further a 
low exposure shows an apparent N. 60° W. strike, but this seems to be due to numer- 
ous close veins running in this direction, for a few fect beyond, the same strike direc- 
tion as before observed reappears, accompanied now by a southeast dip, in a fine 


| 


THE ARCHZAN ROCKS. 469 


grained, greenish, decomposing, pyritiferous, mica-schist (S81). At the fall at the up- 
per end of the channel the rock is hard, very fine-grained, light-colored, distinctly banded 
gneiss (882), containing much quartz and greenish, greasy mica along the lamination 
planes. The northeast strike and southeast dip (50°) show here very plainly. 

It would appear that we have in these exposures the synclinal line at which the north- 
west dip of all the beds further down the river gives place to the southeast one which 
prevails for many miles above. 

Continuing now along the west bank of the Wisconsin, we note next an occurrence 
of kaolin on the land of Mr. L. P. Powers, lot 5, sec. 24, T. 22, R.5 E. The kaolin 
1s exposed naturally in the river bank at several points, and has been at one place laid 
bare by digging,’ several carloads having been sent away for trial. The exposures are 
some ten feet above the river at low water, and show an apparent thickness of about 
three feet. Much of this is pure white, plastic clay, easily removed with a spade, but 
in many places, and especially towards the base of the exposure, it grades into a par- 
tially altered rock of varying degrees of firmness. In much even of the perfectly soft 
clay the lamination planes ot the unaltered rock. are still distinctly to be seen, and thin 
plates of solid quartz remain in their original positions, dipping east of south, at about 
65°, Where these lines are so distinct the clay is frequently of a bluish cast, and then 
appears to be less refractory than usual. All of it tends to be stained superficially by a 
brownish oxide of iron, which may be due to the infiltration of ferruginous waters, and 
is not in sufficient quantity to affect the value of the clay. In a few places, however, 
large dark-reddish patches are seen imbedded in the white clay, and are undoubtedly 
due to the presence of a large and pernicious quantity of iron oxide. Immediately 
above the kaolin is found a layer, 14¢ feet thick, of quartz fragments, mostly angular, 
and evidently derived from the decomposing rock just below. Above this in a few 
places are to be seen one or two thin layers of crumbly, brownish sandstone, a remnant 
of the sandstone which overlies the crystalline rocks everywhere in the vicinity. Above, 
again, is found the soil, three feet in thickness. Below the kaolin, at the water's edge, 
low exposures of unaltered gneiss appear. A series of specimens for analysis obtained 
from this place yielded the following results: — 


822 823 824 825 

“A B A B A B 
Silica ........00- 20689 dwacn. seuss Meer T0225: ase 69.34 
Alumina ........ WB sOB~ uieee: Ohba Creea T7408. dace 19.19 
Tron peroxide..... WD, © sasstesecs DO B4 ica BB. Tae 1.75 
Times o 2 occ sa WOL (semen. Deeee. tener POBU nates 44 
Magnesia ......-. WO” cancer, eee Cases, 1549. cme 39 
Potash........+-5 2.49 1.21 2.30 1.96 1.69 2.33 3.80 
SOda: ienonevawes -10 trace trace trace .89 ~=.10 2.48 
Water .......... 5.45 8.84 ..... 6.30 5.61 8.84 2.67 
Carbonic acid..... 2 -Secckia’) Genie GiSedie,  eneete sets cs 
9986" sel gl Cee. saa 99.76 .... 99.51 
Specific gravity... 2.55 ..... 0 veeee cease 2.50 cee io 


829, A is from the exposure furthest down stream, and was analyzed just as taken 
from the ground, after drying at 100°. It represents a thickness of about three feet. 
Tt will be noticed that the alkali is chiefly potash, a fact which seems to be attributable 
to the greater difficulty with which the potash felspar decomposes, both potash and soda 
felspars entering into the composition of the gneisses of the vicinity. The small trace 


1 This xaolin has been much farther developed since the time of my examination in 1874, 


470 GEOLOGY OF EASTERN WISCONSIN. 


of carbonie acid remains as an indicator of the mode of decomposition which has led to 
the formation of the kaolin. 822 B is the fine portion of the same clay separated by 
levigation in the laboratory from the admixture of coarse sand composed of quartz and 
undecomposed felspar fragments, the former predominating. The smaller percentage 
of alkalies is due to the removal of the felspar fragments and mica flakes. 823 A and 
823 B are raw and washed clay from the next exposure above, along the stream. A les- 
sening of the alkali percentage is again to be observed in the washed clay. 823 repre- 
sents an apparent thickness of nearly three feet. 824 is from the exposure furthest up 
stream. It 1s quite soft and clayey, but in places retains the rock lamination to a 
marked degree. 824 A and 824 B are respectively the raw and levigated clay. It will 
be noticed, that, although retaining the rock structure, this clay is yet pretty completely 
decomposed, the only point indicating alack of thorough decomposition being the larger 
amount than usual of soda. 825 is a still firm, partly decomposed rock from the same 
place as 824. It is of a dirty white color on the exterior, nearly pure white on the inte- 
vior, quite porous, has an evident gneissoid texture, and is speckled with small flakes of 
silvery mica. With the exception of this mica no distinct constituent minerals can be 
seen with the naked eye; with a magnitying glass, however, a fresh fracture reveals in 
a few places minute grains of quartz and undecomposed orthoclase felspar. The large 
tenure of alkalies, especially of soda, and the small amount of water, indicate the only 
partial decomposition. 

Appearances would indicate the existence of a considerable body of kaolin at this 
point. Since my examination the locality has been much further developed and a large 
number of fire brick made. In 1875, Mr. E. T. Sweet, of the Geological Survey, vis- 
ited the place and found that no care was taken to select the clay, nor was it put 

through any washing process to separate the unde- 
Fig. 5. composed portions. He was informed that woodash 
was used largely to counteract the shrinking of the 
clay on burning; an addition, which, of course, in- 
troduced the ingredient most to be dreaded. Asa 
result of this method of manufacture and lack of se- 
lection, a very great variation was observable in the 
quality of the bricks, some even showing a tendency 
to agglomerate in the kiln. The clay from this local- 
ity has also been largely shipped raw to Milwaukec 
where 1t has been used by the Iron Companies and 
Gas Light Company. In 1874, about one thousand 
brick were burned for the Gas Light Company from a 
mixture of the Grand Rapids kaolin and pulverized 
fire-brick, and were found to be of the very best qual- 
ity.' A brick made in this way, and procured for me 
146 by Mr. 8. G. Lapham, yielded 2.06 of potash and 
0.31 of soda. It presented a peculiar jagged, porous 
Vicinity or Grand Rapips, Appearance on a fracture, with blotches of a white 
Woop County. porcelain-like substance, and was said to be an excel- 
Scale, one mile to the inch. lent brick. At the Bayview Iron Works? the clay 
has been tried raw, and found very refractory. 
Bricks made from it and used here were found to vary very much in their refractoriness, 
some being extraordinarily refractory, others succumbing readily to the heat. 

On Mr. H. Canning’s land on the west half of the N.E. qv. of See. 26, T. 22, R. 5 
E., several pits and a well have been sunk into decomposing rock and kaolin. Speci- 
mens from here yielded the following analytical results: 


1 Letter from Dr, I. A. Lapham, Milwaukee, Nov. 13, 1874. 2 Letter from Mr. J.J. Hagerman. 


THE ARCHAAN ROCKS. 


826 
“A B 

DICH snyienin nc sawnee wanwanhatarr 

AM WM ctisee Pose aie sides ga acne tigi mk 
Oxidevol irons. .s0 ox « weaawantaenea.e 1.93 

NING feinaks. aoa oes ates aus staee eee syne 
Magnesian.sives iow coed goes phase ates 
Potas hia: ses acne ye owas eau Abyeeiots 1.84 2.65 
Sod di dctiducadia eeane tiie haan shaded 27.21 
Water: a sitaceiiaiienee seas ack singe suave wees 7.96 
Pine Clay suaigeriany wea voces ean ees 

Coarse residue........scceseeeeeees 


826 A and 826 B are the raw and washed kaolin from Mr. Canning’s well; 827 is 
washed clay from the two pits on the same land, several hundred feet from the well; 
828 is the fine clay levigated from an ex- 
ceedingly white unbaked brick, said to have 


Fig. 6. 


> 


NOY 
4 
wd 
ee 
g 5 
2S 
G 
v8 
S28 
ae 
a 
q 


AM 


well, 


stone. 


Scale 20 feet to the inch. 


2 Embankment 


Kaouin AT GRAND RApips. 


(Fig. 6.) 


Strike NV 55Z 


preissrc 


been made from clay from Mr. Canning’s 


The next rock and kaolin occurrences 
§ that we note in ascending the Wisconsin 
are those in the vicinity of the cities of 
Grand Rapids and Centralia. The localities 
are shown on the sketch map, Fig. 5. 

Here the river makes a long stries of wild 
rapids over gneissic rocks, which on the 
shores, at short distances from the water, 
appear at several points altered to kaolin 
and overlaid by a few, thin layers of sand- 


One of the most instructive occurrences in 
the vicinity is to be seen on the roadside in 
the city of Grand Rapids, near the Rahblin 
House (Point A on Fig. 5). 
ting has been done into the bank for grad- 
ing the street, and kaolin, decomposing 
rock, and overlying sandstone laid bare. 
The following is the section obtained here 


Here some cut- 


Aspecimen of decomposing gneiss (816), 
occurring beneath the sandstone, yielded: 


N Pits hccciad wicsecliceaees 7.16 
pare Rodel face cas deat clase an bec ets 5.02 
RR bey CL 3.55 
N N The very partial nature of the decompo- 
3 R sition is thus rendered evident. In appcar- 
3 8 ance however, nearly all resemblance to the 


original rock has been lost, the color being 


472 GEOLOGY OF CENTRAL WISCONSIN. 


a dirty white, and the interior, though still frm and hard, of a somewhat earthy tex- 
ture. In some fragments a few minute grains of unaltered felspar can be detected 
with the magnifier. 

From the gneiss exposures shown at the water’s edge in the sketch just given (Fig. 6), 
the following measured section was taken entirely across the great ledges of gneiss 
which form the Grand Rapids of the Wisconsin. This section runs N. 20° W., on the 
line A B, or at right angles to the general trend of the layers, which is usually quite 
plainly to be seen. The exposures are not entirely continuous along the line of section, 
but are nearly so, and gaps could he filled with ledges a little distance on one side or the 
other, At the time of our examination, the river was low, and an unusual amount of 
rock laid bare. The measurements given indicate horizontal widths. Since the general 
dip is southeastward the first beds of the section are the highest in the series. 


Feet 
1. Gneiss: at the beginning of the measurement (833) coarse-grained, distinctly 
laminated, black-white-and-pink-mottled; striking N. 80° E., dipping 60° 
S.E. The mica of this rock is greenish and brownish, and aggregated 
into large blotches; the felspar is both pink and white, the latter not plainly 
striated, and occurring in large facets; the quartz is abundant and limpid. 
Pyrite is present in small quantity. Twenty-five feet from the beginning, 
the felspar is much increased in quantity (834). At fifty feet the grain of 
the rock becomes much finer, and the mica is largely restricted to the sur- 
faces of the quite distinct laminz (835). This variety gives place soon 
again to a coarser kind (886), similar to that at the beginning of the section 
(833), but with the quartz somewhat more prominent. At seventy feet the 
bedding directions are quite plain and show a strike of N. 75° HE, and a dip 
of 60° 5. E. Here the rock laminz are contorted, and the mica very 
abundant, almost excluding the felspar. A few pinkish granite veins occur, 
from /4 inch to 2 mches wide, conforming to the bedding of the rock. The 
vein matter (838) is predominatingly of pinkish, flaky quartz, felspar being : 
subordinate, and the mica restricted to the sides of the vein, ............- 100 
2. Covered. DY WALL, Savina preweed stine sins teas pews ve Be Os cied pee Nee ALES 20 
3. Gneiss: at the beginning of the measurement coarse-grained, schistose, con- 
torted in places,’ pinkish-white, very quartzose, carrying pyrite (839), strik- 
ing N. 85° E. Twenty feet beyond, this changes to a finer-grained, dark- 
grayish, schistose kind (840), embracing some thin veins of white quartz 
and pinkish granite. At 30 feet, the strike is N. 80° E., the dip 65° 8. Ki. 
At 80 feet occurs a reddish granite vein six feet wide. The vein-matter 
(843) shows a fine-grained texture and dark reddish color, and appears to be 
a nuxture of very fine, pinkish felspar facets, and translucent quartz grains, 
no mica being apparent. At 100 feet the grain becomes coarser again until 
at 130 feet (844), the rock is again like that at the beginning of the section 
(833). Beyond, the grain again becomes finer (845), the pinkish felspar at 
the same time increasing in amount, and occurring to some extent in a por- 
PhyrilieMMaD Her}. «caw sansa wee wis. cages aealey arareneamneSidmadsann ods wee oe 170 
4,, Covered: Dy Wate asim <csenw seme ard aa mineend S808 Vase nek € 9440) e 4 dectune wad 250 
5. Hornblende rock (846): very fine-grained, highly crystalline, distinctly bed- 
ded; in places thin bedded; dark-colored or black; strike N. 60° E., dip 
GO? S Bay sa irniteno so teen asiacnioe eae emmy et ete ae ya ve oA eu < bee nl 20 
» Covered, onislands: wesestyas ee aababedetinilerccanctacowbuteiees ss galeee ds cecens 70 
7. Hornblende rock: similar to the last described, but much weathered and 
broken by joints; strike and dip obscure........... cc. cececececseuccece 20 
S. Covered ..seees edasrenens ois a eaisis olafe @ayeja sneer Bh sissies need ae ylanteeusiees's 35 


ay 


THE ARCHZAN ROCKS. 


9. Red granite (847): medium-grained, structureless, pinkish to red, highly fels- 


Fie. 7. 


pathic. By following the strike 
directions south-westward for 


some hundreds of feet, the junc- 
tion between this and the preced- 
ing dark-colored rock is found 
on a large water-worn surface 
near the dam at the Grand Ra- 
pids foundry. Here the two rocks 
are seen to interlock in a curious 
manner, the granite occurring 
in large masses, entirely sur- 
rounded by the other rock. The 
contrast between the bright red 
color of one, and the black of 
the other, makes their irregular 
junction-line very marked. Fig. 
7 shows this junction line. Fig. 


JUNCTION OF GRANITE AND HORNBLENDE Rock. 


Scale 100 feet to the inch. 


8 is the part of Fig. 7, at A, en- 
larged. 
were taken the granite (894) is 


somewhat deeper red in color and of coarser grain than on the line of sec- 
tion, its deep red color being due to the abundance of red felspar, which is 
sometimes in facets 1¢ inch in diameter, and is blotched with large patches 


of translucent quartz. 


The rock is a very handsome ‘one, and would have 


value as an ornamental building stone .......... cece cece eee e eee eens 


10. Hornblende rock (848): 
rather fine-grained, 
highly crystalline, dark 
colored; strike and dip 
obscure. Hornblende 
and a whitish felspar ap- 
pear to be the main in- 
gredients. Magnetite is 
present, and with a 
magnifier, can be seen 
in bright, metallic par- 
ticles. Quite coarse 
fragments are held up 
by the magnet. At 100 
feet this rock becomes 
very fine-grained (849), 


Where the sketches. 


val 


Ve 


aan 
ery 


473 


Feet. 


ENLARGEMENT OF PorTIoN oF Fie. 7. 
Scale 4 feet to the inch. 


and rises into large exposures, over which the dip needle stands vertical. fy 
11. Red granite (850): moderately coarse, pink to red; weathered surface bright 
red; much jointed; no bedding; similar to No. 9. The mica in this rock is 
very subordinate, and in patches of small flakes; the quartz is hyaline, in 
considerable blotches of granular appearance; the felspar is pink to red, 
bright-lustred, large-surfaced, and very abundant. ...-.++see-+ patentee 
12. Hornblende rock: fine grained, dark-colored, much jointed; strike and dip 


QUSCLULE ce vcccccecccerccersececsetene srensteneeenesaenereceer seer eee 


120 


57 


474 GEOLOGY OF CENTRAL WISCONSIN. 


Feot. 

13. Gneiss: first 4 feet is coarse-grained, pinkish, and quartzose (851), resem- 
bling that at beginning of section. This grades into a light-gray, coarser 
kind, which has a very jagged fracture, is less micaceous, shows whitish 
felspar predominating over pink, and only obscure lamination, and is much 
cross-jointed (853). At 100 feet the bedding becomes distinct, the strike be- 
ing N. 85° E., the dip 52° S. E. At 230 feet the strike is N. 85° E., the dip 
50° S. E., the rock (854) being coarsely mottled gneiss with much greenish 
mica and large-faced reddish felspar. At 280 feet the bedding is the same, 
and a small red felspar vein occurs. At 300 feet the strike is N. 70° E., the 
dip 55° 8. E. A fine-grained, red granite vein occurs here having the form 
indicated in Fig. 9. 


GRANITE VEIN AT GRAND Rapips. 


At 340 feet the bedding and lamination of the rock become obscure again 

and continue so for a hundred feet. At 360 feet numerous thin veins of 

quartz occur, and at 380 feet one of pure white quartz 4 feet wide. At 420 

feet are some large veins of red granite. One of these is figured in Fig. 9. 

At 440 feet the bedding becomes plain again, the strike being N. 85° E. and 

dip as before. The rock here (856) is much less micaceous and more fels- 

pathic than for some distance back, and is much weathered.............. 494 
TAS COUPEE vee het ee ween Bets hoy bel ek Ah Aletsch ch cot Seal Reaaed earayean argc anaenn eed pewter 190 
15. Granite: pinkish, jointed, without indications of bedding.......... 2.2... 40 
16. Gneiss: dark-colored; at 40 feet this changes to a rock (858) which closely 

resembles that at the close of 3 (856), and is moderately coarse, not very dis- 

tinctly gneissoid, with much hyaline quartz and large-faceted felspar. At 

60 feet a granite vein 50 feet long occurs in this rock, coinciding with the 

bedding, and striking N. 75° E., with a dip 50° 8. E. The vein matter 

(859) is a rather fine-grained, pinkish-red granite, weathering dirty brick- 

red, and showing in places a partial kaolinization. Fine grained translucent 

quartz and pinkish telspar make up most of this granite. Mica is present, 

bubinsverysuiall quantity ncxweas siren gm aeeus tag A sisfacbieis/ctrerssapeue suave re aune-s 130 
CGI BH GUL: usresk pace SPB as ast Sos Sra AIRE che Les Shea Se ceiaed a hon sana aA oreo EOS 30 
18. Gneiss: gray, with much black mica, similar to that of 16 (858). At 10 feet 

a granite vein 2 feet wide occurs, coiaciding with the bedding, which here 

shows a strike of N.73° E., anda dip 55° 8. E. Other smaller granite veins 

occur. Junction with the next rock concealed .........cc ee ceeeeceneceee 100 


THE ARCHAAN ROCKS. 475 


Feet. 
dark green- 

PERT Sraseceanrg nue cited wae 50 
is chulbnwie ew imine ce 120 
she Sal ibid 'Bieidiend Sy PUN A anaivenaverssm ua nmaicenn stag des Alaina teal atsavnects cca ate 40 

e ELLE” 5 

ZZ z_ 

ILLES. 

GRANITE VEIN IN GNEIss AT GRAND RapImps. 

22. Granite: fine-grained, light pinkish, slightly gneissoid; jointed. The three 
ingredients are all perceptible with a magnifier. The mica shows some 
tendency to a stringy arrangement ......-.. 6. cece cece cece ees e eee 805 

DBs NCOCCP OD: moses Sst daecd ad so ucsaand ainle- du etd sholow ned eavdseeesewkey “hein pavaety hewee elsties 45 

24. Granite: same as last described........ 0.60. cece cece eee cece eee ee ene 35 

25. Hornblende rock: strike N. 85° E., dip 75° 8 ....... cece eee cece e ee ee eee 10 

20: COVETED: % Kao 4 Bes AGS MOT SOR GS ERNE PAIR SEG ROUND Bclded, pre beni: sdave arecaeaialatens 150 

27. Granite: pinkish, gneissoid.... 6.6... cece etc e eee eee nnn ee eeene 50 

Total horizontal length of section.........cccec esses enn eeenee eee 2,519 
Approximate thickness of rocks exposed «0.6... ec. ee esses eee cena 2, 200 


From the foregoing details we may construct the generalized section of Fig. 11, the red 
granite of portions of the section being regarded as an intrusive rock. 

At the first dam below the wagon bridge at Centralia, on the west side of the river, 
a ledge of hornblende rock, 40 feet wide, occurs. This rock (884) is moderately coarse- 
grained, dark-colored to black, and appears to be composed of hornblende and a white 
felspar with much magnetite, the latter very distinctly visible, by the aid of the magni- 
fier, in lustrous grains. Quite coarse pieces are lifted by the magnet. On the river 
bank a short distance up stream, micaceous gneiss is exposcd, forming apparently the 


next layer. These beds are higher in the series than any of those in the section at the 


rapids. : abet 
At the pail mill, just below Centralia, is a large exposure of fine-grained, pinkish, 


gneissoid granite, containing much reddish felspar, and fine, glistening, greenish mica, 
with a stringy arrangement. 


476 GEOLOGY OF CENTRAL WISCONSIN. 


On the N. W. qi, of Sec. 5, T. 22, R. 6 E. (point D of map), on the west side of the 
Wisconsin, kaolin occurs on the land of Mr. C. B. Gar- 


ZN gee rison. The clay here is reached about 18 inches to 2144 
AAS ae feet below the surface, and has been exposed in places 
aa Ze for a distance of some rods, by “borrowing” for the 
aR ae railroad near by. Several grades are to be seen. In 
Z| ees some places the spade turns up a brilliant white article; 
Z, =.:5 in others, for the most part nearer the surtace, a kind 
265 that is largely stained with the brown oxide of iron; 
g23 whist at others again, the lamination of the unaltered 
aE rock is still distinctly perceptible in the soft clay, in 
= ee which cases it is more apt to showa slight bluish cast, 
A ES and many silvery mica scales. All of the clay is quite 
Beg gritty from the presence of undecomposed felspar and 
me quartz grains. Rounded, reddish quartz pebbles up to 
4£°° 1 inch in diameter, are occasionally to le seen. Tho 


depth of the clay at this place is said to be at times as 


Can Ss 
: gee much as 4 feet. Samples of the whitest kinds yielded 
A woe the following results: 
P 807 A $07 B s07 C0 
Pa 4 : 49.94 92.86 
BB see, Alumina sss ons «nese 3.43 36.80 2.08 
. 68 a Tronoxyd..........0- 0. 74 J) 74 
a Z 9 BES Lime.................. 64 trace 96 
S & 3° 3 Magnesia ........-++-.- SOU ssdeware .10 
es & 358s Potash................. '37 51 £28 
a ° Eee SO Ulais valianaie nana bigtnliers 07 08 05 
3 BEEE Water... cesses 5.45 11.62 2.53 
B 232 99.60 99.67 99.60 
a ez 5h . 2 
Pag Carbonic acid........... S01 CMaaxiem.. tute rege 
as 2 Specific gravity......... 2.52 Do aes 
35 E 807 A is the raw clay dried at 100° C.; 807 Bis the 
Faptes fine clay obtained from A by repeated stirrings and 
#5° washings; 807 C, the coarse residue from the washing. 
$°2 The composition of this residue is calculated from the 
223 two preceding analyses. Under the microscope it is 
a f2 seen to consist chiefly of angular fragments of quartz 
S23 from 735 to Ys inch in diameter, mingled with very fine 
E22 . fragments of felspar. The approximation in composi- 
eine tion of the roughly washed fine clay to typical kaolinite 
g028 is noteworthy. The unwashed kaolin (A) is composed 
Ee = of 32.7 fine clay (B), and 67.3 coarse residue (C). The 
aD oe following are the compositions of B and C expressed in 
Ss : = percentages of the unwashed clay (A). The manner of 


distribution by washing of the various ingredients of the 
raw clay is thus indicated, and the practical advantage to be obtained by washing 
shown: 


THE ARCHAAN ROCKS. ATT 


807 B 807 C 807 A 
DTIC 6 A a rsercuacet ann aoretc aed et eA ar 16.33 + 62.50 = 78.83 
AlUMIN Ay avacae ccneccr ea aYostorbadas sea sees 12.08 + 1.40 = 13.43 
Tron Ox G sis eg- dees 6 View 4 Siu Dies ees 24 4 0° = 74 
DaiiGidd-e hee Sas oh as haa Y Ree tnd Se nea 00 + 64 = 64 
Mapiiesiancitus tieusimsna cast Setereien Deranrwotinns 00 + 07 = .07 
Potiishieccion ten Woe oes aati ks lB 225) SS 37 
Sod at iii ea ostaueachiclens sae sede node ge x ote 03° + 04 — 07 
WAtel ve224 gcc.0 gona aiec sta ceuetemascie@ nceuccs 3.75 + 1.70 = 5.45 

32.50 + 67.10 = 99.60 


The most ferruginous clays seen at Mr. Garrison’s yielded 1.68 per cent. (808), and 
2.31 per cent. (809) of iron sesquioxide. These are apparently much more plenty than 
the white clay. About 10 rods from the kaolin openings, on the river edge, is a low 
outcrop of a highly micaceous, weathering gneiss (303). having a moderately coarse, 
jagged texture. The felspar of this rock is largely still brilliant, but little white kaolin 
patches dot the surface. Another outcrop near by shows a more highly felspathic kind, 
with very coarse, pinkish orthoclase. These gneisses closely resemble the prevailing 
ones in the Grand Rapids section, but are evidently much lower in the series than any 
of those. 

At the Green Bay and Minnesota depot, Grand Rapids, it is reported that in excavat- 
ing for a turn-table, first a few layers of compact sandstone were penetrated, then 5 to 
6 feet of soft white clay and decomposed rock. Near the center of Sec. 4, T. 22, R. 6 E. 
(point E of map), about two miles above Grand Rapids, on the east bank of the Wis- 
consin, on Mr. Rablin’s land, very white kaolin shows, overlaid by two feet of sand- 
stone. This kaolin has been used with success to line the furnaces at the Grand Rapids 
foundry. The following are analyses of samples from here: 


829 8281-2 
i 
A B B 
Oxide:OF 1rONs Haseweceutk haniiees shee tae ates 4.43 a ‘ne 
PObaSHG chau elo ea oe ewes Sum ee AEX By Basel aes 1.21 .87 38 
GOda wieetaass eetetidodeciecamiwdesaMsee ese -46 sees 08 


829 A and 829 B are raw and washed clay taken from the stock-pile at the foundry ; 
82815 is washed from a sample taken from the opening itself. 

On the line of the Wisconsin Valley Railroad, between Centralia and Junction 
City, are several low cuttings, which expose usually crumbling, and partially decom- 
posed, laminated gneissic rocks. The exposures are very poor and the rock is generally 
out of position. About 314 miles north of Centralia is a cutting 400 feet long, through 
a rather fine-grained, granular textured, pinkish granite (965). This rock consists of 
brownish, translucent. granular, glassy quartz, largely predominating; pinkish bright- 
lustered felspar; and fine black mica sparsely but uniformly scattered. 1t would dress 
readily, but shows some tendency to weather and iron stain. 

West of the railroad line, in the western part of T. 23, R. 6 E., sandstone occurs in 
places, sometimes capping the hills, sometimes low in the valleys, and lying evidently 
upon a very irregular crystalline rock surface. On Sec. 8, near the northwest corner of 
the section, a well passes through sand 6 feet, sandstone 214 feet, soft red and white 
kaolinized rock 20 feet. This is the greatest depth of softened rock that has come to my 
notice in Wisconsin. 


478 GEOLOGY OF CENTRAL WISCONSIN. 


At Conant’s Rapids, sections 18 and 17, T. 23, R, 


; Fra. 12. 8 E., Portage county, are large rock exposures in the 
QS FE J ‘bed and on the sides of the Wisconsin river. The 
\\ ee ISH! sketch-map, Fig. 12, shows the localities of the occur- 


\iaale Teo rences at this place, as also at the Stevens Point rap- 
: ids, above. 

On the west side of the river the rock exposures and 
rapids are found continuing further down stream than 
on the east, on account of the northeast strike of the 
rocks. Beginning at the foot of the rapids on the 
west side, we note first on the N. W. qr. of the N. EB. 
qr. of Sec. 17, a low exposure some 500 feet in length, 
under the river bank, No. I of map. The rock here 
(775) is a fine-grained, pinkish-gray gneiss, showing 
fine-granular, translucent quartz, predominating; fine- 
faceted white felspar, abundant; black mica in very 
fine separate scales, arranged in lines. The lamina- 
tion is quite close and distinct. The weathered sur- 
face of the exposure is brownish in color, smooth, ange 
highly polished by the running action of the river 
From this smoothed and brown-tinted surface numer- 
ous reddish granite veins stand out in bold relief, hav- 
ing resisted the eroding action more successfully than 
the surrounding rock. The bedding is not very dis- 
tinct, being obscured by many cross-joints; the strike 
is N. 81° E., and the dip N. W. 60° to 67°. Other 
18 1 quite prominent joints occur, bearing N. 55° E., and 

SkETCH-MAP sHOWwING LocaLITIES standing vertical, Numerous veins are to be seen 
ie Poche pie Liga) : pik here, both of white quartz, and of reddish felspathic 
Ibs. granite, varying in thickness up to several inches. 
One granite vein 5 inches wide trends N. 26° E., for 
a cistance of 50 feet. The vein matter (775) 1s a very 
fine-grained felspathic granite, in which all the ingredients can, however, be distin- 
guished. Numerous thin feeders extend from the vein into the rock around. The next 
exposure above, No. II of the map, is a large one, stretching across a side channel of the 
river, just about on the line beetween sections 8 and 17. The rock here (773) is a very 
coarse-grained, micaceous, granite, consisting of very large-flaked brilliant black mica; 
white, very distinctly striated felspar, in facets up to 1g inch by 14 inch in size; limpid 
quartz; some brownish-stained mica; and some little hornblende. In some places a 
very distinct tendency to crumble is perceptible, and then the mica is much iron-stained, 
and the rock is blotched with large patches of white, kaolinized felspar. Even where 
exposed to the running water this rock presents nowhere the peculiar smoothed and 
glistening appearance of the exposure below, hut on the contrary shows everywhere a 
rough, coarsely pitted surface. This is rendered the more striking by the innumerable 
reddish granite and white quartz veins which intersect the rock in every direction, mak- 
ing up nearly half of the exposure, for these having resisted better the weathering in- 
fluences, show the smoothed appearance alluded to, and stand out in relief from the 
lighter colored, jagged surface of the surrounding rock. The veins are from 1 inch to 18 
inches in width. The reddish ones are of granite, having a large predominance of red- 
dish felspar, which, in some of them, occurs along the sides of the vein free from ad- 
mixture, and in large crystalline surfaces. One vein 2'% inches wide showed alternating 
bands of white quartz, pink, coarsely crystalline felypar, and felspathic granite (777). 


Scale, one mile to the inch. 


THE ARCHEAN ROCKS. 479 


Exposure No. III of the map is on the road side in the &. W. ar. of the 8. E. qr. of Sec. 
8. The rock here is a fine-grained, light-pink, gneissoid granite (779), having the three 
ingredients distinctly visible, though fine, and showing a few whitish kaolinized patches. 
At No. IV of the map, are large exposures at the top of the bank and in the river be- 
low. Fig. 13 shows the occurrences. 


Fria. 13. 


Scale, 30 feet to the inch. 


At A is a bold exposure of smooth-jointed, fine-grained, light-reddish granite (780), in 
which red-stained granular quartz is the predominating ingredient, mica being very 
subordinate, occurring in fine brilliant brownish flakes, and showing a slight tendency 
towards a stringy arrangement. The numerous joints which traverse this rock strike 
N. 17° W., and stand nearly vertical. At B (782) is a coarse-grained, red-and-black- 
mottled, micaceous gneiss, striking plainly N. 69° E. This rock resembles that of No. 
III, but contains much more reddish non-striated felspar. Whitish kaolinized patches 
occur. Bounding this on the south, at C, and sharply defined from it, is a fine-grained, 
dark-greenish crumbling rock (781), having a marked E. W. lamination. This rock 
appears to contain, predominatingly, fine blackish mica, with which appears to be min- 
gled some fine whitish felspar (mica-schist?). Little pinkish felspathic threads traverse 
the rock. To the south of this again, at D, comes in a fine-grained, very compact, 
greenish, gneissoid granite (783), striking N. 70° E. and showing as constituents, fine- 

- flaked, blackish mica, pink and white felspar, and limpid quartz. 

Passing now to the east side of the river, we note first on the N. E. qr. of the 8. E. 
qr. of Sec. 8, near the foot of the rapids, and just above the mouth of Plover river, 
at No. V of the map, large, but low, outcrops of quartzose gneiss, bearing nearly 
east and west, dipping south 60°, and overlaid by 25 to 35 feet of horizontal sandstone. 
This point appears to be on the anticlinal line where the southeast dips of the Grand 
Rapids series give place to the northeast dips of the Conant’s and Stevens Point 
rapids. 

“On the N. E. qr. of the N. W. qr. of the same section (No. VI of map), large ex- 
posures begin, which extend up stream for a long distance, and show all along a very 
marked trend of N. 25° E.. The southernmost rock examined here is a fine-grained, 
dark-colored, highly micaceous gueiss, traversed by numerous large veins of reddish 


480 GEOLOGY OF CENTRAL WISCONSIN. 


granite and smaller ones of white quartz. In some of the veins, quartz, felspar, and 
yranite all occur separately, as, for instance, in the one shown in Fig. 14. 
The vein rock here :79914) is a fine-grained 
Fra. 14. admixture of quartz and pinkish felspar, mica 
being almost wholly absent. The vein, and its 
ramifications as well, are sharply defined from 
the wall rock. A short distance up stream from 
this vein the gneiss shows an exceedingly fine 
lamination, and becomes much contorted (799). 
*. The lamination is due in part to a general 
stratified structure of the rock, independently of 
its ingredients, but in part, also, to an aggre- 
gation of the fine black mica along the surfaces 
of laminee. The ingredients of the rock are fine- 
grained, colorless quartz, predominating; coars- 
er, pinkish, translucent quartz; black, shining, 
small-flaked nica, very abundant; and small-fa- 
Uy; ceted, white felspar. The exposure of contorted 
FJ 
/; 


( gneiss is quite abruptly limited up stream, by 
/+/ « large, pinkish granite mass, which stands 6 to 
yy y, ‘10 feet above the surrounding rock at No. VII 
of the map. The rock of this large vein (798) is 
“4, similar to that of the vein last described, but is 
somewhat more quartzose. Next above the 
/ granite vein is a fine-grained, felspathic gneiss 
(797), striking N. 35° E., dipping 80° N. W., 
and intersected by numerous cross-joints. Next 
above this are again high exposures of fine- 
, grained, structureless, pinkish granite (796), re- 
sembling the masses and veins further down, 
* but much larger in size. 

/ At VIIL of the map, fine-grained, greenish- 
brown gneiss (795) is exposed, striking N. 50° 
K., and dipping 45° N. W., and composed of 
Yf, silvery mica, pinkish felspar, and translucent 
/ _ quartz. A short distance above, this grades 
7, / into a, coarser kind (794), which is very plainly 
‘ laminated, in places even schistose, and carries 


Y YyVv 
, YY ‘ Y yy, VY, Vj small greenish epidote (?) veins. 

Yt fy YW J. t Stevens Point, on Secs. 
YL a ae 


ble exposures, which are, however, not so large 


s as those at Conant’s Rapids, a mile below. 
WO The localities of the main outcrops in the Ste- 
Li vens’ Point Rapids are shown on the map, Fig. 


Granite Quartz pass 12. At the point IX of the map, on the south 

eldspar line of See. 32, is alow exposure, at the water's 
edge, of a moderately course, laminated, brown- 
ish-stained micaceous gneiss (785), striking N. 
45° K., and dipping 70° to 80° N. W. This 
rock is composed of abundant brilliant black mica, which weathers brownish; coarse 
faceted, plainly striated, white felspar; and limpid quartz. The weathered surface is 


GRANITE VEIN AT Conant’s Barrps. 
Scale, 6 feet to the inch. 


THE ARCHAAN ROCKS. 431 
dark-brownish, and rough, and has underneath a whitish kaolinized crust. Throughout 
small white kaolin patches occur. This rock closely resembles that on the west side of 
Conant’s rapids (778). In the bank above, sandstone is exposed. 

Under the central abutment of the railroad bridge, and about 100 feet northwest from 
the exposure last described, oceurs another of the same rock, but somewhat coarser and 
less predominatingly micaceous. The bedding is the same as before, 

About 300 feet further across the strike, and now on the west side of the river, point 
X of map, is a large exposure of the same mottled micaceous gneiss, extending several 
hundred feet along the river bank. At the lower end of the exposure, the felspar sur- 
faces are very large and very finely striated (787), and the rock is more weathered than 
asnal, the ordinarily brilliant black mica being largely changed to a brownish tint, 
which affects the appearance of the whole rock. Reddish veins, composed almost en- 
tirely of coarse, cleavable felspar, occur, and also others in which the felspar is coarsely 
mingled with white quartz. The chayacter of the rock remains the same throughout 
‘the length of the exposure, as far north as the wagon bridge, the bedding throughout 
being very distinct, and showing a strike of N. 75° E., and a dip of 45° N. W. A short 
distance west from the river bank, at this place, horizontal sandstone is exposed in the 
railroad cutting and in a large quarry. 

The crystalline rock series at Conant’s rapids and Stevens Point may be briefly de- 
scribed as consisting of beds of highly micaceous gneiss, dipping northwest from 45° 
to 80°, trending N. 25° to N. 65° E., with which are interstratified some layers of a 
finer grained, less micaceous gneiss, and penetrating which are reddish granite veins 
and masses. Compared with the gneisses of Grand Rapids, those just described are 
found to be more highly micaceous and usually coarser grained. They differ from the 
Grand Rapids rocks also in having as a prominent constituent a triclinic (striated), 
whitish felspar, and in having no interstratified beds of dark-colored, fine-grained horn- 
blendic rocks. The Grand Rapids rocks dip southeastward, those of Conant’s rapids 
and Stevens Pojnt, except at the southernmost point, northwestward, the strikes in 
both cases heing northeast, but not always equally so. The anticlinal line cannot be far 
from the great bend and long southwestward stretch of the Wisconsin in southern 
Portage and Wood counties, and to this anticlinal line the peculiar change in the course 
of the river evidently hears a close relation. See, in this connection, Atlas plate XV of 
Area F, and its accompanying north and south section. 

On Plover river, in the N. E. qr. of Sec. 12, T. 24, R. 8 E., three quarters of a mile 
north of Jordan, is a low ledge of moderately coarse, pinkish. porphyritic granite (806). 
The felspar is in facets up to 1% inch in diameter, both white and pink, the former finely 
striated; the quartz is both hyaline and abundant; the mica is in medium-sized, brilliant, 
black flakes. Numerous white kaolin patches indicate a tendency to decompose. 

On the line of the Wisconsin Central Railroad, between Stevens Point and Junc- 
tion City, are several small rock cuttings. One of these, on Sec. 22, T. 24, R.7E., is 
in a pinkish, fine-grained granite (800), showing pink and white felspar, quartz, and 
fine black mica. Another, one mile below Junction City, on Sec. 1, T. 24, R. 6 E., isin 
a decomposing, medium-grained to fine-grained, whitish-weathering gneiss (801, 802, 
803, 804), composed chiefly of quartz and pinkish felspar in blotches, with a greenish, 
greasy mineral (chlorite or altered mica) on surfaces and in fine strings throughout. 
Pyrite is present, and white kaolinized blotches are characteristic. The more decom- 
posed portions show a schistose tendency, and in all there is a marked payrallel grain. 
The bedding structure shows a strike of N. 22° E, and a dip of 80° E. These are also 
the directions of the grain of the rock. On Sec. 2, half a mile from J unction City, isa 
small exposure of a decomposed brick-red, ferruginous, schistose gneiss (805), showing 
ou the interior numerous shining mica flakes, but too far altered to show any other 


minerals. 
Wis. Sur. — 31 


482 GEOLOGY OF CENTRAL WISCONSIN. 


On the line of the Wisconsin Valley Railroad, between Junction City and 
Knowlton, there are numerous small rock cuttings, chiefly in more or less decomposed 
gneissic and schistose rocks. The drift along the line is very light, and every little cut- 
ting exposes the rock. Half a mile north of Junction City, in the north part of Sec. 2, T. 
24, R.6 E., small exposures are seen for a distance of 300 feet, of much decomposed, fine- 
gramed, dark-colored mica-schist or micaceous gneiss. A similar rock shows a quarter 
of a mile further north, on Sec. 35, T. 25, R. 6 E. Here the rock is a fine-grained, very 
closely laminated, blackish schist (963). The predominating black mineral is partly horn- 
blende, partly mica. In the north part of Sec. 35, 144 miles from Junction City, a cut- 
ting shows for 50 feet at its south end a blackish schist, similar to the last described, in 
all stages of decomposition, even to a light colored clay. The lamination lines are 
marked, and bear N. 50° E. At the north end of the cut a decomposing, fine grained, 
arenaceous, light-colored schist (962) is exposed, composed apparently chiefly of fine 
granular quartz. On some of the lamine light-colored, altered mica is perceptible. 
One-fourth mile further north is a small, indefinite exposure of the same arenaceous 
schist. In the east part of Sec. 26, 214 miles from Junction City, the railroad cutting 
makes an exposure 200 feet long and 8 feet high. The rock (959, 960, 961) is a finc- 
grained, dark-greenish to black, calcareous mica-schist, or gneiss, showing very fine and 
uncontorted lamination, and a peculiar knotty appearance in places from the occurrence 
of lumps of quartz and calcite between the lamin, which are then bent around these 
nodules. The preponderating black mineral is in fine shining scales, and appears to be 
chiefly mica. Veins, 14 to 14 inch in width, of a greenish, translucent mineral (epidote ?) 
oceur, The lamination of the rock causes it to break out in columnar forms, some of 
the columns reaching a size of 8x 4x4 feet. The apparent dip is N.N. W. 85°. A 
somewhat similar calegreous gneiss occurs on Black river in Clark county. Three miles 
from Junction City, on Sec. 24, T. 25, R. 6 E., is a small exposure of a fine-grained, 
white-weathering, crumbling, arenaceous, talco-mica-schist (858), showing very fine 
lamination, and closely allied to the light-colored rock seen in the cutting 114 miles 
north of Junction City. With a lens, fine-grained quartz is seen to be the predominat- 
ing constituent. Half a mile farther north is an indefinite exposure of a fine-grained, 
dark-colored gneiss, or mica-schist, similar to that seen in the large cutting on Sec. 26. 
About 4 miles from Junction City, on See. 18, T. 25, R. 6 E., light-colored, fine-grained, 
arenaceous mica-schist (999) is again exposed, for 300 fect, on the side of a cutting. 
The lamination planes strike N. 30° E., and dip 80° 8. E. A few small masses of milky 
quartz, and reddish felspathic veins are included, and, in places, stand out in relief from 
the swrounding decomposed rock. On the north part of Sec. 13, 414 miles south of 
Knowlton bridge, an indistinct exposure of pinkish, weathered granite occurs. Another 
indefinite exposure of the same rock occurs a quarter of a mile further north, on Sec. 12. 
In the north part of Sec. 12, 3.7 miles south from Knowlton bridge, the following section 
occurs in a low cutting, the rock exposures not rising more than one or two feet above 
the railroad track, and being considerably out of position. The section begins at the 
north end of the exposure: 


1. Granite (992): very fine-grained, red colored, felspathic; partly kaolinized aces 
on surface; penetrated by veins of white quartz.............0.. cece eee 2 

2. Decomposed gneiss: clayey; containing occasionally seams of partly kao- 
linized reddish granite (993)............ Bedsandearash OVAe Avivo rain aia oaalonaetets 50 

Bi Oia: WIG ana Bind. aco sStaciee since ar ahhaias Bead wacivn Pee Mu gtonaachaw Make Meee 1 

4, Granite (994): partly decomposed; very fine-grained; granular, pink col- 
ored, quartzose; crumbles in fingersto a sand............cccceceeeeeee 8 


THE ARCHAAN ROCKS. 483 


Ft In 
6. Granite (995): similar to No. 4; holding veins and masses of quartz. ..... 10 
7. Decomposed gneiss: similar to No. 5... 66. cece ccc cence eee ee ecees 20: as 
8. Granite: light-pinkish, felspathic............... 000 e cece eee eee e eae ne 4 
9. Decomposed gneiss: similar to No. 7.......- 2 cece eee cee e eens 30 
10. Red felspathic sean: altered; standing vertical ..... ....... 2.00 ee ee eee 2 
11. Dark-green rock (997): composed almost entirely of a fine, flaky mineral, 
which appears like an altered amphibole................00 ce eeeeeeeee Oo ke 
12. Granite: reddish; resembling No. 6...... 066.006 eee ee ce cece eee eee aw 6 
13, Decomposed gneiss: contorted; holding seams of quartz and partly altered, 
fine-grained granite... .. Pius Mend eRe saa ae We sowie ais Galan e Swans 75 
HROteiliass Ses Rsestcaatiees? seed Secs aye Sane, dene any panossyaie cuayeo eset ceranaes or SeNoparanaseh 204 10 


At the south end of the railroad bridge at Knowlton, in the north part of Sec. 29, T. 
26, R. 7 E., is a cutting 100 feet long, and 5 to 10 feet deep, through rock, The northern 
portion of the cut exposes a fine-grained, blackish, hornblende schist (890), having a 
distinct crystalline texture, and resembling much some of the hornblendic beds of the 
section at Grand Rapids. The apparent strike of this rock is N. 55° W., and the dip 
60° N. E. Its horizontal width at right angles to this strike direction is about 40 feet. 
The remainder of the cut is in medium-grained, highly crystalline, grayish, granitoid 
rock (889), which weathers white. Quartz, white felspar, and dark-colored, small-flaked 
mica, the latter showing a slight stringy arrangement, can he seen with a lens. Some 
of the dark-colored mineral may be amphibole. The apparent bedding of this rock co- 
incides with that of the preceding; and its horizontal width is also about 40 fect. 

On the wagon road between Knowlton and Mosinee, on the east side of the Wis- 
consin, several small and indefinite exposures occur of decomposing fine-grained rocks, 
resembling those observed on the line of the Wisconsin Valley Railroad. Two miles 
north of Knowlton, where the road ascends a high ridge, exposures occur of a fine- 
grained to aphanitic, dark colored, slaty rock (892.) This rock is pyritiferous, and dis- 
tinctly attracted by the magnet in coarse powder; it weathers with a dirty-whitc, earthy 
surface. At 3.7 milcs north of Knowlton, another exposure, of a similar rock,-occurs in 
the road. This rock (968), according to Mr. Wright's microscopic examination, is com- 
posed of chlorite, altered felspar and magnetite. These exposures were all too poor to 
show any definite bedding structure. 

At Little Bul) falls, on the Wisconsin river, at Mosinee, Sec. 29, T. 27, R. 7 E., 
Marathon county, are quite large rock exposures. The river here is divided into two 
widely separated channels by a high rocky island about a quarter of a mile in width. 
On its northeast end this island is itself cut by several smaller channels, dry at low water, 
which show high walls of bare rock. Most of the water of the river passes through the 
easternmost channel, which in one place, for a distance of 130 feet, is a gorge only 35 
feet wide. The main fall of the river was formerly in this gorge, but has lately been 
moved down stream by a dam erected below. The rocks of the various exposures at 
this place ae all closely allied and may be designated by the general term of syenite. 
They are all characterized by the presence of much greenish-black amphibole, and white 
striated felspar, the quartz, though present, being always subordinate. Two general 
kinds were noted. ‘The prevailing rock (896, 898, 900) is a moderately coarse-grained, 
highly crystalline, syenite, with a greenish-gray, mottled appearance, and without 
any sign of-parallel arrangement of the various ingredients, which are uniformly 
intermingled. On a weathered surface this rock appears greenish to white, the 
latter color being due to a kaolinization of the felspar. On a fresh fracture the two 
main ingredients are readily perceptible to the naked eye. The hornblende is usually 
of a bright-lustred, greenish-black color; the felspar facets are commonly white 


484 GEOLOGY OF CENTRAL WISCONSIN. 


translucent, and beautifully striated, as can readily be seen with an ordinary lens. More 
rarely pinkish felspar occurs. That variety of this rock which has a medium degree 
of coarseness presents a very handsome appearance on a dressed surface; and, since 
it shows no tendency to iron -stain or decompose, might make a valuable building 
stone. The second variety found here (897, 905, 903) is very much finer in grain, and of 
a dark.greenish-gray color, showing the crystalline texture only under the lens, and 
then not plainly. It is evidently merely a phase of the coarser rock. It occurs both 
in small imbedded patches (879) and in large, distinct outcrops (905, 903). According 
to the microscopic examination, these finer kinds, whilst having the same ingredients as 
the coarser, show a larger proportion of hornblende, and may be designated as ‘‘ horn- 
blende rock."’ Chlorite appears to occur in all, more especially in the finer kinds, as an 
accessory. 

For the most part the bedding of the Little Bull rocks is indistinct. In two places, 
however, it is plainly to be seen. One of these is on the west wall of a dry side chan- 
nel near the head of the main island. Here very marked planes dipping 27° 8. W. and 
striking N. 5° W., are to be seen along a perpendicular exposure, 20 feet in height and 
50 in length, of the prevailing coarse syenite. Across the bedding lines run a number 
of jomts bearing N. 42° W., and dipping 87° 8. W. The other place, distant from 
here 800 feet in a nearly due south direction, is on the same island, and on the west side 
of the east or main channel, just below the dam. Here are a number of distinct layers 
of the finer grained rock (908), averaging 14 inches in thickness, and dipping 20° E., 
with a north and south strike. We have thus indications of a low anticlinal, whose 
nearly north and south axis runs diagonally across the island, and nearly in the direction 
of the river above. 

On the large exposure mentioned as showing a westward dip, the bedding planes are 
cut by a vertical north and south vein of fine-grained, dark-colored, brown-weathering, 
hornblendic rock (899), which is itself traversed and partly faulted by joints that affect 
it and the wall rock ulike. Several large, white quartz veins show under the bridge 
across the first dry channel west of the main gorge. One of these bears N. 40° E., 
dips 17° N. W., is five feet wide, and composed of parallel bands a quarter of an inch 
to three inches in width. A still larger one occurs at the bottom of the gorge, where it 
stands out very prominently, the surrounding rock having been worn away by the run- 
ning water. The wall rock, seen in only one place, is fine-grained, schistose, dark- 
greenish, and apparently chloritic (902). It would seem to be an advanced stage of al- 
teration of the normal amphibolic rock of the vicinity. A less advanced alteration is 
shown by the rock (905) of the large outcrops on the northwest corner of the island. 

The Mosinee hills are two spurs of an isolated elevation on the west bank of the 
Wisconsin, in Secs. 27, 26, 25 and 22, T. 28, R. 7 E., Marathon county. They are 
both of quartzite, and are higher than the rest of the elevated ground around them. 

The Lower Mosinee hill is near the center of Sec. 27, and about a mile from the river 
bank. It is conical in shape, with slopes of about 30° near the summit, and rises to an 
altitude of 880 feet above Lake Michigan, or about 280 fect above the river near by. 
Its slopes and summit are covered with loose masses of quartzite, onc-foot cube to four- 
feet cube in size. This quartzite (923) or quartz, is greyish-white, occasionally stained 
yellow, vitreous, and translucent in thin pieces, and peculiarly brittle. Sometimes a 
slight tendency to a granular structure is to be noticed. 

The Upper Mosince hill is reached from the Lower hill by crossing a saddle between 
the two, On this saddle, on the N. E. qr. of Sec. 27, numerous more or less rounded 
fragments of a fine-grained, reddish felspathic rock occur. The Upper hill is on the 
8. K. qr. of Sec. 23, near the corner of the section. It reaches an elevation of 1,030 
feet, or about 430 feet above the adjacent river. Its slopes, like those of the Lower hill, 
are covered with loose angular fragments of white, vitreous quartz of all sizes, up to five 


THE ARCHAAN ROCKS. 485 


feet in diameter. On the summit are to be seen some large irregular exposures of the 
same rock (924), showing no sign of bedding structure. None of the quartzite of either 
hill has any trace of lamination. 

About three-quarters of a mile immediately cast of the Upper hill, at the water’s 
edge on the west bank of the Wisconsin, is a low outcrop, several hundred feet in 
length, of a reddish syenite. Atthe upper end of the exposure the rock (919) is very 
coarse, composed of a deep-red, cleavable felspar, mottled with patches of brilliant 
black hornblende, up to a quarter of an inch in diameter, and showing:a small quantity 
of translucent, brownish-stained quartz. The deep red color is evidently partly due to 
weathering. Two sets of widely separated joints occur, one set, the most marked, 
bearing N. 30° E., the other N. 10° W. A hundred feet below, this rock changes to a 
very light-colored, fine-grained variety (920), poor in hornblende; and immediately be- 
low again to a very coarse kind (921) bluish-grey in color, owing to the preponderance 
of large surfaces of bluish, cleavable, non-striated felspar, and mottled with black 
patches of hornblende. This is evidently the normal variety from which the reddish 
crumbling kinds result by weathering. The rock of this exposure is the same that is 


QUARTZITE ExPosuRE ON Ris Hrut, MaraTHon County. 


largely displayed at Big Bull falls, five miles to the north, and is entirely unlike any 
rock noticed farther down the stream. 

Rib hill, on Secs. 8 and 9, T. 28, R. 7 E., shows large exposures of the same sort 
of quartzite as that occurring on the Mosinee hills, three miles southeast. This hill is 
a bold isolated crest, about a mile in length, trending north of west, across the southern 
half of Sec. 8, and gradually increasing in height from an altitude of 1,148 feet at its 
eastern extremity, on the western side of Sec. 9, to one of 1,263 feet at its western ex- 
tremity near the west line of Sec. 8. This western end is thus, so far as definitely 
known, the highest land in the state. It rises 660 feet above the Wisconsin river, three 
miles east, and 620 above the railroad track at Wausau. The summit’ of the hill is 
rather flat, and is traversed longitudinally by a line of precipitous exposures of quart- 
zite, from five to forty feet in height. The slopes on all sides are very stecp and are 
covered with a heavy talus of loose, angular masses of quartzite, of all sizes. The 
northern side is the most abrupt. For several hundred fect it slopes away from the 
summit at angles of from 25° to 30°. 

The exposures and talus show everywhere but the one kind of rock (927), a hard, brit- 
tle, non-laminated, glassy translucent quartz, usually of a dirty white color, but often 


486 GEOLOGY OF CENTRAL WISCONSIN. 


almost colorless. No bedding structure was observed, the rock being apparently even 
without any one persistent set of cross-joints, though all of the exposures show frac- 
tures, some quite irregular, and others approaching to plane surfaces. At one point 
several parallel N. E. joints occur. Fig. 15 is a sketch of one of the large exposures 
near the western extremity of the hill. ; 

On the Eau Claire river, at the crossing of the Stevens Point and Wausau road, . 
Sec. 7, T. 28, R. 8 E., there is a fall over coarse, pinkish syenite (926) resembling that 
on the Wisconsm, near the Mosinee hills, and also the prevailing syenite at Big Bull 
falls, a short distance northward. 

On the upper Eau Claire, in Sec. 4, T. 29, R. 10 E., are exposures of a very coarse, 
rough-textured, felspathic granite, consisting of pink, cleavable felspar; very large- 


flaked, black mica; and gray quartz. 
si ce oe At Wausau, on sections 25, 26, 85 and 36, 


Fra. 16. T. 29, R. 7 E., Marathon county, the Wiscon- 
sin makes bold rapids known as Big Bull 
i — falls. Here the river is divided into a series 
of channels by a number of small rocky 
islands, and the exposures are large, the rock 
on all being of one gencral kind, i. e., syenite 
or syenitic granite. This syenite varies in 
cat 0 degree of coarseness, but is commonly very 
coarse, the separate minerals beimg very 
plainly perceptible to the naked eye. There 
is no resemblance between it and any other 
rock observed on the Wisconsin river, except 
that of the Eau. Claire river, and a small 
outcrop previously alluded to as near the up- 
per Mosinee hill, both of these being evi- 
dently merely continuations of the Wausau 
rock. From the rock of Little Bull falls it 
differs, (1) in being commonly much coarser 
in grain, (2) in having usually a more jagged 
25 || fractur® (3) in showing greatcr tendency to 


Center of $¢c.26 


\ 
N iron-stain, and weather, (4) in having the 
s hornblende black instead of greenish-black, 
Si6 (5) m having the felspar orthoclase, and (6) 
by 


in containing usually some blackish mica. 
The bedding of the rocks at Big Bull is for 
the most part sufficiently distinct, the general 
strike being N. 80° E. and the dip from 30° to 
\ 40° N. W., most commonly about 38°. Ina 


few places a marked gneissoid structure, co- 
inciding with this bedding, and owing toa 
parallel arrangement of the hormblende, was 
observed. For the most part, however, the 
several constituent minerals are quite uniformly intermingled, without arrangement 
of any kind. In the exposures in the bed of the stream, and on the walls of the various 
channels, large bedding - plane surfaces frequently show, so that the bedding can usually 
be made out with very considerable accuracy. The separate layers are often not 
more than 2, 3, or 4 inches in thickness. 

The sketch map, Fig. 16, serves to show the localities of the various exposures exam- 
ined at this place. Islands No. 1, 2, 5, 8, 9, 10, 11 and 12 are without bare rock. The 


BIG BULL FALLS 


THE ARCHHAN ROCKS. 


487 


main or west channel of the river, between island No. 4 and the main-land, shows large 
exposures both in the bed and on the walls of the gorge, which are 15 to 20 feet in height. 
A section in this channel on the line A B, bearing N. 10° W., and beginning a short dis- 
tance (100 feet) above the bridge, showed the following succession, the measurements 


being horizontal distances: 


Fie. 17. 1. Moderately coarse syenite (912, 941): brown- 
ish-pink to gray, mottled with black, weath- 
ering with a dark-brown, uniform-tinted 
surface. Of the three ingredients, all of 
which are very plainly perceived by the 
naked eye, the felspar is much the coarsest, 
its facets reaching 4% inch in diameter; in 
color the felspar is brownish-pink to gray, 
and it is without striations. The several 
ingredients are quite uniformly intermin- 
gled. In most of this measurement the 
bedding is quite distinct, except in one or 
two places where it is obscured by cross- 
joints. On island No. 8 prominent joints 
trend N. 78° E. and dip 8. E. 75°. On the 
west side of the stream, just below the 
wagon bridge, the bedding planes show 
finely in a rock somewhat more pink than 
usual, the dip being 38° N. W. and the 
strike N.80° E. The same rock as that of 
this measurement shows also at the north 
end of island No. 4, and on the small rocky 
islet, NO: 6 wanes Gees esas dae eae et 

2. Finer-grained syenite (907): similar to the 
rock of No. 1, but of grayer color from the 
gray color of the felspar; less weathered 
and of a finer grain. In the middle of the 
stream, the surface of the layers of this 
rock dip very plainly 30° N. W. Vertical 
joints occur here nearly along the strike... 

os 3. Still finer-grained syenite (908): dark gray 

Back VEIN IN SYENITE, to black in color; much more hornblendic 
; Wausau. and less quartzose than the preceding kinds. 

The junction of this rock with No. 2 is quite sharp, and shows well on the 
east side of the gorge, where the bedding is also quite plainly to be seen, 
with a strike of N. 75° E., and a dip of 38° N. W. Prominent cross- 
joints occur at this place, trending with the strike direction, and standing 


vertically: .secsecseerseereseteeoseeerepeeneeraesedsenreeragersneeses 


2 BE Nig exponen OF caearseaw cane sud sae ee th a Ke ta Ran Peed oe eee eRe reRa eS 
5. Coarse syenite (911): allied to the rock of No. 1 (912, 907), but contaming 


much more pink orthoclase; penetrated by many patches and veins of a fine- 
grained, but distinctly crystalline, dark-gray to black, hornblendic rock. A 
large one of these veins is represented by Fig. 17..----++-s+ereeeere sees 


6, No exposure ° : : 
7. Very coarse syenite (910): bluish-gray, showing large unstriated grayish fel- 
spar surfaces, and coarse brilliant black hornblende, in pieces up to ¥g inch 


Feet. 


490 


116 


202 
62 


165 
70 


488 GEOLOGY OF CENTRAL WISCONSIN. 


by 1 inch; containing but little quartz. The weathered crust of this rock eet. 
is 7; inch thick, dark-brown outside, and pure white beneath, the latter due 
evidently to kaolinization........ 00sec ee eee e cree eee nee e ene et en eeees 125 
8. Coarse ivon-stained syenite (909): close to the preceding, but not quite so 
coarse, and having the felspar brownish from iron-staining, and more 


AUN ANG: pons cae ae eRe ea SY Te ae Tae ENS SUES Ses FE Rete ROSES 80 
Total horizontal length of section ......c..5 cece cere eet e eee eee eee 1,230 
Thickness of rock layers about..... 0 ..eseeeee cece ee ee ee ee eee tence 600 


On Island No. 7 of Fig. 19, are exposures which lie south of the end of this section. 
At the north end of the island, the rock (941) resembles No. 1 of the section, and con- 
tains a vein of reddish felspathic granite 30 feet long, 1 foot wide, and having a central 
band of white quartz, 1 inch to 2 inches wide. At the south end of the island a long, 
low exposure shows a fine-grained, light-pinkish, distinctly gneissoid syenite, or syenitic 
granite (943), which is very much more quartzose than any of the other Wausau rocks. 
The quartz is granular, glassy and wine-colored. The parallel grain is due to an ar- 
rangement of the black hornblende, which stands out quite prominently against the 
surrounding light-colored quartz. 

At the point C of Fig. 19, on the west side of the river, and near the north lne of Sec. 
26, a large exposure shows rocks quite different from those at the falls below. The 
main rock (915) at this place is fine-grained, dark-gray and hornblendic, having a dis- 
tinctly parallel structure, and weathcring to a light-pinkish color. A number of heavy 
beds of this rock are to be seen dipping 20° to 26° N. W., and striking N. 60° E., thus 
corresponding in bedding with the rocks at the falls. Intersecting the dark-colored rock 
are numerous small pinkish veins. In one place, on the river edge, a large, smooth 
joint-surface shows a nearly horizontal vein 16 inches wide, the vein matter (916) being 
composed of pink cleavable felspar and limpid white quartz. Cutting vertically through 
this vein and the inclosing rock is a mass of a very fine-grained, decomposing, schistose 
chloritic rock (917), 4 feet wide, having its lamination vertical. The lines of demarka- 
tion between the three kinds of rock on this exposure are all very sharply defined. 

On the Jenny road, on the east side of the Wisconsin, N. hf. Sec. 24, T. 29, R.7 E., 
13{ miles from Wausau, are several low outcrops of a white-weathcring, in places iron- 
stained, slaty quartzite (931). On a fresh fracture this rock presents a non-crystalline, 
whitish aspect, and is quite hard. With a lens, a few minute felspar facets are secn. 
Pyrite 1s present in minute cubes. Some specimens show a slight tendency to effervesce 
in hot acid. The schistose structure is evident, the planes striking N. 85° E., and dip- 
ping 50° N. W. 

One and a half miles further north, the same road ascends Marshall hill. All along 
this hillside in sections 12 and 1| are large, angular fragments of a fine-grained, gray- 
ish, aphanitic, silicious-schist (930). This rock is quite soft, very distinctly laminated, 
splitting very readily across the lamination planes. Some specimens effervesce very 
slightly on heating. 

Eastward from Wausau, on the north line of T. 29, R. 8 E., the country rises rap- 
idly, and is traversed by numerous low but abrupt ridges, such as are characteristic of 
large portions of the Archzean area. No rock outcrops were noted on any of these, but 
angular fragments of a white-weathering, porphyritic rock (929) were seen in great 
abundance. This rock has an aphanitic, light grey, not very hard matrix, through 
which are scattered a few felspar facets, and numerous amygdules of translucent, 
brownish quartz, the latter reaching 1g inch in diameter. It was noticed most abund- 
antly on Sec. 33, T. 29, R. 7 E. 

Westward from Wausau, in T. 29, R. 7 E., a number of outcrops oecur. Near its 
south line, this town is traversed by Rib river. In Secs. 21, 22, 27 and 28, there is 


THE ARCHAAN ROCKS. 489 


high ground trendmg north and south, which rises 200 to 800 feet above the Wisconsin 
at Wausau. In theS. E. qr. of Sec. 21, on the south slope of part of this ridge, a. 
peculiar, fine-grained telspathic rock (937, 945) is exposed, and is quarried to some ex- 
tent on Mr. Kolter’s land. This rock has a brownish-pink color, the least weathered 
portions showing a grayish tinge, is rather fine-grained, and has a marked granular 
texture, looking almost like a mechanical rock. The most abundant ingredient is a 
pinkish felspar in cleavable fragments up to sth inch across. With this is much 
granular brownish quartz, and a little blackish mica in fine flakes, making the rock a 
granite. No arrangement of the minerals in parallel lines is perceptible. In the quarry - 
the rock is seen to be nearly horizontal, dipping not more than 10° in a due south direc- 
tion. A total thickness of about three feet was seen. Large thin slabs, 2 inches to 4 
inches thick, splitting off parallel to the bedding, can be obtained. 

Near Single’s Mill, in the north part of 8. E. qr. of Sec. 29, in the same township, 
and on the edge of a part of the same high ground, are exposures of a whitish, slaty, 
granular quartzite (936), in places iron-stained. Under the magnitying glass this rock 
is seen to be made up of rounded grains of glassy quartz. Some few places were noted 
where the variety with granular texture grades into a non-granular glassy quartz. - 
Seales of silvery mica occur on the surfaces of lamin. The bedding structure is distinct, 
and shows a strike of N. 75° E. and dip of 56° 8. E. 

About half a mile from this place, and on the south side of the valley of Little Rib 
river, 8. E. qr. Sec. 29, the northeast face of a ridge shows quartzite in large exposures. 
The rock here (935) is glassy, translucent, and occasionally iron-stained, resembling that 
of Rib Hill. The bedding is obscure. On the slope of the hill below, the roots of the 
trees of a heavy wind-fall have upturned numerous fragments of a brownish-pink, gran- 
ular-textured felspathic rock, similar to that at Kolter’s quarry in Sec. 21. Half a mile 
northeast on the north face of the same elevation, N. E. qr. 8. E. qr. Sec. 30, a high 
ledge shows the same felspathic rock, striking N. 80° E., and dipping 50° N. W. 

At the falls of Rib river, S. E. qr. Sec. 28, T. 29, R. 5 E., are large exposures of 
greenish chloritic schist and syenite. On the south side of the river, at a point near the 
lower left hand corner of Fig. 18, is a rocky point about 15 feet high, showing heavily 
but distinctly bedded, greenish syenite, dipping 20° E., and striking N.8° W. The up- 

permost layer (950), 8 feet thick, is 
Fie. 18. : moderately coarse-grained, mottled 


: 7 een and grey, weathering white. 
Uy er grey g 
Gon 
OG 


m7, 

Yyy % To the lens it shows much grayish 
M, yf, \ quartz, green amphibole, and white 

KMD ase Sai altered felspar, the last least abund- 
Y, Syem par, 

Seay \ \ NA ant, though coarsest of the three. In 

some specimens greenish chlorite ac- 

companies the hornblende. The next 


a 
yaa 
pee 
[=<} 


A layer below (948), 4 feet thick,is a 
wees very much finer- grained, almost 
GY, Rib River aphanitic, greenish-grey rock, con- 
wee Y eee containing apparently a good deal of 

SS = chlorite. The weathered surface is 
Gg white, with numerous green, epidote- 


colored blotches. Microscopic exam- 


Jyenite Senile if e e alt f 
RA RTL OOS ination shows that the ingredients 0 
: \ ARES RE SS this fine-grained rock are the same 

Meee Cee as those of the coarser one above, but 
Rock OccuRRENCES AT THE Fats oF Ros Rivage. that the amphibole and félspar are 


fifty feet to the inch. t 
Beslenit oy fee both more altered. This rock breaks 


490 GEOLOGY OF CENTRAL WISCONSIN. 


out very readily into rectangular blocks, the planes of easiest cleavage lying at right 
angles to the bedding. The lowest layer, 3 feet thick, is again of a coarse (949) variety 
like that of the uppermost bed. 

On the north side of the river, beginning from the point B, we find a continuous low 
exposure, extending several rods up the stream, and showing the same bedding structure 
as seen on the south side of the river. Passing over these exposures on the line B C, 
at right angles to the strike, we find first, for 40 feet, mottled, grayish syenite (951), 
resembling that on the south side of the river, but somewhat finer in grain. The: 
weathered surface is of a uniform green hue, and a cross-fracture shows a greenish 
chloritic crust extending inward as much as }{ inch, with a sharply defined inner edge. 
Beyond on the line B. C. is first seen a similar rock, which is however, more highly 
quartzose and felspathic, the amphibole being almost excluded (952). Beyond again green 
chlorite begins to appear, gradually increasing in quantity, the former dip and strike 
joints at the same time becoming confused by the introduction of schistose planes, until, 
at 80 feet from the beginning, the rock has become a well-marked green chloritic schist, 
the schistose planes bearing N. 45° E., and dipping 60° to 80° 8. E. The gradation of 
the one rock into the other is unmistakable. Beyond again the chlorite-schist is largely 
exposed, and extends entirely across the river, forming the barrier rock of the falls. Its 
most common variety (953) is dark green in color, with large, interlocking, greasy-sur- 
faced laminze. The schistose surfaces are readily seratched with a knife, but much sili- 
cious matter is present. Pyrite is also to be seen throughout. In places the im- 
purity is less than usual, and the rock nearly all chloritic (954). After crossing about 
25 feet of this schist, its lammation lines are seen to become again obscure, signs of the 
former low dip reappearing, and the rock becoming again lke that below (955). 

We seem to have in these rocks an instance of the change of an ampbibolic to a 
chloritic rock, with a simultaneous production of schistose planes crossing the ordinary 
bedding lines. 

At Marathon City, Sec. 6, T. 28, R. 6 E., a low exposure occurs on the edge of the 
water in Rib river, which shows syenite (957) closely allied to the coarser syenite at Rib 
river falls. It is medium-grained, dark-greenish and grayish, showing surfaces of bril- 
liant black lamellar hornblende up to 44 inch in diameter, embedded in a matrix of very 
fine-granular quartz, and coarser, white, glassy felspar. The hornblende facets fre- 
quently show a tendency to alteration, and are then ill-defined on the edges, from the 
surrounding matrix. 

The rocks of Rib river falls and Marathon City bear a resemblance to those found 
crossing the Wisconsin at Mosinee, hut are rather more chloritic, or altered. The strike 
directions at the two places, N. 5° to 10° W. at Mosinee, and N. 8° W. at Rib river 
fails, also correspond. It seems probable that the two are portions of a continuous belt 
trending west of north. If so, the belt must have a considerable width, for the strike 
direction at Mosinee, if carried out northward, would not reach so far west as the falls 
of Rib river. : 


Yettow River Vautey. 


The upper part of Yellow river, in Wood county, north of the Green Bay and Minne- 
sota Railroad, flows over gneissic and granitic rocks, which are exposed nearly continu- 
ously in the beds and on the sides of the stream, for many miles. The same is true of 
the branches of the river in this part of its course. 

On the divide between Yellow and Black rivers, sandstone extends far-to the north- 
ward, covering, and for the most part concealing, the crystalline rocks, which, however, 
occasionally rise through the sandstone. The boundary between the formations it is 
almost impossible to trace accurately, since the irregular surface of the crystalline rocks 


THE ARCHAAN ROCKS. 491 


beneath may bring them up through to the surface at any point. The same is true to 
some extent of the region between Yellow river and the Wisconsin, but here the sand- 
stone does not extend nearly so far north. 

In Hemlock Creek, at the crossing of the wagon road from Grand Rapids to Dexter- 
ville, N. E. qr. of the 8. E. qr. of Sec. 5, T. 22, R. 4 E., are ledges of rather fine-grained, 
flesh-colored, gneissoid granite (967). Translucent, wine-colored quartz, and pinkish 
orthoclase in small, brilliant facets, make up most of the rock; the mica 1s sparse, in 
fine, green-black flakes, which have a distinct linear arrangement. ‘This rock is a hand- 
some one, and would probably dress well, though showing some tendency to weather 
and iron-stain. The bedding directions appear to show a strike of N. 60° E., and a dip 
of 70° 8. E. : 

On Yellow river itself, the southernmost Archzan exposure is to be seen about two 
miles north of Dexterville, in the N. hf. of Sec. 14, T. 22, R.3 EH. The rock here is 
medium-grained, pinkish, quartzose, gneissoid granite (973), composed chiefly of limpid 
quartz and orthoclase felspar, the former the most abundant. Mica is present in fine 
black scales arranged in parallel lines. The strike appears to N. 55° W., and the dip 
60° S. W. Near the top of the river bank, which rises directly from the granite, thin- 
bedded, friable, horizontal sandstone is exposed. 

On Sec. 8, T. 22, R. 3 E., three miles north of Dexterville, there are large flat 
ledges in the bed of the river, of gneiss, bounded on the north by quartz-porphyry. The 
gneiss (969 and 971) is very fine-grained, laminated, dark gray to black in color, and 
consists of a black mineral (mica, hornblende, or both), in small brilliant flakes; and 
whitish quartz and felspar. Its weathered surface is earthy and of a dirty white color, 
but shows the fine lamination even more distinctly than the interior. The quartz- 
porphyry (970) consists of a light greenish-grey, aphanitic matrix, having the peculiar 
flaky appearance that. is characteristic of the quartz-porphyries of the various isolated 
Archzan patches of Wisconsin, in which are imbedded somewhat sparsely scattered 
facets of pinkish orthoclase felspar up to one sixteenth of an inch in diameter. Itis a 
very tough, compact, rock; and is worn by the running water into smoothed and 
polished surfaces. This porphyry appears to penetrate the adjacent laminated rock in a 
very irregular manner. In one place amass of the gneissoid rock, some 50 feet in di- 
ameter, is nearly surrounded by the porphyry, the lines of junction between the two be- 
ing very sharp, and rendered especially noticeable by the different appearances of their 
weathcred surfaces. The lines of junction are not curved, but straight, bearing, re- 
spectively, N. 70° W., N. 30° E., and N. 70° W.; the first and last on opposite sides of 
the enclosed mass. The strike of the gneiss is N. 25° W., its dip 60° N.E. The. 
porphyry is 20 to 30 paces wide, and appears to he bounded on the north by the samc. 
gneiss as before, with the same bedding. Beyond, porphyry again comes in. 

At Pitts’ Mill, five miles north of Dexterville, on Sec. 34, T. 23, R.3 E., are very large 
exposures on Yellow river, which passes here through a narrow rocky gorge, of a very- 
beautifully and coarsely banded gneiss (993), the bands being alternately dark-gray to 
black, and bright pink, and having a northwest direction. The dark-colored bands 
predominate, and run from }4 inch to one or two feet in breadth, but when so broad, are 
rarely free from fine lines resembling the material of the pink bands, which run in 
width from these fine lines up to 6 or 10 inches. The dark-colored portions are fine- 
grained, with an intimate parallel structure, and consist predominatingly of fine green- - 
ish-black mica, with which are seen fine white and red felspar facets, and some fine, 
quartz. In places, greenish black, cleavable hornblende appears to partly replace the 
mica. The red bands consist chiefly of coarse-grained orthoclase felspar, with some 
limpid granular quartz and occasional blotches of mica, and show numerous whitish 
kaolinized patches, the whole rock having a tendency to decompose. Several folds in 
the strata occur, and are rendered especially striking by the very marked red and black 


492 GEOLOGY OF CENTRAL WISCONSIN. 


banding. A complete arch is to be seen on the east bank of the river in front of Mr. 
Pitts’ house. The plane of the bank, which at this point is about 15 feet in height, cuts 
directly across the strike, and slopes towards the northwest at anangle of 45°. Its base 
joins another surface sloping about 10° in the same direction. Along both surfaces the 
individual layers can be traced until they meet near the top of “the bank. The central 
part of the fold as seen on both surfaces is a confused and largely kaolinized felspathic 
mass (994). 

On the N. E. qr. Sec. 21, T. 23, R. 8 E., Rocky Run enters Yellow river, which hero 
traverses for many rods a rocky gorge, below which exposures continue along the river 
for a long distance. About half a mile below the mouth of Rocky Run, gneiss is ex- 
posed, striking N. W. and dipping E., and traversed by a vein 3 feet wide of a fine- 
grained, black, hornblendic rock. The vein cuts diagonally the lamination lines of the 
gneiss. Beginning about twenty rods below the mouth of’ Rocky Run, and extending 
up to it, are ledges of a fine-grained, greenish-grey, micaceous granite (974), which con- 
sists of very fine greenish-black mica, predominating, translucent quartz and pink or- 
thoclase. In places occurs a more highly felspathic, reddish kind (975), which appears 
sometimes to enclose portions of the darker colored variety. No definite bedding struc- 
ture was observed. Traversing this granite are numerous thin veins 4% to 34 inch 
in width, of white quartz, pink, cleavable orthoclase, and greenish epidote. The felgpar 
veins are in places so numerous as to make up a large portion of the rock. The epidote 
veins fault the others, being apparently the most recent. Fig. 19 represents a face 3 
feet hy 11g feet. Nearly all of this rock 
shows a decided tendency to weather, be- 
ing in places altered to an impure kaolin. 
Kaolin is reported to occur in quantity at 
points in the vicinity. From the crumb- 
ling condition of the rocks, this would seem 
very probable. ; 

Five miles north of Pitt’s Mill, in 
the northern part of Sec. 3, T. 23, R.3 E., 
the bed of Yellow river is made for 15 
rods of a coarse-grained, flesh-colored gran- 

Fautrep Vers iw Granrrz, Yettow River. ite, consisting of a very uniform admixture 
of flesh-colored orthoclase, glassy quartz, 
and black mica. No distinct bedding is to be seen. 

At Big Bull Falls, nine miles north of Pitt's Mill, on Sec. 15 and 16, T. 24, R.3 E., 
large exposures of medium-grained, highly felspathic, red granite extend along the 
bed and in the banks of Yellow river for a quarter of a mile. This granite has a base 
of cleavable reddish orthoclase, throughout which is quite uniformly distributed hyaline, 
occasionally smoky, quartz, in irregularly shaped patches syd to 4th inch in diameter. 
Mica is present, but is very fine and sparse. For the whole length of the exposure, this 
rock is nearly uniform, and without any tendency to kaolinize, lts peculiar texture, 
composition and color combine to make it a very valuable and unusually handsome 
building granite. Polished specimens of the rock attracted great attention at the Phila- 
delphia Exposition, where it was regarded by experts as among the finest of the many 
polished granites exhibited. 

On Sec. 7, T. 24, R. 3 E., another exposure of a similar red granite was noted. Above 
this point, Yellow river is reported without exposures, 


PLATE, XVII 


Section on Line AB:-CD 
Vertical Scale, 300 tt =Vinch 


CMI and 22, 
MAP 


showing he 
FORMATIONS along BLACK R. 
le in Nectlous 2 MAAN and22, 


Town 2) Rauge 4\W, 


SACKSON CO. 


Yeale linen 2 in, 
by 
RD. feving, 
IB7T3 
| 
Archaean Lower Silurian 


Do om wa 
Gueiss  Graiite Hornblende Magnesian Ferruginous Potsdam 
Rock Schist Quartz Schist Sandstone 


Ths, Minwariie Leria A iNonCo. 


THE ARCHAAN ROCKS. 493 


Brack River Vary. 


The first exposures of crystalline rocks met with in ascending Black river are found a 
short distance below the town of Black River Falls, T. 21, R. 4 W., in Jackson county. 
From here they occur in the bed and on the sides of the stream, with only occasional inter- 
ruptions, as far north as town 2%, in Clark county. For the greater part of this distance, 
they are concealed, away from the river, by overlying horizontal sandstone, through 
which, however, they occasionally rise in knobby projections. In some of the branch 
streams, also, the sandstone is cut through and the crystalline rocks exposed. Along 
the river the rock ledges, in few places only, rise to any considerable height above the 
water. 

In the vicinity of Black River Falls the exposures are large and interesting. The 
map of Plate XVII shows the relative positions of the various outcropping beds, their bed- 
ding and dip directions being shown by the accompanying section. From these it will 
be seen that at this place a central, nearly structureless, granitic mags is bounded on the 
southwest by layers of gneiss, dipping southwestward, into which it appears to grade; 
and on the northeast, by a succession of schistose beds, dipping northeastward, but not hav- 
ing exactly the same strike directions as the gnciss on the other side. In the following 
detailed descriptions, the various rock masses are numbered as on the map and section, 
beginning with the gneiss on the southwest: 


Fre. 20. 


Goose, Lonatrutted 


H Lae = 
Conglomerae = 
Kaolinized gneiss| 

peer? oS" ____ ees 
hi 
% Gness 
s 

1 

1 


alll YM 


UNcONFORMABILITY, BLAcK RIvER Fats. 


I, Gniess (1,015): rather fine-grained, very plainly laminated, pink and gray 
banded; dipping S. W. 60°, striking N. 32° W. The constituent minerals 
are: pinkish orthoclase, predominating; pinkish and colorless translucent 
quartz; mica in very fine black scales, but quite abundant, and much more 
plenty in certain layers than in others; and also a whitish, partly altered, 
felspar, in fine facets. In some plaecs, especially micaceous portions have 
a much darker color than usual; in others large nests of coarse, cléavable 


404 


GEOLOGY OF CENTRAL WISCONSIN. 


pink orthoclase occur. The lamine are for the most part not over 
1-324 inch in width, remarkably regular and parallel, and without 
contortion. Two sets of veins traverse the rock, both of reddish felspar, 
those of one set being but mere strings and faulting the others, which are 
one-fourth to one-half inch in width. This gneiss is exposed for several 
hundred feet along the river opposite Ledyard’s old mill; and, as shown on 
the map and section, is, at the lower end of the exposure, overlaid by 25 to 
30 feet or more of horizontal sandstone, which fills in the depression in the 
very irregular upper surface of the gneiss. The exact junction of the two 
formations is distinctly to be seen for a long distance. In some places the 
gneiss shows no alteration at its contact with the sandstone; in others 
again, as it is traced upward from the water's edge to the line of contact, 
arapidly increasing decomposition is observed, until immediately below 
the sandstone the change to a soft bluish-white clay or kaolin (1,018) is 
complete. The kaolin retains still very plainly the fine lamination of the 
unaltered gneiss, it being even possible in some cases to trace individual 
lamine from the unchanged into the kaolinized rock. Immediately below 
the sandstone the laminz of the softened rock are seen to be bent over as 
though by the weight of the superincumbent sandstone. This'is a fact of 
some interest, since it would confirm the view already presented, that the 
kaolinization was subsequent to the deposition of the sandstone; having 
been caused possibly by the currents of carbonated water which found pas- 
sage along the junction line of the two formations. A section through the 
sandstone, kaolin, and gneiss, is presented in Fig. 20. Up the river 
gneiss continues to show, losing, gradually, its distinct lamination, to with- 
in a short distance of the wagon bridge, above which, after an interval 
without exposures, granite appears. 


Ia. Granite (1,008): medium-grained, pinkish, consisting of a nearly uniform 


admixture of pinkish orthoclase, in facets up to 1-16th inch, and fine- 
grained translucent quartz. Some mica is present, in fine scales, showing 
sometimes a slightly stringy arrangement. This granite is exposed froma 
short distance above the wagon bridge, as far north as the north line of 
Sec. 14, the river in this distance passing through a gorge whose walls 
sometimes reach a height of 80 feet. In the large exposures at the falls, 
thé parallel grain of the gneiss below is almost entirely lost, being only 
occasionally indicated in an obscure arrangement of the mica. The rock 
here is traversed hy several sets of jomts mostly somewhat irregular, those 
showing the greatest irregularity trending N. 80° E. and dipping 72° S. E. 
but having no corresponding structure in the rock. Above, the granite 
shows the same general characters as at the falls, occasionally — as in the 
railroad cut on the west side of the river, just above the falls — showing a 
darker kind than usual from a greater quantity of fine dark mica. In this 
cut there are to be seen two sets of planes equally marked, one set trend- 
ing N. W. and dipping N. E., the other trending N. E. and dipping N. 
W. A distinct stringy arrangement of the mica was noted parallel to the 
former set. Near the north line of Sec. 15, the granite exposures, cease 
suddenly on the east side of the river, whilst they continue some distance 
farther on the west side — a fact tobe explained by the northwest strike of 
the succeeding slaty rocks. 


Il. Hornblende rock or schist (501): fine-grained, crystalline-textured; dark- 


colored to black; breaking with conchoidal fracture; weathering out into 
rough prismatic fragments, with dirty brown “color; striking, as a whole, 


THE ARCHAZAN ROCKS. 495 


N.W. This rock is exposed in a low ledge on the east side of the river, Feet. 
almost immediately succeeding the granite. It shows also, on a small 
rock in the middle of the stream, where a distinct contorted lamination is 
observable. Horizontal width .........cceecceeecn ee see cesenceeteeee 60 
III. Magnesian slate (516, 522): palo-gray, light-greenish-grey, dark-green, oc- 
casionally pink, or even bright brick-red, from presence of iron sesquioxide; 
sometimes quite soft, at others quite hard and gritty, from the presence of 
fine granular. quartz, which appears never to be entirely absent; highly 
schistose, the lamine striking N. 60° W. and dipping N. E. 70°. The 
magnesian mineral appears to be talc in the light-green kinds, and chlo- 
rite in the dark green, the former kind much predominating, and never- 
sharply defined from the other. The light-gray to nearly whitish kinds are 
the most silicious, and most firm, the others showing much tendency to 
crumble and decompose. This is especially so with those that are stained 
bright-red, their contained oxide of iron arising from the oxidation of py- 
rite, which sometimes is to be seen still unchanged, in minute cubes. These 
schists are exposed on the east side of ‘the river, on a nearly perpendicular 
bank, 100 feet in height, which forms the western end of ‘‘Tilden’s Iron 
Mound.’ About 75 feet along the river bank from the lower end of the 
exposure, a bright-red layer, 30 feet thick, occurs, in which hematite forms 
a prominent constituent, the surfaces of some of the lamine having even a 
bright specular lustre (522) and in which nests and seams of porous, iron- 
stained quartz are quite abundant. At one time this ferruginous schist 
was mined as an iron ore. Averaged specimens from it yielded respectively 
9.81. 28.13 and 31.27 per cent. of metallic iron; the first representing a thick- 
ness of 24 feet, near the water’s edge, the second the same thickness at an 
elevation of 30 feet above the river, the third, 6 feet, more ferruginous 
than the rest, immediately next below (stratigraphically) the preceding 
layer. The six feet layer does not continue the whole height of the bank. 
The length of the exposure of this rock along the river bank is about 700 
feet, its horizontal width aboub.......-. see ee cece cece eee e eee e eens 200 
IV Covered: on Tilden’s Iron Mound... ......6- 00s sees eect eee cere teen eee) OB 
V. Ferruginous quartz-schist: finely laminated, varying from a light gray, 
somewhat ferruginous quartz-schist, to a dark-colored highly magnetic 
rock; in many places weathered brownish, iron-stained, partly crumbling. 
This rock is exposed in a low outcrop on the water's edge on the east bank 
of the river; in a similar low outcrop on the west bank; and again (appar- 
ently the same layer) some distance east from the river on the north flank 
of the Iron Mound, at points indicated on the map. The first exposure 
shows a very much decomposed, crumbly, brown-stained, non-magnetic 
rock, containing 42.32 per cent. of metallic iron. The outcrop on the west 
bank of the river is somewhat larger, showing a material similar to that 
on the east side, with a very plain N. 50° W. strike, and N. E. dip. A 
sample across the whole width of 30 feet yielded 35.96 per cent. of iron. 
The exposures on the Iron Mound are partly artificial, a considerable quan- 
tity of the rock having been removed for smelting purposes. In one of the 
two main openings the rock or ore is brown-stained and magnetic, contain- 
ing 34.22 per cent. of metallic iron; in the other, somewhat cleeper in the 
hill, a much less oxidized material is seen. Of this, the innermost portions 
present a dark-gray to nearly black appearance, and exceedingly fine- 
grained texture, being composed of alternating darker and lighter colored 
(more quartzose) bands, but having this banding much less prominent than 


496 GEOLOGY OF CENTRAL WISCONSIN. 


on the weathered kinds. This dark-colored rock is distinctly magnetic, 
affecting the needle, and adhering to a magnet in quite coarse particles, 
An averaged sample yielded 32.1 per cent. of iron. A partial analysis of 
the same material yielded the writer, in 1872, the following results: 


Per cents. 
Metallic: iOtla ses sa sissd eee ee eer eck aseenen thage ¥ 31.87 
GiliGa> pasta eieedeee teas: Mens Geaae en imiese oe habs 45.72 
Lime ........ a bode deb dae MESS Ese EN oe ae ES Rete e pee a 1.62 
iA [WIM ajies ax eens Ama neele Ghde oma oa Lee Ae Daa See EERE SY 8.56 
Magnesia... 0... cece cree cece ee erence nee en ener renee trace 


Still another sample, averaged from the whole opening, and from the 
stock pile outside, yielded 37.18 per cent. of metallic iron. The horizontal 
width of this schist seen on the river is... -... ee secre eee ete e teen ene 

VI. Magnesian schist: similar to No. II; bedding very plain; strike N. 50° W., 
dip 60° Nis. Bie Wats sieuis pinyin sac iwees waintuasiaie canted edminsbisieinis pines 

VII. Covered. In this interval the west side of the river begins to rise, the east 
side being now depressed into the valley of Levins’ creek. On each side of 

the mouth of this creek, and extending up it for a long distance, are-ledges 

of thin-bedded, horizontal sandstone, which thus overlies and conceals the 
Archeean rocks, filling the depressions in their ancient eroded surface. 

The Archean exposures are now transferred to the west side of the river. 

: The horizontal width of this gap at nght angles to the general strike, is. . 
VII. Magnesian schist: light-colored; silicious; similar to No. VI; showing 
plainly the same bedding structure; Width........ 0... cece cece eee e enone 

IX. Ferruginous quarte-schist (513): fine-grained, dark-gray, very quartzose; 
showing under the lens numerous grains of glassy, quartz, which occur 

more, abundantly on some seams than others. Seams and surfaces stained 

red; non-magnetic; contains. 26.98 per cent. metallic iron; strike N. 45° 

OU spruce kG PLL IE a AG EAE A od ek Lee 

X. Magnesian schist (511,512): in the lower or more southern portions quite soft 
(512); light greenish-gray, and without indication of any quartzose ingre- 

dient; towards the upper portions becoming much more quartzose (511), 
losing the softness and greenish tinge. In these last, the lens reveals 

much granular, glassy, translucent and smoky quartz between the laminz; 

WAC «iss: sie bimwirmerrees nine em aniee Avisuesaianl Aacaies veo tb. Ce weeds poets 

RTs Covered ac o¥s pee vip Sed lve wis Hien dusle vane eau eis WU eS Sa ooo ad eee be ene eS 
XII. Magnesian schist (504): greenish gray; having thin intercalated bands of 
ferruginous quartz-schist; width...... 02... ec ccc cece cece cen ceeeeeeaes 

XIII. Ferruginous quartz-schist: very much weathered. An old pit has been 
sunk on this near the water’s edge. The loose material in the pit yielded 

30.28 per cent. metallic iron. The width seen is ...........cecceeecees 

Nos. XII and XIII are well exposed in the railroad cutting at the top of 
the bank, about 80 feet high, at whose foot the pit alluded to is sunk. The 
cutting is not quite in the line of strike, being nearly north and south. In 
it are exposed, beginning at the north end (a) magnesian schist (508), 6 
feet horizontal width; (b) banded ferruginous quartz schist, containing 
29.17 per cent. of metallic iron, 2 feet; (c) magnesian schist with thin 
seams of ferruginous quartz-schist, 13 feet; (d) ferruginous quartz-schist, 
with small seams of magnesian schist — the more ferruginous portions con- 
taining 26.04 per cent. of iron—16 feet; (e) the samo as the last, but con- 
taining more magnesian bands, grading into the next layer, 16 feet; (£) 
ferruginous schist, with many magnesian bands, cut into small prismatic 


Feet. 


60 


20 


100 


40 


24 


200 
120 


THE ARCHAAN ROCKS. 497 


blocks by close jointing and containing 28.63 per cent. of iron, 48 feet. eet. 
Returning now to the river bank below, we note next; 
XIV. Magnesion schists (502; 508). .2sicag sis sareeaciseae vaaenscteg tine dae eiemaine 60 
XV. Covered: by sandstone. Immediately north of the magnesian schist No. 
XIV, and resting directly against it, horizontal sandstone is seen and con- 
tinues to show in mural exposures 10 to 40 feet in height, all along the 
west bank of the river to a pot beyond the limits of the section The 


width.of thesgap 1s @bOUb: 06. a as dean, Garces alae mde satardseiem amare arandie 3,000 
XVI. Ferruginaus quarte-schist: much oxidized, containing 32.91 per cent. of 

ALON, ia vase nee dcteal ates ae ceaeuatniam Selves a Users am ne eee vette ey oe e <6 8 
XVII. Mica slate: finely laminated; very light-colored; the mica in bright-lus- 

tered plates up to 14 inch in diameter .......... eee eee eee eee ee eee 5 


XVII. Ferruginous quarte-schist (1017): fine-gramed, very thinly and dis- 
tinctly laminated, without contortion; brownish to grayish black in color; 
non-magnetic; streak red; under the lens seen to consist of mingled 
grains of white quartz, and a metallic-lustered black mineral (hematite ?); 


contains iron,.32.49' per COtitii. sa cccsien ed caw cene sees bade wed ew nee 82 
KT Xo, CO CCHER: stssra dasa astesuavayacoiniohefacalaisraasimane uecale GAG a Oye a NRG M AOE brecdie ached easy 22 
XX. Ferruginous quartz-schist: resembling No. XVIII ...--... eee ee eee eee 7 


Nos. XVI, XVII, XVIII, and XX, all show plainly a strike of N. 65° 
W., and dip of 70° N. E. With the exception of XVIII, which rises 
10 feet from the river, they are all seen on very low exposures barely ris- 
ing from the water, and overlaid by heavy beds of sandstone, which shows 
in a perpendicular face im the bank above. The exact junction of No. 
XVIII with the overlying sandstone is well exposed, it being possible to 
obtain hand speeimens showing both formations (1009). One of these 
has already been figured on page 462. Another remarkable feature in 
these exposures is the bending of the sandstone layers above, to conform 
with the irregular surface of the schistose rocks, suggesting the idea that 
a motion upward of the schist had caused the bending, which is seen, not 
only in the lower layers, but also in the heavy ones 6 to 10 feet above. 
This feature is represented in Fig. 21. 

At the junction of the two rocks, the sand is seen to have frequently been 
wedged between the partly separated schist lamin, and in one place in- 
cludes a detached mass of the schist. 


XXI. Covered ly sandstone. .... sce cece sce e cece cence enter ence ee eeeeenee 150 
XXIL. Ferruginous quarte-schist.. .10cs cece cece ccc eee vette tener ees 38 
SORT Cone ed shes itos 5 ea een ica ide hoe Sora s, oS ee Ma a, alee 40) 
XXIV. Ferruginous quartz-schist (519)... +... sce e cece ener eee ees 5 
Total horizontal width of the slaty series measured ....... ee rey) 5,406 
Approximate thickness ....-- ++... sees ee ee ee ee eee eee n en es sis dia didi ta dens 5, 000 


Nos. XXII and XXIV occur on the east bank of the river, and are barely 
seen above the water’s edge, being overlaid by heavy beds of sandstone. 


The existence, in the region about Black River Falls, of isolated hills of ferrugimous 
schist, whic’ rise through the surrounding horizontal sandstone, has already been alluded 
to. These hills are known locally as ‘‘iron ore mounds.’’ They are from 100 to 250 
feet in height, and rise somewhat abruptly from the level sandy plain, which is alsu 
dotted by loftier castellated outliers composed of higher layers of the same sandstone as 
that which forms its basement. The rocks of the ‘‘iron ore mounds ”’ strictly come un- 
der another head, being isolated areas of Archean; but are conveniently alluded to here 


Wis. Sur. — 32. 


498 GEOLOGY OF CENTRAL WISCONSIN. 


on account of their close relations to, and short distance from, the slaty rocks just de- 
scribed as occurring on Black river. For the positions of the various mounds, see Atlas 
Plate XV, Area F. The exposures observed on them are mostly poor, and nearly always 
of ferruginous quartz-schist, like that occurring on Black river, and quartz. On those 
mounds, however, which lie on sections 15 and 14, T. 21, R. 3 W., and Sec. 31, T. 22, 
R. 8 W., the iron oxide, instead of being magnetic, or red, or brown and hydrated, is 
brilliant specular hematite. The specimens from the mound on Sec. 12, T. 21, R. 4 W., 
show chiefly a dark-colored magnetic rock, like that of Tilden’s iron mound. On the 
mound on Sec..17, T. 21, R. 3 W., white quartz only was observed. 

The considerable amount of iron in the schists of Black river, and of the mounds in 
the neighboring country, has for many years attracted attention to these rocks, it being 
supposed that they were of value as ores of iron. Several attempts at smelting have been 
made. One small furnace was built on the banks of Levin’s creek, as long ago as 1855, 
and another begun, but never completed, on the south side of Tilden's mound, near the 
river. In the first-named, the ferruginous quartz-schist of the north side of Tilden’s 
mound was mixed with the hematitic magnesian schists from the west side of the same 
mound on the river bank. As a flux for this mixture, a dolomitic limestone from the Lower 
Magnesian formation was used. It may be readily seen that no successful work was 
ever done. 

In view of the considerable interest that had been excited with regard to these ores, 
and the reputation they had already attained, the writer was sent, during the first year 


Fig. 21. 


PoTspaAM SANDSTONE ON ARCHAMAN SonISTs. 


XVI Ferruginous quartz-schist, 8 feet. XVII Mica Schist, 5 feet. XVIII Ferruginous schist, 
23 feet. XX Ferruginous schist, 7 feet. A, mass of Schist included in the sandstone, BB, Pots- 
dam sar.dstone, top layer 3 feet thick. Scale, 20 fect tolinch. C. D., River level. 


of the present survey, by the then Chief Geologist, Dr. I. A. Lapham, to make an exam- 
and in all the openings seen; and analyses made of most of the samples, especially with 
, regard to their richness in iron.. The ores or iron-bearing rocks are of two general 
kinds: the ferruginous quartz-schists, in which the iron-bearing ingredient is at different 
times magnetite, specular hematite, red hematite, and the brown or hydrated oxide — 
the last two probably from weathermg only —and the ferruginous magnesian schists, 
in which the iron oxide is red hematite. Of the former kind, the various samples yielded 
respectively, 26.04, 26.98, 28.63, 29.17, 30.23, 80.90, 31.87, 32.10, 32.49, 32.91, 34.22, 
35.96, 37.18 and 42.52 per cents. of metallic iron. Of the latter, observed only in one 
place, the samples yielded 9.81, 28.13 and 31.27 per cents.'' In the first kind, the only 
other important ingredient besides iron oxide is quartz; in the second, a silicate of mag- 


1¥or the “hard” or silicious ores of Michigan, 50 per cent. of iron is the minimum amount at 
which the ores can find purchasers, 


THE ARCHHAN ROCKS. 499 


nesia. Though obtained on carefully selected samples, the above figures are probably 
somewhat high.. Whilst iron ores are worked with even lower percentages than these, 
such admixtures as quartz and magnesian silicates would necessitate quantities of iron 
at least balf as large again. The Black river “orcs” then, really cannot be regarded as 
ores, but are properly iron-bearing rocks. Whether valuable working ores may yet be 
discovered in these slaty rocks is another question. Similar rocks occur with the work- 
able ores of Michigan. Taking, however, all the circumstances into account, it is deemed 
rather improbable that such ores can exist. Even if they do, they are not likely to be 
discovered, but rather to remain hidden undemeath the sandstone that forms the surface 
rock throughout the region. 

It has been said on a previous page that the peculiar lithological characters of the 
slaty rocks of Black river, and of the mounds of the vicinity, strongly suggest their 
Huronian age —a suggestion which is partly corroborated by their position on the border 
of the great Archean area of the north part of the state. It has been supposed that 
‘the granite and gneiss of the foregoing section were Laurentian, the slaty rocks Huro- 
nian. From the details given it will he seen that all must be assigned to the sane 
series. 

At Black River Station, on Sec. 3, T. 22, R. 3 W., where the Green Bay and Min- 
nesota Railway crosses Black river, crystalline rocks are exposed in the side and bottom 
of the gorge through which the river passes, and are overlaid at the top of the banks by 
a few thin layers of sandstone. The river here trends about 8. 25° W., or in a direc- 
tion roughly at right angles to the general strike. The southernmost exposure examined 
was about a quarter of a mile below the railroad bridge. Beginning with it, and pass- 
ing northward on the west bank of the river, the following different rocks were noticed: 


ConToRTED GNEISS ON BLacKk RIvER. 


I. Gneiss: showing in a rounded knob some 25 feet above the water, and about 100 feet 
long, and in the river bed below for about 200 feet northward. At the southern 
end of the exposure the gneiss (1,000) is very fine-grained, thinly laminated, pink- 
ish-weathered, and quartzose; cunsisting of fine-granular, glassy quartz, predom - 
inating; fne pinkish felspar, and fine black mica, arranged in lines, the lamina- 
tion of the rock being also independent of the arrangement of the mica; having 
a strike of N. 35° W., and a dip of 62° N. E. A hundred feet northward this 
merges into a kind (1,001) in which the granular quartz still more largely predora- 
‘inates, and the mica is almost wholly absent. A short distance beyond, this changes 
again toa dark colored, beautifully contorted kind (1,002), consisting of fine-grained 


500 GEOLOGY OF CENTRAL WISCONSIN. 


white quartz, partly arranged in separate white bands, up to one inch in width, 
and partly also mingled with fine, brilliant black mica, and fine, white felspar, in 
dark gray bands. The weathered surtace of this is dark brown with a white kao- 
linized undercrust. North of the gneiss no rock occurs for 400 feet, then come 
outcrops some 400 feet long of, 

T[. Diorite (1,003): rather coarse-grained, highly crystalline, grayish, felspathic; com- 
posed of large surfaced, bluish-gray felspar, with coarse hornblende; without det- 
inite bedding structure. Underneath the railroad bridge this rock is terminated 
by a mass or vein of, 

Ill. White quartz: 5 feet wide. Immediately next to which begin outcrops about 200 
feet long of 

IV. Greiss (1,005 and 1,006): rather fine-grained, pink-and-gray-banded, very quartz- 
ose; consisting principally of pink and colorless translucent quartz, with some fine 
greenish-black mica and pinkish orthoclase; in places a quartzite (1,004), the oth- 
er minerals being almost wholly absent. Above this the rocks are concealed for a 
short distance, after which are seen, some 20 feet in width, of 

V. Micaceous schist (1,007): a very peculiar, fine-grained, dark-brown, earthy-textured, 
jointed rock. Under the lens it is seen to consist largely of angular grains of 
quartz. The smooth jointed planes of this rock strike N. W., and stand vertical. 


In the river one mile above Rlack River Station, a ledge 150 feet long and 25 feet 
high, is seen, of fine-grained, dark-reddish granite (990), consisting of a rather uniform 
and close admixture of reddish orthoclase, in fine glittering facets, reddish-brown, trans- 
lucent quartz, some colorless quartz, and a little, sparsely scattered, fine black mica. 
Half a mile further up stream, fine-grained, red and gray banded, quartzose gneiss 
(991) is exposed. The gray bands consist of fine-grained, glassy quartz, fine black mica 
and white felspar; the red of brown and red translucent quartz, mingled with a little 
orthoclase. From here to the mouth of the East Fork, the bed of Black river shows nu- 
merous small ledges, 3 to 4 feet high, of contorted gneiss and reddish granite. 

Above the mouth of the East Fork, which is on Sec. 36, T. 23, R. 3 W., exposures 
of red granite are seen as far as French's mill, on Sec. 25. The wagon road which, 
for half a mile below the mill, follows the west bank of the river has, on the east side, 
ledges of red granite, and on the west, a ridge thirty to forty feet high, composed of 
horizontal, coarse-grained, quartzose, cross-laminated sandstone. In one place, the 
exact junction of the two formations is to be seen. At the mill, the granite exposures 
are especially large, both on the west bank and on a large island in the stream. Two 
kinds of the granite occur, both presenting a prevailing pinkish weathering: (1) a rather 
fine-grained, very uniform-textured, dark reddish kind (988, close to 990); and (2), a 
medium-grained, uniform-textured, pinkish-grey, quartzose kind (987), containing 
both colorless glassy,and pink translucent quartz; pink orthoclase; and fine black 
brilliant mica. Both kinds appear like handsome building or ornamental granites. No 
definite bedding structure is to be seen. 

On the wagon road, three quarters of a mile south of Neillsville, Sec. 22, T. 24, R. 
2W., isa large outcrop 200 yards long, and 10 to 40 teet high, of porphyvitic, cal- 
careous gneiss, striking E. W., and dipping 80°S. At the northem end of the ex- 
posure, the rock (984), is medium-grained, fine-laminated, Imotty, and highly mica- 
ceous. Fresh surfaces show a large quantity of fine-flaked brilliant black mica, white 
quartz in little nests, around which the micaceous lamine curve, and white felspar, 
which sometimes occurs in smaller nests up to a quarter to half inch in diameter. In 
large quantity, the pulverized rock effervesces briskly in muriatic acid. In the middle 
portion of the ledge, the rock (985), closely resembles that. just described; but shows 
much pink cleavable felspar and less mica, the pink felspar forming the knots, At the 


be 


PLATE, XVIII 


Map showiug the relative positions 
of the 
AR CHAKAN 
Sf Wiescoristi « 
R.D. lhving. 


IS OLATHE D 


AREAS 


; 
“4 


MAB ATH O(N 


OCONTO 


~ GRANT 


ES Quartzite 


neal < Yj 
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ee, ant VY CY" 
i y PORTAGE sae Xvi 
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HB Quarts Porphyry MQ Granite 


Seale Linch 247 mites 


BE Forruginous Schist 


Tar Misocrre Cerin A Laan Cn 


THE ARCHAAN ROCKS. 501 


south end, the gneiss resembles that at the northern end, and contains large masses of 
white quartz, up to ten by four feet in size. 

These knotty gneisses resemble closely others which occur on the line of the Wiscon- 
sin Valley Railroad, in Portage county. 

Three-quarters of a mile west of Neillsville, atthe crossing of Black river, on the S. 
W. qr. Sec. 15, T. 24, R. 2 W., fine-grained, light-pinkish, slightly gneissoid, and very 
quartzose granite (983) is exposed, with a vertical dip and E. W. strike. This rock is 
very hard and compact, and appears to be a fine ornamental granite. 

The gneissoid and red granites of Black and Yellow rivers resemble one another 
closely, and appear to he directly continuous with one another underneath the sandstone, 
which nearly everywhere between the two rivers is the surface rock. Occasionally the 
crystalline rocks come to the surface in the interval, and are then of the same character 
as on the rivers; as for instance, on O'Neil’s creek, in Secs. 1 and 2, T. 24 R.1 W., 
Clark county, where red granite is exposed; and on a high bluff in the N. E. part of T. 
23, R. 2 E., whose upper portions are reported to be of red granite with sandstone layers 
at lower levels. 

The amount of these reddish ornamental granites of extraordinarily fine quality occur- 
ring on Yellow and Black nvers, and in the intervening country, appears to be very 
great. 


THE ISOLATED ARCHAAN AREAS. 


I. In General. 


We have next to consider those isolated areas of Archzean rocks 
which are found protruding through the surrounding horizontal Silu- 
rian strata, at points widely scattered over the central part-of the 
state. Plate XVIII is a sketch map showing the relative positions 
of these various areas, as also the nature of the rocks of each area, 
and its distance from the southern boundary of the main Archean 
mass. Near to this boundary line it is not always possible to be sure 
that we have to deal with an isolated area, when we find a mound-like 
exposure of crystalline rocks, with sandstone showing in the vicinity 
at lower levels, on account of the intricate and somewhat indefinite 
nature of the boundary itself. Besides these doubtful areas, which 
may be somewhere connected with the main Archean region without 
intervening horizontal strata, there are, however, many others which 
occur as inch as 50 or 100 miles within the region of the Lower Si- 
lurian rocks. Underneath these, the connection with the rocks of the 
main Archean area is, of course, preserved, the separation being su- 
perficial only. All of the scattered patches are but points of the uni- 
versal Archean basement, upon which all the later strata are built, 
having earned their especial immunity from complete burial by virtuo 
of the resistant nature of their materials. They are properly buried 
mountains, and were high islands and reef-ledges in the early Paleozoic 


seas. 


502 GEOLOGY OF CENTRAL WISCONSIN. 


All the areas, except the one, or rather the group, including the 
Baraboo ranges in Sauk county, are of small size, generally occupying 
much less than a square mile of area. With the same exception, they 
are all mound-like in form, rising, usually, somewhat abruptly from 
the surrounding country, which is frequently level, and showing al- 
ways considerable rock exposures on the flanks and summits, being 
often almost all of bare rock. They reach heights of from 50 to 250 
feet, but are usually lower than surrounding outlying bluffs of the 
horizontal strata. The Baraboo group, unlike the others, constitutes 
a series of bold ridges, one of which reaches elevations of 800 and 900 
feet above Lake Michigan, and a length of over 20 miles. These 
ranges are so important an element in the topographical features of 
Central Wisconsin, that they have already received attention in the 
chapter on general topography. They are still more fully described 
in subsequent pages. 

The nature of the rocks composing the several areas is not always 
the same. The large areas in Sauk county, and a few others, are 
chiefly of quartzite; a number are of quartz-porphyry; still others 
of granite, which is different in different cases; and yet others, occur- 
ing in Jackson county, and close to the main Archean area, are of 
ferruginous quartz-schist. 

Except in the cases of the granitic areas, these rocks are generally 
quite distinctly bedded, and are usually tilted at high angles. 

In many of the areas, especially in those whose elevation is consid- 

erable, horizontal sandstone is found lying immediately against the 
tilted crystalline rocks, pebbles and boulders from which frequently 
occur in the sandstone, giving it often a rough, conglomeratie charac- 
ter, and proving at once the great antiquity and non-intrusive nature 
of the rocks from which they are derived. Some of the arcas have, 
without doubt, been once entirely buried berieath the sandstone layers, 
to whose subsequent denudation they owe their resurrection. 
- The following tabulation gives, in a condensed manner, and ina 
form convenient for comparison, the location, size, nature, ete., of each 
of the known areas. The facts with regard to Nos. II, III, XI, XIII 
and XVIII, are furnished by Prof. Chamberlin, in whose report de- 
scriptions of them will be found. 


503 


THE ARCHAAN ROCKS. 


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oUt GEOLOGY OF CENTRAL ‘WISCONSIN. 


II. Special Descriptions of the Several Areas. 


Tur Barasoo Quarrzire Ranexs. 


The Baraboo quartzite ranges occupy much the largest extent of territory, and are 
at the same time much the most striking and most important as influencing the to- 
pography of the state, of any of the isolated Archwan areas that occur within the region 
of the Silurian rocks. Their bold character, and the dissimilarity between their rocks 
and those of the country around, have drawn to them the attention of previous State 
Geologists, as well as of other scientific men. Percival’ regarded the quartzites com- 
posing the ranges as resulting from a metamorphism of the Potsdam sandstone of the 
surrounding region. Hall? refers them correctly to the Archean, making them Huro- 
rian, but his detailed examinations were not published. Alexander Winchell? calls them 
‘Lower Potsdam,’ on the evidence of some fossils belonging to the middle Potsdam, 
and found in the sandstone lying against the quartzite. This he regards as proving the 
“Lower Potsdam ’’ age of the quartzite, losing sight of the fact that the latter is uncon- 
formable with the sandstone, and projects upwards into the horizon, not only of the 
middle Potsdam, but even far above into that of the St. Peters. The Archean age of 
the quartzite was first definitely proved by the writer in 1872,* and this conclusion has 
since been abundantly confirmed by the work of other geologists,’ and also by his own 
further researches in the region. 

The Baraboo Bluffs constitute two east and west ranges extending some 25 miles in 
length through the towns of Caledonia, in Columbia county, and Greenfield, Merrimack, 
Sumpter, Baraboo, Honey Creek, Freedom, Excelsior and Westfield, in Sauk county. 
The southerm one of the ranges is much the bolder and more continuous, and the two 
are not exactly parallel, but diverge as they are traced westward. At their eastern ends, 
in Columbia county, they unite in a bold point, rising abruptly from the low ground of 
the Wisconsin river, here at the easternmost point of the great bend which the quartzite 
ranges compel it to take. Tracing them westward, we find the two ridges, about mid- 
way in their lengths, some four miles apart, and at their western ends a mile or so more 
than this. Hore a bold, nearly north and south, cross-ridge, also with a quartzite core, 
unites the two, thus finishing an entire cordon of bluffs around a depressed interior. All 
around the outside of this circuit of hills, except beyond the western cross-ridge, the 
country is comparatively low, and often quite level, so that the ridges rise very boldly, 
forming, for a non-mountainous country, quite a striking feature of the landscape. 

The southern quartzite range is broken down in only one place, the gorge in which 
lies the Devil's Lake, and, as seen from the low ground of the Wisconsin river on the 
south, presents a continuous, wavy crest, often with large areas of bare rock, and with 
elevations of from 500 to 700 feet above the river, and of 700 to 900 feet above Lake 
Michigan. Its higher portions have a width of from one to four miles, the outline being 
quite irregular on account of the deep and very anciently eroded valleys that indent its 
sides. The great antiquity of these valleys is evinced by their showing on their sides 
and bottoms layers of horizontal sandstone clinging to the underlying quartzite. The 
sandstone has evidently been deposited in valleys which were originally formed long 
before its deposition, and have been carved out anew in the same places, on account of 


1 Annual Report of the Geological Survey of Wisconsin,” 1856, p, 101. 

2 Geology of Wisconsin, 1862. 

3American Journal of Science II, vol. xxxvii, p. 226, 

4 Am, Journal of Science, Feb., 1872. 

5See J. Il. Eaton “ On the Kclations of the Sandstones, Conglomerate and Limestone, of Sauk 
county to each other and to the Azoic,” Am. J. Sci. IIT, vol. V, p. 144, and T. C, Chamberlin on the 
“ Methods of Upheaval of the Baraboo Ranges,” Wis. Acad. Sci.. vol. IT. 


THE ARCHEHAN ROCKS. 505 


its friable and non-resistant nature. The country on top of the range is heavily timbered 
presenting in this regard, as also in its almost universal heavy clay soil, a marked con- 
trast with the lower country around. This clay soil has caused the making of many ex- 
cellent farms on top of the range. It occurs alike on the quartzite and the high-level 
sandstone. In the eastern extension of the bluffs it might be regarded as of glacial ori- 
gin, but to the westward the glacial drift limit is reached about midway in the length 
of the range, and some other origin must be sought. 

The northern range is much less pronounced than the southern. For about seven 
miles west from the junction of the two, in Columbia county, it forms a continuous ridge 
some 300 to 400 feet in height, but generally much less than a mile in width. Further 
west its height lessens for long distances, the Archean rocks forming its core at the 
same time becoming covered by the overlying horizontal sandstones, through which 
‘they appear here and there in small outcrops. Farther west still this range rises again, 
and where it joins the cross ridge at its western extremity has become again bold, with 
a height of 200 to 300 feet. Although thus indefinite in its middle portions, the higher 
ground never entirely disappears along the line of the range, except at the three points 
where the Baraboo river and one of its tributaries cut through in deep gorges. 

The depressed area within the circuit of the quartzite bluffs is, for the most part, 
somewhat higher than the surrounding outside country, and towards its eastern and 
western extremities rises rather rapidly up to the enclosing ridges. In Columbia county 
much of the area between the ranges is as high as the northern range itself, and is un- 
derlaid by a great thickness of sandstone, which fills in the canoe-shaped trough of the 
uniting quartzite belts. At one time the rest of the valley between the ranges was 
filled in a similar manner, and has since been partially recarved in the friable sandstone 
which still forms its bottom. This valley is now traversed longitudinally by tlhe Baraboo 
river, which enters and leaves it by deep gorges through the northern ridge, having a 
fall between the gorges of about 70 feet. 

The rock constituting the great body of the Baraboo ranges is a quartzite of a non- 
gvanular, usually flaky, texture, and of a color from nearly white, through gray, pink, 
and aimethyst, to purplish-red and even brick-red, the gray and deep-red being the most 
common, the white the least so. Very rarely a distinct granular texture is seen, some- 
what more commonly a slight tendency in that direction. The quartzite is frequently 
very distinctly laminated, the lines of lamination being contorted in a remarkable man- 
ner, and marked by alternating light-colored and dark-colored lines. There is never 
any cleavage parallel to the lamination lines. Next in abundance to the regular quartz- 
ite, and merging into it, are heavy beds of a fine metamorphic conglomerate, usually of 
a grayish to amethystine color, in which the matrix and pebbles are alike of quartzite, 
and not always very well defined from one another. Forming thin layers between the 
thick layers of quartzite, 1s in many places to be seen a peculiar greasy-surfaced quartz- 
schist, the laminze of which are composed of quartzite like that of the regular quartzite 
layers, seamed and covered on the surface with a soft, lilac to white, tale-like, raineral. 
This slate or schist usually exhibits the true slaty or transverse cleavage. The soft 
mineral pervading it-is suspected to be always, as it certainly is sometimes. aluminous 
rather than magnesian. It occurs occasionally forming slaty layers with but little 
quartz admixture, and, in small seams, even entirely pure. It then has rather the 
physical characters of a compacted clay, and this appearance is borne out by the analyses 
given beyond. which show that the pure clay-like kinds are probably not distinct miner- 
als, but rather a mixture of a clayey substance with fine silica. In both physical prop- 
erties and chemical composition this material is closely allied to the pipestone of south- 
west Minnesota, from which it differs only in color. 

Other quartz-schists of quite a different character have been observed forming the 
lowest layers of the north quartzite range, both at the Lower Narrows of the Baraboo 


506 GEOLOGY OF CENTRAL WISCONSIN. 


and at the Upper Narrows of the same stream. These are whitc to straw-colored, dis- 
tinctly granular in texture, the quartz grains being of translucent glassy quartz. The 
whole rock is more or less pervaded by a soft clayey material, and splits out in large 
thin sheets. On the northernmost portions of the north range, at the Lower Narrows, 
and also for a short distance to the westward, a great thickness of quartz-porphyry is 
to be observed. This porphyry resembles that of the several small porphyry areas of 
the adjoining portions of Columbia, Marquette and Green Lake counties and proves at 
once that we must regard these areas as part of the same formation that appears in the 
Baraboo ranges. 

In the quartzite, milk-white veins and nests are frequently to be seen. In some 
places, as at the Upper Narrows, the white quartz veins show frequently geodic cavities, 
lined with quartz-crystals of great clearness and beauty, and not unfrequently of very 
large size, though usually small. In the veins at the Upper Narrows, such crystal- 
lined cavities are exceedingly numerous. Along with the crystals, sometimes compacted 
over them, sometimes loose in the cavities, and again in thin seams by itself, is to be 
seen a soft, white mineral. This is often pulverulent, at, times gritty, at others a nearly 
impalpable powder, and is shown by analysis to be essentially a silicate of alumina. 
With the white quartz, in nests of some size, is often to be observed brilliant specular 
iron in large crystalline surfaces. It occurs also in some of the layers of quartzite, in 
fine scales. Titanic iron is also reported. These, with the peculiar aluminous silicate 
alluded to in connection with the quartz-schists, are the only minerals known to occw 
in the Baraboo rocks. 


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y 7 x g* oa - “a a ae ca a 
Ps 7 B ’ Z yt we - _—— 
7 Z Z ww yf s a _ eee 
z 4 “ ee: y 4 Pa en ae eee ee 
cs 7 7 7 — th 7 aay 
North ange be rhe ye ee Niu giarlzite Range —— fe 
Z < g % Z Zz Z POTS EE_LE_--Z-ZTE- —— 
DLLTIL TIAL LL LS Lo —a 2 = ey 


L 7a 
Levet of the Jea: 


IDEAL SKETCH, SHOWING ORIGINAL STRUCTURE AND AMOUNT OF EROSION OF THE Baraboo 
RANGeEs. 


Scale natural, 12,000 feet to the inch.! 


The quartzites and associated rocks are quite distinctly bedded, though the bedding 
is not unfrequently obscured by cross-jointing, which is often to be observed on a grand 
scale. The dip, wherever observed, is towards the north, through the whole extent of 
both ranges, but varies much in amount. In the southern range it is usually quite 
low, as low sometimes as 15°in the middle and broadest portions. In the northern 
range the dips are always much higher, running from 55° to 90°. The rocks of the 
two ranges appear, however, to be parts of a continuous serics, the quartz-porphyry 
beds of the northern range constituting the uppermost layers. 

For the relative positions of the different ranges and their relations to the surround- 


1A sketch, similar to this, accompanies a paper by Prof. Chamberlin, ‘‘On the Method of Up- 
heaval of the Baraboo Ranges,” Trans. Wis. Acad. Sci., Vol. II, but it is not drawn on a natural 
scale. 


PLATE, XIX 


MAP 


and Cross Nectians illustreding te Structure 
ofthe 


DEVILS LAKE GORGE 
TILN. Ranges VI and VILE. auk County” 
RD Irving, 1076. 


He 


Wy 
Abs 
fino ~~ 


Soe 
K 


a 


Aezpbons 


yay aT 5 a \i 
a ye PAT Hm Wy xe ! 
Qh ai iy . er be | 
3H me : | 
Z 
l 
» B 


Section on tine A.B. 


Section on tine FA OE. Section on tine GH, 


=| 
Quartzite Talus Sandstone 
Topography adapted from maps by WH. Cantield. 
Base line of Sections 200 feet above Lake Michigan. 
Horizontal scate of Sectious and Map linch=1mile . 
Vertical scale linch= 1000 feet 
KL. Level of Devils hake. 


Tar Mawson y beri &) xan Co 


THE ARCHAAN ROCKS. 507 


ing horizontal strata, see Atlas Plate XIV, and the sections of Plate XXI of this vol- 
ume. If the view, just indicated, that there are no folds concealed beneath the sand- 
stone in the intervening valley, is the correct one, the thickness of the entire series musi 
be very great, and the amount of erosion that has taken place correspondingly great. 
Fig. 23 indicates the present structure and relative positions of the ridges, and, by the 
dotted lines above, the possible original structure, and the extent of the erosion that has 
taken place. The figure is drawn to a natural acale, the line of section being the same 
as that of Fig. 1I of Plate XX. The heavy black line represents the overlying Potsdam 
sandstone. It is not impossible that the valley between the ranges owed its existence, 
to some extent, in the first place, to-soft rocks intercalated between the harder quart- 
zites. The hypothesis of Fig..23 is not altogether satisfactory. The entire disappear- 
ance of the other side of the great arch, as well as the peculiar ways in which the 
ranges come together at their extremities are difficult to explain by it. It may be said 
in this connection that the dip observations toward the west are not so satisfactory or 
numerous as they might be. 

The irregular areas over which the Archzan rocks are at surface, are indicated, as ac- 
curately as present knowledge will permit, on Atlas Plate XIV. The greatest difficulty 
in the tracing of the exact boundaries of the quartzite areas lies in the fact that rem- 
nants of the horizontal sandstones which flank and cover them may be found at almost 
any elevation upon the bluffs, so. that no barometrical observations are of avail. The 
areas, as indicated, are, however, very nearly accurate. There are places within them 
where, without doubt, patches of the ‘covering sandstone occur, but the quartzite is in 
every such case but a short distance beneath. The peculiar features of these sandstones 
and their relations to the other Silurian strata of the region are treated of on a subse- 


quent page. 


Beginning the detailed descriptions at the best known, and at the same time one of 
the most remarkable, points about the quartzite ranges, we note first the occurtences in 
the vicinity of Devil’s Lake, in T. 11, ranges 6 and 7 E., Sauk county. Here the 
southern range is cut entirely through by a deep quartzite-walled valley or gorge, 500 
feet in depth, and three-fourths of a mile in width. In its northern portion this valley 
trends due north and south for about a mile; turning then abruptly at right angles it 
extends eastward two miles and a half. In the north and south part lies Devil's Lake, 
with a length of something more than a mile, and a width one-fourth less than this, its 
surface being about 100 feet above the valley surface at the eastern end of the gorge, 
more than 100 feet above the Baraboo river at Baraboo, and more than 200 above the 
Wisconsin at Merrimack. It is held in this elevated position by two immense morainic 
heaps of glacial drift lying at either end of the lake and rising more than 100 feet 
above its level. The lake has a nearly level sandy bottom except near the shores, and is 
over most of its area some 30 feet in depth. It has no outlet, and but one small stream 
running into it. Itis thus probably fed chiefly by springs, and maintains its level by 
evaporation and by filtering through the heaps of gravel and sand which hold it in 
place. Near the northwest corner a small stream running into the Baraboo passes 
within a few rods of the lake, and possibly carries with it some of the lake water. 

As shown on the map of Plate XIX, on its west and south sides the lake washes the 
hases of the bounding cliffs of the gorge. Both east and west cliffs are highest near 
their southern ends, towards which they rise gradually from the north, following roughly 
the dip planes, which also rise southward, and the edges of which can be seen quite well 
marked on either wall of the gorge. By aneroid measurement the highest point of the 
west bluff is 475 feet above the lake level or 860 feet above Lake Michigan, and the 
southern portion of the east bluff but little lower. In their upper portions the cliffs are 
vertical, sometimes for as much‘as 200 feet or more, but their lower parts are clothed 


508 GEOLOGY OF CENTRAL WISCONSIN. 


with a heavy talus or “‘ancle,” composed of great blocks of the quartzite that have 
fallen from the clitls above. These masses are often as much as 20 feet on a side, with 
a somewhat regular shape imparted by the powerful joints that everywhere traverse the 
quartzite, and cut it into blocks only needing to be slightly dislodged in order to fall 
down the cliff. For the greater portion of their lengths both east and west bluffs are 
quite narrow, being backed by deep ravines opening northward. The northern end of the 
east bluff. especially, is a mere crest, having behind it one of the ancient sandstone- 
lined ravines that have before bcen mentioned. 

Tn its east and west extension, the valley preserves the same characters as above de- 
scribed, the cliff on the north side being the highest and boldest, and retaining for a 
long distance the height it attains at the corner where the valley bends. Along the face 
of this cliff the heavy quartzite beds are seen on the strike, and present, therefore, an 
appearance of horizontality when viewed from the valley below. At the mouth of the 
valley, 8. E. qr., Sec. 20, T. 11, R. 7 E, the northern chff is of horizontal sandstone, 
behind which the quartzite passes, whilst the south cliff terminates im a sharp rocky 
point known as the Devil’s Nose. From the summit of this cliff, a short distance west- 
ward from the nose, is taken the view on Plate XV., the Frontispiece of this report. The 
outlook is northwestward through the east and west part of the valley to the lake, be- 
yond which the western cliff of the lake is seen. Doubling the nose, we are on the 
south side of the range, with Sauk Prairie in front, and the high bluff with its roches- 
montonées surfaces of quartzite behind; these surfaces rise in rude steps, which are 
due to the gradual northern dip. 

Near the top of the sides of the ravine shown by the map on the southwest corner of 
the lake, horizontal sandstone and coarse conglomerate occur, the pebbles of the con- 
glomerate coming from the quartzite against which it lies. Nowhere else along the 
sides of the valley until we reach its eastern end are any indications of its ever having 
been filled with sandstone, and, consequently, of its equally great antiquity with other 
ravines about the quartzite ranges. This occurrence itself is not necessarily any such 
indication, for the sandstone is found only at a high level, and may herefore have been 
introduced from the northward, quite independently of the valley of Devil’s Lake, which 
we are thus led to believe is of more recent origin than the Potsdam period. 

This valley has evidently been at some time the passage of a large stream. We can- 
not suppose thatit has been produced by any other process than that of erosion, and 
such an erosion as could only b2 effacted by the agancy of running water. Confirming 
this view, we find, high up on the cliff sides, within 150 fvet of the summit, remnants of 
large potholes, several feet in diameter, presenting smoothed surfaces, and having about 
them many small pebbles and smoothed boulders which may have been engaged in the 
work of their formation. The large size of the valley suggests that it may have been 
the passage of the Wisconsin river, which at the close of the Glacial period found its 
ancient channel obstructed by the great drift heaps that are now to be seen in it, and 
was forced to find its way eastward to the valley of the great river that for long azes 
before the Glacial period drained the whole basin of the Wolf and Upper Fox through 
the valley of the Lower Wisconsin to the Mississippi. This valley, which the deflecte1 
river reached at Portage, and which it subsequently appropriated as its own, passes al- 
together to the eastward of the eastern extremity of the quartzite ranges. If this is a 
bil view, the river inust have had a passage through the northem range also, anl 

his passage would be found in the Lower Narrows of the Baraboo, a much wider 
channel than is needed by that small stream. This explanation of the origin of th 
Devil 8 Lake valley is offered as a suggestion only. The Baraboo may be the stream 
whick the work should he allotted, but, if so, we must imagine it to have been amu) 
larger and more powerful stream than now. Only ten miles above on its course 12 
gorge through which it passes the northern ranz2 p esents no such proportions as se21 


THE ARCHAAN ROCKS. 509 


about the Devil’s Lake valley. For a further idea of the structure of this valley refer- 
ence is made to the sections of Plates XIX and XX. 

The rock in the vicinity of Devil's Lake, omitting reference now to the Silurian con- 
glomerate and sandstones, is nearly altogether the typical quartzite of the region, as 
above described. It generally shows some shade of red. On the weathered surfaces of 
some of the large fallen masses in the edge of the lake, a distinct tendency toa granular 
texture is perceptible, whilst a fresh surface shows generally no traces of it. Fine lines 
of lamination are nearly everywhere to be seen, and are generally quite strikingly 
marked, but there is never any structure parallel to them. They are nearly always bent 
into sharp angles, or curved and contorted, presenting often the irregularities seen in 
the bedding of sandstone. Whilst many of the bendings in these lines may be due to 
original irregularities of deposition, or to contortion at the time of disturbance and alter- 
ation, there are surfaces where they present such a peculiar knotty and concentric ap- 
pearance as strongly to suggest a concretionary origin. A portion about 3 feet square 
of such a surface is figured in Fig. 24. The lines are alternatingly light and dark red. 


Fie. 24. 


Se 
AN 
NN 
SS 


NS 


SURFACE OF QUARTZITE SHOWING CURVED LAMINATION. 


In a few places white quartz veins with geodic quartz crystals are seen, but these do not 
characterize any considerable portion of the rock. All about the Devil’s Lake valley the 
bedding of the quartzite is quite distinct, and is made apparent by the existence of large 
dip surfaces, often beautifully ripple-marked. At the northern ends of both east and 
west, bluffs of the lake many such surfaces occur. Others are seen on the sides of the 
railroad track about midway the length of the lake. These all give an inclination to the 
north of 15° to 25°, the higher figure being seldom reached, and a strike of N. 80° E. 
The quartzite layers are many feet in thickness, showing no internal structure whatever 
parallel to the general dip direction, but being affected everywhere by the curved and 
bent lamination alluded to. Between the quartzite beds occur layers of greasy quartz- 
slate, usually but a few inches in width. Such a layer is well exposed on the side of the 
railroad track on the east side of the lake, the lamine dipping N. 37°, or transverse to 
the bedding planes. The slate is quartzite, like that of the surrounding beds, but is 
penetrated by a soft, greasy mineral, and affected by slaty cleavage. As the cleavage 
planes of the slate approach the surface of the adjoining quartzite, they curve towards 
and penetrate it to a short distance, as indicated in Fig. 25. Large surfaces of quartzite, 


510 GEOLOGY OF CENTRAL WISCONSIN. 


which have had one of these slaty layers removed from above them, show a peculiar 
ridgy appearance, eviuently due to the passage into them of the slaty cleavage planes. 

At the summit of the east bluff, near its southern end, indications of a somewhat 
lower dip than elsewhere are seen, whilst at the Devil's Nose, surfaces occur slanting as 

Fig. 25 much as 29° northward. At the latter place, many 
iaaek cross-joints obscure the bedding, nearly all of the 
Ae Cioran planes, however, sloping northward. Some very 

we mgs el 7 __ large ones were noted, with as high an angle as 82°, 
te et covered with a shining, soft, greasy film. In seams 

and nests in the quartzite, in this vicinity, occurs 
a compact, but soft, clay-like substance (1254) of a 
lilac color, which is penetrated by fine white strings, 
and contains: silica, 62.16; alumina, 29.67; iron ox- 
ide, 4.17; lime, 0.16; water, 2.50=99.36. This sub- 

Oe eles stance appear to be the same as that which per- 

eee === vades and gives character to the quartz-schists of 

a we oe Le ae ae the region, and is closely allied to the red ‘ pipe- 

Svary CLBavagE IN Quarrz Stare ar Stone,” that occurs with the quartzites of Barron 
Devi.’ sLake. county, and again in southwest Minnesota. 

On the summits and sides of all the cliffs about the lake and valley, two sets of very 
marked vertical cross-joints are to be seen, the more prominent and persistent set trend- 
ing N.45° W. These joints have produced, on the upper portions of the cliffs, a striking 
columnar appearance, the separate columns of quartzite, 20 to 40 feet in height, often 
standing entirely detached by the joint cracks from the main cliff. In some cases, in- 
tervening masses of quartzite have fallen, and left entirely isolated needles at a distance 
from the cliff face. 

As in the ravine at the southwest corner of the lake, so also in many other places on 
the north flank of the ridge, horizontal ledges of sandstone and very coarse conglomer- 
ate occur, abutting against, and unconformably overlying the quartzite. At the north- 
ern point of the east bluff, the contact of the two formations is beautifully exposed, and 
the very instructive section represented in Fig. 26 occurs. Here the ends of columnar, 


PoTspaAM BOWLDER-CONGLOMERATR AND SANDSTONE ON ARCILBAN QuaRrzitE 
“ . 

Scale, ten feet to the inch. 
A.B, Quartzite. B.C., Sandstone. C. D., Quartzite. D. E., Sandstone, 


Drvin’s Lake 


THE ARCHAAN ROCKS. j 511 


joint-detached, masses of the quartzite are surrounded and filled between by the hori- 
zontal sandstone, the whole capped with a heavy layer of a conglomerate composed of 
angular, subangular, and rounded masses of quartzite, embedded in a coarse, friable, 
sandy matrix, which is occasionally cemented by the brown oxide of iron, and is not 
unfrequently almost altogether excluded by the included boulders. The quartzite of the 
boulders and pebbles is the same as that of the ledges further up the bluff. Places also 
occur, as shown in the figure, where the sand and quartzite pebbles are wedged down 
into the joint-cracks of the quartzite. 

Eastward from the mouth of the Devil’s Lake valley, in Sec. 29, T. 11, R. 7E, the 
southern face of the quartzite range continues high and bold on the right hand, as far 
as Sec. 25, T. 12, R. 8 E., in Columbia county. On Mr. Fitsimmons’ place, on Sec. 22, 
T. 11, R. 7 E., Sank county, near Parphrey’s glen, and only a short distance from the 
south slope of the ridge, one of the highest points on the whole range of bluffs occurs, 
the elevation being nearly 100 feet greater than that of the Devil’s Lake bluffs. The 
point is in use by the United States Coast Survey, as a signal station. North from the 
signal station, the quartzite range has a width on top of nearly three miles. As far as 
Sec. 3, T. 11, R. 8 E., Columbia county, the south face of the range, except at the 
higher levels, where large surfaces of bare quartzite occur, is composed of sandstone, 
with some coarse conglomerate, which flanks the quartzite in horizontal layers. These 
flanking sandstones are well exposed at the mouth of the Devil’s Lake gorge; in Par- 
phrey’s glen, cn the line between sections 23 and 22, T. 11, R. 7 E., Sauk county; and 
again in Dorward’s or St. Mary’s glen, on the line of sections 18 and 7, T. 11, R. 8 E., 
Columbia county. In all these places, the sandstone layers appear to possess a small 
dip, about 5°, away from the quartzite core. At Dorward’s Glen, the quartzite is to be 
seen at the north end of the gorge, and lying upon and against it sixty feet of horiz- 
ontal sandstone and bowlder-conglomerate, as shown in Fig. 27. These are ex- 
posed on the wall of the gorge, the conglomerate forming the base of the cliff and 
the stream bed, with a thickness seen of four feet. The bowlders of the conglomerate 
are largely irregular, angular masses reaching up to eight inches in size, and are 
almost entirely without surrounding matrix. The quartzite at the head of the glen is 
non-granular, pinkish-gray to red, and without plain bedding. 


Fie. 27. 


ae puartzile ; ‘Potsdam Sandstone and. Conglomerate 


SANDSTONE AND CONGLOMERATE ON QUARTZITE AT DoRWARD’S GLEN. 
Scale 90 feet to the inch. 


East of Sec. 8, T. 11, R. 8 K., as far as the end of the range, the flanking sandstone 
appears to be wanting, outcrops of quartzite in places extending from summit to base of 
the southern face of the range. Such a place occurs on the northern side of Sec. 3, and 
southern side of Sec. 34, T. 12, R. 8 E., near Mr. Fleming's house. Here the quartzite 
bluff rises immediately from the north side of the Portage road, showing for the first 
steep ascent of 250 feet, large loose masses and rough exposures of a metamorphic 
conglomerate, in which matrix and pebbles are both of quartzite, the pebbles beg very 
‘small and in no way different from the matrix. From the top of this slope a gradually 
rising wooded step is crosscd for about a third of a mile to a second nearly precipitous 


512 GEOLOGY OF CENTRAL WISCONSIN. 


rise of over a hundred feet. The summit is of bare rock, and is a mere crest, others 
similar to it occurring east and west along the range. The bedding of the quartzite is 
distinct, the strike being N. 63° E., and dip 60° N. 

On Sees. 34, 35, 26 and 27, T. 12, R. 8 E., numerous other large quartzite exposures 
occur. On the 8. E. qr. of Sec. 27, large outcrops on the roadside show pinkish-gray, 
opaque quartzite (755) with very fine greenish-black streaks (Mica ?). 

The eastern end of the quartzite ranges is on Sec. 25, T. 12, R.8 E., where the 
two ranges unite in the bold point that has been heretofore alluded to. On the north 
side of the point the horizontal sandstone begins again to flank the quartzite. On the 
N. W. qr. of Sec. 25, the road ascending the bluff shows sandstone, with a slight slant 
eastward, nearly tothe top. Near by, on the 8. E. qr. of N. E. qr. of Sec. 26, are large 
rounded exposures (roches montonées) of quartzite showing on the top glacial furrows 
and scratches, and also several large smoothed potholes, the largest two feet wide and 
one foot deep, with connecting furrows. Occurring where no stream could now possibly 
run, these potholes are of interest as showing the great erosion the quartzite must have 
undergone since their formation. 

Along the northern side of the north range and westward from the eastern ex- 
tremity, the flanking sandstone continues nearly to the county line. On the south side 
of section 23, well up on the bluff, a steep ravine has laid bare the sandstone and quartz- 
ite nearly in contact, as shown in Fig. 28. The quartzite here (753) is a fine metamor- 


Fra. 28. 


Dip 60°N 


UNCONFORMABILITY, SEC. 23. CALEDONIA. 


phic conglomerate, in which the matrix of pinkish-white quartz embraces darker-hued 
pebbles 7s inch to $ inch in diameter. The pebbles are very firmly attached to the 
matrix, and are not always well defined from it. Nests and veins of white quartz (754) 
oceur in this rock. 
On the N. E. qr. of sec. 22, T. 12, R. 8 E., a deep ravine shows a great thickness of 
‘sandstone, with a bed of bowlder conglomerate, dipping northward, or away from the 
qnartzite. Further westward along the road from Portage to Baraboo, which follows 
the foot of the bluff, sandstone is seen in numerous places, On the N. W. qr. of Sec. 21, 
high up on the bluff, a well goes through 10 feet of sandstone and then into quartzite. 
It is quite probable that the quartzite core is in places along here entirely covered by 
sandstone. The core does not extend, however, beyond the southern line of sections 19, 
20, and 21, for here wells pass through over 170 feet of sandstone. After passing the 
county line, the north slope of the quartzite is again free from its sandstone mask, and 
is to be seen in small outcrops dipping N. 60°. 


THE ARCHAAN ROCKS. 513 


On Sections 23 and 26, T. 12, R. 7 E., Sauk county, the Baraboo river passes the north 
quartzite range in a gorge known as the Lower Narrows of the Baraboo. Fig 29 
indicates the topography and points of 
Fre: 29. interest in the vicinity of the Narrows. 
3 The passage is nearly half a mile in 
4 width, the level bottom extending to the 
foot of the cliffs on either side. The 
cliffs rise 400 feet above the river, and 
show finely the great beds of quartzite, 
and associated strata. The gorge is 
much wider than needed by the small 
sue stream that now occupies it, and may, 
\\ 


AN as already suggested, have been at one 
time used by the Wisconsin, as the val- 
ley of Devil's Lake seems to have been. 
It is unlike the latter valley in having 
been, in part at least, formed first before 
the Potsdam period, as indicated by the 
way in which horizontal sandstone and 
conglomerate ledges occur around the - 
heads of steep ravines that extend down 
sas bia ere Panos oe Tit Barazoo. the cliff towards the main gorge. Fig. 
30 is a section north and south through 
the west bluff at the Narrows. It is a combination of a paced section made along the 
west line of sections 25 and 26, and of another, not so carefully measured, made about 
40 rods further west. The first follows closely the edge of the cliff, where the quartzite 
beds are exposed to the southern edge of the ridge, the other runs a little west of north 
from Mrs. Garrison's house, in the N. E. qr. of Sec. 27, and passes for along distance over 
horizontal sandstone and conglomerate layers filling an old ravine in the quartzite. The 
scale of the figured section is a natural one, and the contour indicated is quite closely 
that of the range on the westernmost of the two lines. 

Beginnmg with the north end of the section, we find, forming the north face of the 
range, in bold northward sloping ledges, quartz-porphyry about 600 feet in width. 
This porphyry (1244, 1252) is for the most part dull-red to pinkish on the weathered 
surface, which is a good deal altered, often iron-stained, and has generally a whitish 
undercrust. The least altered specimens show a brownish-pink matrix, through which 
are scattered, very thickly, large facets, up to 1g inch in diameter, of bright-red cleava- 
ble felspar, and, more sparsely, minute facets of a white kind. In nearly all speci- 
mens a few small greenish-black blotches, apparently composed of fine mica scales, 
occur, as also small iron-stained cavities, which often show Jinings of minute quartz- 
crystals. The porphyry is very distinctly bedded, showing an E. W. strike, and a dip 
of 58° to 60° N. Towards its lowest portions, and higher up on the bluff, it becomes 
gradually more slaty in character (1245 and 1245a), the felspar facets, though very nu- 
merous, becoming at the same time less well defined, and the surfaces of the lamine 
becoming covered with a soft greasy mineral. This finally changes to a distinct schist, 
about 80 fect wide, containing a large proportion of the soft mineral, and allied to the 
greasy quartz-schists occurring at Devil’s Lake, but without transverse cleavage. Con- 
tinuing the ascent of the bluff southward, quartzite is seen lying immediately under- 
neath the schist, and forming the body of the ridge to the foot of its southern slope. 
At first this quartzite is much veined and seamed with reticulating veins of white 
quartz, in which fine specular iron is occasionally to be seen., At the summit of the 


‘ 


\ 


1 Thi: echist is probably non-magnesian, like the schists of Devil's Lake, ordiuarily called talcose. 
Wis Sur. —33 


1+ GEOLOGY OF CENTRAL WISCONSIN. 


hill this character is less marked, and the rock (1255) is a dark 
3 reddish-purple quartzite with a distinct tendency to a granular 
4 texture, the individual grains being vitreous and translucent, 
i but the rock as a whole having a dull, opaque appearance. The 
# bedding of the quartzite is not everywhere very plain. Towards 
; tke north the layers appear to conform to the directions noticed 
in the overlying porphyry, but further southward the inclination 
is much steeper, and on the south slope, near the end of the 
ridge, beautifiully ripple-marked vertical surfaces are seen. In- 
terstratified with the quartzite in places are some greasy-sur- 
faced schistose layers. At the foot of the hill, near Mrs. Gar- 
rison’s house, the low est member of the series is séen in a pecu- 
liar white to straw-colored quartz-schist or slate (1254). This 
slate occurs in regular smooth-faced, brown-tinted, layers, ~sth 
inch to 3 or 4 inches in thickness, and has a fine granular tex- 
ture, the grains being of more or less angular quartz. Sur- 
rounding the grains and pervading the mass is a fine white 
pulverulent matrix, which renders the rock soft, and has w 
highly argillaceous odor when breathed upon. Only about 15 to 
20 feet are exposed. The northward dip is very plain, the 
edges of the layers in places being much bent out of the true 
inclination, which, as seen in the old shaft near by, is as much 
as 60° to 70°. The whole thickness of the metamorphic rocks 
represented in this section is not far short of 5,000 feet. 

A short distance westward, and a few feet above the quartz- 
schist just described, horizontal sandstone is quarried. Further 
up the bluff, this is succeeded by a great thickness, probably 
a hundred feet, of a horizontally bedded, coarse bowlder-con- 
glomerate, the bowlders chiefly of red quartzite from the rocks 
near by, and the matrix usually a loose friable sand. The con- 
glomerate rises nearly, or quite, to the summit of the ridge. 

The east bluff of the Narrows does not present so fine a sec- 
tion as the one just described; the exposures are, however, very 
large. Atthe south point of the clit, the elevation is 310 feet 
above the Baraboo, and the rock a very compact, red-tinged, 
slightly vitreous quartzite. Near the middle of the cliff, a very 
steep ravine indents its face. On the south side, and around the 
head of the ravine, are horizontal ledges of a conglomerate of 
quartzite pebbles up to 6 inches in diameter, for the most part 
without matrix. What matrix is present appears in many 
places to be almost as much of a quartzite as the pebbles them- 
selves, though in others it is sandy and friable. On the north 
side of the ravine, semi-translucent, amethystine quartzite is 
seen, unconcealed by conglomerate. Further northward, the 
steep N. 70° dip of the quartzite is very plain, the dip surfaces 
being often laid bare for a great distance, and giving a very 
steep slope to the north side of the ridge. The east cliff of the 
Narrows does not extend so far north as that on the wesf. 

West from the Narrows, for about two miles, the north 
x face of the range trends north of west, continuing to show all 
§ along beds of quartz-porphyry. Since the strike throughout is BE. 
8 W.., the existence of a very much broader belt of porphyry than 


Sandstone 


Niggas 


SSeS ‘hide 


Fre. 30. 


red and [eure Gicartzit: 7 me 


Norra anp Soutu SECTION THROUGH THE WeEsT BLUFF OF THE LowER NaRRoWS OF THE BalkazBoo. 
Scale natural, 800 feet to the inch. Section about one mile long. 


"y bedded 


C0 


THE ARCHAAN ROCKS. 515 


shown in the Narrows section is indicated. On the south side of the S. E. qr. of Sec. 16, 
the porphyry reaches its northernmost point, showing in a bold rocky projection. The 
rock here (1,242) presents a dull-brownish appearance on a weathered surface, and is 
much fissured by weathering, the surfaces of the fissures showing generally a brownis|1 
ivon stain. A schistose structure is apparent in places, and the bedding is plain, with an 
I. W. strike, and dip of 55° N. A fresh fracture shows a compact, flaky matrix, of 
dark-brown to nearly black, sometimes grayish color, the last being characteristic of al- 
tered portions. The color is not quite uniform, but is mottled with fine strings and 
specks of whitish er pinkish color, and of indefinite outline. This matrix fuses easily to 
a black glass. In altered specimens it is easily scratched by the knife, in unaltered ones 
the knife makes almost no impression. Sparsely scattered through it are minute white 
and pink felspar facets, and still fewer large brick-red ones. In this regard the rock is 
quite different from that of the Narrows section. 

About one-eighth to one-fourth of a mile eastward from this rocky point, in the N. E. 
qr. of the N. E. qr. of Sec. 21, the porphyry is seen again in a large exposure, showing 
the same weathered appearance, and bedding structure. Specimens from this place 
(1,243) resemble the rock last described, having somewhat more numerous felspar facets, 
and containing: sihca, 71.24; alumina, 12.20; iron peroxide, 1.71; iron protoxide, 5.44; 
lime, 0.98; magnesia, 0.13; magnanese oxide, 0.97; potash, 1.86; soda, 4.29; water, 0.81 
=99.63. The large content of soda, as compared with potash, is noteworthy. 

The quartz-porphyries have thus been traced along the north flank of the range from 
the Baraboo Narrows, in Sec. 23, to the south side of Sec. 16. 
Judging from the bedding directions, thei whole width can- 

not be less than three-fourths of a mile, nor their actual thic'- 
ness short of 3,200 feet. They are found nowhere else in 
the Baraboo region. From the descriptions and analysis given 
it will be seen that these rocks have a matrix too silicious to 
be purely felspathic, through which are scattered crystals of 
orthoclase, possibly also of a soda felspar, the porphyrite 
quartz crystals generally characteristic of quartz-porphyry be- 
ing absent. They are evidently nearer to true quartz-porphy- 
ry, however, than to the non-silicions porphyrites.' 

Further west again, and until we reach the Upper Nar- 
rows of the Baraboo, in the town of Excelsior, the quartzite 
exposures along the north range are only occasional, as on the 

: low ridge north of Baraboo, and on the N. E. qr. of Sec. 33, 
\_. T.12,R.6E. 

On Secs. 28 and 29, T. 12, R. 5 E., in the town of Excel- 
sior, the Baraboo river breaks southward through the north 
quartzite range in a narrow gorge, 200 feet in depth, and 
something more than half a mile in length, known as the 
Upper Narrows of the Baraboo. For most of its length 
Scale, 1% inches to the the yavine is just wide enough to admit of the passage of the 

mane river, railroad and a wagon road. Here the quartzite core of 
the north range is finely shown, flanked on either side, and even overtopped, by the 
horizontal sandstone and conglomerate. Fig. 31 is a map® showing the shape and 
character of the gorge. Fig. 32 is a section on the line A B C of Fig. 31, drawn to a 
horizontal scale of 750, and a vertical of 300 feet to the inch.? 


Fie. 31. 


Uprer Narrows OF THE 
BARABOO. 


1 Von Cottas Lithology, pp. 168 and 214. 

2 Copied from Mx. W. H. Canfield’s map of Excelsior. 

3 In Fig. 32, the inclined lines in the * veined quartzite” are meant for shading only, and do not 
indicate any structure to the rock, which, as described, is without distinct bedding, . 


516 GEOLOGY OF CENTRAL WISCONSIN, 


quartzitic and friabie sandstone; 


together again 
by milky-white 
vein quartz, the 
numerous cavi- 
ties in which 
are lined with 
small, brilliant, 
and very per- 
fect quartz crys- 
tals. The ex- 


3 
A 
pet 
na 
“od 
a 
os 
3 
2 
2 
3S 
ea 
Ow 
ond th a 
Bs dish, sometimes 
NS : se ite, which has 
NS SN 8 © been shattered 
\ obs : 
NG WN 2 £5 throughout into 
Sn a ot 
Si AB small, sharply 
St H# 2 angular frag- 
SS B #8 
™ £2 ments, and 
o 4s 
a ~.; these cemented 
=) EB e.. 
& 
A 
< 
a 
4 
2) 
vy 
ad 
p 


e] 


Fie. 32. 
a, a, a, cross-laminated sand 


matrix; e, quartzitic sandstone 


Norra anp Sovutu SEcTIoN 
g. 31. 


At the southern end of the section — the ‘‘ Jaws of the 
Narrows *’— horizontal sandstone layers, alternatingly hard 
and quartzitic, and soft and friable, are seen abutting 
against and overlying heavy beds of northward-sloping, 
pinkish-gray, dark-gray, and purple, vitreous quartzite 
(1273, 1274). The exact contact of the two formations is 
finely exposed, the sandstone filling the cracks between the 
layers of quartzite and including large detached masses of 
the latter rock. A short distance northward, along the wall 
of the gorge, this quartzite is terminated by a steep ravine, 
on the north side of which comes in the veined quartzite 
that forms the body of the ridge. This curiously veined 
rock (1267, 1275) may be described as a light to dark-red- 
purple, usually somewhat vitreous, quartz- 


Fie. 33. 


g , 
: f a4 
Vp Dy 0 a 
) —$$odieCavitiel 


Ee tensive fissuring 
83 to which this 
23 

= rock has been 
os 

a 

3s 

Se 

Oo. 

io) 

2s : : 
»s ments of the quartzite. 
aa 

a2 

ca 

ag 

a3 

23 

Lomo) 

ia) 

cs 

ad 

oO 

Pid 

° 

oo 

rat 

o 

roll 

<q 


VEINED QUARTZITE. 


subjected is indicated not only in the interlacing veins of 
white quartz, which often make up half the mass, but al- 
so in the frequent juxtaposition of different looking frag- 


Certain portions of the rock are 


more fissured than other neighboring portions, and then 
appear like wide veins into which numerous fragments 
of the wall rock have fallen. Fig. 33 represents a small 
area, two feet by one and a half feet, of the veined 
quartzite, the white representing the vein-quartz, the 
black the fragments of red quartzite. In some of the crys- 
tal-lined cavities a soft white coating is noticed on the crys- 
tals. The same material is seen sometimes lying loose in 
the cavities and again filling minute cracks in a more com- 
pacted condition. According to Prof. Daniells’ analysis ‘it 
contains silica, 53.15 per cent , and alumina, 45.09 per cent., 
the balance being water. The bedding of the veined 


quartzite is indistinct. Jt appears to stand at a high angle to the northward. 
North of and overlying the veined rock is another belt of quartzite (1277) without 


THE ARCHEAN ROCKS. 517 


vems, of a pinkish color, and containing much of the greasy, tale-like mineral, which, 
m places, imparts a highly schistose character to the rock, Sometimes predominating 
over the quartz. In these cases the slaty laminze incline westward 15°, whilst the whole 
rock is intersected by E. W. planes standing at nearly 90°. The schistose layers are 
ouly in the upper portion of the belt which further south is purer quartzite with an evi- 
dent northward dip. 

As indicated in the figure, the quartzite is over-topped, for nearly the whole length 
of the section, by horizontal sandstone and conglomerate layers. The conglomerate 
capping the bluff in its higher portions, and overlying the veined quartzite, shows a 
mass of pebbles and small bowlders of the veined rock, compacted together without 
matrix, or with one that is very hard and quartzite-like, and of a brownish color. A 
fine exposure of this conglomerate is to be seen at the top of the cliff, at a point just 
east of the southernmost of the two railroad bridges within the Narrows, and on the 
south side of the bend which both gorge and river here make to the eastward. At the 
top of the cliff, on the north side of the bow, 140 feet above the railroad track, sand- 
stone, partly hard and brownish, with a vitrified appearance, and partly friable, is un- 
derlaid by horizontal ledges of a conglomerate, having a hard quartzite matmx, and 
including red quartzite pebbles and bowlders of all sizes. Twenty-five feet below the 
top of the cliff, the junction of the conglomerate with the underlying vertically-bedded 
quartzite is seen. As viewed from the track below, the unconformability is very striking. 
The conglomerate extends northward from this point, and.down the side of the ravine 
next north of the bend of the river, to within 30 feet of the railroad track. Its lower 
portions (1278) show a loose, friable, bownish matrix of coarse sand, the quartzite peb- 
bles running up to a foot in diameter, but being usually smaller than this. Below the 
conglomerate, and abutting directly upon the railroad track, is a cliff 20 to 30 feet high, 
of coarse, brownish, friable sandstone, without pebbles, showing cross-lamination on a 
grand scale. North of the ravine, a low sandstone ridge is capped by the lower layers 
of bowlder-conglomerate. . 

On Sec. 31 of the town of Excelsior, is another gorge, known as the Narrows of 
Narrows Creek. In its structure and rock occurrences, this gorge is similar to the 
Narrows of the Baraboo, the veined quartzite, however, being less developed than at 
the latter place. Between the two gorges the summit of the range is quite level. 

Westward from the passage of Narrow’s Creck, the north quartzite range curves south- 
ward to meet the north and south ridge that connects it with the southern or main 
range. In the road near the center of Sec. 36, T. 12, R. 4 E., Reedsburg, well up on 
the ridge, quartzite is exposed with an E. W. strike and dip of N.70°. This is its north- 
ern limit, and the western end of the range, for just west of the road a rocky ravine, 
over 100 feet in depth, shows the quartzite flanked on the north by heavy beds of coarse 
conglomerate and friable sandstone, the quartzite occurring only on the eastern wall of 
the ravine, the western side being altogether of sandstone. 

South from the center of Sec. 36, along the connecting ridge, the ground rises steadily 
for several miles. For the first mile, horizontal sandstone ledges are seen rising to an 
elevation of 520 feet. In the north part of Sec. 13, T. 11, R. 4 E., Westfield, eleva- 
tions of over 600 feet are reached. In this vicinity, and over a considerable area in sec- 
tions 11, 12, 18, 14, 23 and 24, low outcrops of quartzite occur, the area including them 
being all very high, and constituting a rounded swell above the general level. A long, 
low outcrop near the Lutheran church in 8. W. qr. Sec. 13, shows dark, purplish-red, 
flaky-textured quartzite (1322), which is plainly bedded, and laminated, and dips 57° 
N. W., the strike being N. 47° E. 

Southward from the quartzite outcrops the elevation continues to be between 500 and 
600 feet, in sections 23 and 26, but the only rock to be seen is horizontal sandstone. 
Westward from these sections, the elevation remains about the same, and one passes 


518 GEOLOGY OF CENTRAL WISCONSIN. 


insensibly on to the Lower Magnesian limestone. Eastward, in sections 24 and 25, the 
descent of 200 feet to the headquarters of Seeley creek is very rapidly made, and sand- 
stone is exposed through nearly the whole vertical distance. 

On Sec. 35, a large exposure of reddish glassy quartzite occurs in a ravine, at an ele- 
vation much below that of the country occupied by sandstone to the northward. A few 
rods up the ravine, sandstone ledges occur at a higher level. Taken together with the 
construction of the high country all through the east side of the town of Westfield, this 
outcrop is believed to indicate the existence throughout of a quartzite core only slightly 
covered with sandstone layers. 

The outcrop just referred to is on the slope downward towards the valley of the Wis- 
consin, and is really the western end of the southern quartzite range. From here east- 
ward to Devil's Lake, we find this range as bold and wide as it is east of the lake, aad 
characterized by the same heavy timber and clay soil. In T. 10, R. 5 E., Honey 
Creek, the southern slope of the range is in the northern row of sections. In the south 
side of T. 11, R. 5 E., Freedom, are very high rounded swells, some of which are 
amongst the highest points on the range. On the northern slope, in this town, the 
streams flowing north into the Baraboo set back mto the ridge in deep ravines, about 
which sandstone sometimes occurs at high levels. On the N. W. qr. of Sec. 22, the 
quartzite shows in two bluffs, 150 feet high, on either side of the creek, with a distance 
between of about one-eighth of a mile. The rock here is for the most part closely like 
that at Devil's Lake, but portions are unusually light-colored (1,271), showing a light- 
brown weathered surface, and a nearly white, slightly granular, fresh fracture. Regu- 
larly interbedded is a soft, light-gray, greasy, finely laminated, clay-slate (1,272), con- 
taining according to analysis by Mr. A. C. Prescott: silica, 59.84; alamina and iron 
oxide, 35.39; magnesia, 0.10; water, 4.67100; the iron oxide being in very small 
amount only. Both quartzite and slate are plainly bedded, the strike being N. 23° W., 
the dip 16° N. 

On the road extending southward from Bloom’s Station across the range, into Honey 
creek, horizontal sandstone ledges axe seen, as far as the N. W. qr. of Sec. 23, at an ele- 
vation of 530 feet. In the southern part of the same section, quartzite is exposed at an 
elevation of 700 feet, and along the east side of Sec. 26, an elevation of 830 feet is 
reached. 

In the southern row of sections of T. 11, R. 6 E., Sumpter, the south slope of the 
range is very bold and prominent, owing to the low ground of Sauk Prairie, which 
stretches from the foot of the bluffs for eight or nine miles to the southward. All along 
the slope towards the prairie are large rough exposures, — as, for instance, on the west 
Sauk road on Sec. 34; in the ravine on Sec. 27; on the east Sauk road, in Sec. 35, and 
all along the range eastward from here to the Devil’s Nose. On the north slope of the 
range in the N. E. qr. of Sec. 15, T. 11, R. 6 E., dark-grayish, somewhat granular 
quartzite shows in a large exposure, with a dip of 26° N. 

Within the circuit of the quartzite ranges, are a few isolated points of quartzite 
and schistose rocks, which rise through the sandstone that forms the basement of the 
valley. One of these, on the south line of Sec. 29, T. 12, R. 7 E., on Peck’s Prairie, is 
a low rounded ridge 75 fect high. The rock here (1,247) is a light pinkish-grey meta- 
morphic conglomerate, composed of small rounded pebbles of quartzite 1-16th to 1-8th 
inch in diameter, embedded in a finer-grained matrix of similar character. An obscure 
N. 70° dip is to be seen at a few points, and veins of milky quartz occur, carrying nests 
of large-surfaced brilliant specular iron (1,248). One of these veins is 75 fect long and 
2 feet wide, with nests and seams of specular iron, 1 to 3 inches wide. A few rods west 
of the quartzite, at the center of the north line of the N. W. qr. of Sec. 32, horizontal 
sandstone ledges are seen. ; 

Other areas showing quartzite and slate occur on See. 5, T. 11, R. 6 E.; Sec. 4, T. 11 


THE ARCHAAN ROCKS. 519 


B.5 E.; and Sec. 2,'T. 11, R.5 Ey The two former are high, rocky points, the latter 
a low outcrop on the river side. Siill another occurs on the 8. E. qr. of Sec. 33, T. 12, 
R.5 E., near Ableman’s. Here a railway cutting passes through the point of a ridge, 
near the north bank of the Baraboo river. At the west end of the cutting coarse white 
sandstone, in horizontal ledges, lies against a craggy cliff of hyht-colored quartz-schist 
(1284), resembling that at the south side of the section at the Lower Narrows of the 
Baraboo (see Fig. 30), but less regularly slaty. At the junction of the two rocks large 
bowlders of quartzite are included in the sandstone, which itself fills in the cracks be- 
tween the layers of schist. One hundred and thirty feet from the west end of the cut- 
ting, the light-colored schist gives place to a gray or greenish clayey rock (1283). Some 
of the layers are bright green in color, and marked with very fine lines of lamination. 
These layers are apparently quite silicious. Seventy feet further, pinkish granular 
quartzite (1282) is indefinitely exposed. The exposures throughout the cutting, though 
in places 40 feet high, are very much jointed and confused. The position near the end 
of the ridge has caused much weathering and alteration. There is evidently a high dip, 
apparently to the north. 


Tue Marcetton Qvuartz-Porpuyry. 


On Sec. 7, in the town of Marcellon, Columbia county, on each side of the road in the 
south half of the section, are two low rounded hills, 40 to 60 feet in height, of quartz- 
porphyry (759). The rock exposures are large, and are much rounded and weather- 
worn, being separated into numerous bowlder-like masses by wide-open, earth-filled 
joints. The weathered surfaces have a prevailing pinkish tinge, giving the idea that 
the rock is largely composed of pink felspar. On obtaining a fresh fracture, however, 
only a very few, sparsely scattered, minute felspar faces are to be seen, the mass of the 
rock being composed of a brownish to blackish compact matrix. Two general varieties 
occur, one presenting a light brownish color, showing a tendency to flake off in frag- 
ments that are translucent on the edges, and containing no distinguishable felspar 
crystals, the other having a dark-gray to black matrix, in which are to be seen a few 
distinct crystals of felspar and numerous copper-colored points of iron-sesquioxide. The 
rock has nearly the hardness of quartz, and fuses only with the greatest difficulty. A 
more silicious character as compared with other quartz-porphyries of the state is thus in- 
dicated, and the indication is borne out by the content of silica —76.98 per cent. — as 
shown by analysis. We have evidently, in this case, a porphyry which, in its large 
content of silica, and in the sparseness of its felspar crystals, approaches the true felsites 
(petrosilex, hilleflinta). Quite a distinct and uniform set of bedding joints occurs, the 
strike being N. 32° E., the dip 65° to 75° N. W. Numerous cross-joints traverse the 
rock, and, on weathered portions, cause it to fly into smooth-faced, angular fragments, 
at the least blow of the hammer. The surrounding country is occupied hy the Potsdam 
sandstone, which is exposed at many points. 


Tur Onservatory Hitt Quarrz-PorpPuyrry. 


Six miles north of the Marcellon outcrop, in the S. b. qr. of Sec. 7, in the town of 
Buffalo, Marquette county, a knob of quartz-porphyry rises 250 feet above the general 
level, and 490 feet above Lake Michigan. On the flanks of the hill and up to a vertical 
distance above the base of 125 feet, are horizontal sandstone ledges. Above, to the 
top, are nearly continuous outcrops of porphyry, with a not very plain N. 32° E. strike, 
and 60° N. W. dip. These bedding directions are the same as on the Marcellon out- 
crop. 

The porphyry (762) has a dark-grayish to black compact matrix, in which are thickly 
scattered quite large (one-eighth to one-fourth inch in diameter) brownish to. pink facets 


520 GEOLOGY OF CENTRAL WISCONSIN. 


of felspar, the whole presenting a very dark-colored appearance. The silica content is 
73.56 per cent., and the specific gravity, 2.60. Numerous close joints occur throughout 
the exposure, causing the rock to split like that of the Marcellon outcrop into small, ir- 
regularly shaped, smooth-faced, angular fragments. 

The surrounding country shows everywhere the Potsdam sandstone as the surface 
rock. A high bluff of this sandstonc, some 100 feet lower than the top of the Observa- 
tory, lies on the S. W. qr. of the same section. 


Tue Mounpvirre Quarrz-Porrnyry. 


On the edge of the Fox river marsh at the head of Lake Buffalo, on the line between 
sections 8 and 5, T. 14, R. 9 E., Moundville, Marquette county, are three low rounded 
outerops of quartz-porphyry. These are five miles, in a direction 10° N. of W., from 
Observatory Hill, which is the nearest Archaean outcrop. No other rock shows in the 
neighborhood, the country being heavily drift-covered. The largest outcrop is on the 
east end of a low bluff 35 feet high, and several hundred feet in length. ‘There are 
quite marked appearances here of the same N. E. strike, and N. 60° dip, as seen at 
Observatory Hill and in Marcellon. The rock (1480) has a dark brown matrix, re- 
sembling in this regard the Marcellon porphyry, from which it differs, however, in show- 
ing throughout traces of crystalline structure, and quite thickly scattered, large, brown- 
ish felspar surfaces. A few crystals are white and translucent. The weathered sur- 
face is often of a bight pink color. Mr. Wright’s microscopic examination (Appendix) 
shows that fine magnetite particles are abundant. Their existence is not renctered evi- 
dent even by the use of the ordinary lens. The silica content is 72.76 per cent. 


Tur Seneca (Pine Bivrr) Quarrz-Porpuyry. 


A rounded elliptical knob of quartz-porphyry, 100 feet high, }gth mile long, and 4th 
mile wide, lies on the north side of the White river marsh, in Sec. 2, T. 17, R. 11 E., 
Seneca, Green Lake county. The greatest extension of the hill is in an east and west 
direction. Itis largely rocky, but there are no abrupt rock ledges, the exposures being 
almost entirely surfaces conforming to the general contour of the lull, and on a level 
with the surrounding sod. In places, the slopes of the hill are covered with angular 
fragments, apparently split off by frost. This is a peculiarity not noticed on any of the 
other porphyry outcrops, and appears to be due to the large content of comparatively 
coarse, cleavable felspar. The hill is only about two miles south from the granite hills 
of Spring Lake, in T.18, R. 11 E., Waushara county. The surrounding country is 
marshy and drift-covered, and shows no outcrop of horizontal rocks. The loose frag- 
ments are many of them smoothed on one side, and some surfaces are most beautifully 
striated. Owing to the broken condition of the outcrop, no definite bedding planes were 
made out, though weathered specimens brought away show distinct traces of lamination. 

This porphyry in its least weathered portions (1410) shows a light-gray to whitish fine- 
grained matrix, made up largely of fine glassy felspar crystals, and containing numer- 
ous large surfaces of the same kind. The more weathered specimens (1412) have a pink 
to white, quite distinctly granular matrix, in which with the lens can be seen what ap- 
pear to be angular grains of quartz. The glassy felspar crystals are also abundant. 
The weathered surface is brownish, with a kaolinized undercrust. Nearly all of the rock 
shows signs of weathering. The silica content is 76.39 per cent. 


Tar Marquerrzy anp Bertin Quartrz-PorpuyRries. 


The large outcrops of quartz-porphyry on scctions 34 and 35, T. 15, R. 11 E., and sec- 
tions 2 and 3, T. 14, R. 11 E., near the village of Marquette, Green Lake county, were 


THE ARCHAAN ROCKS. 521 


originally regarded as within the Central Wisconsin district, of which, however, by sub- 
sequent agreement, the Fox river was made the southem boundary. They will, there- 
fore, be described by Prof. Chamberlin, in whose district is also the outcrop at the city 
of Berln, Green Lake county. As the writer has examined both localities carefully, he 
may be permitted to allude to the nature of the rock of each, for the sake of coviparison 
In the Marquette outcrops, the prevailing rock (761, 1,426), noticed, has a black, com- 
pact, flinty matrix, which is streaked with white non-continuous lines. These lines are, 
for the most part, very prominent, and are frequently much contorted, the whole rock 
having a very evident parallel grain. The felspar crystals are minute and sparse. The 

* silica content (1,426), is 70.29 per cent. Jess than obtained from any other of the Wis- 
consin porphyries. The general course of the contorted lamin points to the same 
N. E. strike direction, as observed on the Marcellon, Observatory Hill, and Moundville 
outcrops. 

The Berlin rock has a dark bluish-gray matrix, much streaked with white, and hav- 
ing a peculiar fine-granular, quartz-like texture, as seen under the lens. The tfelspar 
crystals are small, greyish to brownish, and rather numerous. The lamination is very. 
fine and distinct, and often contorted, and the silica content 74.37 per cent. 


A comparison of the rocks of the several porphyry areas shows 
that though all present the same general kind of rock, no two of the 
areas are exactly alike in this regard. The porphyry associated with 
the Baraboo quartzite has a dark brown to black matrix, numerous. 
large, pink, felspar crystals, and 71.24 per cent. of silica. The Mar- 
cellon porphyry has a brown to black matrix, is almost without felspar 
facets, and contains 77 per cent. of silica. The Observatory Hill por- 
phyry has a black, flinty matrix with numerous large, brownish felspar 
facets, and contains 73.56 per cent. of silica. The Moundville porphyry 
resembles the Marcellon rock in the color and appearance of the matrix,. 
but contains much brownish felspar, some magnetite, and only 72.76: 
per cent. of silica. The Seneca porphyry is altogether different from 
the others, in having a light colored, nearly white, somewhat granular, 
and distinctly quartzuse matrix, and in containing much white, glassy 
felspar, the percentage of silica being 76.39. The Marquette porphyry 
has a black, flinty matrix, in this regard resembling closely the Obser- 
vatory Hill rock, from which, however, it differs in being almost with- 
out felspar facets and in having its matrix streaked with white, and 
thus presenting a very marked lamination, the silica content being 70.29, 
orless than that obtained from any other of these rocks. The Berlin 
porphyry resembles that from the Marquette outcrop in having a 
marked lamination, but differs in the color of its matrix, in contain- 
ing plentiful felspar faccts, and in having a larger percentage (74.37). 
of silica. Its peculiar fine granular matrix is also a very distinguish- 


ing characteristic. 
Tur Monretto GRANITE. 


Jn the village of Montello, on ‘the west side of Sec. 9, T. 15, R. 10 E., Marquette 
county, iy an elliptical-shaped rounded mound of pink granite, about a third of a mile 


522 GEOLOGY OF CENTRAL WISCONSIN. 


in length, and 40 feet high. Over iumost of the hill the rock (756, 758, 764, 765) is quite 
uniform on a fresh fracture, though presenting a weathered surface from bright pink to 
dull grayish-pink in color. The weathering is very slight, however, and the rock shows 
almost no tendency to decompose. It has a medium grain, close texture, is of a bright 
pinkish color, and without sign of arrangement of the ingredients in lines. These are: 
rather large-flaked, pinkish, cleavable felspar, predominating; somewhat granular, 
fine, pinkish, translucent quartz, abundant; and greenish-black mica, sparsely scattered, 
in blotches made up of very fine flakes. In places, thin light-green epidote-colored 
seams occur (757). Somewhat irregular N. W. joints traverse the rock which is, how- 
ever, for the most part structureless, and is quarried by firing, the pieces that crack off 
presenting a conchoidal fracture. On the north side of the west end of the mound oc- 
curs a vertical layer (or vein?) three feet wide, trending N. 55° E., of a soft greenish, 
highly schistose, decomposing chloritic rock (758). The least weathered specimens show 
a blackish color and some tendency to a crystalline texture. The vein is weathered 
down for two or three feet below the enclosing granite walls, both of which are seen. 
The schistose lamine are parallel to the walls. Greenish epidote seams in the rock near 
by have the same trend as the vein. Though this granite might be somewhat difficult 
to obtain in dressable masses, it would undoubtedly make a very handsome and durable 
stone. 


Tur Marion Granrre AREAS. 


Tn the the town of Marion, T. 18, R. 11 E. Waushara county, are three low granite 
knobs. Two of these, Stone and Pine Bluffs, are on the N. E. qr. Sec. 27, about two 
miles in a N. N. W. direction from the quartz-porphyry hill of the town of Seneca, 
Green Lake county; and the third, a larger and bolder hill, lies on the eastern border 
of the marsh, on Sees. 12 and 13, and stretches to some extent over the line into the 
town of Warren, On all of these areas the rock (766, Sec. 27; 767, 768, Sec. 12) ob- 
served is nearly the same, a pinkish felspathic granite, mottled with gray and green, 
closely resembling the Montello granite, from which it differs, however, in having a 
coarser grain, less close texture, and a marked tendency to decompose. Reddish cleav- 
able felspar is the principal ingredient, occurring in facets up to 1yth and 44th inch in 
diameter; quartz is abundant, fine-granular and translucent; mica is sparse, and 
scattered in small, greenish-black blotches. Large whitish porphyritic felspar occurs. 
There is no sign of any arrangement of the ingredients, or of any parallel grain to the 
rock. No definite bedding planes were observed on any of the outcrops, though numer- 
ous crossing joint planes cccur, and quite regular flat slabs are sometimes obtainable. 
Veins of white quartz occur. The most marked characteristic of the rock is its tendency 
to weather and shell off in crumbling masses. Some of the large flat surfaces are so far 
crumbled as to be penetrated readily by a horse’s hoof. The rock from these outcrops 
would polish easily, but its tendency to crumble renders it less valuable than the Mon- 
tello granite. 


Conclusions. As indicated by their common character and strike 
direction, as well as their relative positions, the quartz-porphyry and 
granite patches of Columbia, Marquette, Green Lake and Waushara 
counties, which have been described in the foregoing pages, are doubt- 
less to be regarded as but projecting points of one northeastward 
trending belt, the rest of which is buried beneath the Silurian sand- 
stone and later superficial deposits. All, both granites and porpby- 
ries, belong evidently to the same formation. Moreover, the occur- 


THE ARCHAAN ROCKS. 528 


rence of similar porphyry with the quartzites of the Baraboo 
ranges, throws all the areas, without question, into the same category 
as those quartzites. We have thus a great quartzite series, including, 
also, quartz-porphyries, and associated with these pinkish, close-tex- 
tured, (intrusive?) granite. Such an association is not a new one. 

Percival’ in alluding very briefly to some of the porphyry and 
granite areas, the rocks of which, however, he calls by other and in- 
correct names, intimates that the granite patches (his syendte) form a 
belt altogether to the westward of the others. This conclusion is not 
borne out by the facts. The Moundvyille porphyry lies on a line, as 
indicated by the N. 32° E. strike, altogether west of the Montello and 
Marion granites, which are thus, evidently, but portions of the same 
series. 

The entire width of the granite and porphyry belt, at right angles 
to the trend, is not less than twenty-five miles, the Mackford area ly- 
ing on the extreme east, that of Montello on the extreme west. The 
length from the Marcellon area on the south, in a N. 32° E. direction, 
is 30 miles. Regarding the belt as continuous, as it undoubtedly is, 
with the Baraboo ranges, it is evident that it must make a great bend 
northeastward, in the region about Portage. A glance at Plate 
XVIII of this volume, will suffice to show that, towards their eastern 
ends, the quartzite rangés are already on the turn. 

The parallelism of the belt thus made out with the edge of the. 
main Archean area to the northward, is striking, and strongly sug- 
gests that we have here part of a once continuous band of Huronian 
surrounding the old northern core, after the manner of the later Silu- 
rian formations. 


Tar Necepan QUARTZITE. 


Dotting the great sand plain of the Wisconsin in Juneau and Adams counties, are 

numerous bold castellated outliers of the Potsdam sandstone, rising abruptly from the 

_ plain, and constituting very marked features of the scenery. From the same plain, and 
only about three miles west trom one of the greatest of the sandstone bluffs — Petenwell 
Peak —rises the quartzite hill at the foot of which the village of Necedah is built. The 
rounded contour of this hill serves to mark it at once as different in nature from the 
sandstone bluffs of the adjoining region. 

The main Necedah bluff lies on the N. W. qr. of Sec. 25, T. 18, R. 3 E., the town 
line crossing over its eastern end; it is about half a mile in length, with its greatest ex- 
tension east and west, and is highest, and at thesame time most bold and rocky, on its 
eastern end, which rises 170 feet above the street below, and about 510 feet above Lake 
Michigan. A short distance southeast of the main bluff, on the N. W. qr. of the 8. W. 
qr. of Sec. 19, T. 18, R. 4 E., is a small, craggy hill, 75 feet high, of the same rock as 
that composing the main hill, the intervening low ground being underlaid by horizontal 


sandstone. 


1 Annual Report of Geological Survey of Wisconsin for 1655, p. 105. 


524 GEOLOGY OF CENTRAL WISCONSIN. 


The exposures on the main hill are mostly on the eastern and southeastern portions 
where in places they rise nearly precipitously from the low ground at foot. The rock 
seen here is for the most part (1354) a glassy, translucent, subgranular, grayish quartz- 
ite, much more nearly allied to the quartzite of Rib and Mosinee hills in Marathon 
county, than to that of the Baraboo ranges. Much of the rock is quite dark-gray in 
color, the quartz then being still glassy but smoky-tinted. Numerous small cavities 
and seams occur, lined with half crystalline quartz, and carrying a soft, pinkish, clayey 
substance; bluish-white quartz veins (13551) one-half to two inches in width, and 
nests, are also common, and these carry frequently fine-flaked, brilliant, specular iron, 
which occurs also occasionally in quite large masses, similar to those found in the Bara- 
boo quartzite. No parallel grain is to be seen in this rock, nor any definite bedding 
plancs. Numerous quite close joimts occur, however, and these cause the rock to weath- 
er into smooth-faced, sharp-angled fragments. On the smaller bluff a very distinct 
parallel grain is to be seen trending N. 75° W., and showing a corresponding dip of 
45° N. Here much of the quartzite is of a light pink color, looking, on w fresh fracture, 
almost like a fine-grained, pinkish granite (1358), but the only prominent mineral is sub- 
granular, translucent, pinkish quartz. Some specimens show mica plainly in very 
sparsely scattered, small scales. In many places little centers of iron-staining seein to 
be decomposing mica scales. Other portions of this rock (1348, 1357) are opaque, white, 
and distinctly granular, and are seamed with fine black lines, arranged so as to show 
discordant stratification. These seams when split open, appear to be composed uf 
blackish mica. Bluish-white veins and nests occur here also. 


a 
ee 


Th Miowanaee Ler 


no Kwon Co 


POTSDAM SANDSTONE, 


Souther end of Roché a Cris Blaff, Adams Go, 225 Mhigh, 


THE LOWER SILURIAN ROCKS. 5Q5 


CHAPTER IV. 


THE LOWER SILURIAN ROCKS. 


I. In General. 
THE LOWER, OR POTSDAM, SANDSTONE SERIES. 


Forming the base of the pile of Silurian strata everywhere in the 
states bordering the Upper Mississippi, but having a much greater 
surface development in Wisconsin than elsewhere, and resting di- 
rectly upon the irregular surface and upturned edges of the older 
crystalline rocks, is a great thickness of sandstone, which, through the 
larger part of its mass, is made up of rolled grains of quartz, of vary- 
ing size, cemented together by a minute quantity of hydrous iron 
oxide. Towards the upper part of the formation, in Central Wiscon- 
sin, this sand becomes mingled with more or less dolomitic and cal- 
careous material, which further up tends to aggregate into thin bands 
of limestone, finally forming, at 35 to 50 feet below the base of the 
next great formation, the Lower Magnesian limestone, a well marked 
and very persistent yellow limestone layer, which has a thickness of 
30 feet, and is so well marked and important a horizon in Central 
Wisconsin, that I have given it the specific name of Mendota lime- 
stone, from a large exposure at MacBride’s point on the north shore 
of lake Mendota. Above the Mendota horizon, sandstone, 35 to 50 feet 
in thickness, again comes in, the larger part of which is either nearly 
pure white quartz sand, or sand turned brown by oxide of iron, thus 
approaching more nearly in character to the Upper or St. Peters 
sandstone than to that immediately beneath the Mendota beds. To- 
wards its upper portions, however, just beneath the overlying lime- 
stone, it generally becomes again somewhat dolomitic, the upper limit 
being frequently marked by layers of greensand and oGlitic chert. 
To this layer I have given the name of Madison sandstone, it yield- 
ing large quantities of a very excellent building sandstone at Madi- 


son. ‘These names are not meant to be of anything more than local 


importance. 7 
For some distance above the Madison horizon the Lower Magnesian 


526 GEOLOGY OF CENTRAL WISCONSIN. 


itself often shows alternations of nearly purely dolomitic, and distinctly 
sandy layers, even including thin seams of white sand, whilst some 
sandy material occurs at horizons well towards the summit of this for- 
nation. The two series thus evidently graduate into one another, 
and in many parts of the northwest it is undoubtedly difficult to fix 
upon the dividing line. In Central Wisconsin, however, the alter- 
nating beds are well defined, and two horizons are well marked by 
beds of greensand. These are the base of the Lower Magnesian prep- 
er, and the base of the Mendota beds, 65 to 100 feet below. During 
the writer’s earlier work in this field, the lower of these limits was 
adopted, in.mapping, as the line of division between the two forma- 
tions, whilst subsequently both horizons were mapped, the upper one 
being: taken as the base of the Lower Magnesian, in order that that 
name might cover the same beds as included under it by other mem- ~ 
bers of the geological corps. 

The facts which led at first to the use of the lower limit may be 
briefly given here. In Dane and Columbia counties, where the Men- 
dota and Madison horizons are very prominent, and were first made 
out, the entire thickness of the Lower Magnesian, between the upper 
surface of the Madison beds and the base of the St. Peters or Upper 
sandstone, was found to be only 50 to 80 feet. It was well known 
that not far to the westward, along the Wisconsin, this formation 
attains a thickness of 250 feet. It was not thought so great a thick- 
ening as this could exist, and to explain the difference, it was sapposed 
that the Mendota and Madison beds were a local modification of the 
lower portion of the Lower Magnesian formation. This supposition 
was encouraged by the great similarity between the Mendota, as seen 
in the typical localities in Dane cuunty, and the limestone beds im- 
mediately overlying the Madison sandstone, the former here being al- 
most a pure dolomite, with only two or three percent. of insoluble resi- 
due. Subsequently, however, it was ascertained beyond a doubt that the 
Mendota beds are to be recognized occupying the same position below 
the Lower Magnesian, even where that formation attains its greatest 
thickness, its irregularity in this regard being proved to be due to its 
having suffered a surface erosion prior to the deposition upon it of the 
St. Peters sandstone. The Madison and Mendota beds were therefore 
thrown back into the Potsdam series as its uppermost layers, and are 
so mapped on all of the Atlas maps. 

For all those portions of the maps, however, which represent the 
Central Wisconsin district, except southwestern Junean county, on 
Area H, the base of the Mendota beds is indicated by a brown line 
within the color for the Potsdam series, the space between this line 


THE LOWER SILURIAN ROCKS. 527 


and the brown-colored Lower Magnesian area being oceupied by the 
Madison and Mendota beds. In the sections also, both of the Atlas 
plates and of the plates in this volume, the Mendota and Madison 
beds are given separately from the Potsdam. Having been mapped 
out with some care, it was thought best not to lose the work done on 
them by not so distinguishing them. Moreover, the close likeness 
often borne by the Mendota to the Lower Magnesian, and the gradu- 
ation of one series into the other, render it a matter of doubt-whether 
to affiliate these beds of passage with the upper or lower of the two 
series. Constituting so important a feature as they do in the Central 
Wisconsin stratigraphy, they deserve separate mention; they are 
really beds of passage, and as such are separately considered below. 
The term Potsdam, then, as used in the detailed descriptions and sec- 
tions of this chapter, applies only to those beds terminating upwards 
at the Mendota base. 

Of the two names given to the series the term “ Lower Sand- 
stone’? was used by Dr. D. D. Owen, as distinguishing it from an- 
other much thinner, but very prominent, sandstone, which overlies 
the Lower Magnesian — the Upper or St. Peters sandstone. Hall and 
Whitney first used the term “Potsdam,” transferring it from the 
sandstone series which forms the Silurian base in the state of New 
York, and contains a few fossils close to those in the Wisconsin beds, 
which, however, contain many that are not found in New York. 
That the two formations are somewhere nearly the equivalents of one 
another appears evident, as Hall has shown.! The extension of the 
New York name, originally given to a comparatively small thickness 
of rock which occupies a restricted area, to the lowest of the fossil- 
iferous Silurian beds all over the country, seems, however, unfortunate, 
and especially so in the case of the Wisconsin formation, which has 
a thickness of 800 to 1,000 feet, comes to the surface over an extended 
area, and is far more fossiliferous than the New York beds. : 

Of former investigations on the Potsdam series, Dr. Owen’s seem 
to have been much the most exhaustive. He presents a scheme of 
the subordinate structure of the formation which may be considered 
quite remarkable for so early a day. His detailed investigations, 
however, did not extend far away from each side of the Mississippi, 
and the great central area of Wisconsin, where the formation spreads 
over a district 100 miles in diameter, and presents elements of strat- 
ification contrasting much with those exhibited along the Mississippi, 
he left hardly touched. Having no data from Artesian borings, he 
greatly underestimated the thickness of the formation, putting it at: 


146th Annual Report N. Y. State Cabinet Natural History. 


528 GEOLOGY OF CENTRAL WISCONSIN. 

500 feet as an extreme, instead of 800 to 1,000 feet. Into this error 
he appears to have been led by committing the graver one of sup- 
posing that he had to do with the base of the sandstone whenever he 
found it in contact with the crystalline rocks, losing sight altogether 
of the great irregularities of the upper surface of the latter rocks, by 
virtue of which they rise high into the upper parts of the sandstone 
series. In cases like that exhibited at the Dalles of the St. Croix, 
where the Copper-bearing rocks are seen to rise nearly perpendicularly 
through many feet of the sandstone, he regarded the traversing rock 
as “ intrusive,” or of later origin altogether. 

Hall’s investigations in the Central Wisconsin region do not ap- 
pear to have been any more extensive than those of Dr. Owen, to 
whose descriptions of the stratigraphy of the series he adds little that 
isnew. As regards the fossils of the formation, however, he makes 
a very important contribution,’ giving a list to which little has been 
added by the present survey, as far as Central Wisconsin is concerned, 
and a grouping of the fossils into those characterizing the lower, mid- 
dle and upper beds, which, in its general order, proves to be quite cor- 
rect. Je commits the same error as Dr. Owen, however, with regard 
to the thickness of the formation, placing it at only 500 feet? Asa 
result of this, his list of fossils from the lower beds must be assigned 
to about the middle of the series, below which are full 500 feet, about 
whose fossils, or lack of fossils, we know nothing at all. This may be 
regarded as a point of some importance in comparing the Wisconsin 
Primordial with that of other regions by the fossils contained. Whit- 
ney, who reports on the Lead Region in Ifall’s volume on Wisconsin 
Geology, follows the latter gentleman in his under-estimate of the 
thickness of the Potsdam series. 

Of all of the earlier accounts of the geology of Central Wisconsin, 
T have found that of Dr. Percival, who worked after Owen and before 
Tall and Whitney, by far the most reliable. Dr. Percival published 
two small annual reports, in pamphlet form, whilst geologist of the 
state, in both of which he gives descriptions of the Wisconsin forma- 
mations, whilst one of the two gives an account of a reconnoisance in 
the Potsdam sandstone region of the heart of the state. He recog- 
nizes distinctly the very great thickness of the formation, its lack of 
uniform character, and the fact that much confusion had been caused 
by the reference to the Lower Magnesian,by Dr. Owen and his assist- 
ants, of several distinct limestone bands separated by sandstone strata, 
and regarded by Percival as included in the Lower sandstone, this 


116th An. Rep. N. Y. State Cabinet of Nat. Hist. 
2 Report on the Geology of Wisconsin, Albany, 1862, p. 16. 


THE LOWER SILURIAN ROCKS. 599 


applying especially to the suctession of strata exposed along the St. 
Croix river. He notices also, distinctly, the bed I have called the Men- 
dota, and also numbers of other minor points mentioned by no other 
geologist. 

The surface distribution of the Lower Sandstone exceeds that of 
any other of the formations of the Central Wisconsin district. The 
region occupied by it embraces all of Juneau, Adams, Waushara and 
Marquette counties, as also more or less of Portage, Wood, Clark, 
Jackson, Sauk, Green Lake, Columbia and Dane counties —in all, an 
area of over 6,000 square miles. The total area occupied by the for- 
mation outside the Central Wisconsin district, and within the state, 
is probably as large again, but nowhere else is there one continuous 
area of so great diameter as in the central counties. Over a large 
portion of this district, in Jackson, Wood, Clark, Portage, and por- 
tions of Juneau and Adams counties, there is no distinct evidence 
that the newer formations ever spread. Another large portion, in- 
cluding Waushara, Marquette, northern Green Lake, western Colum- 
bia, northern Sauk and southern Juneau, well away from the re- 
gions of the newer rocks, was originally, beyond doubt, overlaid 
by at least the Lower Magnesian, this formation occurring on two out- 
lying bluffs in the northwest corner of Marquette county, 25 miles 
distant from the main area of that formation. There are again sinall- 
er areas, as the strip along the Wisconsin below the great bend, and 
the district about the head waters of the Catfish, in Dane county, 
which occur altogether within the country of the newer formations, 
and have, beyond doubt, been reached by erosion along the existing 
valleys. 

On the north, the main area occupied by the lower sandstone is 
limited by the larger one in which the crystalline rocks are at the 
surface. The boundary between the Potsdam and Archean areas 
is quite difficult to trace. As stated on a previous page, the streams 
flowing southward from the Archean area cut through the sandstone 
beds down to the crystalline rocks, for many miles after entering the 
sandstone district, whilst on the divides between the streams the sand- 
stone stretches as far north into the Archean regions. The difficul- 
ties in tracing the boundary line in any greater detail than thus 
stated lie in the peculiar irregularity of the upper face of the 
older rocks, which may bring them to the surface at any point; in 
the once greater spread northward of the sandstone, as a result of 
which it is liable to be found in little patches, filling the depressions 
of the older rocks; and in the heavy coating of drift that conceals the 
rock beneath over considerable areas. To these difficulties may be 

Wis. Sur. — 34 


530 GEOLOGY OF CENTRAL WISCONSIN. 


added the fact that the country is largely unsettled, and covered by 
heavy forests and swamps. The former spread northward of the 
sandstone beyond its present limits is indicated by the occurrence on 
the highest part of the dividing ridges of outliers of that formation, 
100 to 200 feet in height, and also by the occurrence in the northern 
drift of large quantities of loose sand. 

Notwithstanding these difficulties, it is believed that the boundary 
line, as indicated on Atlas Plate XV, Area F., is not far from correct. 
The principal facts upon which it is based may be here briefly stated. 
On the east side of Area F., sandstone is seen in a small quarry on a 
ridge on the west side of Plover river, on whose bank, just east, and 
at points all along whose course to the mouth, the crystalline rocks are 
exposed. From the quarry mentioned to Stevens Point, sandstone 
appears to underlie the surface. At Stevens Point, it appears at the 
top of the bank on both sides of the Wisconsin river, whose bed is on 
crystalline rocks. A short distance north of Stevens Point, on the 
road to Wausau, and also on the road following the west bank of the 
river, crystailine rocks are to be seen, and no sandstone is met with 
further north, The Wisconsin Central Railroad cuts through 
sandstone at Stevens Point, but farther to the west and north 
it is altogether on crystalline rocks, as shown by several cuts between 
Stevens Point and Junction City. The Wisconsin Valley Railroad, 
from Knowlton, Marathon county, to Centralia, Wood county, is also 
altogether on the crystalline rocks, which, for the most part, lie near 
the surface, with very little drift covering. Along the east side of 
the Wisconsin, below Stevens Point, sandstone 5 to 40 feet in thick- 
ness is constantly to be seen in the east bank of the river, the crystal- 
line rocks appearing in the river bottom as far as Point Bass, Sec. 15, 
T. 21, R. 5 E., Wood county. At this point the crystalline rocks 
disappear, and the sandstone in turn forms the river bed. North- 
ward from Point Bass, along the west bank of the river, sandstone 
shows again, at intervals, as far as Centralia. The Wisconsin Valley 
Railroad, north from Centralia, as already said, is always on the older 
rocks, but a considerable thickness of sandstone occurs in a ridge on 
the south side of Mosquito creek, Secs. 29 and 30, T. 23, R. 6 E. 
Farther north, along the line between sections 7 and 8 of the same 
town, small thicknesses of sandstone fill depressions between the 
ridges. On the north side of the Wisconsin, between Mosquito and 
Mill creeks, sandstone occurs at several points, but does not stretch 
far north, for crystalline rocks are at surface over the northern parts 
of T. 23, R.6 and 7 E. Mill ereek is altogether on the crystalline 
rocks. Along the line of the Green Bay and Minnesota Railroad, 


THE LOWER SILURIAN ROCKS. 5381 


westward from Grand Rapids as far as Merrillon, Sec. 15, T. 28, R. 4 
W., Jackson county, thin, shaly sandstone is frequently exposed in 
low cuts, but having evidently a small thickness only, for, at the cross- 
ing of Black river, gneiss is exposed, as also on Yellow river, a short 
distance north of the railroad crossing. Between Grand Rapids and 
Dexterville, the sandstone does not stretch far north of the railroad 
line, for along the wagon road hetween the two places granite is seen 
at the surface. . 

On Yellow river the crystalline rocks are first exposed about two 
miles above the railroad crossing, beyond which point they are con- 
stantly exposed in the bed of the river, sandstone appearing at points 
on the west bank as far north as the northern side of town 24. Rocky 
Run, in towns 23 and 24, is on crystalline rocks. In the towns on 
the divide between Yellow and Black rivers, sandstone appears to be 
generally the surface rock, the Archwan only occasionally appearing 
through it. All along the road from the crossing of Yellow river, on 
the south line of T. 25, R. 2 E., Wood connty, to Neillsville, in Sec. 
14, T. 24, R. 2 W., Clark county, the country is generally high and 
heavily drift-covered, wells passing through 5 to 100 feet of drift 
into sandstone. Sandstone is also occasionally seen at the surface, as 
in the road on the S. E. qr. of Sec. 12, T. 24, R. 1 W., and in an out- 
lying bluff at the center of the S. E. qr. of Sec. 12, T. 24, R. 1 E. 
Sandstone also occurs in angular fragments on the ridges along the 
west fork of Yellow river in T. 25, ranges 1 and 2. E. Further north, 
in towns 25 and 26, ranges 1 E. and 1 W., drift covers the rocks 
heavily, and the exact extent of the sandstone has not been ascer- 
tained, as indicated by the blank space left on the map. O’Neil’s 
creek, in T. 24, ranges 1 and 2 W., cuts down to the older rocks. On 
Sec. 11, T. 24, R. 2 W., sandstone occurs by the side of the road, and 
again in a high outlier on Sec. 3, of the same town, on the west side 
of Black river. Westward from this outlier the country shows sand- 
stone at the surface. Similar bluffs occur in T. 25, R. 2 W., the erys- 
talline rocks showing along the river, and at least one snch bluff oc- 
curs in T. 26, RB. 2 W., its exact location not being known to the 
writer. In T. 26, ranges 3 and 4 W., sandstone is reported by Dr. 
Randall! as extending as far as the Eau Claire river, beyond which it 
is absent. At the crossing of Black river, one mile west from Neills- 
ville, S. W. qr. of Sec. 15, T. 24, R. 2 W., granite is exposed in the 
river, and is overlaid by sandstone in the banks. Similar conditions 
hold all along the river, as far as the falls in T. 21, R. 4 W., the 


1 Owen’s Geological Survcy of Wisconsin, lowa and Minnosota. 


5382 GEOLOGY OF CENTRAL WISCONSIN. 


Archean rocks becoming more and more rcstricted to the stream bed, 
until they finally disappear. 

The boundary between the Potsdam and Lower Magnesian areas 
is much more easily traceable, it being possible in the driftless dis- 
trict to map it with almost any degree of accuracy, the only limit be- 
ing the amount of time spent in following its windings. In drift- 
covered regions this degree of accuracy is not attainable, but a dis- 
tinct break in the topography generally suffices to give the line very 
closely. It has already been said that in the Central Wisconsin dis- 
trict there occur well-marked beds of passage between the Lower 
Magnesian and the Potsdain, whose surface distribution has been 
separately mapped. These layers, however, only occasionally have a 
wide surface spread, appearing generally on the steep flanks of the 
higher ground occupied by the Lower Magnesian, and thus forming 
on the map a narrow strip along the outer edge of the Lower Magne- 
sian area. The limits of the Lower Magnesian, and of the beds of 
passage, are so close together that, in a general description like the 
present, they may be regarded as one. On the east we find this 
boundary without the limits of the Central Wisconsin district until 
the northern line of Columbia county is reached. This county it 
crosses in an irregular line, curving from northeast to southwest, and 
marked by a prominent and deeply indented escarpment. North and 
west of this line the country shows everywhere the Potsdam as the 
surface formation, except on the summits of the numerous outliers 
which flank the escarpment. At the sonthwest corner of Columbia 
county, the Wisconsin enters upon: the territory of the Lower Mag- 
nesian, through which it cuts, however, deeply into the underlying 
sandstone, so that along the valley bottom we have a broad strip of 
the latter formation at surface, and along the numerous tributary 
streams on each side, strips of greater or less width. In the Four 
Lake country, about the city of Madison, the upper layers of the 
Lower sandstone are again brought to the surface by a different sys- 
tem of erosion, that of one of the main branch streams of Rock river. 
The valley surface is never, however, more than 30 to 50 feet below 
the summit of the sandstone (the Mendota base), and south of Lake 
Monona the southerly dip carries even the uppermost beds below the 
valley bottom. In Sauk county, north of the Wisconsin, the boundary 
of the main Potsdam area follows the west side of the town of Honey 
Creek, then bending around the western end of the Baraboo quartzite 
ranges, in the towns of Westfield and Honey Creek, crosses Reedsburg, 
Ironton, La Valle and Woodland, in a northwesterly direction along 
the west side of the valley of the Baraboo river to the very south- 


THE LOWER SILURIAN ROCKS. 533 


western corner of Juneau county. -This line is, however, anything 
but a regular one, the Lower Magnesian occurring in more or less 
detached areas crowning the summits of the higher grounds. In 
Juneau county only a few small summits in the southwest corner 
reach the Lower Magnesian horizon, the rest of the county being 
well down in the Potsdam series. West of Juneau county the 
boundary is without the Central Wisconsin district. 

The topographical characters of the regions in which the Pots- 
dam is the surface rock have already been generally given in the 
chapter on Surface Features, and further details are given in the 
latter half of the present chapter. It may be said, in general, that 
where this formation is at surface there is usually a loose, sandy, 
sterile soil, a sparse growth of small oak timber, mingling with and 
becoming replaced by small pine towards the north, and a general 
plain-like character, the plain dotted with lofty and rocky outliers 
of the same formation, or of the next higher one. To these general 
statements there are exceptions, the principal of which .may be here 
given. Excellent soil is found within the Potsdam area where the 
drift covering is heavy, as in parts of Waushara county, or where 
alluvial depositions exist in the valley bottoms, as in places along 
the Wisconsin valley, or yet again where a rough, ridgy charac- 
ter to the country prevails, as in southwestern Juneau county, where 
good land occurs on the top of the ridges, being due possibly to the 
tendency of the loosened sand to wash downwards towards the valleys. 
To the general plain-like character of the Lower sandstone area, south- 
western Juneau county and northwestern Sauk make an exception, 
the Baraboo river and its tributaries having worn the ridge that bounds 
the central sand plain into an adruptly ridgy country. Another ex- 
ception is found in parts of Waushara county, where morainic drift 
occurs in great abundance. 

The general lithological characters and stratigraphical ar- 
rangement of the Lower sandstone series will be best understood 
from a brief summary of the main facts obtained in the different dis- 
tricts in which the formation is at surface. 

At Madison, Dane county, the Artesian well in the Capitol park 
passes through 126 feet of loose materials, apparently all belonging 
to the Drift, 704 feet of sandstone, for the most part purely silic- 
fous, light-colored, and fine-grained, the constituent grains being 
all more or less rolled, and cemented by a varying, but always 
very small, amount of hydrous iron oxide —and 10 feet of a red shale, 
underneath which are the crystalline rocks. Similar results are ob- 
tained from the well at the Milwaukee and St. Paul depot at Madi- 


534 GEOLOGY OF CENTRAL WISCONSIN. 


son, the summit of this well being at a lower level, and the drift 70. 
feet in thickness. In the former well, the top of the rock is 68 feet, 
in the latter, 100 feet below the base of the Mendota limestone, as ex-, 
posed in the neighborhood. On the banks of Lake Mendota, near 
Madison, we find exposed, beneath this limestone and above the lake 
level, one foot of greensand and 31 feet of fine-grained, light green- 
ish, very friable, sandstone, including very thin dolomitic seams, and 
carrying throughout some dolomitic and calcareous matter, the con- 
tent of purely silicious sand being 84.45 per cent. Altogether, then, 
we find in the Madison region, the following succession of layers. 
between the Mendota base and the Archean: 


Feet. 

1. Greensand layer «oi sic osivie siaiessie ae eisieindiein e ticve ee oie te nin antenna ose a9 eas 1 
2. Calcareous and dolomitic, friable, fine-grained, greenish, sandstone... 31 
SINGH AMOWN’ weeds heer de Sere e dees eye eee Us Eady eesl Ge aen Saenetenmen 31 
4, Light colored sandstone, for the most part purely silicious, being made 

of rolled quartz grains; but no specimens obtained from the upper- 

most layers .......eeeeee ce eee i Sk erevass en eae eee 704 
5. Red Shale wcicesssdar dee ea nee nano wane weedeloornesewswaNe sais sea ee 10 

Totdliinscwareeweee Kade ewes sHeebned ck Geese dGe ts OE alee Sore MeareiS 717 


Along the Wisconsin river bluffs in Columbia, Sauk and Dane 
counties, the Mendota horizon is very prominent, the sandstone 
showing below it for a thickness of 150 to 200 feet. The very bold 
bluff that rises from the north bank of the Wisconsin river at the: 
mouth of Honey Creek, in the town of Prairie du Sac, Sauk county, 
shows the following section, from the Mendota base downwards: 


1. Greensand with thin, brown, calcareous layers; the greensand layers made aes 
up of fine grains of glauconite and white sand, mingled with crystalline 
CALCIEE beset aale Goes Seas Se 924 4a LG Ee GOly es aes Mentor see ones edd ss Bes 
2. AN6 CXPOBUTE 4 sessed cae Se tea en's Ca Raat nee Ber Meneame wiles 7 
3. Fine-grained green and brown sand, calcareous ....... 6c e eee eee ee eee 2 2 
4. Loose white and brown sand, some lnyers partly calcareous.............6 10 
5. Firm and heavy layers of yellowish, porous, calcareous, sandstone, inter- 
stratified with layers of white sand............ 6. cess cess ee eee eee eee 6 3 


6. Alternations of pure white, non-calcareous, fine-grained sand, with nodular- 
weathering, yellow, calcareous layers, and layers of dark greensand, the 
whole showing fine cross-lamination; the white sand layers predominating, 45 

7. Fine-grained light-colored sandstone; often pure white, and loose; in parts 
cross-laminated, the lines of cross-lamination being marked by rows of 


SlaUCONIte SrA sass ss auld eed MAE REN H Rd PON WORE Ke fale damm eMlnle® 9 6 

8. Porous, yellowish-brown, slightly calcareous layers.......... cesses evens 4 11 

ONO OxPOSULO Memes tam hates adie tieu.s CoaSKOET AOR aa Grd Agile ceauiaNtahtens ll 6 
10. Fine-grained, friable, greyish sandstone, only slightly calcareous, carrying 

a few yellow calcareous layers as AbOVE...... 0. eee e eee eee e eee ences li 5 


11. Firm layers of-ferruginous sandstone, more calcareous than the last....... 5 66 


THE LOWER SILURIAN ROCKS. 5835 


Ft. In 
12. Loose brown Sands docew.enidais scale pou vag 004 404 40 Glere vena eewe nee ¥en caoaws 11 
15. UNGkDOSEE rides tea wasouvina ene aedecnessagadacen aks CREE Tess 7 
14. Porous and crystalline-textured, yellow limestone, with much coarse and 
bright green glauconite.......... ce ccc cee c eee e eee eecseeseeeneueeaes 1.2% 
15: WNERPOSEd ses ,c. FSA ear ncan cone euhelal cia restanugsd ansputoeitabieee alee Lee a oes 83 6 
16. Like No. 14, interstratified with bright green seams............000.0000% 2 4 
17. Heavy brown layer of slightly calcareous sandstone .............eeeeeeee 3 
18. Greensand layer; a mixture of very fine white sand and glauconite grains, 
~ with some crystalline calcite.... 00.6... c ccc cece eee s ee ceeeereeenees -» 10 
19. Light yellow, friable sandstone; only slightly calcareous; cross-laminated, 5 4 


20. Greensand layer, like 18, false bedding very marked, cross-lamine very 


plain, yiwse sek ses bana edenencee ake) Biecdes aaa ese sna sh ebnee ade - 13 

21. Porous, yellow, slightly calcareous sandstone...........ccceeeeseeeeeees 6 
22. Fine-grained, cross-laminated, slightly calcareous sandstone, with much 

precnsalid s «seosree. acersed Sole cneldey J. eeee eas cect beeansaesen 1 ou 

23. Greensand, like No. 20....... 0. cece cece e cee cette tenes seen eeeeenens .. 10 

24, Fine-grained, friable, white sandstone, slightly calcareous.............+. Es 

25. Unexposed isc ya sirtieas canis eauie ao dup vs CEES ev eed Cees EERE Se coe bea 127 
26. Fine-grained, white sandstone, entirely non-calcareous; made up altogether 

of fine rounded grains of limpid quartz....... 0... cece cece eee ee ceee 29) a3 

PObalianentevacoduse Fea Meas Sitnesth at rae pial a heehee el atseced 189 3 


The horizon of the base of this section is 146 feet below the top of 
the rock in the capitol well at Madison, thus covering the gap in the 
Madison section. Combining the two sections, we obtain for the 


whole series the following general succession: 


Feet. 
1. Alternations of layers of purely silicious white sand, ferruginous brown sand, 


yellowish calcareo-arenaceous layers, and layers of greensand; the calcareous 
bands increasing in amount of lime and in number towards the top, as is also 


the case with the greensand layers ...........ccee esse eee eet e cence eeeeees 165 

2, Entirely non-calcareous, white and yellow, sandstone; friable to indurated; fine 
£0 COAYSE~PTHINE 6. eso snes cana cnn GHGS RO HESS AML AG Eee ine 602 
D Red shale.:cc'eds ve vena panet arenteteaacuan bisa itstay eta tahestec aban stot Ao ahs OS et Sok hy 10 
Total vs ie used 6000 oy ha as Behe oe amet se eee Rte tS wake aS o's 117 


The calcareous layers have never been observed extending more 
than 150 feet below the Mendota base. The “greensand” layers 
mentioned are mixtures of green grains of a mineral probably closely 
allied to the glauconite of the Cretaceous formation, rounded grains 
of quartz, and usually more or less of angular pieces of calcite. These 
layers are very characteristic of the lower sandstone, occurring, ac- 
cording to Dr. Owen, at many different horizons throughout the series 
as developed along the Mississippi. In Central Wisconsin, however, 
none have been recognized more than 160 feet below the Mendota 
base. No chemical investigation of Central Wisconsin greensand has 
ever been made, but Dr. T. S. Hunt has given an analysis of a green- 


536 GEOLOGY OF CENTRAL WISCONSIN. 


sand from the Lower Magnesian limestone of Minnesota, at Red Bird, 
on the Mississippi, which is beyond doubt the same material. This 
analysis (I), as also another, by the same gentleman, of the Cretace- 
ous greensand of New Jersey (II), is given below:' 


I. II. 
Silda. ccvsiasaveceeege Mac eeee rd cere ee ew nee egee eine dian 46.58 50.70 
ATWMIG siccahs seeder uae PRG DIGS Lage Cee ewe SO es 11.45 8.03 
Tron protoxide.... 0... cc cece cece ee eect eee e eee nee en ene 20.61 22.50 
Magnesia .... 00.0 cece cece eee een eee n cnet cence eee nnees 1.27 2.16 
Tami Seen chaeley ives vaturens 18 eT eAe tea e eee 2.49 1.11 
Sodaiass desc veweseee saa car ca ceeW obi dy siete eee 0.98 0.75 
POtaShicskiles eaten See eae eae ve chops paws sai 6.96 5.80 
Wiaibebarcccan's soaevek ond ahs sabe arden Gane a Mei ete’ Saale 9.66 8.95 


The green grains of both Cretaceous and Silurian greensands, as 
also of similar deposits in existing seas, are often found as casts of 
the shells of rhizopods. So far as the writer’s knowledge goes no 
such observation has ever been made with regard to the Wisconsin 
greensand. The greensand layers are by no means restricted to the 
Potsdam series; they occur in both the Lower Magnesian and St. 
Peters. Greensand grains occur also apart from the regular green 
layers. The thin, yellow and brown, rough-textured, calcareous 
bands, that characterize the layers immediately beneath the Mendota, 
are often dotted with coarse grains of glauconite, which are not in sut- 
ficient quantity to impart their color to the rock. 

The generalized section given above for the Potsdam series, below 
the Mendota base, holds true for a large part of the Central Wiscon- 
sin district, and would be satisfactory for all of it, but for the facts 
next to be stated. Proceeding northward from the valley of the Wis- 
consin, we encounter, traversing Sauk and eastern Columbia counties 
for 25 miles from east to west, the Archean quartzite ranges described 
in the last chapter. The Mendota horizon continues well marked di- 
rectly up to the ranges, whilst in the country west and east, it extends 
much further to the northward. Everywhere about the quartzite, 
however, we find, lying unconformably upon it, layers of sandstone 
and bowlder-conglomerate, which, as regards altitude, appear to oc- 
cupy the entire distance between a horizon considerably below the 
Mendota, and one nearly as high as, if not higher than, the summit of the 
Lower Magnesian. These layers of sandstone and conglomerate can- 
not, in all, be less than 400 feet in thickness, being nearly always 
without calcareous admixture. Single cliffs occur showing 225 feet 


' Geology of Canada, p. 488. 


THE LOWER SILURIAN ROCKS. 537 


of friable, entirely non-caleareous, sandstone, the summits far above 
any apparently possible position of the Lower Magnesian, whilst be- 
low their bases numerous other sandstone exposures oceur, carrying 
the sandrock down further. Nor are these occurrences of thick and 
high-level sandstone at any considerable distances from points where 
the regular succession of Lower Magnesian, Madison and Mendota is 
to be observed. In places in the town of Westfield, on the western end 
of the quartzite ranges, it is possible to pass within a quarter of a 
mile from Mendota limestone, oceupying its normal position, to sand- 
stone ledges which rise from the same level for over 250 feet. 

As already described, the quartzite ranges almost completely en- 
circle the intervening valley, whose altitude is somewhat greater than 
that of the surrounding outside country. Within the valley, non- 
caleareous, occasionally much-indurated, sandstone, with local con-' 
glomerate beds, is to be seen at almost all levels to the summits of 
the quartzite ranges, but at two points limestone is known to occur. 
These localities are described fully ina subsequent page. It is now 
merely necessary to say that at one of the places, on the south flank 
of the north quartzite range, near the Lower Narrows of the Baraboo, 
are to be seen 20 feet of limestone, containing a number of fossils, 
mostly of new species, which Mr. R. P. Whittield regards as unques- 
tionably not lower than the Lower Magnesian. Below on the side- 
hill are numerous but not continuous exposures of sandstone, those 
nearest the limestone evidently forming the next lower layer, and re- 
sembling closely the Madison beds. Across the valley, one-half mile 
southeastward, is a vertical cliff of red-and-white-banded, fine-grained, 
friable sandstone, rising from 75 to 165 feet above the summit of the 
limestone, whose altitude is what would be expected for the Lower 
Magnesian, from the occurrences of that formation a few miles to the 
southward. One mile further west sandstone and bowlder-conglom- 
erate, flanking the quartzite, rise similarly above the limestone. 

At the other point, not far from the village of Baraboo, and on the 
north slope of the south quartzite range, exactly similar limestone is 
found, without fossils, covering a small sum mi t, and underlaid by ferru- 
ginons, fine-grained sandstone, carrying Scolithus and Dicellocephalus 
Minnesotensis. At a still lower level, near by, a fine-grained, yel- 
lowish, aluminous limestone occurs, the three different layers having 
just the characters and relative positions for the Lower Magnesian, Mad- 
ison and Mendota beds. Below the lowest limestone layer, and within 
a few rods of it, are, however, ledges of much indurated, non-cal- 
careous rock, entirely unlike the friable dolomitic sandstone normally 
occurring beneath the Mendota. Three miles south of cast from here, 


538 GEOLOGY OF CENTRAL WISCONSIN. 


about Devil’s Lake, the high level sandstones, with bowlder-conglom- 
erate beds, are again found, with a total thickness exposed of over 300 
feet, the base being nearly ona level with the lowest of the limestones 
at the locality just described. In one place, a short distance north- 
east of Devil’s Lake, large loose masses of this sandstone occur at an 
altitude between 100 and 150 feet above the last named limestone, 
carrying fossils, among which are Dicellocephalus Minnesotensis and 
others supposed to indicate the upper layers of the Potsdam series. 

For these anomalous occurrences, which will be more fully under- 
stood from a study of the sections of Plates XIX and XX, and Figs. 
48 and 49 of this volume, and of the detailed descriptions in the fol- 
lowing pages, it is not easy to find a satisfactory explanation. It ap- 
pears altogether inadmissible to attribute the great elevation of the 
high-level sandstone to a sudden affection of the nearly horizontal 
strata by a violent northern rise as they near the quartzite ranges. 
This supposition is forbidden by the utter lack of any indication of 
such a rise in the large exposures that occur, by the normal success- 
ion of beds that holds true in all the region east, west and north of 
the quartzite ranges; and by the great amount of rise that would be 
necessary. In Westfield it would have to be 300 to 400 feet to the 
mile. Moreover, within the space enclosed by the quartzite ranges, 
as described, occur the Lower Magnesian, Madison and Mendota, in 
their normal succession, and with their normal lower level, whilst in 
one ease the limestone and perfectly horizontal high-level sandstone 
are so near by that no amount of dip could possibly account for the 
occurrence. It may be regarded as beyond question that entirely 
non-calcareous sandstone with bowlder-conglomerate and Potsdam 
fossils does, not only apparently, but actually, occupy the whole space 
between the horizon of the base of the Mendota, and that of the sum- 
mit of the Lower Magnesian. 

It might be supposed that the wear of the quartzite ranges contin- 
ued to produce sandstone and conglomerate beds during the growth 
of the limestone in the deeper water near by, but the suddenness of 
the transitions, the occurrence of Potsdam fossils in the sandstone, 
and the existence of the limestone layers close to and within the 
quartzite ranges, appear great difficulties in the way of such an ex- 
planation. That the high-level sandstones represent really an older 
series, upon whose eroded upper surface rest the calcareous sandstone 
of the Potsdam, the Mendota, the Madison, and the Lower Magnesian, 
as indicated in the ideal sketch of Fig. 34, appears a, more satisfactory 
explanation, but one which meets a considerable difficulty in the oc- 
eurrence of upper Potsdam fossils in the high-level beds, and one 


TOE LOWER SILURIAN ROCKS, 539 


which I am somewhat loath to advance, as too bold a generalization 
from the facts in hand. It is not impossible that the true explana- 
tion may lie in the supposition that during the deposition of the Pots- 
dam series the quartzite ranges, being high islands and reefs in the 
ancient seas, received synchronous littoral depositions at high and ab- 
normal altitudes, the sand and bowlders for these depositions coming 
from the wear of the quartzite itself. 

Leaving now the Baraboo region, and proceeding northward along 
the eastern side of the district, we find, everywhere in the neighbor- 
hood of the escarpment that forms the western edge of the main area 
of the Lower Magnesian, the same succession of layers as seen along 
the Wisconsin in Columbia and Sauk counties, i. e., Madison and 
Mendota beds, underlaid by 100 to 150 feet of calcareo-arenaceous 
layers, and these again by brown and white non-caleareous sandstone. 
This succession holds true at least as far as Waupaca county, and 
probably further than this. West of the escarpment, in Waushara, 
Marquette and Columbia counties, the country surface is generally 


— AZ A, 
IpeaL STRUCTURAL SKETCH, SHOWING PossIBLE RELATIONS OF THE HORIZONTAL FoRMATIONS IN 
THE VICINITY OF THE BARABOO QUARTZITE RANGES. 


well down in the Potsdam, and much drift-covered. In central Wan- 
shara county, however, are some high hills reaching into the limy 
beds just beneath the Mendota, and showing the normal succession 
of layers; whilst in the very northeast corner of Marquette county, 25 
miles from the boundary of the main Lower Magnesian area, are two 
isolated bluffs, capped by that formation, which show also the usual 
layers. It is thus evident that for all this region there are no de- 
partures from the Madison section. At several points in Marquette 
and Waushara counties quarries are opened in beds that lie about 200 
feet below the Mendota, and yield a much indurated, white sandrock, 
which is occasionally quite coarse, and is made up of nearly glassy 
quartz pebbles. 

Proceeding now westward into Adams and Juneau counties, we 
find again some apparently abnormal occurrences. One mile west 


540 GEOLOGY OF CENTRAL WISCONSIN. 


from the lime-capped bluffs at the northwestern corner of Marquette 
county, are other bluffs, showing large exposures of the limy layers 
that come immediately beneath the Mendota. One and a half miles 
northwest from here, on Sec. 3, T. 17, R. 7 E., across an intervening 
level stretch of sand, is one of the towers of sandstone that chaz- 
acterize the central plain—known as Pilot Knob. This peak rises 
25 feet above the top of the calcareous layers seen just across the 
valley, and 65 feet above their base, and yet from its summit down 
for 150 feet, we find only altogether non-calcareous sandstone, much 
of which is highly ferruginous, and all of which is quite unlike any 
of the layers that are usually found within 200 feet of the base of the 
Mendota. Moreover, two fossil horizons, yielding Ptychaspis Minis- 
ceensis, and other forms, supposed to be characteristic of the middle 
portion of the lower sandstone, occar in this exposure. We have, 
then, here, to some extent, a repetition of the anomalous occurrences 
of the Baraboo region—noncalcareous, red, ferruginous sandstone, with 
fossils indicating a horizon full 300 feet below the Mendota, rising 
through the horizon of the upper calcareous beds, into that of the 
Mendota. Some nine miles west of Pilot Knob, near Friendship, 
Adams county, occur other similar sandstone towers, all showing en- 
tirely non-caleareous, friable rock. On the summit of one of them, 
the Roche 4 Cris, is to be recognized the uppermost of the fossil 
horizons of Pilot Knob, the lower one of which, marked by a 
peculiar lithological character, is still more unmistakably to be re- 
cognized on another bluff, some five miles south of Friendship. Both 
of these horizons indicate a slight rise of the layers eastward towards 
Pilot Knob. , Still another one of these outliers, the Friendship 
Mound, ries 85 feet higher than the Roche a Cris near by, carrying 
the light-colored, friable, non-calcareous sandstone all the way. The 
horizon of the summit of this bluff is, then, $5 feet above that of the 
summit of Pilot Knob, or, if the latter rises into the horizon of the 
Mendota, as high as the position that would be expected for the 
Lower Magnesian, from its occurrences in northeast Marquette 
county. 

At the southern end of Adams county, the Wisconsin passes the 
gorge known as the Dalles. At the northern end of the gorge is 
another of the large sandstone outliers like those just. mentioned — 
the Elephant’s Back. This bluff, with the walls of the gorge below, 
gives a nearly continuous section of 310 feet. At Kilbourn City, two 
miles below, an Artesian boring penetrates into the underlying Arch- 
ean. Combining the results of the section and boring, we have the 
following general succession: 


THE LOWER SILURIAN ROCKS. 541 


; . . : Feet. 
Fine-grained sand layers; of varying colors, in upper portions; with gaps of 10 to 
720 feet; including at base some quite coarse-grained sand layers; all formed of 


rolled quartz, and all entirely non-calcareous..... vives dune SRaWEwaw RE nara 310 
The same continued in the Artesian well ...........c cece cece cceucrecuneeecens 885 
Red Shale iarsd sis: asiias ardleapiceaeserite aus we eeanaddidles ans aba vanciaie emmear facies Acedia deta ole 15 

Dba sa dig lah g saith winks @iaiets eatin clebere natal eine a aicieeiaia a detaisidediedy Aistabandeadad wie 710 


At the summit of the Elephant’s Back, fragments of trilobites 
occur in the loose sand rock, and the horizon may be the same as that 
on the top of Roche & Cris. The occurrence here of the same red 
shale as observed in the Madison wells is worthy of notice. The 
same layer has been reached by Artesian borings in other parts of the 
state. 7 

_ Returning now to the Baraboo ranges and passing northward from 
their western ends along the west side of the district, we find in the 
town of Reedsburg, Sauk county, the Lower Magnesian, Madison and 
Mendota, with their usual characters. In the same town, at points 
some miles apart, exposures of a bed of red shale are to be seen whose 
horizon is 140 feet below the Mendota base. Further north, in north- 
western Juneau, a high, ridgy country is met with, carrying sand- 
stone at high levels, in what would be expected to be the Lower 
Magnesian horizon. This, however, appears to be due to a thicken- 
ing of the Madison beds, since the Lower Magnesian is found capping 
a few very high points, and the Mendota beds below continue recog- 
nizable. In southwestern Juneau county, on the inner side of the 
high ground bordering the central plain, are numbers of isolated 
sandstone outliers. Some of these show a bed of red shale and soft 
greensand, which appears to be the same as that seen in the town of 
Reedsburg. This greensand layer, about 130-140 feet below the 
Mendota, is the lowest seen anywhere in the Potsdam series of Cen- 
trai Wisconsin. 

Still further north, the country is generally eroded well down into 
the middle of the Lower sandstone, so that the Archeean rocks are not 
very far beneath the surface, which they come nearer and nearer to, 
towards the north. Over much of Portage, Wood, Jackson and Clark 
counties, the thickness of the sandstone cannot be more than 25 to 
60 feet. In places in this region, the sandstone lying within 20 to 40 
feet of the crystalline rocks is a much indurated, coarse, white rock, 
which yields a valuable quarry stone, and appears to occupy the same 
horizon as a similar rock in Waushara and Marquette counties. It is 
probably to be referred nearly to the middle part of the Lower sand- 
stone. The sandstone immediately in contact with the crystalline 


542 GEOLOGY OF CENTRAL WISCONSIN. 


rocks is usually a quite friable, fine to coarse-grained, brownish rock, 
containing pebbles from the rock below. . 

It is not at all impossible, as already indicated, that the anomalous 
occurrences about the Baraboo quartzite ranges, and in Adams county, 
may mean that the Lower sandstone really consists of two series, the 
one, including the ordinary calcareous sandstone that comes beneath 
the Mendota, and an unknown thickness below, resting upon the 
eroded surface of the other. Dr. Owen gives sections from the St. 
Croix region, showing the Lower Magnesian occupying positions 
lower than the Potsdam in the immediate vicinity, which may indi- 
cate the same thing. These occurrences on the St. Croix are also 
described by Dr. Percival in some detail, he considering them best 
explained by the existenve of several alternations of limestone and 
sandstone. Still more strongly confirming the idea, are the occur- 
rences in the vicinity of the Archzean patches at Berlin, in Green 
Lake county, and Portland, in Dodge county, as described to me by 
Professor Chamberlin. In the former case, a mound of quartz- 
porphyry projects into the horizon of the Lower Magnesian, but is 
flanked by sandstone containing the fossils regarded by IJall as be- 
longing to the middle Potsdam. In the latter case, several distinct 
mounds of Archean quartzite lie in the horizon of the St. Peters 
sandstone, which shows on the margin of the low ground in which 
the mounds occur. Flanking the quartzite, however, are layers of a 
bowlder-conglomerate carrying Scolithus, which is usually regarded 
as restricted to the lower sandstone. It is quite evident that even if 
the lower sandstone really does include two formations so distinct in 
age as these facts seem to suggest, such a division of the series would 
be quite difficult to demonstrate, on account of the great lithological 
similarity between the two divisions, whilst, if proved, the separation 
of the two in mapping would be even more difficult. 

The beds of passage between the Potsdam and Lower Magnesian 
series include, as already said, two well marked beds, 60 to 90 feet in 
combined thickness — the Mendota limestone and the Madison sand- 
stone — which, from their prominence in Central Wisconsin, are 
worthy of separate mention. or the most part these layers come to 
the surface only on the flanks of the higher levels occupied by the 
Lower Magnesian, so that they present on the map only narrow bands 
bordering the areas of the last named formation. In that part of the 
Catfish valley, however, which lies between the southern shores of 
Lakes Monona and Kegonsa, they are at the surface over a wide area, 
whilst in some parts of Columbia connty the belt occupied by them 
sometimes reaches two or three miles in width. Both beds are to be 


THE LOWER SILURIAN ROCKS. 543 


distinctly recognized throughout the Central Wisconsin district, 
wherever the base of the Lower Magnesian can be inspected. The 
northernmost point at which 1 have recognized them is at the north- 
west corner of Marquette county, the southernmost on the south 
shore of Lake Kezonsa in Dane county; the two points being about 
7 miles apart. The most distant points east and west at which they 
have been seen in Central Wisconsin are about as far from one 
another. To the northeast, however, Prof. Chamberlin thinks he has 
recognized the Mendota as far as the Michigan line, whilst Mr. Strong 
’ earries the same layer westward to the Mississippi. 

The Mendota and Madison beds often have a marked effect upon 
the topography, producing, by their different hardnesses, benches in 
the sides of bluffs. Where the Mendota is at surface over any con- 
siderable area, it produces generally an excellent clayey soil; whilst 
the Madison soils, as in a large part of the town of Otsego, Columbia 
county, are as loose and sandy as those of the Potsdam proper. About 
Madison, where the two layers were first distinctly recognized, the 
Mendota has a thickness of 30 to 35 feet, of which the lower 20 feet 
are of a heavily-bedded, dark-yellow and brown, jointed, conchoidal- 
fracturing rock, which is stained in seams and patches by the red oxide 
of iron, and leaves on solution 3 to 10 per cent. of an aluminous and 
non-arenaceous residue. This rock quite closely resembles the lower 
portions of the Lower Magnesian proper, having sometimes the con- 
eretionary structure characterizing that formation. The upper part 
of the Mendota about Madison resembles the lower, except in being 
in thin, rough-surfaced, layers, and in carrying a somewhat larger 
percentage of silicious matter. To show the close similarity in com- 
position which this phase of the Mendota bears to the Lower Magne- 
sian, the following analyses are given, I being the Mendota, from the 
quarry near Greenbush, Madison, and II, Lower Magnesian from 
Williams’ quarry, on the south line of the town of Madison: 


I. Il. 
SiGe paais Gases, Rika Sie d vise phan SATS. G cae ame Se aan a 4.18 1.09 
MiMi awiesescee bret ciel: Bodh Laeenaee coke eee ada tA 2.17 44 
Tron sesquioxide ....-....eeeeee eet e een eee e eens ceeees 1.45 43 
Jron protoxide ...... eee ee cece eect een e teen een een ees eaed -63 
Lime carbonate... 0... ccs ec cece ence eeene seeneeeeee 55.68 66.82 
Magnesia carbonate .... +... e esse e ce eee een e eee e eee en es 36.52 30.40 
Water sas iiatsnsaeeae + imesstherdeckany has eens os .58 .80 


It will be noticed that in both the proportion of lime to magnesia 
carbonate is greater than in true dolomite (1.19:1). Both yield, also, 


544 GEOLOGY OF CENTRAL WISCONSIN. 


or solution, an argillaceous residue, differing in this regard from the 
limy layers of the Potsdam proper, which always yield a residue of 
white quartz-sand, with or without glauconite grains. The close 
earthy texture of the Mendota also contrasts greatly with the porous 
and highly crystalline character of the lower calcareous seams. 

The Madison beds, in the country about Madison, are about 35 feet 
thick, and consist usuaily of pure white, frequently loose, sand, over- 
laid by brown and yellow, firmer rock. The upper layers show gen. 
erally a slight calcareous admixture, which locally increases to 10 or 
15 per cent., the rock then becoming a good building material, and 
not being very sharply defined from the limestone above. The calca- 
reous layers show well in the quarry just west of the city of Madison, 
where they are as much as 15 feet in thickness, and also in the large 
quarry near the village of Middleton. The section at the latter place, 
given in detail on a subsequent page, is of interest as showing the 
gradation of the Potsdam series into the Lower Magnesian, there be- 
ing a number of thin alternating sandstone and limestone layers, 
whilst the upper Madison beds contain as much as 50 per cent. of 
lime and magnesia carbonates. West of Lake Kegonsa, in the town 
of Dunn, the Madison sandstone is as much as 50 feet in thickness, 
closely resembling the St. Peters, and grading downwards into the 
Mendota. 

About the village of Lodi, in Columbia county, both Madison and 
Mendota are frequently exposed, with characters like those just de- 
scribed. Further northeast, along the western edge of the Lower 
Magnesian, they undergo some change. At Rio the lower portions 
of the Madison are composed of a firm, white, purely silicious mate- 
rial, which is made up of sharply angular quartz, whilst above, the 
ordinary brown, fine-grained rock comes in. Near Cambria, still 
farther north, the same thing is to be seen, the Mendota layers be- 
coming at the same time largely replaced by reddish clay-shale, but 
still retaining in parts the typical yellow appearance. Near Mar- 
quette, in Green Lake county, the Madison has its usual brownish, 
friable character, whilst the Mendota is largely composed of a light 
yellow, regularly bedded, aluminous limestone, and is not well defined 
from the sandstone below. 

Along the valley of the Wisconsin, in Sauk and Dane counties, both 
of the layers are well marked, the Mendota having most comnionly 
the character last described. Its regular bedding makes it valuable 
as a building stone, and it is hence frequently quarried. Near Spring 
Green it reaches a thickness of as much as 45 feet in all, its upper 
layers being shaly and fossiliferous. The Madison sandstone in this 


THE LOWER SILURIAN ROCKS. 55 


section has also an increased thickness, reaching 45 feet, but other- 
wise it shows the characters before noted. Northward, along the west 
side of Sauk county, both layers continue well marked as for as the 
Baraboo river. Still farther north the Madison beds thicken to 60 
feet, are made up of fine-grained, red and white, saccharoidal sand- 
stone, closely resembling the St. Peters, and have at top one or two 
feet of cherty quartzite-like material. 

To the list of fossils of the lower sandstone series given by Hall, 
but little has been added by the present survey, as far as Central Wis- 
consin is concerned. It has already been said that his general group- 
ing, of upper, middle, and lower species, appears to hold true as re- 
gards the order, but that his lower species must really be assigned to 
the middle of the series, since its thickness is about twice as great as 
Mr. Hall supposed. Fossils are not plenty in the Central Wisconsin 
Potsdam. In the ordinary non-caleareous rock they occur as mere 
ferruginous coatings on the loose sand, trilobite fragments being the 
most common. In the upper shaly layers of the Mendota beds, very 
large impressions of Dicellocephalus Minnesotensis are quite abund- 
ant. The pygidium is most frequently found, some specimens. meas- 
uring as much as six inches across. The same fossil, however, is 
found in the loose friable sandstones that lie upon the quartzites of 
the Baraboo ranges, and not improbably has a considerable vertical 
range, since it is quoted by Hall from the Lower Magnesian of Min- 
nesota. One new fossil of some interest has been added to Hall’s 
list. This is a very large new species of the genus Palwacmea, which 
was originally established by Hall and Whitfield, in 1867, to cover a 
“conical, patelliform, univalve shell,” which occurs in the Potsdam 
sandstone of New York. The Wisconsin species is twice as large as 
that from New York, and is found ina very hard quartzite, which 
occurs interstratified with loose, friable sandstone on the Trempealean 
river, in Jackson county, in the middle portion of the Potsdam series. 

The economic contents of the Lower sandstone come under the 
heads of building stones, glass sand, and iron ores. These are des- 
eribed here in general only, all details, exact locations, etc., being 
given in subsequent pages. 

The Madison sandstone, in the vicinity of Madison, yields a buff. 
colored calcareous sandstone which is largely quarried and used for 
building in that vicinity. This rock contains about ten per cent. of 
the carbonates of lime and magnesia, is easily cut, and obtainable in 
large blocks. It has a very pleasing appearance in the fresh state, 
but has some tendency to darken and become blotched under the ac- 
tion of the weather. The same rock is opened upon at Middleton, 

Wis. Sur. — 39, 


546 GEOLOGY OF CENTRAL WISCONSIN. 


and in one or two places in the town of Westport, Dane county, 
and probably exists in considerable quantity in the country about 
Lake Mendota. The peculiar phase which yields the Madison build- 
ing stone is, however, local, and quite inconstant. More commonly 
the formation is made up of white and brown friable sandstone, nearly 
or altogether without calcareous admixture. The brown layers are 
occasionally quite ferruginous and firm, yielding a fair quarry stone. 
The white sandstone is frequently a loose, white, purely silicious sand, 
and would be of considerable value for glass making. In one place 
on the western side of the town of Honey Creek, the Madison sand- 
stone has a very unusual character, containing layers of a much indu- 
rated, fine-grained, smooth-faced, pink-tinted rock of very pleasing 
appearance. 

The Mendota limestone is more frequently quarried than the Mad- 
ison sandstone. It is not anywhere burnt into lime, being usually 
too impure, and always too dark colored, but the heavy yellow layers 
that characterize some ten to 15 feet of its middle portions, are to be 
seen in scores of quarries, most numerously along the Wisconsin 
valley. These layers yicld a very regular stone, of any thickness 
from a few inches to two or three feet, which is commonly used for 
flagging or foundations, but occasionally for constructing entire build- 
ings. The mill at Cambria, Columbia county, is built of rock from 
the Mendota horizon. 

The Potsdam sandstone itself is generally altogether too friable to 
be used as a building material. At numbers of points in the Baraboo 
valley, however, a firm, fine-grained, white rock is obtained in large 
blocks. A similar rock is quarried on several of the isolated bluffs . 
in Juneau, Adams and Jackson counties, the horizon being about 200 
to 300 feet below the summit of the series. .A very much indurated, 
frequently quite coarse, rock is obtained ata still lower horizon at 
Packwaukee, Marquette county, near Wautoma, Waushara county, at 
Stevens Point, Portage county, near Grand Rapids, Wood county, and 
at Black River Falls, Jackson county. This rock is very regular in 
bedding, white to straw colored, and makes a very durable and sightly 
building stone. 

Limonite iron ores, of good quality, and in sufficient quantity to 
run two small blast-furnaces, occur in conuection with the Lower 
sandstone in Sauk and Richland counties, just west of the limit of 
the Central Wisconsin district. Within that district, the only ore ob- 
served in any promising quantity occurs in the upper layers of the 
high-level sandstone that flanks the quartzite range in the eastern 
part of the town of Westfield, Sank county. Here, at a number of 


THE LOWER SILURIAN ROCKS. B47 


points several miles apart, this sandstone may be seen very highly 
charged with the brown iron oxide, which, at times, almost entirely 
excludes the sandstone, having then mingled with it much of the red 
or anhydrous oxide. It appears quite probable that the amount of 
merchantable ore to be obtained in this neighborhood is sufficient to 
warrant exploitation. Very ferruginous sandstone, at a similar ho- 
rizon, occurs at other points along the Baraboo ranges, but nowhere 
else have promising indications been observed. 


THE LOWER MAGNESIAN LIMESTONE. 


Succeeding the uppermost layer of the Potsdam series, the Madi- 
son sandstone, is a very persistent and wide spread bed of magne- 
sian limestone, to which Owen gave the name of Lower Magnesian, 

to distinguish it from another equally persistent, and in many respects 

quite similar, magnesian limestone, that occurs higher in the series. 
To the latter the name Galena limestone has since become attached, 
whilst no other designation has been given to the lower formation. 
In neither case can the term magnesian be regarded as at all dis- 
tinctive, since almost all of the limestone beds of Wisconsin, including 
the whole of the great thickness belonging to the Niagara group, are 
highly magnesian, the only exception to the general rule being the 
Blue limestone of the Trenton group. There appears to be but little 
doubt that the Lower Magnesian is nearly the exact equivalent of 
the Calciferous Sandrock of New York and Oanada, with which form- 
ation, indeed, it is nearly continuous through the northern peninsula 
of Michigan and Canada West. 

The surface extent of the Lower Magnesian limestone in Central 
Wisconsin is not nearly so great as that of the Lower sandstone, being, 
in all, not more than about 75 square miles. The main belt oceupied 
by the formation enters Columbia county on the northeast ,with a 
width of about 6 miles, and, spreading further and further west as it 
is followed southward, occupies much, or all, of the towns of Randolph, 
Scott, Springvale, Courtland, Lowville, Otsego, Fountain Prairie, 
Columbus, Hampden, Leeds, Arlington, Lodi, and West Point in 
Columbia county, and large portions of Roxbury, Berry, Dane, 
Springfield, Vienna, Westport, Windsor, Bristol and York, in Dane 
county. Still further south, again, the formation occurs only in nar- 
row areas, crowning the summits of the ridges between the valleys in 
which run the several head streams of the Catfish river, or forming 

_narrow strips between the low ground of the valley of that stream, 
and the higher country which on each side is occupied by the St. 


548 GEOLOGY OF CENTRAL WISCONSIN. 


Peters standstone, and Trenton limestone. On the southern side of 
Dane county the Lower Magnesian sinks to the level of the Catfish 
valley, spreading over a considerable area in the towns of Rutland, 
Dunn, Pleasant Springs and Dunkirk. The numerous narrow steep- 
sided valleys, tributary to the valley of Sugar river, in Primrose, 
Springdale and Cross Plains, and the valley of Sugar river itself in 
Verona and Montrose, cut down to the upper surface of the Lower 
Magnesian, which thus forms narrow strips along their bottoms. 

Along the edge of the main area, in Columbia county, and north- 
western Dane, and usually not more than two or three miles west or 
north from it, though occasionally more than this, are many small 
isolated bluffs crowned by the Lower Magnesian. These vary in area 
from a few acres to three or four square miles. North of the Wis- 
consin river and along the west side of Sauk county, as far as the 
southern side of the Baraboo valley, the Lower Magnesian, in areas 
of varying size, occupies all the higher ground, the country being 
characterized by numerous narrow ridges, with intervening narrow 
valleys. North of the Baraboo, in northwestern Sauk county and 
southwestern Juneau, the Lower Magnesian occurs only in rare and 
very small cappings on the highest ground. 

The topographical characters of the regions occupied by the 
Lower Magnesian differ much, according as they occur within or 
without the drift-bearing area, and also according to whether the 
formation exists on the higher grounds only, or has sunk down to the 
lowest levels. All of these regions, however, are alike in possessing 
a most excellent soil, the Lower Magnesian area including the best 
agricultural land in the district. In Columbia county the formation 
occupies a region which is for the most part very fertile, high, rolling 
prairie, the prairie areas forming a nearly continuous belt from the 
towns of Scott and Randolph, in Columbia county, southwestward to: 
Middleton, in Dane county. This high belt breaks down suddenly to 
the westward, but the escarpment, though quite bold, is without the 
great cliff-like exposures so characteristic of the Lower Magnesian as 
it appears along the lower Wisconsin and upper Mississippi rivers. 
The same is true of the sides of the limestone ridges about the heads 
of the Catfish river. Along the Wisconsin, however, below Sauk 
City, the Lower Magnesian crowns the river bluffs often with bold 
cliffs, the ditference being chiefly due to the absence of drift materials. 
Along the western side of Sauk county, the drift is also absent, and 
the usual abrupt, ridgy topography of the driftless regions is every- 
where apparent, the limestone capping to the ridges being often a mere 
crest of rock, large fallen masses from which dot the side-hills below. 


THE LOWER SILURIAN ROCKS. 549 


Whilst in minor details the Lower Magnesian varies much as to its 
lithologicai characters — even individual horizons not showing any 
great constancy in this regard —all parts of it have some features in 
eommon, which serve to distinguish it from the newer limestone 
formations of the region. In general, it may be said that the Lower 
Magnesian is a magnesian limestone, varying in composition from 
varieties that contain not more than one or two per cent. of insoluble 
ingredients, to those that are for the most part sand. An analysis 
has been given, a few pages back, of one of the purest phases, whilst 
in the detailed descriptions of this chapter, numerous determina- 
tions of the quantity and nature of the insoluble ingredients of 
both pure and impure varieties will be found. These in the 
purer kinds are exceedingly fine and clay-like, whilst in the less 
pure they are usually quartz sand of varying degrees of fineness, 
the constituent grains always much rolled. The analysis above 
cited, as also others made for the survey, do not show the car- 
bonates of calcium and magnesium in the right proportion to make 
a true dolomite, the first-named carbonate being always in excess. 
Older analyses show a nearer approach to the composition of dolomite. 
The purest kinds have usually a grayish-white color, a minutely crys- 
talline texture, and marked conchoidal fracture. More commonly the 
white back-ground is blotched with yellow, whilst other layers again 
occur, in which the buff color is uniform. These are usually charac- 
terized by a close, even, granular texture, which may be due to an 
admixture of sand grains, or may characterize a quite pure lime- 
stone. 

The bedding of the Lower Magnesian varies much. Usually those 
layers from 40 to 60 feet above the base are the heaviest, the indi- 
vidua] layers running sometimes to a thickness of 4 to 6 feet, whilst 
the bedding lines are exceedingly indistinct. In the upper and lower 
portions of the formation, the layers are usually much thinner, and 
more distinct, although: commonly quite irregular, very rough-sur- 
faced and internally porous, with drusy cavities that are lined with 
calcite and dolomite crystals. Occasionally, however, the lower layers 
are exceedingly regular, being obtainable in large, smooth-surfaced, 
compact, and finely granular slabs. Highly concretionary layers, some 
of which appear even to have a brecciated structure, occur at many 
different horizons in the formation, the structure sometimes affecting 
in the highest degree a layer not more than a foot thick, whilst above 
and below, for many feet, no trace of a concretionary structure is ap- 
parent. In other cases much greater and less well-defined thicknesses 
are affected in this manner. One of the most prominent features of 


550 GEOLOGY OF CENTRAL WISCONSIN. 


the formation is the rough-weathering seen on nearly all outcrops, in 
some cases due to the concretionary structure of the rock. 

Shert oceurs very abundantly throughout the Lower Magnesian, 
and of three or four different kinds. In many places above the Mad- 
json sandstone there is to be seen a thin layer of greensand, and above 
this a thinner one, one to ten inches in thickness, of a pure white, 
oolitic, chert, which, on examination under the microscope, appears 
to consist of egg-shaped aggregations of fine glassy quartz grains, em- 
bedded in a still finer silicious matrix. This layer is very persistent. 
in the country about Madison. A sample from the Madison quarries 
yielded: silica, 98.01; alumina, 0.52; iron peroxide, 0.73; lime, 0.67; 
magnesia, 0.21; water, 0.24=100.38. The same odlitic chert occurs 
Jisseminated through the layers of limestone in the lower beds, to the 
whole mass of which it often gives the appearance of an odlitic struc- 
ture. The older writers on Wisconsin gevlogy all speak of odlitic 
limestone as characterizing the lowest portions of the Lower Magne- 
sian; so far as my observation goes, the limestone is not odlitic itself, 
but carries disseminated odlitic chert. Tigher up, beginning usually 
some 30 feet above the Madison sandstone, a more compact chert 
comes in, increasing in quantity as the formation is traced upward. 
This chert is either quite compact and flinty, occurring in irregular lay- 
ers or nodules, or is more or less cavernous, the cavities being lined 
with drusy quartz. Associated with the greyish-white beds of the 
least silicious limestone, is a chert occurring in well-marked layers 
and rows of nodules, which, in external shape and soft silicious coat- 
ing, resemble closely the flints of the Chalk, whilst within they are 
often beautifully banded and jasper-like. Still higher in the forma- 
tion, about 100 feet above its base, the thin layers of limestone are 
often replaced bodily, for considerable thicknesses, by a compact iron- 
stained chert. 

Black dendritic markings are very common in the Lower Mag- 
nesian, but occur in the greatest abundance and beauty in those layers 
that are fine-granular and buff-colored, and not more than 30 to 40 
feet above the upper surface of the Madison sandstone. The mineral 
causing these markings is supposed to be the black oxide of man- 
ganese. 

In stratigraphical arrangement, the Lower Magnesian appears 
to show but little persistent regularity. An attempt to make out a 
thoroughly reliable and detailed scheme of the stratigraphy of this 
formation, meets with two considerable difficulties. The first of these 
lies in the fact that, althongh exposures are very numerous, it is only 
rarely that any considerable thickness can be scen at one place; so 


. 


THE LOWER SILURIAN ROCKS. 551 


that numerous small, often somewhat distant, exposures have to be 
thrown into place by means of aneroid observations, a not very satis- 
factory guide. The other difficulty arises from the irregular nature 
of the upper surface of the formation, which is due to erosion before 
the deposition of the St. Peters sandstone, and as a result of which 
the Lower Magnesian varies from 51) to 250 feet in thickness. From 
this it follows that all determinations of horizon within the Lower 
Magnesian, made by measuring from the base of the St. Peters sand- 
stone downwards, are worthless. Varying so greatly as it does in thick- 
ness, beds immediately underneath the St. Peters may, in fact, be 
nearer the base than the summit of the formation. 

In the region around Madison, the Lower Magnesian has usually a 
thickness of about 70 to 80 feet, though it may run from 50 to 100. 
feet. The following outline scheme of the succession of its layers in 
this region is an abridgement of a more elaborate one, which ac- 
companied the annual report on the tield work of 1874, to which was 
also attached a large chart of grouped sections. These are not here 
reproduced, because the work of later seasons proved them to have 
only a local value. The numbers in the scheme are from below 
upwards, on account of the uncertainty as to any measurements from 
above, downwards. The exposures cited are only single instances out 


of many representing the different layers. 
. ee 
VII. Concretionary, brownish-yellow layers, which at times are quite sandy, oe. 
and at others contain not more than 3 to 4 per cent of fine aluminous 
impurities; Veerhusen's quarry, Sec. 25, Westport; Williams’ quarry, 
Sec. 33, Madison. Thickness about........... 0 cece ence ee eee ee ennee 10 
VI. Heavy. indistinctly bedded layers, which appear to vary much in charac- 
ter, being sometimes, as at Williams’ quarry, Sec. 33, Madison, greyish- 
white, nearly free from foreign ingredients, minutely crystalline, con- 
choidal-fracturing and compact, but with small cavitics lined with dolo- 
mite crystals. Interstratified are continuous seams, and rows, of white 
surfaced nodules of jaspery chert. At other times, as at Veerhusen’s 
quarry, Sec. 25, Westport, these layers have a greenish-tinted buff color, 
and a fine-granular texture, containing 30 to 40 per cent. of fine quartz 


sand, and little or no chert. Thickness, in all, about.........----..+- 15 

V. Thin, regularly bedded, greenish yellow, fine-granular layers, with very 
abundant and large dendritic markings; Veerhusen’s quarry .......--- 10 

IV. Very irregularly bedded, alternatingly heavy and thin, white-and-yel- 
low-mottled, rough-textured, very cherty, layers; Middleton quarry.... 20 


II. Thin, irregular, usually somewhat sandy, brownish layers, including oc- 
casionally beds of 1 to 2 feet in thickness. Near the top a very highly 
breceiated layer, 1 foot thick, often comes in (quarry near the school 
house, Middleton); whilst below, oolitic chert pervades the limestone, and 
alternations of more and less sandy layers occur, constituting a passage 
downwards into the Madison sandstone (Middleton and Madison quar- 
ries). In some cases this gradation is not marked, the transition from a 


552 GEOLOGY OF CENTRAL WISCONSIN. 


nearly pure limestone to a ncarly non-caleareous sandstone being quite Fé. In. 
abrupt (cut on Chicago and Northwestern road, Sec. 35, Madison; also, 


cut on same road at Mendota Station, Westport). Thickness ....-...- 15 
II. White odlitic chert layer (Madison quarries)... -..+ ++: ++ esse eee eres , 

J. Greensand layer (Madison quarries) ....+.++s sere sere cere eer eens nate = 
Totals ccsequs ae seeeeaee Ona wae de tod ss eee Pea oe eee eG o 71 


The bold bluff that rises from the mouth of Honey creek, Sauk 
county, has already been cited as giving an unusually complete sec- 
tion of the upper part of the Potsdam series. It shows, also, the 
largest continuous exposure of the Lower Magnesian that I have ever 
seen — a vertical cliff over 50 feet in height. The following is a de- 
tailed section of this cliff, beginning above: 


ft. In 
1. Heavy layer of brown-and-yellow-mottled limestone, which leaves on solu- 
tion 2.2 per cent. of very fine clayey residue....+..+-.e eee ee cere eee 1 
2. No good CXPOSULE.. 16... - cece cece ete e eee eee eer teen ee eee t eee ae 5 
3. Heavy layer of very close-textured, nearly white, Vaxiestond; with many 
dendritric markings; residue 9.09 per cent. and clayey...-.-+..++-.+5- 1 2 
4, Thin layers, 3 to 4 inches each, of limestone like the last; residue 5.8 per 
Cent,, Clayey... 2... cc cee eee ree cece cece eens et en ee near ers taenenes 3 
5. Thin layers of brown-and-gray-mottled limestone with minute cry tel lined 
cavities; residue 2.9 per cent., Clayey..... 66. cee reece eee eee cece ca 16 
6. Heavy layer of light gray, close-textured limestone, with cavities like No. 
5; residue 8.35 per cent., clayey... ....e. cece eee reece eee eee eee eee 3 6 
7. Two heavy layers like No. 6; residue 6 per cent., clayey...+..+e.++eereee 5 2 
8. Shaly layers of porous, yellow-and-gray-mottled, crystalline limestone; 
residue 7.2 per cent., clayey... - +. ees c cece rece eee e eee e ere ete teens 2 3 
9. Three layers of yellow-and-gray-mottled, close-textured limestone; residue 
18.85 per Cenk, Clayey.c iss. wane tees pees Pees Gaeedsenss sixes OS 
10. Heavy layer of yellowish, sandy Limestone; residue 40.17 per cent., fine, 
GVA SANG 23 trates odoin dhemas, dat bse ga Quod RNC ata. eshch OvncS mapa a oea Gunes 2 
11. Heavy non-arenaceous layer, with very indistinct subordinate bedding... 3 (6 
12. Very irregular, brownish, close-textured limestone, occurring in thin een 
layers, the cracks being lined with white stalactitic lime carbonate; resi- 
due 4.38 per cent., clayey... ....-. cece cece ener eters eeeae oteee 1 6 
13. Two heavy layers of brownish-gray, close-textured limestone; residue 3.42 
per cent.;: Cayey onesies dees vied parbad Hem siediemnbls sve sale arate smeurs 2 6 
14. Trregularly thin bedded, very close-textured chonchoidal-fracturing gray 
* limestone; residue 9.3 per cent., clayey......- Ao Sig BeBidisinie bode. east ones 1 4 
15. Very indistinctly bedded, nodular-weathering, close-textured, mottled lime- 
stone; residue 7.17 per cent., clayey... 1.0... cece ce eee ence eee ene e ees 8 8 
16. Very irregularly bedded, rough-surfaced, close-textured, gray limestone; 
residue 28.97 per cent., fine sand and clay. «0... .... cess eeee eee eee es 3 «6 
17. Thick layer of porous, brecciated, highly-crystalline limestone; residue 
13.67 per cent., fine sand and white clay.... 2.6... cece e eee 1 9 


18. Thick layer of compact, yellowish brown, granular, smooth-fracturing 
limestone, with much dendritic manganese oxide; residue 16.65 per 
Cont, ClAYCY see cece eee tee ee ee enh eee cee ne we ene nen etaneeede 


THE LOWER SILURIAN ROCKS. 553 


The foot of the cliff is evidently very close to the top of the Mad- 
ison sandstone, whose first exposure, however, is 15 feet below. Al- 
though the foreign impurities increase slightly in quantity down- 
wards, we find no distinct evidence of a gradation into the sandstone 
below. In fact the whole cliff shows a nearly uniform material, the 
differences being but slight between the several layers. 

North of Dane county the Lower Magnesian has the same general 
characters as described, with some local variations; but no scheme of 
elementary stratification for these districts has been made out. In 
the high prairie country of southern Columbia county the formation 
attains a thickness of 120 to 140 feet or more, the highest beds being 
generally very cherty, or even replaced bodily by chert. In central 
and northern Columbia the lowest layers have lost their irregularity 
of bedding and rough texture, and have become very evenly bedded 
and closely granular, at the same time showing little or no sandy ad- 
mixture, and no passage downwards into the Madison sandstone, 
which itself continues non-calcareous upwards to contact with the 
Lower Magnesian. Along the western side of the district, in west. 
ern Sauk county, the same lack of gradation downwards is generally 
to be noticed. In a large region lying south of the Baraboo quartz- 
ite ranges, small pebbles of red quartzite are frequently found in the 
Lower Magnesian. 

The irregular upper surface of the Lower Magnesian, already 
mentioned, is one of the most striking features of the formation. 
The first demonstration of the existence of such an eroded surface was 
made by Prof. Chamberlin, in eastern Wisconsin, but since then 
numerous confirming facts have been collected in other parts of the 
state. The valley of Sugar river, and its numerous branch ravines, in 
the towns of Verona, Montrose, Primrose, Springdale and Cross 
Plains, cut down to the Lower Magnesian, the St. Peters sandstone 
forming the stecp valley sides. At numerous points in these valleys, 
exposures of the Lower Magnesian are found at higher levels than 
those of the St. Peters, and under such circumstances that they can- 
not be regarded as proving a distinct and hitherto unrecognized layer 
of limestone; for they are often near to large sandstone ledges, which 
rise continuously from lower to higher levels than those at which the 
limestone is seen. A still more striking proof is found in the patches 
of St. Peters sandstone that are to be seen lying directly in the hol- 
lows of the Lower Magnesian, in the southern part of the town of 
Arlington, Columbia county; whilst the evidence is perhaps even 
stronger in the case of Gibralter Bluff, in the town of West Point, 
Columbia county, where a vertical cliff 135 feet high, of St. Peters 


554 GEOLOGY OF CENTRAL WISCONSIN. 


sandstone, has its base 40 to 60 feet lower than the exposures of Lower 
Magnesian in the immediate vicinity. About Madison, in Dane coun 
ty, the Lower Magnesian is only from 50 to 80 feet thick; just north 
in the high prairie country on the borders of Columbia and Dane 
counties, it has thickened to 125 to 140 feet, a fact in itself sufficient 
to suggest the existence of an eroded upper surface. It is not improb- 
able that some of the swells of this high region are directly due to 
the irregular surface of the underlying limestone. 

The fossils of the Lower Magnesian are not common, and when 
found are but obscure gasteropod and orthoceratite markings in the 
chert of the uppermost layers. If the two small patches of limestone 
already alluded to as occurring in the region between the quartzite 
ranges of the Baraboo be regarded as belonging to this formation, 
quite an interesting addition is to be made to the hitherto meager 
list of Lower Magnesian forms. The limestone of one of these small 
areas has yielded a number of fossils which are regarded by Mr. R. 
P. Whitfield, as “certainly not lower than the Lower Magnesian,”’ to 
which formation the composition, lithological character, and position 
of the rock would also refer them, the difficulty lying in the peecu- 
‘liar conclusions that are thus led to with regard to the Lower sand- 
stone in the vicinity, as explained on a previous page. These fossils 
are: Stromatopora, und. sp.; Orthis Barabuensis?; ITolope, n. 
sp.; Jaclurea Swezeyi, n. sp.; Lllenus antiquatus, n. sp.; Dicello- 
cephalus Barabuensis, n. sp.; D. Hatoni, n. sp.; and triangular 
sheath-like bodies. 

The economic contents of the Lower Magnesian are limestone for 
burning into lime, and building stone. Galena, in small quantities, 
has been obtained from crevices in the Lower Magnesian, but the 
only occurrence of this kind known in Central Wisconsin is that near 
Doylestown, in Columbia county, where a limited crevice in the lower 
part of the formation has yielded several hundred pounds of this ore. 
This occurrence is interesting because at such a distance from the 
productive lead region. I have seen no other indication that the 
Lower Magnesian is ore-bearing. Lime is burnt from the Lower 
Magnesian at a great many points, and from quite different horizons. 
The lime produced is uniformly quite slow in slacking, making, how- 
ever, a very strong mortar. It is rarely very white. Many of the 
lower beds are too sandy for lime burning, the best for the purpose 
being apparently the heavy grayish-white layers 40 to 50 feet above 
the Madison sandstone. Twenty thousand bushels annually are burnt 
from these layers, on Sec. 33, T. 7, R. 9 E., the product being widely 
known as “ Madison lime.” The Lower Magnesian is in general too 


THE LOWER SILURIAN ROCKS. 555 


roughly or too indistinctly bedded to make good building stone, but 
the heavy beds just alluded to sometimes take on a different character, 
becoming fine-granular, and very evenly bedded, and yielding a 
superior cream-colored stone. Such a stone is quarried at one or two 
points in the town of Westport, and has been used in the construction 
of the State Hospital for the Insane, and the United States Court, 
House at Madison. 


THE UPPER OR ST. PETERS SANDSTONE. 


To the layer of sandstone which, everywhere in Wisconsin, Iowa and 
Minnesota, is found resting upon the eroded surface of the Lower 
Magnesian, Dr. Owen gave the name of “ Upper” sandstone, to dis- 
tinguish it from the “ Lower” or Potsdam sandstone. He also desig- 
nated it as the “St. Peters ’’ sandstone, from its prominent exposures 
on the St. Peters river in Minnesota. Mr. Hall regards the St. Peters 
sandstone as the equivalent of the Chazy limestone of New York, on 
account of its stratigraphical position. As to the correctness of this 
reference, J have not the means of forming an accurate opinion; cer- 
tainly, however, between the periods of deposition of the Lower Mag- 
nesian and St. Peters, there was a long gap, whose record is found in 
the eroded surface of the first-named formation. 

For a purely silicious sandstone, and one only 20 to 100 feet in 
thickness, the St. Peters has an extraordinarily wide distribution. 
It is known in Wisconsin at points 250 miles apart from east to west, 
and 180 from south to north, whilst to the west, south and east it ex- 
tends far beyond the limits of the state, In the last named direction 
it is known to extend, because a number of Artesian wells at points 
along the shore of Lake Michigan show it with an unusual thickness. 
To the westward, in Minnesota, it is recognized for an additional dis- 
tance of at least 100 miles, whilst to the southward also it is known 
to extend 100 miles beyond the Wisconsin line. Throughout all this 
large region, there is no question whatever of the identity of the 
formation, or of its actual continuity. Moreover, as far south as Mis- 
souri, the St. Peters is in all probability represented by the upper- 
most of the alternations of sandstone and limestone that form a large 
portion of the Lower Silurian strata of that section. Thus it appears 
that a nearly purely silicious sandstone of inconsiderable thickness 
has an unbroken extent over a region whose diameters are 500 and 
400 miles. 

In the Central Wisconsin district the St. Peters has never a very 
wide surface extent, forming more commonly narrow bands around 
the areas of the Trenton limestune. It is wholly confined to Colum: 


556 GEOLOGY OF CENTRAL WISCONSIN. 


bia and Dane countics. In the former, it is met with in the north- 
east corner of the county, in the towns of Randolph and Courtland, 
with a thickness of only 20 feet, and forming strips not more than a 
few rods wide around several areas of Trenton limestone. Further 
south its main area lies altogether east of Columbia county, but it is 
found again in the southeast,-in the towns of Colambus and Hamp- 
den, with the same small thickness and distribution in a narrow belt 
around an area of Trenton limestone. The St. Peters is absent every- 
where else in Columbia county, except in five small patches on the 
high prairie of Arlington, and in a still smaller area, but with a thick- 
ness of 125 feet, in the high peak known as “Gibralter Bluff,” in the 
town of West Point. In Dane county, the St. Peters is found under- 
lying the Trenton on both sides of the Catfish valley, sometimes 
coming to the surface as a narrow band only, at other times having 
quite a surface spread, as in Sun Prairie, Medina, Cottage Grove, 
Deerfield, Fitchburg, Oregon, Montrose, and Verona; these larger 
areas including a number of small patches of Trenton limestone, 
which caps the summits. On the west side of Sugar river, though 
having its full thickness, the St. Peters comes to the surface only in 
narrow bands, forming the sides of deep and narrow valleys. The 
same is true of the south side of the valley of Black Earth creek in 
Cross Plains and Middleton. In Berry, Springfield, and northern 
Middleton, the St. Peters occurs only in a few limited arcas on the 
highest ground. The whole surface spread of the St. Peters, in Col- 
unbia and Dane counties, is not more than 225 square miles, all but 
6 or 8 of which is in the latter county. 

Jn eastern Columbia and Dane counties the St. Peters sandstone 
does not contribute any marked topographical features to the coun- 
try, being comparatively thin and generally drift covered. Where it 
occurs in narrow bands around the Trenton areas, its place is not un- 
commonly marked by an abrupt change of level. On the west side of 
Dane county, however, and especially west of Sugar river, which 
forms the western boundary of the region of the Glacial Drift, the St. 
Peters affects the scenery of the country in a marked degree. Here 
we find it having its full thickness of 80 to 100 feet, and producing, 
by its friability, abrupt, and not infrequently precipitous and rocky, 
valley sides, whose summits are capped by the Trenton limestone, 
whilst the valley bottoms are on the Lower Magnesian. In the val- 
leys themselves, isolated towerlike rocks of the St. Peters occur, of 
varying size, and occasionally of greater area at top than at bottom. 
Some of these contain the full thickness of the St. Peters, 
crowned with the lowest layers of the Trenton. 


and are 


THE LOWER SILURIAN ROCKS. 557. 


The St. Peters does not usually much affect the soil, since it forms 
only steep side-hills, or else is buried beneath the drift. Occasion- 
ally, however, where it comes near the surface over small level areas, 
as in part of the Sugar river valley, in the town of Verona, it pro- 
duces a loose sandy soil. 

Tn lithological characters the St. Peters is remarkably uniform. 
So far as my observation extends, it is invariably formed of a fine, 
purely silicious, sand, whose constituent grains are muchrolled. No 
sign of crystalline surfaces to the grains has been observed in the 
many specimens examined with the microscope. The only foreign 
materials in the St. Peters are the hydrous and anhydrous iron oxides, 
which ocenr in all parts of the formation, banding it, or staining it 
for great thicknesses, with yellow, brown, or red. The iron oxide 
acts as a cementing material, but is not commonly in sufficient quan- 
tity to give the rock any considerable coherence. In the more west- 
ern development of the St. Peters, it is described as often wholly with- 
out the iron oxides, and made up of pure white, entirely incoherent, 
sand, but this is not common in Central Wisconsin. Greensand lay- 
ers, like those that occur in the Lower sandstone, are found also in 
the St. Peters, but none have come under my observation. No gra- 
dation downwards or upwards into the adjacent limestones by mingling 
with calcareous material has ever been noticed. No subordinate divi- 
sion of the St. Peters sandstone exists. It is quite uniform in char- 
acter throughout. The bedding, however, is usually distinct, the lay- 
ers being ordinarily very heavy, though sometimes quite thin and 
shaly. The lines of lamination are often marked by a red and white 
banding when no planes of separation can be detected. The surfaces 
of large exposures frequently show the hard, vitrified crust so charac- 
teristic of the Lower sandstone. To this induration is evidently due 
the maintenance of tower-like forms and cliffs in so friable a material. 

The older geologists describe the St. Peters sandstone as very uni- 
form in thickness placing it at from 70 to 100 fect, with a nearly 
constant thickness of 80 to 90 feet. According to the results of the 
present survey, although such constancy probably holds true for south- 
western Wisconsin, elsewhere the formation is exceedingly variable 
in this regard. On the east side of the Catfish valley it is 50, 40 and 
20 feet in thickness. Further northeast along its line of outcrop, 
Prof. Chamberlin has found it but a few inches in thickness, and then 
suddenly expanding to 80 or 100 feet. The same irregularity is ob- 
served along its line of outerop to the Michigan line. 

The St. Peters has been reported hitherto as entirely barren in fos- 
sils, but recently a few have been found in the Eastern Wisconsin 


558 GEOLOGY OF CENTRAL WISCONSIN. 


district. No traces of fossils have ever been observed in Central Wis- 
consin. 

The only esonomic contents of the St. Peters are to be found in 
the sand of which it is made. This can be shoveled out and used for 
all purposes to which sand is ordinarily applied. Frequently the 
sand is of such purity and whiteness as to be of excellent quality for 
glassmaking, but, as already said, this phase of the formation is more 
characteristic of its development in the western part of the state and 
along the Mississippi. 


THE TRENTON LIMESTONE, 


In Wisconsin and the adjoining portions of Minnesota, Iowa and 
Illinois, the St. Peters sandstone is succeeded by 300 to 350 feet of 
limestone beds. These are apparently the equivalents of the Treaton 
series of New York, but comprise two well marked members, the up- 
per one of which has no exact representative among the eastern rocks, 
whilst the lower and thinner of the two, as indicated by its numer- 
ous fossils, represents exactly the Birdseye and Black river limstone. 
To this lower member exclusively it has become customary in Wis- 
consin to attach the name of Trenton, the upper being known as the 
“Galena”? limestone, from the fact that it is the main repository of the 
lead ores of the Upper Mississippi lead revion. This nomenclature is 
retained in the present report. 

In the Central Wisconsin district the Trenton limestone has a sur- 
face distribution of about 220 square miles, being confined wholly to 
Dane and Columbia counties. In the latter county it occurs in two 
principal areas, one in the northeast occupying the eastern and cen- 
tral parts of Randolph, and the northeast part of Courtland; the 
other, in the southeast, covering southern Columbia and southeastern 
Hampden. In Dane county the formation has a much wider spread. 
In the towns on the east side of the Catfish valley it covers all the 
higher grounds, occurring in a number of detached areas of very dif- 
ferent sizes. Some of these are quite small, running from a few acres 
to one or two square miles in extent, as in Medina and Deerfield, 
where they are very numerous; others, however, cover the greater 
part of a township, or even two or three townships, as in the case of 
the large one which ocenpies nearly all of Christiana and Albion, with 
considerable portions of Pleasant Springs and Dunkirk. On the west 
side of the Catfish, in Rutland, Oregon, Fitchburg, Verona and Mont- 
rose, are a number of small areas of Trenton, occurring as isolated 
ridges ainidst a lower country occupied by the St. Peters. A large 


THE LOWER SILURIAN ROCKS. 559 


area of Trenton occupies the high ground at the head of Sugar river, 
in Cross Plains and Middleton, whilst the numerous narrow ridges 
between the branch streams of Raeee river in Primrose and Spring- 
dale are everywhere crowned by this formation, which in the highest 
ridges is present in its full thickness. The high Trenton area of 
Middleton and Cross Plains constitutes the divide between the heads 
of Sugar river and Black Earth creek. On the south side of the val- 
ley of the latter stream it breaks down quite suddenly. Further 
north, in northwestern Middleton, southwestern Springfield and south- 
ern Berry, a few very sniall Trenton areas are met with. 

No very distinctive topographical characters mark the region oceu- 
pied by the Trenton limestone. Most commonly the areas underlaid 
by it are prairie areas, and in some cases the coincidence of Trenton 
and prairie areas is striking. In all cases the soil derived from it is 
very fertile. In eastern Dane and Columbia, it oceupies areas of 
gently rolling to level country, whilst on the west side of Dane it 
forms the rounded summits of steep and narrow ridges. Hardly ever 
forming natural outcrops of any size, it contributes no especially pic- 
turesque features to the scenery. 

The lithological characters of the Trenton limestone contrast 
strongly with those of the Lower Magnesian, it being throughout very 
evenly bedded, commonly close-textured, rarely cherty, and having 
aluminous (clayey) rather than silicious (sandy) impurities. More- 
over, though largely dolomitie, it includes a considerable thickness of 
non-magnesian limestone, standing, in this respect, alone amongst the 
Silurian limestones of the northwest. In the lead region, according 
to Hall and Whitney, only the lower 18 to 20 feet of the Trenton are 
dolomitic, constituting the “ Buff” limestone of their and other re- 
ports, whilst above, all of the remaining 50 to 80 feet of the forma- 
tion are true limestone, into which a small and gradually increasing 
amount of magnesia enters as the upper layers pass into the overly- 
ing Galena. The lower of these divisions, the Buff limestone, with a 
thickness of 25 feet, is well marked throughout Columbia and Dane 
counties, as is also the lower portion of the Blue limestone immedi- 
ately above. The higher portions of the formation, which have for 
the most part been removed by denudation, and are hence but rarely 
seen, do not seein to bear out Hall’s and Whitney’s descriptions, since 
they certainly include some dolomitic layers, in appearance quite like 
the Buff beds. The exposures of these higher beds are, however, so 
infrequent, that I would advance this statement with some doubt, but 
for the fact that in the Eastern Wisconsin district, where all parts of 
the formation are well developed, Professor Chamberlin has made out 


560 GEOLOGY OF CENTRAL WISCONSIN. 


definitely an alternating series, all the beds of which are magnesian. 
This succession, beginning below, is as follows: Lower Buff (the 
“ Buff” of the Lead Region), dolomitic, 23 feet; Zower Blue, also 
magnesian, 23 feet; Upper Buff, dolomitic, 55 feet; Upper Blue, 
also magnesian, 15 feet. Only the two lower ones of these are ordi- 
narily seen in the Dane county quarries. 

The Buff (or Lower Buff) limestone is a very evenly bedded, bluish 
to buff-colored, close-textured dolomite, in layers from a few inches 
to 2 or 3 feet in thickness. Externally the layers are usually a 
brighter yellow than within, owing to a partial peroxidation of the 
iron-protoxide contained in the rock. The following analysis is one 
from the Buff layers only a short distance below the junction with the 
Blue, from Barth’s quarry, in the southern part of the town of Bris- 
tol, Dane county: 


Carboriate-Of limes s: eaccainan oiheusseun cea eenae beet Spee Gnes Ga eR WERS 56207 
Carbonate’ of mbion es1a os siisiccuipasien a wnealeen ween seal dele eee ale a os 35.32 
MLC Aisrss 2 cna eavomiale avn aremnales 8 we NHS OM arace eionierde uaaunentieaw ass 4.45 
JA ania Bh caiestoverd si cietisaitie iptetin dibcevorntielanvar dle genase uae uliie peels ks eee’ 2.08 
THON, SESQUORIGE. gisociiiscavanine dead CulanomadWcanPiniit- susie oegee teks eva ce es 69 
Lron <provoxide: :s.s04 sec neysawus vets ae nd baeseones owes oeeeeesunccns 58 
Wailers siinwnineietnaiar salunnme soe: ee ieee eainar nave Ge: deenves ag, Bobs Roaierererane -46 

99.65 


In the upper part of the Buff limestone, purplish-brown, close- 
textured, conchoidal-fracturing layers occur, which contrast much 
with the remainder of the stratum. The Buff limestone yields a good 
building stone and is very frequently quarried. 

The Blue (Lower Blue) is to be seen ordinarily only in its lower 
half, 2 to 10 feet of which are not unfrequently laid bare in quarries 
on the Buff beds. These lower layers are very thin, nodular-surfaced, 
and made up of dark bluish-gray, flinty-textured limestone, in which 
small specks and strings of calcite are thickly scattered, and in which 
also numerous fossil fragments are imbedded. Included between 
these layers are seams of a very thinly and regularly laminated, dark 
brown, fragile, caleareous shale, showing numerous black graptolite- 
like markings. Of the following analyses of the Blue limestone, No. 
Tis of rock taken from the same locality as the Buff, of which an 
analysis has just been given, and nearly at the junction of the two. 
Of the other analyses, added for comparison, No. II is cited from the 
report of Mr. Moses Strong on the lead region, and is from See, 36, 
T. 5, R. 2 E., whilst No. III is of Blue limestone from near Benton, 
on the Fever river, and is cited from J. D. Whitney’s report on the 
lead region: 


THE LOWER SILURIAN ROCKS. 561. 


I. Il. TI. 

Carbonate of lime..... 2.0... cece cece cece eeeees 84.02 85.54 97.92 
Carbonate of magnesia.. .........cecceeceue ee 5.83 3.98 1.60 
SULLG eas oie'y stays us daiact se cutsolasambiieeianieendes emis wnwkeeaie es 7.03 6.16 

AlGININ GS << <0. dsicuarecaatoniiadeeeeas veaecnuies sexe -Q.21 2.26 

Tron sesquioxide....... 2.0.00. c cee cc ees eeeeeee 83 95 aay 
Tron protoxide............ccccececececeececeseee 39 95 
OWaten “<vaase nic tanesusedwundsdaacoeeee dice maine Get 93 0 oo... 


F 100.42 99.87 100.62 


The following list of fossils includes all that I have observed in 
the Trenton beds. The determinations are mostly by Mr. R. P. Whit- 
field: 


Name. Horizon at which found. 
Petraia (Streptelasma) corniculum, Occurs throughout the 
Buff but most com- 
mon in the lower part. 

Columnaria alveolata, - - - - - Lower part of Buff. 
Graptolitic markings, - - - - Lower part of Blue. 
Crinoidal columns, Upper part of Buff. 
Orthis tricenaria, - - Buff. 
Streptorhynchus filitextus - - - Buff. 

S. deflectus - = = — Buff. 

Strophomena camerata, - - Buff. 

S. incrassata, - Buff. 

Rhynchonella, n. sp., - Buff. 

R. n.sp., - Blue, 

Tellinomya cuneata, - - - Buff. 

Cypricardites ventricosus Buff. 

Raphistoma lenticulare - Buff. 

Rk. Nasoni, Buff. 

Trochonema umbilicatum - Butt. 

Murchisonia bicincta, Buff. 

M. tricarinata, - - - Buff. 

Pleurotomaria subconica, - Buff, 

Helicotoma planulata, - - Buff. 

Orthoceras annulum, - Buff. 

0. vertebrale, - - Buff. 

Gyroceras duplicostatum\n. sp., — - - Buff. 

Oncoceras pandion, - Buff. 

Cyrtoceras, und. sp., - - - - Buff. 


Beside these, obscure and fragmentory casts of Orthoceratites are 
very numerous indeed in the Buff, varying greatly in size, some 
occurring as great as 6 feet in length and 8 inches in diameter. The 
fossils of the Buff are almost wholly in the state of casts of the in- 
terior, or impressions of the exterior. Of those in the list, the most 
frequently met with are the coral Petraza, and the gasteropods, 
amongst which Trochonema wmbilicata is the most abundant. These 

Wis. Sur. --36 


502 GEOLOGY OF CENTRAL WISCONSIN. 


gasteropods are frequently of very large size, their rough casts and 
impressions filling entirely a two-inch layer, whilst for a number of 
feet above and below the rock may be entirely barren. 

The economic contents of the Trenton beds are building stone and 
limestone for flux. Certain beds of the Blue in the lead region are 
said to be hydraulic, and the property is probably not entirely con- 
fined to the rock in that district. The Trenton limestone is also one 
of the layers in which the lead ore of the lead region occurs. A 
small crevice oceurs near the base of the Trenton, in the town of 
Fitchburg, Dane county, from which a few hundred pounds of galena 
have been taken. For the most part, however, the Trenton is with- 
out sign of mineral wealth until the limits of the lead region are 
reached, in the western towns of Dane county. East of this it occurs 
usually in such small thickness that it could not be looked to to yield 
any amount of ore, even if it should be metalliferous, of which, how 
ever, there is no indication. ‘ 

The Buff limestone is used for building everywhere where it occurs. 
It can. be obtained in quite even blocks and slabs of suitable thickness 
both for building and paving, presenting, when laid in wall, a uni- 
form straw color. The thinner layers are also frequently used for 
stone fences. 

The application of the blue or non-magnesian limestone layers as a 
flux in iron smelting is certainly worthy of attention. For most of 
the furnaces in Wisconsin and the northern peninsula of Michigan, 
limestone is brought all the way from Kelley’s Island, in Lake Erie, 
whilst others use unsatisfactory native dolomites. The Kelley’s 
Island rock contains much more magnesia (15-20 per cent.) than the 
Blue limestone, but is otherwise often purer, carrying almost no 
earthy or silicious impurities. It is without doubt this purity that 
makes it prized for smelting the hard silicious ores of Lake Superior. 
All of the silica, however, in the Blue limestone is in the state of clay, 
whilst in freedom from magnesia it ranks far above the Kelley’s Island 
stone, and moreover, as shown by the third of the analyses above giv- 
en, it is at times free also from the earthy impurities. 


THE GALENA LIMESTONE. 


This formation is found in the Central Wisconsin district only in a 
few small cappings in the town of Christiana, eastern Dane county, 
and on the top of some of the narrow ridges of the towns of Spring- 
dale and Primrose, on the west side of Dane county. Since it is so 
unimportant, and at the same time plays so large a part in both the 


THE LOWER SILURIAN ROCKS. 563 


Lead Region and Eastern Wisconsin districts, in the reports on which 
it will be found fully described, it is not thought necessary to give it 
any attention here. 


If. Local Details. ! 


Porraer, Woop, Crarg, anp Jackson Counrizs. 
(ATLAS PLATE XV, Arza F.) 


The only one of the Lower Silurian formations occurring in these counties is the 
Potsdam sandstone, which forms the basement rock of the southern portions of the 
three first named, the Archean rocks rismg to the surface in their uorthern portions. 
In Jackson county only the bed of Black river and a few scatterimg mounds show the 
Archean rocks. 

The peculiar irregularities of the line of junction between the two formations, the ex- 
tension southward along the stream valleys of long strips of the crystalline rocks, the 
corresponding northward extension, along the divides, of the sandstone, and the difficul- 
ties met with in tracing the bonndary, have been before alluded to. The facts upon 
which the junction line for the region covered by the map of Area F. of the Atlas is 
based, including the location of a number of outcrops, have also been given briefly, and 
will not be repeated here. 

A very large proportion of the sandstone area in these countiés is level, and is, to a 
considerable extent, occupied by large marshes. Towns 21 and 22, ranges 7 and 8 east, 
Portage county, are almost all included in one great marsh, as are also towns 21, ranges - 
2, 3 and 4 east, in Wood county, the latter marsh extending also over considerable por- 
tions of the towns to the northward, and having a still greater extent into Juneau and 
Jackson counties on the south. Underneath these marshes, which, to a large extent, 
have peat bottoms, sandstone is commonly found at shallow depths. On some of the 
dividing ridges again, the sandstone country becomes considerably elevated, and has 
more or less a rolling character.* Such is especially the case with the divide between 
the Black and Trempealeau rivers in western Jackson county, which is without duft 
covering, and is worn into the deeply ravined surface characteristic of driftless regions, 
The divide between Black and Yellow rivers, in western Wood and eastern Clark coun- 
ties, is considerably elevated above the surrounding country, but is very heavily coated 
with glacial materials, and preseats therefore a much more even surface. 

The larger part of the sandstone area of Portage, Wood, Clark, and eastern Jackson 
counties, is within the region of heavy timber, chiefly pine. In the southern portions of 
the three first named, and in a large part of western Jackson, small pines mingle with 
the small oaks that are characteristic of nearly all of Central Wisconsin, the growth of 
timber in all of these portions being scant and small, and associated with a loose, sandy 
soil, On the northern part of the divide between Yellow and Black rivers, however, 
the sandstone is deeply buried beneath clay drift, as a result of which we find excéllent 
clay soils, and a heavy growth of hard wood timber, for the most part maple. 

Usually the sandstone of these counties is but a thin covering upon the crystalline 
rocks, which appear in all of the deeper stream-valleys. High bluffs of the sandstone, 


1Jn the manuscript, this division of the report includes a fall description, hy townships, of a 
large part of the country occupied by the Lower Silurian formations, embracing topography, sur- 
face features, rock outcrops, etc. It has been found necessary, in order not to exceed the limite 
originally assigned to this report, to throw out most of this material, and a number of important 
outcrops are therefore not alluded to. This omission can be, in part, made up for, by any one woo 
wishes further information than given, by a stndy of the Atlas maps in connection with the lists of 
altitudes of Chapter I. The whole amount of matorial thrown out would make abont 45 pages of 


the small type. R. D. I. 


564 GEOLOGY OF CENTRAL WISCONSIN. 


however, occur, carrying its thickness up into the hundreds of fect, and bearing witness 
to the great thickness which once must haye existed over all the region. 

In Sec. 23, T. 21, R.8 E., Portage county, on the edge of the great Plover marsh, 
rises a prominent knob of sandstone, known as Mosquito Mountain. The bluff is about 
100 feet high, with its main extent east and west. Just west of it, on the west side of 
the Portage and Stevens Point road, is a second lower knob. Near the base of the main 
hill, the sandstone, as seen in a quarry (789), is rather fine-grained and light-colored, with 
brownish spots and laminz, and very friable indeed. It is composed of grains of limpid 
quartz, that are all somewhat rolled, but are still subangular in shape, and has a very 
minute quantity of a brownish cement. The bedding here is very distinct, the layers 
running from 2 inches to 1 foot in thickness on a quarry face of 15 feet. One hundred 
yards to the east of the quarry, on the same hill, are ledges of a much coarser and more in- 
durated sandstone (790), which is in places almost like quartzite, having a whitish color, 
and composed of much-rolled grains of vitreous quartz, closely cemented. A similar rock 
(791) occurs in small exposures up to the summit of the bluff. On the western bluff a 
quarry exposes coarse-grained, brownish, moderately firm sandstone (792), having a 
semi-vitrified appearance on the exterior. 

At the foot of Conant’s Rapids, 8. E. corner Sec. 8, T. 23, RB. 8 E., 30 feet of hor- 
izontally bedded sandstone show in the river bank, overlying gneiss. The lowest layers, 
in contact with the gneiss, are hard and quartzite-like; but the body of the exposure is 
thinly bedded, coarse-grained, friable, and of a light-brownish color. 

At Steven’s Point, just below the railroad bridge, on the east bank of the river 
(Plate IX, of Fig. 12), thin-bedded triable sandstone shows at the top of the bank, the 
gneiss being exposed below. 

On the west side of the river, Sec. 31, T. 24, R. 8 E., is a low outlier of sandstone, 
rising 51 feet above the nver. The sandstone is cut into deeply at the south end of the 
mound, for the railroad, and this citting is expanded into a quarry at one point. 

_ Another large quarry is worked on the northwest side of the hill. In the cutting, the 
upper layers are thin-bedded, whilst the lower seven feet is in heavy layers, and shows 
a light brownish, white, much indurated, rock (774), of a medium grain, and composed 
of highly glassy, subangular, quartz grains. Fresh surfaces are quite uniform in ap- 
pearance; weathered surfaces much iron-stained. Strong joints occur trending N. 15° 
W.and N 50° E. Pieces 4 by 4 by 4 4¢ feet can be obtained easily, also thin slabs fit 
for flagging, The quarry on the west side of the hill shows a similar stone, taken from 
higher layers. The topmost layer in the quarry is very beautifully ripple-marked. The 
stone from these quarries is a valuable one, and is much used in building at Stevens Point. 

About four miles north of Grand Rapids, in the town of Rudolph, S. E. qr. Sec. 20, T. 
23, R. 6 E., Wood county, « large and excellent sandstone quarry has been opened neat 
the summit of the ridge, whose slope for half a mile southward shows sandstone ledges. 
The quarry face is 20’ feet, and shows very plainly bedded layers 1 inch to 2 feet in 
thickness. These are traversed by very strong joints, trending N. 10° W. and N. 70° 
to 80° E. Some of the joints are inclined, especially the former set, most of which dip 67° 
W., and others are vertical. All the stone is tolerably firm, but most of it is not unusually 
indurated, crumbling easily in the fingers. Certain layers, however, are very highly in- 
durated, and are susceptible of quite a high polish. These are both plain white and 
white heavily streaked with dark red, are of a rather fine grain, and consist of sub- 
angular grains of highly vitreous quartz. Large blocks can be obtained, as also thin 
flags 10 by 18 feet. The stone is much used at Grand Rapids, and has a considerable 
value. 

Along the Wisconsin river, from Grand Rapids to Point Bass, sandstone is fre- 
quently exposed. Several sections in the vicinity of Grand Rapids, showing sandstone 
overlying kaolin, have already been described. 


THE LOWER SILURIAN ROCKS. 565 


' Near Point Bass, on both sides of the river, heavy ledges of sandstone overlic gneiss 
(see Figs. 2,3 and 4). On the east side of the river the sandstone cliff is 30 to 40 feet 
high. Qn the west side, near the north line of Sec. 15, on a side channel of the river, 
dry at the time of our examination, 5 feet of very friable, coarse, brownish sandstone 
shows in the bank, the upper layer heavy, the lower ones thinner. The bottom of the 
channel is formed of large flat slabs of the same sandstone, one inch thick. Beneath four 
one inch layers of this sandstone are two inches of sandstone highly charged with the 
greenish-tinged iron sulphide, marcasite, which m places almost entirely excludes the 
sand, Specimens taken ot decompose to the sulphate very rapidly. Immediately be- 
low, and in contact with; the pyr tous layer, is the Archean gneiss, much decomposed, 
but retaining still its firmness and bedding. 

Three-quarters of a mile east of Mapleworks, on the 8. E. qr. of Sec. 12, T. 24, R. 
1E., Clark county, is an isolated sandstone bluff 100 feet high, 500 yards in diameter at 
the base, 100 yards long and 10 wide at top, rising above the general level of the divide. 
The slopes are covered with clay and fragments of sandstone. At the summit 5 feet of 
very coarse grained, rather firm, brownish sandstone (982) is exposed, consisting of very 
much rolled grains of dull white quartz. The layers are 6 to 18 inches in thickness. 

About one mile north of Neillsville, on the S. W. qr of Sec. 11, T. 24, R. 2 W., 10 
feet of cross-laminated, coarse-grained, yellowish sandstone, shows alongside of the 
road. Clay seams, one to two inches thick, are included between the layers of sand- 
stone. Similar sandstone is seen at the crossing of Black River, one mile west of Neills- 
ville, 8S. W. qr of Sec. 15, T. 24, R. 2 W. The base of the sandstone is 40 feet above 
the river; below is a slope 10 feet in height, without exposure, and below this, again, 
30 feet of light-colored pinkish granite. 

Along Black River, from Neillsville to Black River Falls, T. 21, R. 4 W., Jackson 
county, sandstone is quite frequently exposed in or near the banks of the river, the bed 
of which is on the crystalline rocks. 

-On the S. W. qr of Sec. 3, T. 24. R. 2 W., west of the river, is a sandstone outlier 175 
feet high, and about one-third of a mile in length, the upper portions of which are per- 
pendicular ledges of hare rock. The sandstone is heavily bedded, indurated, coarse- 
grained, and light-colored. From the summit of the bluff a number of other similar 
outliers can be seen, dotting the country to the west and south, and one or two to the 
north, in T. 26, R. 2 W. 

For half a mile below French's mill, Sec. 25, T, 23, R. 3 W., the Neillsville road fol- 
lows the west bank of the river, at an elevation of about 30 feet above the water. On 
the east side of the road, granite is exposed in the river bank, and on the west side a 
ridge of horizontal sandstone, 30 to 50 feet high. The sandstone is cross-laminated, 
coarse, yellowish, and made up of much rolled quartz grains, which reach sometimes as 
much as one-eighth of an inch in diameter. 

In T. 21, R. 4 W., and T. 22, R. 4 W., ledges of sandstone form the river bank for 
long distances, rising 20 to 40 feet from the water, and are in a number of places to be 
seen overlying, or abutting against, Archean schists, as heretofore described (see Plate 
XVII, and Figs. 1, 20 and 21). This sandstone is usually of light yellowish color, 
coarse, and somewhat indurated, and includes beds of red and green sandy shale. The 
lowest layers are often affected by a very marked cross-lamination, the thickness so af- 
fected being often as much as six to ten feet. 

At Black River Falls, sections 15 and 22, T. 21. R. 4 W., the crystalline rocks are 
largely exposed, the river passing through a gorge in the gneiss and granite. The 
ground rises rapidly from the river on both sides. especially the western, and on hoth 
sides the granite and gneiss are overlaid by sandstone. At the top of the hill on which 
the High School building stands, wells pass through 80 feet of sand and gravel into sand- 


stone. 


566 GEOLOGY OF CENTRAL WISCONSIN. 


. Opposite Ledyard'’s old mill (Fig. 20), in the bend of the river below the village, 25 

feet of sandstone overlie the gneiss. The sandstone here is the usual coarse crumbly 
rock, and includes layers of greenish and reddish shale, the lowest layer being a fino 
conglomerate, 8 inches in thickness. 

Near the railway depot, on the west side of the river, is a quarry in the sandstone 
layers belonging just above those exposed at the mill. The quarry face is 15 feet high, 
and traversed by strong vertical joints. The stone (1012) is heavily bedded, much in- 
durated, of a light color, and composed of alternating very coarse and finer grained 
layers, all being composed of rolled grains of glassy quartz. Some of the layers show 
cross-lamination. This stone isa valuable one, and resembles that from the quarries 
already alluded to as occurring near Grand Rapids and Stevens Point. 

About a mile southeast of the depot, on Sec. 23, is a very bold sandstone outlier rising 
about 250 feet above its base. In the lower slopes the sandstone is mostly concealed. 
Above is a perpendicular-faced, jagged crest, over 100 feet in height, the prevailing 
rock (1013) on which is a white to buff-colored, fine-grained, firm sandstone, composed 
of sub-angular to rounded quartz-grains, and containing near the top numerous 1ron- 
stained impressions of Oboledla polita, but no shells. 

About one mile west of Black River Falls, on the road westward to the Trempealeau 
valley, is an exposure of thin-lyedded, coarse, brownish, crumbling sandstone (1010), 
with numerous white fragments of shells of Ololella polita, which, in some of the layers, 
make up most of the rock. Thin clayey layers occur in which a few shells were noticed, 
one of Lingulepis pinneformis. The outcrop appears to be 130 to 150 feet below the 
Gbolella sandstone of the bluff near the depot. : 

In the various exposures in the vicinity of Black River Falls, we have a total thickness 
cf sandstone of about 350 feet, with two fossil horizons made out, one 200, the other 300 
feet, above the gneiss base upon which the pile rests, and both showing Obolella polita. 

On the west side of the Trempealean valley, Sec. 2, T. 22, R. 5 W., Jackson county, 
is a peculiar isolated bluff known as the Silver Bluif. At the east end the bluff is 
165 feet high, the lower slopes being covered with a talus from the ledges above. Near 
the summit is exposed a horizontally and very plainly bedded, hard, white quartzite (1011), 
which rings like steel when struck with the hammer. The layers are alternately thin 
and thick, and brownish-weathered, and include interstratified layers of friable sand- 
stone. The quartzite shows distinctly lines of lamination, and has a very plain granular 
texture, being composed of grains of vitreous quartz which appear as if fused together, 
and is quite highly translucent. It is unlike the quartzite of the Baraboo ranges, or 
that of the hills near Wausau, Marathon county. It contains very abundant fragments 
of casts, more rarcly perfect casts, of a very large conical fossil which Mr. Whitfield de- 
termines as a new species of Paleacmea. Following the bluff along the brow of its 
southwest face, the quartzite layers are seen to continue for about a third of a mile, 
when a sudden rise in the bluff of 80 feet exposes thin-bedded, firm, dark reddish- 
brown, highly ferruginous, sandstone (1016), of a medium prain, and composed of 
rounded grains of glassy quartz, which are stained both externally and internally by 
iron-oxide. On the north flank of the hill, at the same elevation as the quartzite on the 
opposite side, an § inch layer of hard, white quartzite is seen, between heavy beds of 
whitish friable sandstone. 


Junrav AnD Apams Countius. 
(AtLas PLates XIV anp XVIII, Annas E. anp H.) 
These two counties constitute a rectangular-shaped district, lying in the very heart of 


the state, about 42 milcs from north to south, by 36 from east to west, and having an 
area of about 1,475 square miles. Throughout the whole area, except on the small 


THE LOWER SILURIAN ROCKS. 567 


quartzite bluffs at Necedah, and in one or two very small and somewhat doubtful cap- 
pings of limestone in the southwestern towns of Juneau county, the Lower sandstone is 
the surface rocx. 

The larger portion of the district presents vhe character of a level plain, which has, 
for the most part, a surface of loose sand derived directly from the disintegration of the 
Lower sandstone, but showing many marshes, some of very large size, and occasionally 
prairies. Except on the marshes, and the few small prairies, this plain is nearly every- 
where covered with a growth of stunted oaks, with which, towards the north, small 
‘“‘jack-pines ’’ intermingle. It is traversed centrally from north to south by the Wiscon- 
sin river. and is surrounded on all sides by higher ground. ‘The elevation on the north 
is due mercly to the gradual rise of the plain in that direction, the general altitude on 
the southern edge, along the Lemonweir river, being about 300 feet, that along the north 
line of Juneau county, 400 feet. The high ground on the east is also due to a steady, 
but very much more rapid, rise of the plain in that direction, the dividing ridge along 
the line of Adams and Waushara counties having an altitude of some 200 feet above 
the Wisconsin. On the south, southwest and west, however, the edge of the plain is 
very sharply defined by a narrow and much indented dividing ridge, which is especially 
marked in the southwestern towns 6f Juneau county, where it has on its western side 
the deeply carved valley of the Baraboo, with its numerous branch ravines. 

Dotting the central plain, and rising quite abruptly from its most level portions, are 
the isolated mounds and castellated peaks of rock that constitute its most marked and 
peculiar characteristic. Except the quartzite mound at Necedah, these are altogether 
of sandstone, being the only portions that have been left from the-denudation of the 
Lower sandstone. Although none of them exceed 300 feet in height, and but few 200 
feet, they register a denudation of fully 500 feet; that is to say, over the larger part of 
this plain there has been at one time a thickness of 500 feet of rock, which no longer 
exists, and possibly there has been a much greater thickness than this. There are two 


Fig. 35. 


Priendshijze™ Mound Poche a Oris ¢ 
, | a ee 


OUTLINEs OF RocHE a CRIS AND FRIENDSHIP MOUND, AS SEEN FROM Pitot KNnozs. 
Seale 2,480 feet to the inch. 


classes of these remarkable outliers: the larger and more prominent ones, which reach 
elevations of from 150 to 300 feet, have lengths of from 7; to 1 mile, and show more or 
less vegetation on top; and the smaller and less conspicuous ones, which are frem 30 to 
100 feet in height, often of bare rock, and cover comparatively small areas. The larger 
outliers are few in number, and are, for the most part, quite distant from one another. 
Two of these are especially prominent, showing from any point on or around the plain 
high enough to be above the tree tops. These are the Roche 4 Cris and the Friend- 
ship Mound in the southwest part of T. 18, R. 6 E., Adams county. Their prominence 
is due both to their heights above the plain at their bases and to the comparatively 
great clevation of the portion of the plain on which they stand. The Roche a Cris is a 
thin, wedge-shaped mass of rock, without pinnacles, having a length of about 4 mile, 
and a height of 225 feet above its base, or about 660 feet above Lake Michigan, and 
standing up like a fragment of a great wall. Friendship Mound is about half a mile 
south from Roche 4 Cris, which it exceeds in height by 50 feet, having also a much 
greater length and thickness and a more rounded contour. The ontline of these two 
bluffs, as sketched from the summit of Pilot Knob, 10 miles east, is given in Fig. 35. 
Amongst the other large outliers may be mentioned the very larye wooded mound, in T. 


568 GEOLOGY OF CENTRAL WISCONSIN. 


20, R. 6 E.,13 miles north of Roche 4 Cris; Petenwell Peak, a very narrow bluff 230 
feet high, and with serrated crest, on the west shore of the Wisconsin, Sec. 9, T. 18, R. 
4E.; the group of bluffs 6 to 8 miles south of Friendship; the large wooded bluff 6 
miles southeast of Mauston, T. 15, R. 4 E.; and the Elephant’s Back, near Kilbourn 
City. The last two, though high, do.not stand out very prominently, as seen from 
points within the plain, on account of their nearness to the high ground that limits it on 
the south. The quartzite bluff at Necedah is also quite prominent. Of the smaller 
sandstone outliers there are a great number and varicty. Many of them are simple 
peaks or towers of rock, having a diameter at base of only a few feet, and 40 to 60 feet 
in height, in some cases the diameter at base being less than that at the summut. Oth- 
ers are a series of pinnacles or rounded towers joined together, and others again are 
massive bluffs with wooded summits and perpendicular sides of rock. 

The high ground that bounds the pla on the west enters Juneau county on the west 
side of T. 16, R. 2 E. (Fountain), carrying on the county line a capping of the Lower 
Magnesian limestone. From here it trends southeastward across the towns of Foun- 
tain, Plymouth, Lindina, Wonewoc and Summit, reaching elevations of 500 to 660 feet, 
and then, vecring snore to the eastward, across the towns of Seven Mile Creek and Lyn- 
don to the Wisconsin river, where it is cut through by that stream in the gorge known 
as the Dalles of the Wisconsin. This ridge is very well marked on its northern side, 
rising abruptly from the plain, towards which it presents a face deeply indented by the 
streams flowing northward from it, and flanked by isolated outliers of sandstone. Until 
it nears the Wisconsin, it constitutes the divide between the waters of the Baralhoo 
and Lemonweir rivers. The former of these streams enters Juneau county on the west 
line of the town of Plymouth, through which, as also through the next town on the 
south, it passes in a nearly southerly direction to the south line of the county, having all 
along a narrow rock-walled valley, into which tributary streams come through deep 
ravines, that set back into the higher ground on each side. Thus throughout all of these 
southwestern towns of Juneau, the country bears quite a different aspect from that of 
other portions of the county, being, in general, an elevated region, carved into numer- 
ous ravines, and presenting, on the higher portions, a very excellent clay soil, although 
entirely without the drift area. As the Dalles are approached, the ridge lessens in 
elevation, and shows on its northern side many sandstone escarpiments, which are often 
worn into fantastic shapes. East of the Wisconsin, the encircling high ground 
continues, curving rapidly to the northeast and north, through the towns of Dell Prairie 
Springville, Jackson and New Chester, running thence northward along the east line 
of Adams county, and reaching elevations of 200 to 300 fect above the Wisconsin river. 
Its character, however, is now quite changed, the slopes being no longer abrupt nor 
worn into ravines, whilst the whole surface is heavily drift-covered. 

The plain, thus encircled by high ground, would, over the greater part of its area, be- 
come covered by water, if the gorge at the Dalles were closed. That such may actually 
have been the case at some time, is indicated by the general appearance of the plain and 
its surroundings, by its namerous large marshes, by the finely laminated (lacustrine ?) 
clay deposits that occur in places over it, and by the great bank of rolled pebbles and 
bowlders of quartzite that flanks the quartzite bluff at Necedah, far within the driftless 
region. 

In the valley of the Upper Baraboo, and on the adjoining high ground, in the 
towns of Fountain, New Lishon, Plymouth, Lindina, Wonewoc and Summit, Juneau 
county, the sandstone is frequently exposed. The immediate valley of the river is nar- 
row, and frequently bounded by rock wails, 20 to 120 feet in height, which show gen- 
erally rather friable, medium-grained, brownish to white, sandstone, without trace of 
calcareous or dolomitic ingredients. In places, as on the east side of the river at Elroy, 
near the railroad bridge, firm quarry layers occur. The high ground on either side of 


THE LOWER SILURIAN ROCKS. 569 


the valley rises rapidly from it, 200 to 300 feet, but shows sandstone only, except in one or 
two places where exceptional elevations are reached. One such piace is on the county line 
in the southwest corner of the town of Wonewoe, just south of which, on the S. E. qr. of 
the N. E. qr. of Sec. 6, T. 18, R. 2 E., Sauk county, the Lower’ Magnesian limestone is 
quarried, at an elevation of 300 feet above the railroad track at the village of Wone- 
woe, or at a total altitude of 630 feet. Only a small thicknoss (3 to 4 feet) of limestone 
is exposed, and immediately below are seen ledges of coarse, brownish, non-¢alcareous! 
sandstone, intermingled with which, and in the uppermost layers predominating, is a 
whitish, chert-like material, having somewhat the appearance of a grayish, granular 
quartzite (1350). Limestone appears also to cap the high ground in Sec. 1 of Wonewoc, 
and in portions of the corner sections of the three adjoining towns. The limestone was 
not seen here in place, but on the north side of the ridge large, fallen masses were noticed, 
showing the ordinary characters of the Lower Magnesian; and the sandstone exposures 
do not extend to the summit. On the west side of the ridge, where the Mauston and 
Wonewoc road descends into the valley of a small stream on the north side of Sec. 12, 
50 feet of red and pink, friable, finely laminated, non-calcareous sandstone, with firm, 
white bands (1340) are exposed. The white bands are exceedingly fine-grained, and 
made up of sharply angular grains of glassy quartz, being in this respect quite different 
from most of the sandstone of the Potsdam series. Scolithus occurs quite abundantly 
in this rock. On tho south side of the stream, sandstone is again exposed of similar 
character, and rising higher, the uppermost layers containing the peculiar quartzitic or 
cherty material (1353) mentioned above as occurring just beneath the limestone on Sec. 
6, T. 13, R. 2 E. The highest point of this sandstone is about 15 to 20 feet below the 
summit of the ridge in Sec. 1. 

From the lowest exposures along the Baraboo river to the limestone on the tops of tho 
ridges, the whole thickness of sandstone is not less than 300 feet. The peculiar red- 
and-white-banded and cherty sandstone occurring just beneath the limestone appears 
to be without doubt.in the Madison horizon, but with an unusual thickness. The Men- 
dota limestone was not noticed anywhere in the region, though benches occur on tho 
hills, at the proper elevation, which might be due to its presence. The dolomitic bands 
that characterize the Upper Potsdam further southward, were also not seen. 

Along the northern face of the watershed between the Baraboo and Lemonweir rivers, 
from Camp Douglas to the Dalles, numerous isolated bluffs and towers of sandstone oc- 
cur. AtCamp Douglas Junction, Sec. 28, T. 17, R. 2 E., is a group of these bluffs, 
and a number more oceur within a radius of two or three miles. Target Bluff, a few 
rods west of the depot, is a flat-topped mass of sandstone about 4 of a mile long, and 
120 feet high, with nearly vertical sides. The lowest layers are thick, cross-laminated, 
coarse, non-calcareous, brownish, and exceedingly friable, having almost no coherence. 
The same characters, except the cross lamination, are persistent nearly to the top, where 
thin, lighter-colored, medium-grained layers (185314) are seen, made up of much rolled 
grains of dull, translucent quartz. It is noteworthy that many of the bluffs in this vicin- 
ity have the same elevation, a fact evidently to be attributed to the existence at that ele- 

, vation of some peculiar layer in the sandstone series. 

Immediately south of the village of Mauston, on Sec. 13, T. 15, R. 3 E., is a large 
and very prominent sandstone bluff, about 200 feet high, half a mile long ina north 
and south direction, and surrounded on all sides by vertical cliffs flanked below with a 
long talus of loose sand and sandstone fragments. The cliffs are boldest on the eastern 
face, where they run from 50 to 100 feet in height. One hundred and eighty feet above 
the base is a flat bench, above which a narrow ridge rises some 20 to 80 feet, carrying 
the summit of the bluff to a total altitude of about 500 feet. The bench is due, un- 
doubtedly, to the presence of alayer of green ard red shale, which is not exposed, 


| 1 Whenever this adjective is uscd without qualification, the rock has been directly tested. 


Fa 


570 GEOLOGY OF CENTRAL-WISCONSIN. 

but has been reached by a small shaft sunk on tie summit of the bluff. The shaft pen- 
etrates: (1) sandrock, lower layers thin, white and shaly, 25 feet; (2) green and red shale 
214 feet; and ends in (3) sandrock again, the same as that seen on the cliffs. The green 
shale appears to be of the same kind as that known at several horizons in the Lower 
Sandstone in other parts of the state, but is soft and clayey, unusually free from sili- 
cious sand, and of a deep green color.!' The red shale (1342) 1s soft, slightly sandy, non- 
calcareous and of a brick-red golor. This shaly layer has influenced the denudation of 
other bluifs seen to the southeast, which have their summits at the same elevation as 
this bench. 1t appears probable that the Camp Douglas bluffs may owe their con- 
stancy of elevation to the same cause. All the sandstone on the cliffs of the Mauston 
bluff is non-calcareous, generally moderately coarse, brownish, pinkish and light-colored 
in different layers, and much of it firm enough to usc in ouilding. It is quarried near 
the south end ot the bluff, at the base of the cliff, where firm, heavy layers are ob- 
tained of a light-colored, medium-grained rock (1347); and also at the summit of the 
cliff, near the north end of the bluff. At the latter place, immediately above the quarry 
beds, and just beneath the green shale, are a few layers of a porous, very friable brown- 
ish sandstone, with numerous iron-stained points and cavities and indistinct fossil im- 
pressions, which consists of subangular grains of glassy quartz. On the cliff below the 
quarry the sandstone is penetrated by numerous brownish veins, one-sixteenth to one- 
half an inch in width, which, on close examination, are seen to be made up of the 
grains of the sandrock, more glassy than usual, and closely cemented by a small amount 
of hydrous iron, oxide. 

In the southern part of the town of Lyndon, on Sec. 28, T. 14, R. 5 E., a narrow, 
ridgy crest rises 200 feet above the general level of the watershed, reaching an altitude 
of nearly 700 feet above Lake Michigan. At the summit a white, cherty material (1330) 
resembling that described as occurring on Sec. 12, town of Wonewoc, remains in place. 
[t.is peculiar in showing numerous little rounded holes, that give to the mass some ap- 
pearance of an organic structure. Ten feet below the chert, fine-grained, non-calcareous, 
whitish sandstone (1332) is exposed, made up of grains of very fine, sharply angular, 
glassy, quartz, and resembling that seen below the chert on Secs. 12 and 1, town of 
Wonewoc. The horizon is evidently the same, and is just beneath the base of the Lower 
Magnesian limestone. 

The gorge known as the Dalles of the Wisconsin has been briefly described on a 
previous page. Along the walls of the gorge, which are from 50 to 100 feet in height, 
the rock is quite uniform in character, being coarse, very friable, light to dark brown in 
color. non calcareous, and consisting of very much volled grains of quartz (1443). The 
most remarkable feature of these exposures, which are nearly continuous for as much as 
seven miles, is the cross lamination which affects layers as much as 12 feet thick, and is 
abruptly terminated above and below by horizontally bedded layers. The transverse 
lamine themselves are quite thin, and easily separable trom one another. They are not 
plane, but constitute much warped surfaces. The structure is quite well shown in the 
view represented on Plate 1A, which is taken from one of Mr. H. H. Bennet’s excellent 
photographs. Plate I, also from one of Mr. Bennet’s photographs, shows a peculiar 
erosion form, known as Stand Rock, which occurs well up on the north face of the high 
ground through which the Dalles are cut, and far above the gorge itself. It illustrates 
well the way in which much of the lower part of the Potsdam series is wom—thin layers, 
somewhat more ferrugincus and firm than the rest, though still quite friable, protecting 
the softer, scarcely coherent rock below. Half a mule east of the upper end of the 
Dalles, on the east side of the 8. E. qr. of Sec. 21, T. 14. R. 6 E., the « Elephant’s 


‘This green shale hag been the object of exploitation as a copper ore, a considerable amount of 
money having been expended 1n sinking shafts, etc. It is hardly necessary to say that the money’ 
is thrown away. 


THE LOWER SILURIAN ROCKS. 


571 


Back” bluff, an isolated sandstone outlier, rises from the general level. From the sum- 
mit of this bluff to the water in the river a measured section was taken, showivg in all 


a thickness of 3810 feet of the sandstone. 


beginning at the top of the bluff:— 


1. 
2. 


» OD ay DH Ot 


9. 


14. 


15. 


WER DOSEd gs avanasieuie ie Sieh eae ale gala eas Qe ayconrareseuea ted woachauc ick bac doly 

Fine-grained, porous, friable, light-brownish sandstone (1431); com- 
posed of subangular grains of glassy quartz; showing numerous 
small iron-stained cavities, and larger ones filled with loose ferrugin- 
ous sand; fossiliferous, containing Scolithus, numerous small indefi- 
nite trilobite fragments, and the pygidium of a large trilobite, ap- 
parently Dicellocephalus Minnesotensis ; resembling exactly the fossil- 
iferous rock on top of tie bluff, and just below the greensand = 
at Mauston; elevation of the Mauston rock, 470), of this rock, 530.. 


& LIMO RPORER sine styra Mola accurate ae taae alae denw Moree eka. ars 


Yellowish sandstone’ (1482), sessrabting No. 2; in upper part with a 
vitrified crust; below, very loose; carrying Scolithus bidet Sot cuenta oat 


WOR POSEO <A nasincnaeraiscsmueiny) smaudemaemiedes Wetec anes eds 
eSamne AS NOthasuieniesie Ca seis’ d ON eamoR Meads wdleee seddde ata 
s UMEXpOsed ase ec2 hang aint buocngn Gell anecarntag oases aean 
. Rather coarse-grained, dark-brownish, friable sandstone (1433); com- 


posed of much rolled grains of dulled quartz; thickly coated on exte- 
rior by hydrous iron oxide; containing Scolithus, and numerous 
iron-stained cavities; ‘erepulacly bedded... ab yanbe acme caer See etee a 
Unexposed to foot of steep ascent..... ce. eee e eee eee cece een ee oe 
Total height of steep ascent.....-.....cceee eee ee cee eeeeeeee 
Unexposed; on flat bench 150 paces wide... .....0... ccs ee eens eee 


. Heavily-bedded, coarse-grained, friable, brown, ferruginous sand- 


rock, at top: of-vertical Clues... 6c0 sansa csreaes, Syeidiesieweuie® ova ee 


. Heavily-bedded, white-and-brown-handed, coarse sandstone; almost 


without coherence; having in places an exterior hardened crust..... 


. Alternating layers of pink, brown and white sandstone; medium to 


fine-grained, saccharoidal; thin pink layers stand out in knife edges 
from the body of the rock; all affected by a vitrified crust composed 
of glassy, closely adherent, quartz grains, on removing which the 
rock within falls to loose sand; the crust is one-thirty-second to one- 
half inch in thickness, and has an ill-defined inner edge............ 
Votal height of cliff... .... cece cece cece cece wen ceaetanee 
Unexposed; a. long slope one-half mile to top of the cliff at the river 
bank (Rood’s Glen): 0ciccesscadeveesdeaee rece se pad ede slemnnmervecs 
Thin layers, one-eighth to two inches thick, of light-colored, brownish- 
tinted, medium-grained, sugary, friable sandstone (1437, 14374, 
1438); composed of much rolled grains of dulled quartz; layers pro- 
necting an Shelves.(s.s04..scsaivereab ses tone eae sree eenave ses eos 


. Heavy, coarse-grained, firm, ferruginous layer. ......-..+eeeeee eee 
. Heavy, projecting layer, with under surface ripple-marked, of medium- 


grained, light-brownish sandstone (1439); grains much rolled...... 


. Thin layers like No. 17....-ceeece cece eet ee ence seer ee ceeeneees 
. Thin-bedded, coarse, sugary, very friable sandstone (1440); in alter- 


nate pink and brownish seams; cross-laminated; the transverse lam- 
ine thin, warped, and abruptly terminated above and below........ 


. Heavy layers, resembling No. 19; not cross-laminated, grains some- 


Ft. 
20 


The following are the details of the section,’ 


In. Ft. 


572 GEOLOGY OF CENTRAL WISCONSIN. 


times very coarse, giving to the rock an appearance of being made 2%. Zn. Ft. 


Up OF Bras OF NCOs ses ci cesses sees ese aS edededewedt ne de re yeas § 6 
21. Alternating thin and heavy layers, light-colored, friable (1441), with 
some dark brown ferruginous layers (1442); all very coarse and rice- 
like; some of the thin layers very regular and persistent........... 54... 
Total height of river cliff... 00.0... c cscs cece eens ceeeeeenees &5 
Top of Elephant’s Back above river.......6eesee cece eee ees 310 


None of the sandstone of this section has any trace of calcareous or dolomitic ingredi- 
ents. 

On the Wisconsin river, above the Dalles, the sandstone is very frequently seen, both 
in low mural exposures on the river bank, and also in high isolated peaks. Of these, 
the most remarkable, as to height, is that known as Petenwell Peak, which riscs 
abruptly from the west margin of the river, on Sec. 9, T. 18, R. 4 E., Juneau county. 
The total height of the peak above the river is 230 feet, the upper 50 to 75 feet being 
a narrow vertical crest, worn into partly separated crags, not more than 20 to 30 feet 
wide on top and about 300 feet in length. The rock of this crest is a light-colored, fri- 
able sandstone, with a hard, vitrified crust. Below there is a long talus of sand, with 
exposures of thin crumbly rock at base. Thecountry around is a level sand plain, 40 fect 
above the river. 

The Roche a Cris, on the N. E. qr. of the 8. E. qr., of Sec. 30, T. 18, R. 6 E., Adams 
county, has already been mentioned as one of the most striking of the great sandstcne 
outliers of the central plain. It rises abruptly from the surrounding level stretch of 
sand, a wedge-shaped mass of bare rock, 225 feet high, 1,300 feet long at base, and 
about 1,100 at the summit, which is a nearly level area 10 to 200 feet in width. The 
greatest length of the rock les in a nearly due north and south line. The southern end 
is a sheer precipice, over 200 feet in height. On the west side there is a steep talus of 
sand creeping up in places to within 80 feet of the top. On the east there is also quite 
a long talus, but the cliffs are generally as much as 150 feet high. At the north end 
the rock is somewhat broken down, making an easy ascent. The summit is without 
the pinnacles that characterize Petenwell and others of the more western outliers, and 
is grassed and wooded with a few small pines and scrub oaks. It has the shape and 
dimensions indicated in Fig. 36, the measurements being made to the edge of the ver- 


Fig. 36. 


arth South 


Suarez or TnE SuvaurT or RocusE a Cris. 
Scale 300 feet to the inch. 


tical cliff on all sides. The view given in Plate XIV is taken from a photograph by Mr. 
H. H. Bennett of Kilbourn City, and represents quite accurately the cliff at the southern 
end of the bluff. From top to bottom of this cliff, the rock is a friable aggregation 
of rolled quartz graius, showing only slight and somewhat indefinite variations in the 
different layers. A detailed section along the face of the cliff, beginning above, is 
as follows: 


10. 


16. 


THE LOWER SILURIAN ROCKS. 


. Fine-grained, porous, very friable, light-brown-tinted; composed of sub- 


angular grains of very glassy quartz; containing numerous small cavities, 
stained by iron-oxide; weathering with a thin vitrified crust, and occa- 
sionally with a brown iron-stain; fossiliferous, containing numerous frag- 
mentary impressions of trilobites and other fossils, the markings being 
merely thin ferruginous filnis coating the nearly loose sand; most of the 
fossils too indefinite and fragmentary to be determined, two species of 
Conocephalites-like trilobites, and Triplesia ? primordialis, being the 
only ones made out: (1365) a. scevcecsee sees seeded eden ceveceavseeveas 


. Moderately coarse-grained, much finer than the last, pure white; composed 


of sub-angular to round grains of limpid quartz, the larger grains very 
much rolled; weathering in places with dark brown blotches, and every- 
where with a hard quartzitic crust; for the most part a solid layer, though 
lines of bedding are to be seen on weathered surfaces; forming a narrow 
crest at the summit of the cliff, only 3 or 4 feet wide (1366)........... 


. Medium to coarse-grained, moderately firm, brown; constituent grains 


much rolled; in thin irregular layers 1 to 2 inches in thickness; weather- 
ing with a thin vitrified crust (1867)............. ere Sarwan 


, Resembling Noi Qicnaieninnag- saan cagsmaceldiewmes tains ene eee antes ene 6 
. Medium to fine-grained, moderately firm, brown and reddish-brown; grains 


glassy, sub-angular to rolled; in the interior a massive bed, Eee weather- 
ing out in places into thin layers (1368) ...-...--.05 cece beeen ee eee 


. Fine-grained, friable, yellowish-tinted; composed of much rolled grains of 


dulled quartz; containing little seams and patches of greensand; irregu- 
lar shaly layers with rough surfaces (1369)........+e--s esse e eee ences 


. Medium-grained, rather firm, dirty white; grains glassy and somewhat 


rolled; one Jayer, subordinate lamination not apparent (1370).........- 


. Medium to fine-grained, brown-and-white-banded; in very thin shaly 


layers of almost loose sand, without hard weathering; occasionally run- 
ning into firmer material (1371) ...-.. 6-60 e ee ee eee eee eee eee eee e ee 


. Medium to fine grained, white to yellowish, moderately firm and compact; 


in one heavy uniform mass without perceptible subdivision into layers; in 
places a thick quartzitic crust (1372) ...-. +--+ ++ eeee rete ee eee eee 
Medium to fine-grained, close textured; white, dirty white, brownish; 
Brains all somewhat rolled; hardened crust; in a massive layer without 
distinct subdivision; top of the layer ripple-marked on a large scale, the 
summits of the ridges 2 inches apart (1373)... --.ee sees cece eee ee eee 


. Medium-grained, friable, dark reddish-brown; grains much rolled and 


stained superficially with hydrated iron-oxide; one layer (1874) ......-. 


. Medium to fine-grained, very friable, brownish and yellowish; weathering 


into narrow ridgy lines; in some parts, I foot thick, cross-laminated; sub- 
ordinate layers not very well defined, but marked off by different colors. 


. Medium to fine-grained, friable, dirty white to yellowish; grains rolled and 


glassy; in places brown-weathered; upper layers thick, lower ones thin 
and weathering out in ridges (1375)... 0. esse cece ce ee eet e rete ees 


. Very coarse-grained, porous, friable; white with brown- weathering ...... 
5. Medium to coarse-grained; dark-brown, reddish-brown, red, white, and 


yellow, in irregular bands 2 inches to 1 foot in width, some layers very 
ferruginous; grains glassy and much rolled (1378)..--.++++++++eeeee++ 
Very friable, cross-laminated, yellowish layer, constituting a waiarked hor- 
izon in the series, as seen from below ....-+-+-esseeereeer cers ee 


B73 


Ft. 


21 


In. 


5i4 GEOLOGY OF CENISAL WISCONSIN. 

17. Very fine-grained layers, almost loose sand; in alternating red, white, yel- 2¢. In. 
iow, pink and brown bands; the bands usually very thin, and on close 
inspection often divisible into still thinner different colored stripes 
(1379); near the top the following succession was observed: 2 feet white, 
streaked below with pink; 11, feet pink; 3 feet white, streaked with 
pink; 114 feet pink, cross-laminated; 5 feet thin pink and white streaks — 

the lowest portions weathering with a vitrified crust (1980) ..-.... «++. 20 


Total height of section .....+eeeeeeeeereee eee e ees reser eee: 2S - 10 


None of the sandstone of this section shows any sign of calcareous or dolomitic mgre- 
dients. 

Half a mile south of Roche 4 Cris, across the valley of the north branch of the Littie 
Roche 4 Cris creek, is the much larger outlier, known as Friendship Mound, which 
lies in the east part of Sec. 31, stretching southward into the north part of Sec. 6, T. 17, 
R. 6 E., where its southern eud rises abruptly from the northern side of the Little Roche 
ad Cris creek. The bluff is over three-fourths of a mile in length, trending a little west of 
north, and at base is as much as a third of a mile in width. Allaround, at an elevation 
of 150 feet above the base, it presents a marked bench, bounded by sandstone cliffs 50 
to 100 feet in height, which are flanked below by a long talus of sand. Above the flat 
bench rises a wooded crest. with several rounded surimits, the highest of which is 280 
feet above tha base of the bluff, 310 feet above the bridge at Friendship, and about 750 
feet above Lake Michigan. The whole of the bluff is wooded with oak and pine, pre- 
senting in this regard quite a different appearance from the Roche 4 Cris, and affording 
much poorer opportunity for examination of the rock beds. Below the bench the suc- 
cession of layers appears to be closely like that on the Roche 4 Cris. At one point on 
the west side of the mound, just below the edge of the bench, the sand rock is quarried. 
The quarry rock is moderately firm, uniformly brown-tinted and compact, with distinct 
lamination lines. The base of the quarry is 20 feet below the top of the bench, and iy 
finely ripple-marked. Similar ripple-marks occur again at a lower level, but neither 
horizon seems to be the same as that at which similar markings were observed on the 
Roche 4 Cris. Above the bench the rock is mostly concealed, but is seen at 40 fect be- 
low the summit, where it is coarse, friable, and brown-colored, and intersected by little 
veins of brown iron-oxide. Exposures occur again at 60 feet below the sununit, where 
the rock is white, friable and Scolithus-bearing. 

On the south bank of the creek, at. the Friendship bridge, thin-bedded, crumbling, 
brown-and-white-banded sandstone is exposed down to the level of the creek, adding 
about 45 feet to the Roche & Cris section, 

Five to ten miles south from Friendship, a number of outliers of sandstone occur. 
One of these, Rattlesnake Rock, is about five miles south from Friendship, in the soutl- 
ern part of the town of Adams. The bluff is about half a mile in length, is cut into two 
parts by a central depression nearly to the level of the adjoining low ground, and is 
mostly grassed and wooded. On each side of the gorge, and on all sides of the bluff, 
are considerable exposures, the cliff on the west side reaching 50 or even 75 feet in 
height. A marked bench is 180 feet above the base. Above the bench the bluff rises 
90 feet, the summit being 255 feet above the bridge at Friendship, and 655 feet above 
Lake Michigan. So far as observed, the rock and the succession of layers are the same 
asin the Roche 4 Cris section. At the top of the bluff, the rock (1389) is fine-grained, 
very friable, whitish sandstone, made up of glassy quartz grains, and closely resembling 
the fossil rock on the sumuut of Roche & Cris, to which horizon it evidently belongs, as 
indicated by its having the same altitude, and numero fossil fragments, as well as by 
its lithological character. The fossils are chiefly trilolte fragments, belonging, so far 
as can be determined, to the genus Conocephalites, end Scol.thus-borings. Ten feet 


THE LOWER SILURIAN ROCKS. 575 


below the fossil horizon, the rock (1,890) is somewhat the same, but often brownish and 
containing numerous iron-stained cavities. It is traversed also in every direction by 
films and veins of dark-brown and reddish black hematite. Some of the veins are as 
much as an inch in width, and often show an interior cavity or ‘‘ vug,”’ lined with black, 
dull metallic-lustred, crystalline plates, which have a distinct cubical cleavage and red- 
dish streak. Amongst the plates are concretionary balls, chiefly of the browner oxide, 
1th inch in diameter, and made up of concentric shells. The structure of the erystal- 
line plates indicates that the hematite has resuited from an oxidation of pyrite. 

One mile southwest from Rattlesnake Rock is another quite remarkable pile of rock, 
lying in the midst of a large marsh. The summitis a flat, oval-shaped area, about 300 
by 1,500 feet in size, the greatest length being in a N. 25° W. direction. The base is 
about 35 feet lower than that of Rattlesnake Rock, and the summit is 155 feet higher, 
or about 555 feet above Lake Michigan. On the east face the cliffs are 50 to 75 feet in 
height; on the west, over 100 feet. At the northern end the rock is exposed for most 
of the height of the bluff, being worn into towers partly separated from the main rock. 


A section of the bluff, taken chiefly on the east side, is as follows: a 
< n. 


1. Very fine-grained, non-friable but porous, yellowish, non-caleareous; dotted 
with fine shining scales of mica; made up of very sharply angular quartz 
grains; weathering with a light yellowish smooth surface; thin lamina- 
tion indicated by fine lines, parallel to which there is a tendency to split- 
ting; filled with minute fragmentary fossil impressions, chiefly of trilo- 
bites; among these were determined Ptychaspis (n. sp.), Conocepha- 
lites minor, and Orthis Barabuensis; not found definitely exposed, but 
lying in fragments thickly strewn over the surface of the bluff, which is 
grassed, the rock being thus concealed; lying ahout 100 feet lower than 
the fossil horizon on Rattlesnake Rock, and the same horizon on Roche 
a Cris; not a mere local layer, because found again with exactly the same 
tossil contents, and peculiar hthological characters, and occupying the 
same position, 10 miles eastward on Pilot Knob; not appearing in the 
Roche a Cris section, where, however, it might easily have been over- 


looked on some of the less accessible portions of the cliff (1400)........ .. 6? 
2. Very coarse, triable, reddish brown; weathering into thin layers........... 9 
3. Very coarse and friable, white-and-brown banded; carrying large ripple- 

wnarks at top... -. see e er eee reece es Sits baatalnievdnuass sane tate wei wh oe hea 16 


4. Moderately coarse, friable; uniformly white in color, except on weathered 
surfaces, which show brown-stained layers 2 inches to 4 inches in thickness, 18 
5. Finer-grained, very friable, pink-and-white banded, white predominating 


below... cece cece cee eee eee ere eee nee een ete n sees 14 
6. Coarse-grained, very friable; whitish with dirty colored ridgy projections, 
which on exposed edges are vitvified; near the base including some pink 
layers...-.++++ Be Sy Slee was abate ota rena ceedeac “attra, Coauaoniion BN giiaisbiauiieteaabe euateaacpuene eNGusin 19 6 
7. Fine-grained, very friable, brown-and-white-banded; thin-laminated...... 8 
8. Not seen in detail ..... ces e eee eee cee teen eee tect e ee et nen eee e ene ees 50 
9, Alternating very coarse and finer sand layers, all very friable; alternating 
also in color, being banded white and brown; finer layers cross-lamin- 
ated; coarser ones (1401) very plainly banded, and containing rolled 
grains up to qs to xy inch in diameter; all showing very marked surface 
vitrification, which in the coarser parts extends in much further than in 
the finer, the grains being glassy and closely adherent; seen at the foot 
of the north end of the Cliff... .---+eereeeerer ee ce ree tee e terres eees 20 
155 


Héightiof tha Wulf, 21-1 «censssensnse eteiarancenitataaiinn torte means 1B es 


576: GEOLOGY OF CENTRAL WISCONSIN. 


Nine miles east from Roche 4 Cris and Friendship Mound, on the N. E. qr. of Sec. 3, 
T. 17, R. 7 E., is the outlier known as Pilot Knob. This is a narrow jagged crest, 75 
feet long, 10 to 15 feet wide, and 80 feet high, resting upon a hill with gentler slopes, 


and about 400 paces in diameter. A section from above downwards is as follows: 
Feet. 


1. Medium to fine-grained, brick-red (1420, 770); composed of rolled grams of 
quartz, coated externally with red and brown iron oxides; containing some 
hard curving seams, 4% to 1 inch in thickness, of a dark brown color, made 
up of glassy quartz grains cemented by much brown iron-oxide, and evi- 
dently of a concretionary nature; including some lighter colored brown and 
even white layers, the latter (1419) porous, friable, medium-grained, and 
weathering with a very hard vitrified crust; containing near the base about 
a foot of light reddish, very friable, fine-grained, fossiliferous rock, con- 
taining Ptychaspis Miniscaensis and other trilobite impressions......... 45 
2. White, friable, non-fossiliferous sandstone, to foot of crag....-....+-.+. 64 40 
. Unexposed, on graflual slope «2... eee ere eee eee cece eter teen ener ners 30 
4, Fine-grained, non-friable, yellowish sandstone (1421), consisting of fine angu- 
lar quartz, and containing a few scales of mica; thin-bedded and marked 
by fine lines of lamination, pavallel to which it splits with some readiness; 
fossiliferous, containing Ptychaspis, Conocephalites and disks of crinoidal 
columns; exactly reseralling the fossil rock at the summit of the last sec- 
tion given, to which horizon it undoubtedly belongs ....... ....---..--. 1 
. Unexposed, on steep slope. ... 0... eee cece teen eee e tenes eacie Ape dean end pinnae 10 
. White-and-brown-banded, thin friable layers .......... 000. e cece cence eee 20 
. Unexposed to base «10... se eee cece ere tence ete ene eens Lane Siete deka eres seals 20 


eS Fat ot eats coh naa e ener eae 166 


ja] 


a1 om oF 


The two fossil horizons of the above section appear to be the same as recognized on 
Roche a Cris, and the bluffs south of Friendship, though apparently somewhat nearer 
together. The base of Pilot Knob is 545 feet, the lower fossil horizon 595 feet, the up- 
per fossil horizon 665 feet, and the summit 705 feet above Lake Michigan. These 
figures indicate a slight rise, about 4 feet to the mile, of the strata between Roche & 
Cris and Pilot Knob. It is possible that this rise may be exaggerated by unreliable 
barometrical observations; there is, however, certainly no rise westward between these 
points. 

A mile and a half southeastward from Pilot Knob, the intervening ground being low, 
on the N. W. qr. Sec. 12, T. 17, R.7 E., is a long ridge facing northwestward, with 
rock outcrops on the flanks. The highest outcrop seen is some 20 feet below the top of 
the ridge, and about 25 feet lower than the summit of Pilot Knob. From this point 
aownwards for 40 feet, are seen layers of incoherent white sandstone, with intercalated 
yellowish calcareous bands, 2 to 6 inches in thickness, and 5 to 15 feet apart. The 
rock of these bands (1405, 1406, 1407) is rough-textured, porous and moderately firm, 
but crumbling under the hammer. It has the appearance of being coarse-grained, but 
on close inspection most of the apparent large grains are seen to be due to the aggrega- 
tion of smaller ones, and the rock is seen to consist of an admixture of fine, yellowish, 
angular grains, and larger ones of white and much-rolled quartz, with sparsely scattered 
greensand grains. On solution in acid, the yellowish matter is entirely dissolved, leav- 
ing a residue of not over 40 per cent., which is made up entirely of the white quartz 
grains. Cleavable calcite is occasionally to be seen by the naked eye, and from tho 
ready effervescence and solution in cold acid, it is judged that the rock is much more 
largely calcareous than dolomitic. These layers arc, beyond doubt, those that are to Lo 
seen in more southern counties immediately underlying the Mendota limestone, which 


THE LOWER SILURIAN ROCKS. 577 


possibly exists as a capping on this hill. From the figures given, it will be scen that 
these layers extend as much as 60 feet lower than the summit of Pilot Knob, which, 
moreover, is of an entirely different kind of rock. In order that the Pilot Knob layers 
may pass beneath those across the valley, they must have a descent of at least 50 feet 
to the mile in that direction, an amount of descent that would he altogether extraor- 
dinary in Central Wisconsin. 

One mile eastward from the exposures just described, on the N. W. qr. of Sec. 7, T. 
17, R. 8 E., Marquette county, is a large isolated blutf capped by the Lower Magnesian 
limestone. Another similar bluff lies a mile northeast of this on Sec. 4 of the same 
town. The first named, known as ‘‘Glover and Merriman’s lime bluff,’’ shows the fol- 
lowing section: 


1. Lower Magnesian limestone (1409): close-textured, very finely crystalline, yel- sa 
lowish-gray to nearly white; holding small cavities lined with brown-tinted 
dolomite crystals, and others lined with stalactitic lime carbonate; in places 
marked with fine pencilings of the dendritic oxide of manganese; dolomite— 
dissolving only in heated acid, with a residue of very fine, white, angular 
silica, constituting 13.96 per cent. of the whole — but containmg no sand 
whatever; containing little greenish blotches and streaks; weathering with 
rough surface; occurring in layers 3 to 4 feet thick, some of which are much 
displaced ......-...00005 5 eA Gwaet RG EG Sih ge DeagnacurreG nA Aue pigeons ctaavesmu cee 30 

0. Unmexposed aininis 2280s «tsknniana gaye YANG MeNaiaseauias EMeuAt eae Behe 10 

8. Madison sandstone: coarse, whitish, moderately firm; forming a prominent 
ledge on the side of the bluff..........6ec cece eee cee e eee eee eee e nes 10 

4, Unexposed.... ..-..-- Ses y SIGs ecole oc a eS a rach re ene veered tanta ova ebadiose Rast ates 40 

The following occurs on an outlying hill south of the main bluff: 

5. Mendota limestone: lowest layers only seen; brownish and yellowish....-..... 10 

6.. Uniexposed., .s.ceio: 443 4h 4 ge: meinen eer ede eine cia oe ed Goede 15 

7. Potsdam sandstone: white, crumbling sandstone, with intercalated yellowish, 
coarse-textured, calcareous layers (773, 1408), exactly like those seen at 
the last locality deseribed aac xae0 a8 ae euadigvessves peeved eg ees eaety 10 

8. Unexposed ta base Of DIU, essauccsucsdesscteeeteneeuecnersnes ceangeeaes 35 
Total height of bluff... + xis sswsseieswscuseuee. cues ges cgersecntseeees wees 160 


The base of the bluff is 570 feet, and its summit 730 feet, above Lake Michigan. 
These figures indicate some descent from the locality on Sec. 12, T. 17, R. 7 E., but ex- 
actly how much is not ascertainable, from the somewhat indefinite position in the series 
of the limy layers at the former place. It has been said that Friendship Mound and the 
Roche 4 Cris rise respectively to altitudes of 750 and 665 feet above Lake Michigan. 
Neither, however, shows any sign of limestone at top, or any indication of reaching 
within 100 feet of its horizon. This might be explained readily enough by supposing a 
continuation westward of the somewhat rapid rise of the strata that is indicated in the 
vicinity of the Lime Bluffs. It has been shown, however, that the strata of Pilot Knob 
indicate not only no westward rise, but even a slight eastward one. 

The occurrence of two limestone outliers as much as 25 miles from the nearest points 
of the area occupied by the Lower Magnesian is interesting, and of considerable economic 
importance. That this formation once extended as far north as this is thus rendered 
certain. Having reached the highest land in the region, it may possibly have had also 
a still wider spread northward. 

Wis. Sur. — 37 


578 GEOLOGY OF CENTRAL WISCONSIN. 


Marquerre ann Wavsnara Counrims, anp Green Laxe Covnry, 
Norru or tue Fox River. 


(AtLAs PLaty XIV, Arges E.) 


This district lies chiefly to the north and west of the Fox river, towards which it slopes 
steadily from the summit of the dividing ridge in western Waushara and southern 
Adams counties. It includes a total area of about 1,239 square miles. Throughout the 
region the Potsdam sandstone seems to be the surface formation everywhere, except in 
the few places where the crystalline rocks come to the surface, and in one or two limestone- 
capped bluffs. The sandstone, however, is not frequently exposed, being for the most 
part very deeply buried beneath the glacial drift, or Champlain lacustrine clays, the 
former occurring in portions of the region in a morainic condition, and of unusual thick- 
ness. It is not possible to be certain that the superficial deposits do not in places rest 
directly upon the crystalline rocks without intervening sandstone, but the known facts 
render such an hypothesis improbable. 

This region, though similar in its basement rock and general sandy soil to the central 
plain of Adams and Juneau counties, differs from it in being without the plain-like 
character, presenting as it does a steady descent from northwest to southeast of over 
300 feet, and a surface in general much roughened by morainic drift. Another striking 
difference is found in the absence of the castellated outliers that characterize the Adams 
and Juneau district. A few small ones dot the summit of the high ground in north- 
western Marquette county and the adjoming part of Waushara, but these are of 
rounded shape, comparatively stout, and without the fragile appearance of the more 
western peaks. Further east, the outliers disappear altogether. The general south- 
eastward descent gives that direction to the many tributaries of the Fox, which, as al- 
ready described, are large, clear and rapid streams, furnishing many excellent water- 
powers. In places quite large areas are level, as for instance Burr Oak prairie, in west- 
ern Waushara county, but these are but small portions of the whole district. In the 
town of Mount Morris and the adjacent country, northeast of Wautoma, Waushara 
county, is a small district which owes its irregularity of surface chiefly to subaerial ero- 
sion of the rocky strata, presenting the ordinary phenomena of deep and narrow val- 
leys. Southeastern Marquette county includes a small part of the south side of the 
Fox river basin, in the towns of Packwaukee, Buffalo and Montello. The character of 
this area is similar to that of the rest of the region, the sandstone outcrops being some- 
what more frequent, but the surface im general much heaped up with drift. 

The soil of the region is largely sandy. This sand, however, though originally com- 
ing, without doubt, from the Potsdam sandstone, is directly derived from the glacial 
drift, which has also contributed much calcareous and clayey matter. Thus it comes 
that, although based upon the sandstone, and presenting in many places a very sandy soil, 
excellent farming land is by no means uncommon in these counties. In the eastern 
towns of Waushara county, where the red Champlain clays make up the body of the 
soil, much very excellent land is found. Except in the clay region of eastern Wausha- 
ra, where hard wood (ash and elm) is plenty, the only timber is for the most part the 
small oak growth that characterizes most of Central Wisconsin, the oaks becoming 
mingled with pines towards the north. 

From what has been said, it will be seen that the exposures of horizontal strata are 
not frequent. The lime blufts of the town of Springfield, in the northwestern corner of 
Marquette county, have already been described. On Sec. 15, T. 19, R. 11 E., Waushara 
county, the high ground known as Mount Morris reaches into the limy layers that 
underlie the Mendota limestone. On top of the hill, 240 feet above Mount Morris post 
office, are exposed 3 feet of thin layers of coarse-grained, yellowish, firm sandstone 


1000 feet 


Vertical Scale,linch 


4timiles. 


East and west sections in 


COLUMBIA COUNTY 


Horizontal Scale 1linch 


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THE LOWER SILURIAN ROCKS. 579 


(1416), alternating with finer-grained, more friable layers (1415). The coarser rock is 
the most calcareous, consisting of much-rolled grains of dulled quartz, with 30 per cent. 
of yellow-stained, cleavable calcite (and dolomite?) grains, and dark, smooth-surfaced 
grains of greensand. The horizon is probably within 25 feet of the Mendota, and is 
from 600 to 650 feet above Lake Michigan. On the N. W. ar. of Sec. 16, 260 feet below 
the rock on top of the mount, light brownish, very fine-grained, firm, non-caleareous- 
sandstone (141419) is exposed. With the exception of Mt. Morris, the lime bluffs of north- 
western Marquette county, and a few points m the town of Buffalo, Marquette county, 
the whole region appears to be eroded well down into the Potsdam series, probably 
everywhere as much as 100 feet below the Mendota, and in general 200 to 300 feet. 
Kven in the eastern towns of Waushara, just east of which, in Winnebago county, the 
Lower Magnesian is well down into the low ground, the erosion into the Potsdam has 
been very considerable, the lacustrine clays reaching a thickness of over 100 feet. At 
the limestone bluff on Sec. 7, T. 17, R. 8 E., Marquette county, the base of the Lower 
Magnesian is 700 feet above Lake Michigan. Thirty-eight miles from here, in a N. 10° 
E. direction, on Sec. 27, T. 19, R. 14 E., Winnebago county, the same horizon is at an 
altitude of about 200 feet. The total eastward descent thus shown is 500 feet, or about 
13 feet to the mile. This descent is, however, by no means uniform, being very much 
greater in the eastern half of the distance, for the place of the base of the Lower Mag- 
nesian at Mt. Morris, as indicated by barometrical observations, is not less than 700 feet 
above Lake Michigan. These observations were far from any known point of altitude, 
but allowing all chances for error, the altitude of the Lower Magnesian base, at this 
place, could hardly be less than 650 feet. 

Very good, hard, white sandrock is quarried about 3 miles from Wautoma, in the 
town of Mount Morris, Waushara county; at a point about the same distance north of 
Montello, Marquette county; and again near the village of Packwaukee, in the latter 
county. The stone from all resembles somewhat the sandstone from the Stevens Point, 
Grand Rapids and Black River Falls quarries, and may be at the same horizon. The 
Packwaukee quarry is opened in the top of a low ridge, on the edge of the Fox river 
marsh, and a short distance from the shore of Lake Butfalo, N. E. qr. of Sec. 30, T. 15, 
R.9E. The quaxry face is 15 feet high, and the rock very regularly bedded in layers 
from 2 iaches to 30 inches in thickness, the heavy layers occurring below, the thin ones 
at top. Strong, smooth-faced joints intersect the layers, trending N. 75° W., N. 35° 
W.,N. 17° W., and N. 14° E. The top layers are somewhat soft and brownish, the 
whole quarry face bemg much iron-stained by weathering. The heavy layers below, 
however, present a very much indurated, nearly white, fine-grained sandrock (760), 
made up of grains of sharply angular, glassy quartz, and obtainable in very large, 
straight-edged, smooth-faced blocks, which dress readily. The rock is a quite unusually 
good building material. 


Sauk anp CoLumBra OcunTIES. 
(Arias PLarEs XIII anp XIV, Angas D anp E.) 


Those portions of Sauk county lying west of the west line of R. 4 E., are not here in- 
cluded. The remainder of this county, and Columbia, constitute a nearly rectangular 
area, 54 miles from east to west and 24 from north to south, lying just midway between 

‘Lake Michigan and the Mississippi river. Sauk county, in its southern portion, along 
the Wisconsin, oversteps the limits of the rectangle, adding three entire townships and 
parts of three others. The whole area of the district, as given by the land-office plats, 
is 1,351.5 square miles, including 785 square miles for Columbia, and 566.5 square 
miles for that portion of Sauk county here described, the whole of Sauk county having 


‘an area of 796.5 square miles. 


580 GEOLOGY OF CENTRAL WISCONSIN. 


The main topographical features of the district — the east and west ranges of the 
Baraboo; the Wisconsin river, which traverses the area centrally from north to south, 
making a great bow eastward to double the eastern point of the uniting quartzite 
ranges; the remarkable course of the Fox river, which after flowing southwest directly 
towards the Wisconsin, tums abruptly north when but one and one-half miles from it, 
the two rivers traversing a flat sand plain, without dividing ridge, und passing the one 
into the St. Lawrence, the other to the Gulf of Mexico; the escarpment of the Lower 
Magnesian hinestone, which crosses Columbia county from S. W. to N. E., having its 
face tumed westward and much indented by the head waters of the streams tributary 
to the Wisconsin; the gentle eastward slope of the country east of the escarpment, with 
its streams flowing eastward to the Rock river; the sandy plain-like character of the 
country west of the escarpment; the isolated erosion peaks and outliers that dot the sur- 
face of this plain — have all already been more or less briefly alluded to. 

The Lower Magnesian escarpment enters Columbia county on the southern side of 
the town of Lodi, projecting in bold points that rise 250 to 3800 feet above the valley of 
Spring creek. Thenea it trends northward through the eastern row of sections of that 
town, with the same character, having on top the elevated prairie land of Arlington. 
At the northeastern corner of Lodi, it turns nearly at right angles, crossing the north- 
ern row of sections of Arlington in an eastward direction. Passing into the northwest 
corner of Leeds it turns again northward, traversing Lowville from southeast to north- 
west. In this town, though still well marked, the escarpment is much lessened in bold- 
ness und height, because of the increasing eastward descent of the strata, and because 
also it has in front a wide area occupied by the Madison and Mendota beds, beyond 
which a second escarpment leads to the lower level occupied by the Potsdam sandstone. 
‘From the northeast corer of Lowville it crosses the northwest part of Otsego, not far 
from the village of Rio, and passing into Springvale about the nnddle of its south line 
traverses that town in a northerly direction, projecting westward in long points. In 
Springvale the Mendota and Madison escarpment is the most marked of the two, it pre- 
senting long narrow and bold points projecting westward between the branches of Duck 
creek, which head in the towns to the eastward. The main branch of Duck ereek, in 
the northern part of Springvale, has the widest valley, and has on each side the longest 
of the Lower Magnesian points, that on the north side extending all the way to the west 
hne of the town. On this branch of Duck Creek, also, the low ground extends far east- 
ward into the towns of Courtland and Randolph. Across the town of Scott the escarp- 
ment presents the same character as in Springvale, the westward projecting points re- 
ceding eastward, however, in the north part of the town, and having between them the 
head streams of the Fox river, instead of tributaries of the Wisconsin. The remarka- 
ble manner in which the Lower Magnesian escarpment recedes from the Wisconsin after 
forming for so many miles the southern boundary of the valley of that stream, and the 
bearing of this upon the former southern discharge of the Fox river system, have been 
previously alluded to. A 

Immediately south and east from the limestone edge, the country is on a level 
with its summit, but further south and east sinks gradually with the decline of the 
strata in those directions. Along the western part of the south line of Columbia county 
the direction of the greatest descent of the strata is nearly due south: further east and 
north, however, it veers to the eastward, being at the middle of the east line of the 
county abont due east. Still further north, in the town of Randolph, a northern de- 
scent begins to be distinctly perceptible. The surface slopes in general correspond 
with these changes in direction of the slopes of the strata. The greatest elevations are 
thus evidently reached towards the southwest, where the escarpment is highest. Thus, 
the high prairie of Arlington and Leeds reaches altitudes of from 450 to 500 feet, whilst 
further east, in Columbus and Hampden, the general elevation is 200 to 250 feet less. 


PLATE, XXIII 


rth and sovwth sections mn 


COLUMBIA COUNTY 


Horizontal Scale lineh 


No 


: ee 
z 3 ANA a EMT 
aa eit fi ne 
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Mendota 


Low ville 


Re a aE 
Fountain Prajrie 


aa] az | aa 1s 


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3 

a 


Heads of Creavlish Raver 


West Point 


Leeds 


Columbus 


THE LOWER SILURIAN ROCKS. 581 


Further ideas as to this structure can best be obtained by exammation of the sections of 
Plates XXII and XXIII, in connection with the map of Area E. In southeastern Lodi, 
Arlington, Leeds, Hampden, southeastern Lowville. southwestern Otsego, and southern 
Fountain Prairie, the country above the escarpment is generally rolling prairie, much of 
it very high. Further north, in northern Otsego and Fountain Prairie, and southern 
Courtland and Springdale, the prairie belt is broken by a belt of the ordinary oak tin- 
ber. Still further north again, prairie spreads widely over the limestone country of Court- 
land, Randolph, Springdale and Scott. Nearly all of the country east of the escarp- 
ment shows a most excellent soil, being underlaid for the most part by limestone, which 
is, however, frequently buried beneath much glacial drift. An exception would be those 
portions of Fountain Prairie and Otsego where erosion has carried the surface into the 
horizon of the Madison sand beds, the result being a loose, sandy soil, like that of the 
regular Potsdam regions. The streams watering this district are mostly small, and all 
flow eastward towards the Rock river. 

Immediately west of the limestone edge, there is an abrupt descent of 100 to 300 
feet, and, beyond, a more gradual slope cf 50 to 100 feet to the Wisconsin river. This 
area has, in general, the character of a sandy plain, timbered with small oaks, with 
marshes along the streams, and dotted here and there with isolated bluffs, 100 to 400 
feet high, from a few acres to several square miles in area. and generally surmounted by 
a capping of Lower Magnesian limestone. But very little prairie is met with. Some 
occurs in the town of West Point, including both low land and limestone outliers. The 
streams are larger than those on the east of the divide, increasing in size as the escarp- 
ment recedes from the Wisconsin. Spring creek, in Lodi, Okee creek, in southem De- 
korra and northem Arlington, Rocky run, in northern Dekorra and Lowville, the 
several branches of Duck creek, in Pacific, Wyocena, Springvale, Courtland and Ran- 
dolph, and the Fox river in Fort Winnebago, Marcellon, Wyocena and Scott, are the 
principal streams. The towns of Lewiston, Newport and Fort Winnebago, west of the 
Fox river, and north of the Wisconsin, are similar to the rest of this sand district in 
many respects; but are more roughened in surface, the northern portions of the two for- 
mer rising up to the high land through which the passage of the Dalles is cut. 

West of the Wisconsin river we find the topography influenced primarily by the 
quartzite ranges of the Baraboo, which have already been sufficiently described. For 
our present purpose it is merely necessary to remember that they are two east and west 
ranges, some twenty miles in length, uniting at both ends, and thus entirely enclosing 
the low ground between them. They are made up of Archean quartzite and quartz- 
porphyry, but the country around and between them is all occupied by the horizontal 
formations. Outside of the ranges in the towns of Caledonia, Columbia county, and 
Fairfield, Merrimack, Prairie du Sac, and Sumpter, Sauk county, the country is in most 
respects like the level sand district immediately east of the Wisconsin, showing in the 
more southern portions a few limestone-capped outliers. Farther west, however, we 
pass beyond the western limit of the glacial drift, and find the topography presenting 
the usual marked change, being characterized by narrow ramifying ridges and valleys, 
the former, in the more southern towns, commonly capped by the Lower Magnesian lime- 
stone, but in the more northern formed entirely of sandstone. In the southern part of 
Sauk county, immediately west from the drift limit, the ridges are found frequently 
worn into narrow, isolated crests, 100 to 200 feet high, and with frequent rock exposures, 
constituting a very marked and peculiar scenery. Farther west, the ridges are broader, 
and large areas of limestone occur on the higher levels. In the town of Westfield, west 
from the ends of the quartzite ranges, the high ground continues, capped now by the Lower 
Magnesian limestone, and forming the divide between Honey and Narrows creeks. 
Honey creek enters the Wisconsin about five miles below Sauk City. Following it to- 
wards its source, we find it, separating, in the northern part of the town of Troy, into 


582 GEOLOGY OF CENTRAL WISCONSIN. 


two principal branches, the southern one setting back westward nearly parallel to the 
Wisconsin, and only about six miles from it, the other coming from the south side of the 
divide in the town of Westfield. Between the wide valley of the south branch and the 
Wisconsin, is 2 long line of limestone-capped bluffs, which present a bold front, 200 to 
300 feet high, along the north shore of the Wisconsin. North of the Westfield divide 
the various head streams of Narrows creek are found running northward, with narrow 
ind sharply defined intervening ridges. Narrows creek itself runs in a level valley two 
to three miles wide. North of it, again, the same narrow limestone-capped ridges are 
found, until the still broader valley of the Baraboo is reached in the northern -part-of 
Reedsburg. Beyond this again the ridgy topography continues, the ridges now alto- 
gether of sandstone, and leading up to the high ground which forms the southern rim 
of the sand plain of Juneau and Adams counties, and through which the Wisconsin 
passes at the Dalles. On the slope towards the Dalles, in the northeastern part of Sauk 
county, the small tributary streams of the Wisconsin cut down through narrow rock- 
walled cafions, similar to the Dalles, though on a smaller scale. The valley of the Bar- 
aboo, between the quartzite ranges, is generally higher than the country outside the 
ranges, and is considerably roughened in surface by the wash from the enclosing ranges 
towards the Baraboo. The streams watering the district west of the Wisconsin are 
much larger than those on the east side of that river. The largest of these is the Bara- 
boo river, which, entering Sauk county on the northwest, traverses it in an casterly direc- 
tion, passing between the two quartzite ranges, and reaching the Wisconsin at the ex- 
treme eastern point of its great bend, having in this distance a fall of about a hundred 
feet. Its numerous tributary streams, dividing into many smaller branches, drain the 
country for a width of ten miles on each side of the river. South of the southerm quartz- 
ite range and of the limestone divide in Westfield, the only streams of importance are 
Honey and Otter creeks. The former is much the larger; separating into numerous 
small branches, each with its own ravine, it drains an area of about 185 square miles. 
Otter creek drains a considerable portion of the southern slope of the main quartzite 
range in the town of Sumpter, and then, taking a due south course towards the Wis- 
consin, sinks into the sand when within two miles of the river. Except on and about 
the quartzite ranges, the soil and timber of the district west of the Wisconsin follow the 
same rule as observed east of the river, 7. e., on the lower levels, loose sandy soils, whilst 
on the higher limestone ground, the soil is clayey and excellent. Good land, however, is 
sometimes found on the lower levels, as, for instance, on Sauk prairie, where it is due 
partly to drift materials; in the town of Honey Creek, where stream detritus forms 
much of the soil, and in the northern part of Excelsior, where no such causes can be 
assigned. Occasional pine groves are interspersed amongst the ordinary oak timber, 
whilst amongst the quartzite ranges there is a heavy growth of hard wood, largely maple. 

The list of geological formations represented in Sauk and Columbia counties in- 
cludes all of the Central Wisconsin formations, from the Archwan to the Drift, except 
the Galena limestone. The Potsdam sandsto.te is the surface rock over all the lower 
levels along the Wisconsin and its many tributaries, besides forming considerable por- 
tions of the slopes of the outliers and highcr lands. On all sides of the quartzite ranges it 
is found attaining very considerable altitudes, apparently rising into the horizons of the 
higher strata, whilst within the circuit of the ranges it occupies all levels, limestone being 
found in one or two small patches only. Farther north again, in northem Sauk and 
northwestern Columbia, it occupies all levels, having attained now a much increased al- 
titude by virtue of its general northern rise. The Mendota and Madison beds occupy 
parts of the slopes, or else cap the summits of many of the outliers that flank the lime- 
stone escarpment in Columbia county, and of the ridges of western and southwestem 
Sauk. They also form the surface rock along the slope of the western edge of the lime- 
stone country of Columbia county, occasionally, as in the towns of Lowville and Spring- 


. THE LOWER SILURIAN ROCKS. 583 


vale, coming to the surface over a, belt of country several miles i in width. Even east of 
the limestone edge, a considerable area of the adjoining portions of Utsego and Foun- 
tain Prairie is eroded down to the level of the Madison sand beds, and yet surrounded 
entirely by the higher formations. Such an effect is a peculiar onc, and takes place only 
where the inclination of the surface bears such a relation to the changing inclination of 
the strata as indicated in Fig. 37. The Lower Magnesian limestone caps many of the 
outlying bluffs east of the Wisconsin, forms the summit of most of the higher ridges in 


Fie. 37. 


Diacram Suowine LOW AN AREA oY A LOWER ForRMATION MAY BE ENTIRELY SURROUNDED BY 
A HIGHER ONE. 


western and southwestern Sauk, and is the surface rock nearly everywhere in Columbia 
county, east of the limestone edge. In this latter district, however, it is overlaid by the 
St. Peters sandstone and Trenton limestone, in southeastern Hampden, and southern Co- 
lumbus, over a small area in eastern Fountain Prairie, and over a much larger one in 
northeastern Courtland and eastern Randolph. The St. Peters sandstone occurs also in 
several patches in southwest Arlington, lying upon the irregular upper surface of the 
Lower Magnesian, and forms the upper part of a remarkable bluff in the northeast part 
of West Point. The characters of the several formations are indicated in the following 
detailed descriptions. ‘Their thickness, relative positions, etc., are shown by the sections 
of Plates XX, XXII and XXIII of this volume, and those attached to the Atlas Plate of 
Area E. 

Beginning ovr detailed descriptions in the northeastern corner of Columbia. county, 
we note first, on Sec. 31, T. 18, R. 12 E., Randolph, two quarries on the Mendota and . 
Madison beds, on the walls of a ravine at the head of Duck creek. The quarry on the 
west wall of the ravine shows the following section: 


MENDOTA BEDS. 
Ft. In. 


I. Very fine-grained, yellowish-brown, calcareo-silicious rock (1206); only: 
slightly arenaceous in feeling, but leaving a residue, on treatment with 
acid, of 69.03 per cent., which consists of exceedingly fine, white, angu- 
lar quartz; thinly and regularly laminated, the layers running from one 
bo FOUL in ChERs :-eaiyecaeGiseiecd lense, Cb.84.\ sw hebsastlecw asoyngs Beateraeanaar emcees 10 

II. Very fine-grained, close-textured, salloais -and-purple-blotched, calcareo- 
argillaceous rock (1207); the yellow parts like I, the dark-colored a 
sort of clay-shale, occasionally finely lammated, but not in distinct layers; 
residue on treatment with acid, 44.53 per cent.; layers, two to eight 


II. Very: fine-grained; milk-white, ailieiond rock, without calcareous admix- 
ture; non-arenaceous; similar to II of next section..........+-++52++- .. 6 


58t GEOLOGY OF CENTRAL WISCONSIN, 

Fi. In. 

[V. Similar to IL.......-. cece cece cece e eee eee eee e teen enter e eee nn eens 

V. Compact, yellowish-brown-and-red-blotched, calcareo-magnesian rock 

(1210); differing from Iin having a very fine crystalline texture, and 

cavities lined with dolomite crystals; insoluble residue, 41.73 per cent.; 

layers a foot thick; quarry-rock, used in building at Cambria and other 

places in the vicinity: obtainable in large well-shaped blocks. ise ceess 4 
POTSDAM SANDSTONE. 

VI. Greensand layers; moderately firm, rough-surfaced, brownish, speckled 

with green; calcareous; leaving a residue, on treatment with acid, of 

fine, sharply-angular quartz, mingled with dark-green grains......... 


1 & | vo 
lol 


The greensand appears without doubt to be that generally recognized as marking 
the base of the Mondota horizon, which is here more largely silicious than in the typical 
localities in Dane county, though still sharply contrasting in character with the Madison 
and Potsdam saridstone layers. A quarter of a mile up the ravine, on its east wall, 
another small quarry opening shows the following: 


MADISON BEDS. 
Feet. 


I. Fine-grained, brownish, ferruginous, friable sandstone (1226); non-calcareous; 
j composed of rolled grains of dulled quartz; scolithus-bearing ............. 4 
II. Very fine-grained, firm, pure white, silicious rock (1212); composed of excecd- 
ingly fine, sharply angular quartz; non-calcareous; non-arenaceous; contain- 
ing 97.52 per cent. of silica; close to III of last section; upper layers shaly.. 3 
MENDOTA BEDS. 


UT, Similar to II, but stained yellow and pink (1213); very hard and firm; con- 


taining 98.12 per cent. Silica ....- 6. eee e cece eee ce eee eee eee een teens 8 
LV. Reddish-yellow rock similar to I of last section, and apparently the same horizon. 3 
13 


At P. Scheasman's quarry, on the west line of the 8. W. qr. of Sec. 6, in the same 
town, a ten-feet quarry face shows below, in thin and very regular layers, a close- 
textured, buff-colored, nearly pure dolomite (1205), which weathers with a smooth, yel- 
_lowish surface, is marked finely with dendritic manganese oxide, and is coated in places 
with white, stalactitic, lime carbonate, and at the top a heavy layer of concretionury, 
dark-colored dolomite. On the hill above are exposures of the ordinary rougti-textured 
Lower Magnesian, near the base of which formation the quarry layers appear to lie. 

In the railroad cutting at Rio, in the northwest corner of the town of Otsego, T. 11, 
R. 12 E., the Madison and Mendota beds are exposed. The following is the section:. 


MADISON BEDS. 


I. Brownish, friable sandstone........ 0... ee eee ccc e cee nee eee n eee eenees 
lL. Very fine-grained, pure white, firm, silicious rock; non-caleareous; in upper 
portions slightly arenaccous in texture (1219, close to 1212); lower portions 
without trace of granular texture; rough-surfaced and pink-tinted (1216, 
close to 1213); bedding not distinctly seen; composed of exceedingly fino, 
angular qQuartd 2csveekcts ees) cede eekesawndsee eeawentiodinccees taawe 12 
MENDOTA BEDS. 
HI. Red-and-yellow-mottled calcareo-arenaceous rock. ....scceescccesesreectees 4 


22 


THE LOWER SILURIAN ROCKS. 585. 


Fig. 88 is a section from south to north along the center line of 
Sees. 2, 11, 23 and 26, in the town of Scott, T. 13, R. 11 E., and 
serves to give a correct idea of the topography and stratigraphy 
of that township. 

Large ledges of Potsdam sandstone rise on the south side of a 
small creek in the N. E. qr. of the N. KE. qr. of Sec. 8, Arling- 
ton, T. 10, R. 9 E., a short distance south of the village of 
Poynette. Here are exposed 15 feet of whitc, heavily-bedded, 
friable, non-calearcous sandstone, with some thin greensand lay- 
ers, the base of the ledge being 60 to 80 feet below the base of 
the Mendota horizon. Similar but higher ledges occur along 
the creek in Pine Hollow, in the adjoining parts of Secs. 3 and 4. 

The St. Peters sandstone remains on top of the Arlington prai- 
ne in five isolated kmobs, the highest 70 to 100 feet in height. 
Three of these are close together on each side of the line between 
Secs. 28 and 29. The bluff on Spocnam’s land, N. E. qr. of the 
8. E. qr. of Sec. 29, shows large outcrops, in a disturbed condition, 
of fine-grained, friable, white-and-brown-mottled sandstone (725, 
726), composed of glassy quartz grains, the larger ones of which 
are rolled, the smaller ones angular. Most of the rock ig affected 
by a very hard, vitrified crust, 14 to 14 inch in thickness, in 
which the quartz grains appear to possess distinct crystalline sur- 
faces. No trace of calcareous matter is present. Fine-lamina- 
tion and cross-lamination are plainly perceptible. The knob on 
Mrs. A. D. Forbes’ land has on the south side a vertical cliff, 80 
feet in height, of similar but distinctly horizontal and undisturbed 
sandstone. In the 8. W. ar. of the 8. W. qr. of Sec. 27, and ex- 
tending into Sec. 28, and again in the N. ht. of Sec. 34, are other 
similar bluffs. On the prairie around these sandstone mounds, 
exposures of the Lower Magnesian limestone are seen at several 
points whose elevation is greater than that of the base of the 
sandstone ledges, whilst at least two points, on the south line of 
Sec. 21 and in the north part of Sec. 29, show the limestone ris- 
ing as high as the top of the St. Peters. The wregular nature of 
the upper surface of the Lower Magnesian is thus cistinetly 
proven. P 

In Fort Winnebago, T. 13, R. 9 E., the’ only formation is the 
Potsdam sandstone, which, in the middle and western portions, 
and again in the southeast, rises in isolated bluffs. At T. Cough- 
lin’s quarry, N. E. qr. of 8. W. qr. Sec. 20, are exposed 10 feet 
of heavily-bedded, fine-grained, white, porous, friable sandstone 
(741), which is composed of glassy, sub-angular, quartz grains, 
and js blotched with ferruginous spots. Rows of little brown- 
stained pores mark the lamination very plainly. Large fucoidal 
impressions occur, identified by Mr. Whitfield as Palewophycus 
duplex, and Paleschoida,n. sp. Large regular shaped blocks are 
: obtained. ‘The isolated bluff on the adjoining parts of Secs. 25 
: ‘ and 36 shows numerous small exposures of white, cruntbling, 
non-calcareous sandstone, for a thickness of about 90 feet. Fig. 39 is a section from 
this bluff across the Wisconsin at Portage to the quartzite bluffs of Caledonia. The 
contour of the section is copied from Gen. G. K. Warren's report on the Fox and Wis- 


consin rivers. 


Nortu anD Soutu SEcTION In Scorr. 
Vertical scale 1,000 feet to the inch. 


586" GEOLOGY OF CENTRAL WISCONSIN. 


In Lodi and Westpoint, T. 10, R. 8 E., and T. 10, R.7E., rock exposures are very 
frequent along the bluff sides, but only a few prominent points can be described. 
Kingsley’s bluff, on the edge of the high country in the N. i. qr. of Sec. 26, and 8. E. 
qr. of Sec. 23, T. 10, R. 8 E., has the structure shown in Fig. 40. The succession of 


layers is indicated in the following, beginning above: — Feet 


I. Drift-covered slope with- 
out exposure........ 20 
II. Lower Magnesian lime- 
stone: in quarry; 
thin-bedded, top gla- 
ciated ..... site banaartite 5 
Ill. Drift- covered slope: 
without exposure ... 100 
IV. Madison sandstone: 
white, incoherent; on 
the edge of a flat 
bench in the hillside. 5 
V. Mendota limestone: yel- 
lowish, regularly bed- 
ded, fine - grained; 
containing: silica, 
44.57; alumina, 8.68; 
iron peroxide, 1.18; 
iron protoxide, 0.22; 
lime carbonate, 26.69; 
magnesia carbonate, 
17.97; water, 1.28= 
99.83; exposed in a 
small quarry ....... 10 
VI. Flat drift-corered slope 
without cxposure.... 40 
VI. Potsdom sandstone: 
white, fine - grained, 
loose; alternating 
with harder, yellow, 
calcareous bands; 
forming the edge of 
& bencliiscs soeassces 40 
VIII. Steep slope without 
exposure, the rock 
covered by sand from 
its own disintegra- 
WON. tee 6 saci ek se 90 


IMEBAGO, 


FY WIN) 
dee 


Fie. 39. 


above Lake Michzgait 


River 
rg 


» 


SCORNSUL 


RITER DETRITUS 


Vis 


PROFILE-SECTION ACROSS THE VALLEY OF THE WISCONSIN, AT PoRTAGE. 
Vertical scale, 400 feet to the inch; horizontal scale 11%4 miles to the inch. 


tever level 208 


The Mendota is quarricd again 
on the side of the hill just west 
of the depot ‘at Lodi, where it 
presents the typical yellow color’ 
and reddish stains, and is over- 
laid at the top of the hill by 


ARCHAEAN QUARTZITE 


THE LOWER SILURIAN ROCKS. 587 


white, incoherent Madison sandstone. Another and much larger Mendota quarry is on 
the south side of the bluff in the S. hf of Sec. 18, T. 10, R.8 E. Here are some ten 
feet of very regularly bedded, yellow, sandy limestone, the layers below heavy, above 
thin and shaly, with fine large impressions of Dicellocephalus Minnesotensis. 

. The very prominent isolated bluff on the N. KE. qr. of Sec. 20, T. 10, R. 7 E., shows 
the following section at its north end: 


LOWER MAGNESIAN, 


Feet. 
1. Grassy slope, without exposure ........ 6c cece ecceeeeeeeaceueencecccees 35 
2. Coarse, crumbling, brownish sandstone......00c.cccceee eeee cevececce... 2 
3. Slope without exposures .......... : Macieiiteanelg wee anges EPs O RS Weis Sea statiaeascas 18 

4. Brownish-yellow, rough, open-textured limestone, somewhat crystalline; contain- 

ing cavities with calcite crystals, numeorous red quartzite pebbles and green- 
SANG QIANG) waiss ge siiisuciny, Garedeeeescas dete ve cvig yee ads bvedenencos cd 10 

MENDOTA AND POTSDAM, 
5. Coarse, brownish sandstone, in perpendicular NGM 6S Aasieachiss xcs ayaa aleve 10 
6. Slope without exposure... 6.6... cece eeeeec eee cse cee eeee ceeesueseseeecs 85 
7. Friable, non-calcareous light-colored sandstone .......000..cccccceuececeecee. 15 
8. Sand-covered slope without exposure............ cece cece cb eeecececececec ce: 60 
Height above road at foot ..... 0.0... cece cee ececeeceeaneececnucesenececs 23: 
Fia. 40. 
Section 25 |Sectton 23 Séo 


Z ==EMADISON BEDS 
ee. Jon _@to._ | Faeselan | Fe Teter 
Yellow Lramestoze, 


<a 
ESE ENDOA BEDS 
ee 


SW. Direction of Section N27°E. 
SzcTion or Kinasizey’s Buurr, Lopr. 


NE 


Horizontal scale 1,0)9 feet to 1 inch. Vertical scale 20) feet to linch. Figures indicate altitudes 
in feet above Lake Michigan. 


The occurrence of a thin layer of non-calcareous sandstone within the Lower Magne. 
sian is unusual, but this is not an isolated instance. The limestone No. 4 is interesting 
because of its similarity to the rock from Eiky’s and Wood's quarries in the Baraboo 
valley, the accurate determination of whose stratigraphical position meets with soma 
difficulties, and because of its somewhat peculiar characters as compared with the 
ordinary Lower Magnesian, the base of which formation there can be no doubt that it 
marks. From a similar, and equally prominent bluff, on the south side of the samy 
section, the profile of Fig. 41 is taken, running across the Wisconsin to the quartzito- 
range of Merrimac. ; 

Gibralter Bluff is the name given to the bald cliff of St. Peters sandstone which sur- 
mounts the western end of a large outlying area of Limestone-capped bluffs, nm Secs. 17 


5838 GEOLOGY OF CENTRAL WISCONSIN. 


and 18, T. 10, R. 8 E. The area over which the sandstone is present is not more, prob- 
ably, than 40 rods in diameter, but the top of the bluff reaches an elevation of about 
630 feet above Lake Michigan, or upwards of 450 feet above the adjacent river; so that. 
it constitubes one of the most striking points in the scenery of this part of the valley of: 
the Wisconsin, rising far above all of the immediately surrounding country. Section [, 


Fie. 41. 

Ae 
Ks) 
fo 
Kare oH 
“ CEH 

EaaZ: ower UMagnesuan a 

4 A 

crams CSOT S 
C1 4 5 = * 
Moraine Drive 


S 
ess 


S "ey a 

yee ea tatetes 
x. SOMO 
SOSA 


= a 
WS S& ae 


SN 


Sack 4 


| 
| 
T 
| 
| 
! 
{ 


, Suction Aoross THE VALLUY OF THE WISCONSIN IN WE3T Porn AND MpRRIMAC. 


A B—Line of profile. Horizontal scale 9-10ths inch cquols 1 mile. Vertical scale, 400 feet equals 
1 inch. 


of Plate XXIII, and the north and south section attached to the Atlas Map of Area E, 
show its relation to the neighboring elevations. Fig. 42 is a rough diagrammatic sketch 
meant to give some idea of the character of the western face of this remarkable bluff, 
whose structure is further indicated by the section of Vig. 43, which.is drawn to a nat- 
ural scale. 

Fie. 42. 


Pg é 

a a eo OD) Oa ES. A OOO ™, 

aT saa i) C mel, CO me 
es oi, A ee eee ae 2 


ee 


_———_— 
oa eee 


SKEtTcu oF THE WESTERN Face or GrpraLter Buurr. 
Natural scale, 1: 3660. 


THE LOWER SILURIAN ROUKS. 589 


The western face of the bluff is precipitous in its upper portion for over 100 fect. At 
the top of the cliff is a rounded summit composed in part of glacial drift, but showing 
in one place a few broken layers of limestone (736), which are inthe proper position, and 
have the proper characters for the ‘‘ Buff’ or Lower Trenton limestone. ‘The cliff itself 
is made up of fine-grained, light-colored to nearly white, friable sandstone (735), which 
is composed of angular and subangular quartz grains, and possesses a hard, vitrified 
crust. In the uppermost parts of the cliff the horizontal bedding is distinct, the layers 
being quite thin; below, however, it is not plainly perceptible, whilst the whole has a 
sort of vertically columnar appearance, due to jomting. On the upper part of the long 


Fie. 43. 


i , Fallen Masses 


Pete So 
Potsdam Sandstone 
Nakural Saale 
—s880- 
Sporion oF GranaLTER BLurr. 
wooded slope below, are numerous very large sandstone masves, evidently fallen from 
the cliff. At the lower edge of this slope the Mendota limestone is partly exposed, as 
shown in Fig. 43, and below it the upper layers of the Potsdam, with intercalated cal- 
careous bands. To the right and left of the line of section, lower non-calcareous sand- 
stone layers are exposed, in low cliffs rising from the edge of the marsh. At the point 
F, Fig. 42, on top of a bare hill, only a few rods from the sandstone cliff, but at an 
elevation of 40 feet above its base, is an outcrop of much disturbed Lower Magnesian 
limestone. Numerous points on the surrounding bluffs also show limestone at 
elevations above the base of the sandstone 
Fro. 44. of the Gibralter cliff, proving the exist- 
ence of avery irregular upper surface to 
the Lower Magnesian. 


Bin Qua recite For the district west of the Wisconsin 
, river, where both topography and strati- 
graphy are so largely affected by the 
quartzite ranges, it will be most suitable 
=| to take up in order: the area south of the 
:} the quartzite ranges; that west of the 
“1 ranges; that within them; and that north 
=] of them. 

South of the quartzite ranges. Tig. 44, 


‘4 
ogee, 


Suction Acnoss THE VALLEY OF THH WISCON- 


SIN IN SOUTHEAST CALEDONIA. which is a section from the top of the 

Vertical scalo, 350 feet to theinch. Horizontal quartzite range near the northwest cor- 
y i a 3 

atela a mile te Ena ner of Sec. 2, T. 11, R. 8 E., Caledonia, 


to the top of a bluff in Dekorra, serves to give an idea of the structure of this part of 


the Wisconsin valley. ; 
On the flanks of the quartzite in western Caledonia, the Potsdam sandstone rises to 
altitudes apparently in the horizon of the Lower Magnesian, having then a slight ap- 


590 GEOLOGY OF CENTRAL WISCONSIN. 


parent dip southward, or away from the quartzite. This flanking sandstone is well ex- 
posed at Dorward’s Glen, on the north side of Sec. 18, where it is seen overlying the 
quartzite, as heretofore described and illustrated in Fig. 27, which is a section along the 
wall of the glen. This wall shows the following succession of layers, the numbers of 
the layers being the same as in Fig. 27:— 


Ft. In. 

VI. Yellowish, fine-grained, friable and heavily bedded sandstone ......... 14 8 

V. Pink, fine-grained and thinly bedded sandstone ........-+.-eeeeeee eee 4 8 
IV. Whitish and brownish, very coarse, heavily bedded sandstone, the con- 

stituent grains much rolled translucent quartz ....-.. 0 see ee eee eee 10... 

IIT. Similar to the last, but yellowish and finer grained .........-00. 0000008 17 4 

Th, Veryconrse; like: [Vics wider apeasiiwmensartee baer  aeuceeeee tees’ 5 10 
1, Bowlder-conglomerate, almost without matrix, made up of bowlers 

mostly angular, up to 1 foot in diameter; forms the stream bed...... 4 2 

Hei GEC cissewsGatdipeaiioeeumatimentwat sath eae Ua) HEEL eaare yee E 58.2«#8S 


In the town of Merrimac, Sauk county, sandstone at high levels continues to flank 
the quartzite. This sandstone may be seen at Parphrey’s Glen, on the N. E. qr. of Sce. 
22, T. 11, R. 7 E., where 20 feet of friable, brownish, Scolithus-bearing, regular-bedded 
sandstone is exposed, including thin layers of a conglomerate of red quar‘zite pebbies; 
on the N. E. qr. of Sec. 28, in a high, narrow bluff, which is partly detached from the 
quartzite; and again, lying directly against the quartzite. on the N. E. qr. of the 8. E. 
qr. of Sec. 20, T. 11, R. 7 E., where it forms a perpendicular cliff directly north of, and 
across the valley from, the Devil's Nose. The rock at this place is medium to fine- 
grained, friable, red-and-white-banded, purely silicious, and superficially vitrified, and 
contains throughout small pebbles of red quartzite, which are, however, aggregated 
niore numerously into two bands, the upper one 2 feet thick, and 25 feet below the 
summit, the lower one 10 feet thick and 59 feet below the summit. The whole height 
of the vertical cliff is 210 feet, the whole thickness of sandstone seen, 227 feet. The top 
of the sandstone has an altitude of 622 feet; its base, one of 397 fect, so that the cliff 
rises entirely across the horizon of the Lower Magnesian, as indicated by the occur- 
rences of that formation in the country to the south east and west. The sections of 
Plates XTX and XX show the structure and stratigraphical relations of this cliff. 

The isolated knob rising from the west bank of Otter creek, near the center of Sec. 
15, T. 10, R. 6 E., Sumpter, shows the following section: 


Foct. 
I. Madison sandstoue in small separated exposures; upper portions very highly 
ferruginous and firm; near the middle (1227) very fine- -grained, lighter 
colored and slightly calcareous; at the base white, fine- -grained, much 
induitated::vssyexey estes Tubheca ped Aged hick ecee ee vexechwylo: 4a wae 25, 
AL, Unexposed axis 9 2eey%edsess 42a tan canaaiebne deigainnnes noes wens isk ed cae 20 
III. Mendota limestone; yellow, shaly, in small quavry- OPeNING.........00.00 5 
DV WUMORPOSEd a ia. asceusclyre gyn ud nmneue sau winie s a dala seecnase Ne metide ahtindataline 10 
MV. Greensand layer ssiics bconun sen ea sctaceaian tunis a eabaecuibwen eed ¥eecetceen: 1 
Vi. Umex posed 2 sin tonee eaaitses ate ile wes een Centodeawadae ie paca cates : 5 
VII. Potsdam sandstone, upper layers fine, white, friable, banded with cleunesias 
layers, lower portions rising in an abrupt cliff from the bank of Otter 
creek; heavily bedded, non-caleareous, alternating hrown and white. . 140 
Heishtrot nobis «2a2's-ceciuiad aio weeeene dan eoavon aetoroacanmoved eens oe 
Alltibude of SUINMIL neds owielsieiea'e stad sy wtiba ve Sens altind seen std es 116 


PLATE, XX 


Gross Sectious in 
SAUUK COUNTY 


& 
K 
va 
o 
q 
+ 
fT 
a 
3 
I 
- 
=“ 
faa 
og 
© 
Dh 
a 
Q 
s 


of Scetion 


line 


Base 


SOUTH 


II 


South Quartzite Range 


NORTH 


EAST 


“yl 


Alsi 
af 


IN 


SOUTH 


oF il 
4 
< 


Jt 


ML 
“ 


3 Bok 
Spring Greew | 


TAILR.LE. 


és 
Zz be 
Winfield | Reedsburg 


THE LOWER SILURIAN ROCKS, 591: 


Fig. 45 is a section across the valley of the Wisconsin from the high bluff just west of 
Rowell’s Mill, N. W. qr. Sec. 17, T. 9, R. 6 E., Prairie du Sac, in a N. 68° E, direc- 
tion to the bluits back of Clifton, Dane county. 


Fig. 45, 
~~ Ww 


__floney SS 


SPEEA VEAL 


Section Across THE VALLEY oF TAE WISCONSIN, AT PRAIRIE DU Sac, 


Vertical scale 400 feet, 1 inch; horizontal scale 1% miles, 1 inch. 


The very bold and prominent blu® rising from the bank of the Wisconsin at tho 
mouth of Honey creek, Sec. 21, T. 9,R. 6 E., has already been cited as giving a mag- 
nificent section, and portions of this section age been given in some detail in the gen- 
eral descriptions of the formation. Abbreviated, the section is as follows: 


Ft. In, 
J. Lower Magnesian, in a vertical chff facing towards Honey Creek, including. 


subdivisions as given on page 552.11... cece eee e cece cece e eee eeene 52 5 
2. Madison, including: slope without exposure, 15 feet; white and brown sand- 

stone for the most part non-calcareous, 16.5 feet; slope without exposure, 

7 feet; coarse, non-calcareous white and brown sandstone, 2 feet; in all’ 40 5 


8. Mendota, including : slope without exposure, 33 feet; brown, earthy, very com- 
pact limestone with 34.15 per cent. of white clay, 1 foot; like the last, 
but with 26 per cent. of clay, 21g feet; in all............ ..0., 36 6 
4, Potsdam, including subdivisions as given on page 534; rising abruptly for Lb 
the Wisconsin..........+.- PRINS PARA AN aReds hae 4 aa ee caw dae 189 3 
Total height: of DW, «0.006 joes oes Bday cai 96 oie Seni  mvelk wea a anes 318: °7 
Altitude-of sumMiibssg.cciica onsale asivedanee tiaederenavaaieees ABE». 


Fig. 46 is a section across the valley of the Wisconsin, from the bluff just described, 
414 miles in a southeasterly direction to the bluff on Sec. 1, T. 8, R. 6 E. 
South of the quartzite 
Fie. 46. range, over all of T. 10, 
HONEY CREEK BLUFF R. 4 E., Honey Creek, 
the country is one char- 
acterized by numerous 
high, narrow, branching 
ridges, which are, for 
the most part, severed 
scons RR. into entirely separate 


Stzd Atak GY ____s hes 
Wise IT TEP acpi parts, showing frequent- 


; ly walls of bare rock, 
¥ CREEK , aes iz 
SECTION ACROSS THE al From Tlongy © and often rising in- 


; ; : ; to the horizon of the 
Vertical scale 400 feet to the inch; horizontal, 1% mi'es to the inch, Mendata. beds, mere 
rarely into that of the Lower Magnesian. In many cases, the sides of the ridges are 
worr into bold and fantastic forms of hare rock, whose very plain horizontal stratifica- 
tion renders the effect more striking. On the N. W. qr. of Sec. 17, T.10, 2.5 E., a 
narrow, precipitous spur from a higher bluff is worn entirely through, forming a natural 


is es Hadison Sandstone 
weeecene ee wUexdala Limestone 


592 GEOLOGY OF CENTRAL WISCONSIN. 


bridge of considerable dimensions. The arch is about ten feet thick, its under side being 
30 feet from the ground, and the width of the archway 30 to 40 feet. The rock is the 
upper portion of the Potsdam, containing the usual calcareous bands, and is highly 
charged with small pebbles of red quartzite. The bases of the cliffs on both sides of the 
valley of that branch of Honey ereek which follows the west line of T. 10, R. 5 E., are 
made up of a layer 50 feet thick. of white, non-calcareous sandrock, which is rendered 
very prominent by its strong contrast in color with the darker hued layers at higher 
levels. Its upper surface appears to be about 155 feet below the Mendota base, and the 
layer is evidently the same as seen at the foot of the great bluff at the mouth of Honey 


creek. 


Fria. 47. 


40’ Bench no panies ; 


faci 


wen yee---- oe Limestone nannaneens) a aki a 


Section oF RivEFR BLUFF NoRTH OF SPRING GREEN. 
Iforizontal scale, 225 feet to the inch; vertical scale, 100 foet to the inch. 


The Mendota is quarried on the side of a steep ravine in the river bluffs immediately 
north of Spring Green, N. W. qr. Sec. 3, T. 8, R. 4 E. The point of the blutf at the 
mouth of this ravine shows the profile and section as indicated in Fig. 47. The succes- 


sion of layers, including the quarry across the ravine, is as follows: 
: Feet. 
I. Lower Magnesian limestone: in numerous small, rough-weathered expo- 


sures; upper layers concretionary; about midway ot the measurement, 

close-textured, white, crystalline, with chert and a few dolomite-lined cav- 

ities; at 20 feet above base, sandy, and including red quartzite pebbles; 

lowest layers seen, brownish, concretionary, rough-surfaced, with chert and 

facings to the layers of stalactitic carbonate; at base a greensand layer; 

exact junction with the next formation s@en...... sss sce e cee ae eee wees 65 
II. Madison sandstone: in perpendicular ledges, including: white, indurated 

sandstone, with red quartzite pebbles, 13 feet; loose, white, cross-lami- 

nated sand, 7 feet; unexposed, about 15 feet; in all ..............00... 45 
Il. Mendota beds: including: unexposed, about 25 feet; thin, crumbling, lime- 

stone layers, 51g feet; yellow calcareous shale 114 feet: seven very regu- 

lar, heavy, yellow, limestone layers, with a 6 inch parting near the hase, 


THE LOWER‘ SILURIAN ROCKS, 593 


, and capable of being split into thin slabs (1292) 104 feet; unexposed, 10 
feet; brownish, red stained, porous limestone, 2 feet ; Inallahout....... 45 


with sand, 84 feet; in all about..............ccec cece cece cee eee. 110 
BLiahd OF Dale vata dance cas ednhdaiahets item saa een oars ace, “960 
Altitude of summit....... 0... cece cee c ec cee cece cceeeeeee eA oe 465 


West of the western end of the quartzite ranges. The sandstone lying at high levels 
about the quartzite, in the eastern part of the town of Westfield, T. 11, R.4E., is, without 
doubt, both in and above the horizon of the Lower Magnesian limestone, i" indicated 
by the exposures of that rock to the westward. Half a mile south of the Mendota 
quarry, on the point of the ridge in the E. hf. of Sec. 10, the road crossing the same 


Fia. 48. 


Map anp SEcTION SHOWING THR RELATIVE Positions oF E1xy’s LIMESTONE, AND THE SURROUND- 
Ing Rock ExposvReEs. 


Horizontal scale 2 miles to 1 inch. Vertical scale 40) feet to1 inch. A BC D, line of section. 


ridge eastward is-cut into brown, friable sandstone, having the proper position and 
character for the Madison beds. Continuing eastward, the road rises, the ground be- 
coming full of the cherts characteristic of the Lower Magnesian, but on the southeast: 
corner of Sec. 10, non-calcareous, indurated sandstone is again in place, at an elevation 


Wis. Sur. — 38 


594 GEOLOGY OF CENTRAL WISCONSIN. 


of 80 feet above the Mendota in the quarry above named. From this point, sandstone 
continues in place as the road ascends through the N. W. qr. of Sec. 14 to the center of 
that section, and beyond, reaching an elevation of 250 feet above the Mendota base., 
The same thing is to be observed on the road ascending through sections 2, 3 and 11; 
whilst on the eastern slope of the ridge, towards the valley within the quartzite ranges, 
sandstone is constantly seen with a great total thickness, lying within and above tho 
Lower Magnesian horizon. 

Within the quartzite ranges. In the town of Caledonia, Columbia county, more or 
less of Secs. 27, 28, 29, 30, 31, 32 and 33, T. 12, R. 8 E., lie between the converging 
ranges, which unite on Sec. 27. The area thus included appears everywhere to be un- 
derlaid by sandstone, which is of considerable thickness. In the northern portions of 
Secs. 28, 29 and 30, the altitude is 500 to 550 feet, as great as that of the northern 
quartzite range, and wells pass through many feet of sandstone, one near the north 
line of Sec. 30 penetrating 170 feet of that rock. 

Along the east line of Sec. 25, T. 12, R. 7 E. in the town of Greenfield, the 
high sandstone-filled country,just described as occurring on the south flank of the north 
quartzite range in Caledonia, breaks down suddenly, in a vertical cliff 135 feet high, at 
the foot of which a slope continues the descent to the Baraboo river, through an 
additional vertical distance of 275 feet, and a horizontal distance of two miles. In 
the northern part of Sec. 25, T. 12, R. 7 E. on the south flank of the northem 
quartzite range, and within half a mile of this cliff, is a small lmestone quary. 
Fig. 48 gives a, map and section showing the relative positions of this limestone and 
the other rock exposures in the vicinity, The whole thickness of limestone exposed 
is about 25 feet, the layers running from 1 to 6 inchets, but much displaced, and cov- 
ered by debris. The rock (1251) is rough-textured, brownish-yellow, and non-arena- 
ceous, carrying many small cavities lined with calcite crystals, 4s also much greensand 
in course grains; these much more abundant in the lower layers, at the base of 
which is a regular greensand layer such as is often to be seen at the base of the 
Lower Magnesian. The composition of the limestone is indicated by the following 
analysis, made gratuitously for the survey by Mr W. A. Hover at the State Uni- 
versity: lime carbonate, 51.61; magnesia carbonate, 38.51; silica, 5.66; alumina and 
iron oxide, 2.26; water, 0.40. The uppermost layer in the quarry is finely glaciated, 
and casts of fossils are found throughout. The following have been identified by 
Mr. R. P. Whitfield, from a collection made at this place by the late Prof. James 
Ti. Eaton: Stromatopora, und. sp.; Orthis Barabuensis? ; Metoptoma, n. sp.; Mac- 
lurea Swezeyi, n. sp.; Holopea, n. sp.; Illenus antiquatus, n. sp.; Dicellocephalus 
Barabuensis, n. sp. Immediately above the quarry, the grouni rises rapidly to 
the northward for 60 feet, without exposure; becoming then nearly level on top of 
the quartzite range. A short distance along the road which ascends to the eastward, 
are small exposures (‘‘”’ of the map of Fig. 48, corresponding in elevation to a” 
of the section) of brownish, non-caléareous, sandstone, 20 feet higher than the top 
of the quarry. Down-hill, a short distance to the westward, are ledges of finc- 
grained, friable, light-colored, non-calcareous, sandstone (746) coming immediately 
below the quarry layers, some ten feet in height; whilst still farther west, sandstone ex- 
posures are seen at different levels (b, ¢, of Fig. 48), down to 140 feet below the quarry 
base, but not continuously. The base of the sandstone cliff lying half a mile southeast 
across the intervening valley, is 75 feet above the top of the quarry layers. Its lower 
layers (748) are medium-grained, very friable, brownish, banded sandstone, composed of 
very much rolled quartz grains; further up, some bands of bright red sandstone are in- 
cluded, whilst: near the summit (740, 750) are a number of rapidly altemating, red, 
white, and yellow bands of quite fine-grained and saccharoidal sandstone, the whole 
thickness being 135 feet. The determination of the true stratigraphical position of tho 


‘THE LOWER SILURIAN ROCKS. 595 


Eiky lLmestone meets with considerable difficulties, and has quite important conclusions 
depending upon it. This subject is discussed briefly in another place, in connection 
with facts from other localities bearing on the same conclusion. It is only necessary 
to say here that the fossils from this limestone are regarded by Mr. Whitfield as cer- 
tainly not lower than the Lower Magnesian, and that, if we receive this reference, it 
Gecomes necessary to believe that the surrounding Ingh-level sandstone, apparently 
without doubt of the Potsdam series, had been extensively eroded before the deposition 
of the limestone, and that the latter forms merely a nest lying upon the eroded surface 
of the older sandstone, as indicated by the dotted line of Fig. 48. 

Sandstone is quarried, of excellent quality, at several places near Baraboo. One of 
these is on the south side of a ridge on the N. E. qr. of Sec, 1, T. 11, R. 6 E., just east 
of the village. The quarry here has a six-feet face, showing heavy and regular beds of 
moderately fine-grained, white, non-calcareous sandstone (1230), which is marked with 
fine brownish lamination lines, is made up of glassy, subangular quartz grains, and 
splits easily into thin slabs. Another and much larger quarry is opened on the 
“‘stossed "’ point of a ridge, southwest of Baraboo, on the N. E. qr. of Sec. 2, T. 11, R. 
6 &. The end of the ridge is planed and scratched on a large scale. The total thick- 
ness seen is about thirty feet, the sandstone being white, fine-grained, firm, and obtain- 
able in large, well-shaped blocks. In places, a net-work of thin quartz seams is notice- 
able. This stone, as well as that quarried at other points in the Baraboo valley, is an 
unusually good sandstone to come from the Potsdam series, much of which is so loose 
and friable, or badly colored, as to have no value as a stone for building. 


Fie. 49. 


RP 
Sere 
ener 
Oe eage BIR ORE 
SBN, SEP 622 
MIX 


iron OQ = Sandstine’"~____ Shi ets falls 
Ks ex ‘ SNe Lower Len ee 
ee Lguegtone sae va 


LEER 


i 
( f = 
SP DORE , Didureded Sand stone 
er, 


ee ere 


RS (eae 


[ EEN 
| cS 
| RR Ze 


Map anp SEITION Suow1ne THE ReELative Posrttons oF THE Rock OUTCROPS AT Woop’'s, NUAR 
Barazoo. 


On the N. W. qr. of the S. W. qr. of Sec. 10, T. 11, R.6 E., on Mr. Joseph W. 
Wood's land, is a small quarry, on the point of a ridge, of limestone closely like that at 
Biky's quarry in Greenfield. The rock (1260) is brownish, porous, rough-surfaced, and 
minutely crystalline, with, in places, a conerctionary structure, and contains only 9.03 
per cent. of insoluble ingredients, which are aluminous rather than silicious. In places 
an indistinct columnar, coral-like structure is noticeable, but no undoubted fossils were 
observed. On the south face of the same ridge, and on the south line of Sec. 10, is a 
long ledge of fine-grained, reddish-brown sandstone ( 1262), which is composed of rough- 
surfaced, subangular grains of glassy quartz, and contains many pebbles of red 
quartzite. numerous Scolithus borings, and fine, large impressions of Dicellocephalus 


596 GEOLOGY OF CENTRAL WISCONSIN. 


Minnesotensis. The top of this sandstone ledge is on a level with the base of the lime- 
stone in Wood's quarry, directly beneath which a small exposure of smilar sandstone is 
seen. South of the sandstone ledge, on the south line of Sec. 10, as shown on the map 
and section of Fig. 49, is the valley of Skillet’s creek, and south of this, again, rises the 
southern quartzite range. About 1s mile north from Wood’s quarry, and 40 feet be- 
low its base, in the high bank of Skillet’s creek, is an exposure of yellowish, rough-snr- 
faced limestone (1263), which closely resembles the typical Mendota rock, leaving on 
solution 23.68 per cent of a very fine aluminous residue. The exposure is somewhat 
broken, but a thickness of about 15 fect is seen. At the foot of the bank, sandstone is 
in place. This yellowish limestone would appear to be the rock alluded to by Dr. B. F. 
Shumard in Owen's Geological Survey of Wisconsin, Iowa and Minnesota, p. 522, as 
occurring ‘in the bank of a small stream 3{ths of a mile south of the Baraboo.” He 
refers it to the “ encrinital bed of F. I,” the same as the Mendota horizon of the writer's 
reports. It will be noticed that the quarry limestone, the sandstone carrying Scoléthus 
and Dicellocephalus, and the yellowish limestone on Skillet’s creek, have the proper re- 
lations and characters for the Lower Magnesian, Madison and Mendota beds. The up- 
per limestone has just about the same altitude as that at Eiky’s quarry, and appears 
beyond question to belong to the same horizon. Below the Mendota normally there is 
always found loose, fine-grained sandstone, with some calcareous matter, and narrow, 
brownish, calcareous bands, this character holding for a thickness of 40 to 60 fect. Be- 
low the lower limestone on Skillet’s creek, however, we find no such layers, but at the 
falls, a few rods down stream, are seen fifteen feet of very regular beds of much in- 
durated, entirely non-calcareous, sandstone having a slight slant southward, and bear- 
ing no resemblance whatever to the ordinary infra-Mendota layers. Do the two lime- 
stone layers, with the intervening sandstone, form a patch lying upon an eroded surface 
ot much older sandstone, represented by the indurated rock at the falls, as suggested 
already in the case of the limestone of Eiky’s quarry ? 

A short distance northeast of Devil's Lake, on the east linc of the N. FE. qr. of Sec. 
18, T. 11, R.6 E., on the south flank of a projecting point of the south quartzite range, 
are numerous large masses of fossiliferous sandstone, evidently near home. The rock 
is medium-grained, friable and brownish, containing many Scolithus markings, and 
other fossil fragments, chiefly of trilobites, among which casts of large cephalic shields 
of Dicellocephalus Minnesotensis are most readily made out Prof. A. Winchell iden- 
tified and described also the following, in specimens from this place, sent him a number 
of years ago: Orthis Barabuensis; Stranarollus (Ophileta) primordialis; Pleurotoma- 
ria? advena; Dicellocephalus Pepinensis; Ptychaspis Barabuensis. The altitude at 
which these sandstone masses occur is 540 to 560 feet, or 70 to 110 feet above the lime- 
stone at Wood's and Eiky’s quarrics, and 110 to 155 feet above the Mendota-like rock 
in the banks of Skillet’s creek, Sec. 10, T. 11, R.6 E. Across the ravine on the north 
side of which these fossils are found, are bowlder-conglomerate and sandstone beds seen 
lying directly upon the quartzite, as previously described and figured. These occur at 
the north point of the east cliff of Devil's Lake, a north and south section through 
which is given on Plate XIX of this volume. The summit of the cliff, which for some 
distance is a mere crest, rises rapidly southward, horizontal sandstone layers flanking it 
on the side away from the lake, and rising with it to an altitude of over 600 feet. The 
sandstone cliff immediately opposite the Devil's Nose, shown also in one of the sections 
of Plate XIX, has already been described as extending between the altitudes of 391 
and 622 feet, or from 50 feet below Wood's quar y, to 175 feet above it, and as ex- 
tending far above any apparently possible horizon of the Lower Magnesian. The same 
appears to be trae of the sandstone in all of the region about Devil's Lake. At the 
south end of the west bluff, for instance, are horizontal sandstone ledges at an altitude of 
over 700 feet. 


PLATE, XXIV 


outh sections in 


DANE COUNTY 


North and s 
rizontal Scale Linch =+4imiles. Vertic 


; | 


IN 
i 
Na 
HN 
HIN 

Na 

iN 


a 
N 


Ve 


Pree 


T 


al Scale, linch = 1000 feet 


s—level of Lake Michigan 


; | 
E | 
wn o ' 
Lk: 3 
+ ~ = 
ns 
% F 8: 
ie : $8 
é s 
“ * 
4 


Base line of Scetion: 
3 + 


Ho 


ARE 
Mendota 


Ore. 


— 
——| 
Pots dam 


THE LOWER SILURIAN ROCKS. 597 


On the eastern side of the north and south quartzite range in Westfield, T. 11 R. 4 
E., in the eastern row of sections of that town, sandstone similar to that just described 
occurs with a considerable thickness. Certain layers at high levels are peculiar in being 
charged with the red and brown oxides of iron, which are at times in quantity sufficient 
to constitute an iron ore. This ore is to be seen in a pit on F. W. Schulte’s land, 8. W. 
qr. of the 8. E. qr. of Sec. 13, with a thickness of about10 feet. It is plainly stratified, 

; and is a more or less sandy admixture of the red and brown oxides of iron, the former 
occasionally showing metallic surfaces, and greatly predominating. The inner part of 
the purer fragments presents a dark-colored, compact appearance, yielding a red streak. 
Occasional stalactitie portions are to be seen, and some of the layers are almost without 
iron oxide, consisting then of greyish sand with some greensand (glauconite) grains. 
The following analysis (1269) is from a sample averaged from the ore pile outside, and 

. covers all degrees of richness except the nearly pure sandstone layers: Silica, 19.59; 
alumina, 3.60; iron sesquioxide, 70.24; manganese oxide, 0.54: lime, 0.76; magnesia, 
0.04; phosphoric acid, 0.17; sulphur, a trace; water, 5.19 = 100.33: metallic iron, 49.30. 
Much of the ore of the pile is better than shown by the analysis, which itself represents 
an ore of some value. The locality is worthy of close investigation, the indications be- 
ing that a considerable quantity of a good ‘soft hematite’ might be obtained. 

North of the quartzite ranges the Potsdam is everywhere the surface rock, making 
frequent exposures, many of which are very interesting, but the space is not available 
for their description. 


Dane County. 
(ATLAS PuaTe XIII. Anza D.) 


Dane is one of the largest counties in the settled portions of the state, having a total 
area of 1,237.84 square miles. Its shape is that of an almost perfect rectangle, the 
northwestern corner of which is cut off by the Wisconsin river. From north to south it 
measures 30 miles, including towns 5, 6,7, 8 and 9; from east to west, 42 miles, includ- 
ing ranges 6, 7, 8, 9, 10, 11, 12; thus embracing 34 entire townships and one fractional 
one. The western tier of townships, range 6, is included within the arca of the lead 
region, and will be found described in the report of Mr. Moses Strong. The balance of 
the county has an area of 1,080 square miles. 

Dane county has a position just about midway in the width of the state, its eastern 
line being 57 miles from Lake Michigan, and its western, 63 miles fyom the Mississipp‘. 
Its southern line is 24 miles north of the Illinois state line, 

With the exception of an area of about 120 miles, in the northwest, that crains towards 
the Wisconsin, the drainage of the whole county is shed southward and eastward 
through different channels into Rock river. This result is due to the fact that nearly 
the whole area lies on the south side of the limestone dividing ridge that limits the val- 
ley of the Wisconsin on the south. This ridge enters the county on the north side of 
the town of Vienna, trends thence south of west across Dane, and then, bending more 
to the south, passes through the adjoining portions of Roxbury, Berry, Springfield, Mid- 
dleton and Cross Plains, and leaves the county on the west side of the last named town. 
The ridge has a general altitude of 500 to 600 feet, and a width sometimes of a whole 
township, but on both sides is rendered quite irregular by erosion, the nortkern side 
especially projecting in long, ‘bold points into the valley of the Wisconsin. The summit 
of the ridge is largely occupied by prairie— a continuation of the prairie belt that char- 
acterizes the same ridge in its passage across Columbia county — and has always, except 
in Middleton and Cross Plains, the Lower Magnesian as the surface rock. In these 
towns it rises into the St. Peters and Trenton horizons. In the northern portions of 
Middleton, Cross Plains, Berry and Mazomanie the dividing ridge is cut entirely through 
by a valley half a mile toa mile in width, 18 miles in length, and 100 to 200 feet in 


Bus GEOLOGY OF CENTRAL WISCONSIN. 


depth — which connects the ground about the west end of Lake Mendota with that 
bordering the Wisconsin. The highest point of the valley is 85 feet above Lake Men- 
dota, and in it are streams running in either direction. Black Earth river — the larger 
of the two — which runs westward to the Wisconsin, heads within three miles of Lake 
Mendota, and at only 80 feet above its level. It has been suggested by Gen. G, K. 
Warren in his report on the Fox and Wisconsin rivers, that this valley indicates a former 
outlet, westward to the Wisconsin, of the Madison system of lakes. It is not impossible 
that such an outlet may have existed, but there is nothing in the structure of the region 
to show that we have here anything else than a case where two systems of erosion have 
approached one another until the dividing ridge has been partially broken down. South 
of Black Earth river the high ground comes in again, and, taking a turn westward to 
accord with the changed direction of the Wisconsin river, passes out of the district. 

To the north and west, in the towns of Dane, Roxbury and Berry, the dividing ridge 
presents a very abrupt escarpment, which projects in long bold points into the valley of 
the Wisconsin. Beyond the escarpment the low ground is occupied by numerous out- 
lying patches of the high country of varying sizes, similar to those already described as 
occurring in the adjoining towns of West Point, Lodi, etc., in Columbia county. 

Southward from the dividing ridge there is a general and much more gradual descent to 
the south and east, conforming with the descent in those directions of the underlying 
strata. West of a line drawn centrally north and south through the county, the general 
descent of both the country-surface and strata is southward only. East of such a line, 
the line of greatest descent veers more and more to the eastward, until along the north- 
ern part of the east line of the county, it is almost wholly in that direction. The drain- 
age system corresponds with this general structure. In the northeast, in the towns of 
York, Bristol, Sun Prairie and Medina, the drainage is eastward into Waterloo creek. 
Farther south, in Cottage Grove, Deerfield and Christiana, the drainayre is also eastward 
towards Koskonong creek, which itself has a general southerly direction. In the central 
part of the county the drainage along the Catfish valley is in a southeasterly direction, 
whilst farther west, the Sugar river system runs almost exactly southward. In minor 
detail, of course, the directions of the streams are due to other causes. 

The Catfish valley, with its chain of lakes, is the central topographical feature of the 
county. The head-waters of the Catfish are a number of small streams which rise on 
the south side of the divide in Springfield, Dane, Vienna and Windsor, and conte to- 
gether in the southern part of the town of Westport. From here to the junction with 
Rock river, the valley has a southeasterly course, a length of 27 miles, and a width from 
high ground to high ground of from 4 to 9 miles. Its surface lies generally at from 250 
to 300 feet above Lake Michigan, but is quite irregular, the irregularity being largely 
due to considerable accumulations of drift, but also to the occurrence of small rock out- 
liers, and to the projection into the valley on either side of low rock ridges. These have a 
general northeast southwest trend, and tend to divide the valley into more or less sepu- 
rate, parallel, cross-valleys, which are very marked, and are undoubtedly to be attrib- 
uted to the movement over the country of glacier ice, to which cause also is to be assigned 
the lincar nature of the topography of all of the eastern part of the county, The several 
lakes of the region about Madison are expansions of the Catfish into such cross-valleys, 
the ridges between which here run entirely across the main valley, though not formed 
throughout of rock material. Lake Mendota occupies two of the cross-valleys, partially 
separated by the low ridge of Picnic point and McBride’s point. Lake Monona lies in 
one similar valley, which extends far to the southwestward, and holds also the smaller 
sheet of water known as Dead Lake, or Lake Wingra. Further south, the glacial move- 
ment had a more nearly southerly direction, and the directions of the cross-valleys cor- 
respond, There is no prairie in the Catfish valley proper. Along the head streams in 
Springfield, Westport and Burke, the marshes are of consideralle extent. 


F THE LOWER SILURIAN ROCKS. 599 


Immediately east of the Catfish valley the country lies higher, but soon sinks 
again, descending with the eastward descent of the strata, this part of the county run- 
,ing from 240 to 400 feet in altitude. Here we find a gently undulating surface, the 
ridges having a flowing contour, and all topographical features showing the linear di- 
rection induced by the glacial movement. Numerous narrow and linear marsh strips 
are found on the lowest portions, whilst prairies of some size occur on the highest, be- 
ing for the most part underlaid bv limestone. 

On the west side of the Catfish valley is a high and hilly belt of country from 400 to 
600 feet in altitude, which extends southward from Middleton, along the adjoining 
parts of Verona, Fitchburg, Oregon and Montrose. Crossing the divide in the Sugar 
river valley, we find ourselves in an entirely different looking country — one where all 
irregularities are due solely to subaerial erosion, where the ridges are high and bold, and 
the branch valleys ramifying, narrow, and steep-sided. The two main branches of 
Sugar river separate on the southern line of the town of Montrose, one setting back in 
a more westerly direction than the other. Both have numerous branch-streams, each 
of which has its steep-sided flat-bottomed ravine. Here the ridges rise to 500 or 600 feet 
in altitude, and are nearly aiways occupied by fertile prairie, whilst the valley bottoms 
stand at 300 to 400, are wooded with a growth of small oaks, and show, rarely, narrow 
strips of marsh. 

As to fertility of soil, Dane ranks as one of the best counties in the state. The 
prairies, found for the most part on the higher ground, owe their especial fertility, usu- 
ally, to the underlying limestone, but the low ground of the Catfish valley, though often 
on the upper sandy layers of the Potsdam series, has everywhere an excellent soil, which 
it owes to alluvial depositions, or to the drift materials. A poor soil is seen only on the 
low grounds adjoming the Wisconsin river, where the sand comes from the Potsdam 
sandstone. The St. Peters sandstone rarely affects the soil over any considerable aren. 
East of the drift limit. it is buried beneath drift materials, whilst west of the same line 
it appears only on the steep sides of ravines. The prevailing timber of Dane county is 
small oak, occurring in patches or groves, constituting what are known as *‘ oak open- 
ings.” 

The Dane county list of geological formations includes nearly the whole Wisconsin 
series. The Cincinnati and Niagara, however, occur only on the Blue Mounds, and in 
that portion of the county that is not included in the Central Wisconsin district. 

The Archean does not come to the surface in Dane county, vut the Artesian borings 
at Madison reach it at some 800 feet below the surface, and 480 feet below the level of 
Lake Michigan, at which point a dark-grey felsitic rock is struck. Into this one of the 
wells penetrates for 187 feet, reaching a point 667 feet below Lake Michigan, and 82 
below the level of the sea. The Potsdam sandstone comes to the surface along the val- 
ley of the Wisconsin, and along the bottoms of a number of smaller tributary valleys in 
Dane, Roxbury, Berry and Cross Plains. It is also at the surface over a considerable 
area, at the head of the Catfish valley, and in the bottoms of branch valleys, in Spring- 
field, Westport, Windsor, Burke, etc.; but in all this area only the uppermost layers of 
the formation are at surface. The Mendota and Madison beds arc the surface rocks over 
a large portion of the Catfish valley, reaching from the south side of Lake Monona to 
the south side of Lake Kegonsa. These layers are at surface along some of the valley- 
bottoms of northern Middleton, southern Springfield, and adjoining towns, as also on 
the flanks of the higher ground and outliers that border the valley of the Wisconsin. 
The total thickness of the two layers in Dane county is about 70 feet. The Lower Mag- 
nesian limestone forms the upper part of all the dividing ridge of the north part of the 
county. It fo ms, also, the flanks of the high ground on both sides of the Catfish valley, 
whose hottow + becomes in the region south of Lake Kegonsa. It comes up again un- 
derneath tnw ov marshy ground that borders Waterloo creek in York, Bristol, Sun 


600 GEOLOGY OF CENTRAL WISCONSIN. 


Prairie and Medina, its eastward descent having carried it here far below the altitudes 
at which it is found on the west side of the county. It lies also at the bottom of the 
valley of Sugar river and its numerous branch valleys, crowns the outlying bluffs of the 
Wisconsin valley, and occurs also in several small isolated patches, within the Potsdam 
area of the Catfish valley. The thickness of the Lower Magnesian in Dane county seems 
rarely to be more than 80 feet, whilst its very irregular upper surface brings it often into 
the horizon of the next formation above. The St. Peters sandstone occupies a large 
tract on the east side of the Catfish valley, where it appears to be never more than 50 
feet in thickness. It is found, also, forming a narrow band around the Trenton areas 
of York, Bristol and Windsor. West of the Catfish valley it occupies much of the high 
ground forming the divide from the valley of the Sugar river. In the Inst-named valley 
and its branches the St. Peters forms the lower part of the bluff sides, having its full 
thickness of 80 to 90 feet. It occurs also in several detached areas in the high country 
north of Black Earth creek. The Trenton limestone occurs in detached areas, mostly of 
considerable size, capping the high ground on both sides of the Catfish valley. Some of 
the areas, however, are quite large, covering one or two townships, as in Middleton, 
York, Christiana and Albion. In Springdale and Primrose the narrow ridges between 
the streams, carry the whole thickness of the Trenton limestone, being at times capped 
by the Galena. For the most part, the Trenton areas of Dane county include only the 
lower part of that formation. The Galena limestone occurs only as a capping on tho 
higher parts of the ridges of Springdale and Primrose, and in two or three small areas 
in Christiana. 

Cross sections for Dane county, both north and south, and east and west, are given 
on Plates XXIV and XXV, showing both the surface contour, and the succession and rela- 
tions of the several strata. Two other sections through the county, drawn on a larger 
scale, will be found attached to Plate XIII of the Atlas. ‘hese sections, with the col- 
ored map, render unnecessary any further general descriptions. 

On the east side of the county the lower or Buff portions of the Trenton shows in nu- 
merous quarries, many of which yield a good building stone. Amongst many quarries 
we may list the following: N. E. qr. Sec. 25, York; N. E. qr. Sev. 26, Medina, a large 
quarry with a 12 feet face; on Secs. 29, 35 and 36, Deerfield; N. E. qr. Sec. 22, N. E. 
qr. Sec. 24, and N. E. qr. See. 23, Christiana, the last one showing 15 feet of regular, 
heavy layers; N. W. qr. Sec. 2, N. E. qr. Sec. 15, S. W. qr. Sec. 22, N. W. qr. Sec. 27, 
Albion; 8. E. qr. See. 30, Dunkirk, where there is a 15 feet face; 8S. W. corer Sec, 3, 
N. W. qr. Sec. 4, N. E. qr. Sec. 10, where there are 10 feet of even, heavy layers, S. E. 
qr. Sec. 18, N. E. corner Sec. 14, N. W. gr. Sec. 35, 8. E. qr. Sec. 36, Pleasant Springs; 
Sec. 4, Cottage Grove; N. W. qr. Sec. 14, N. E. qr. Sec. 23, Sun Prairie; N. W. qr. 
Sec. 17, N. E. qr. Sec. 30, and in the north part of Sec. 34, Bristol; 8. E. qr. Sec. 14, 
N. E. qr. Sec. 23, Windsor; 8. W. qr. Sec. 2, 8. W. qr. See. 26, N. W. qr. Sec. 35, 
Burke; N. E. qr. Sec. 14 and N. E. qr. Sec. 11, Windsor. 

The quarry on the N. W. qr. Sec. 35, Pleasant Springs, is on the western edge of 
a Trenton area, and shows 15 feet of the lowest part of the formation. The upper 
layers are thin, whilst the lower six feet are taken up by two very heavy firm layers, 
between which is a persistent thin seam. 2 inches thick, which affords large regular 
paving slabs. The limestone is yellowish, much marked by dendritic oxide of man- 
ganese, and is easily trimmed into smooth blocks. The thin upper layers show numer- 
ous nests of erystals of limonite, pseudomorphous after pyrite, as also large casts of 
orthoceratites. The top layer is glaciated, the striae running almost due youth. At the 
bottom of the quarry, the junction with the St. Peters is exposed. A woll near by 
is 58 feet in the latter formation. The quarry is an old one, having been opened 22 
years, durmg which time 4,000 cords of stone have been removed. 

The quarry in the north part of Sec. 4, Cottage Grove, shows 20 feet of thin, and 


ich = LOO0 feet 


ns—_level of Lake Michigan 


stand. west sectious iu 


DANE COUNTY 


Ka 
neh s-bimiles. 


izontal Seale li 


Vertical Scale lin 


5 
St.Peters 


Base line of Sectio 


1 
=| 
Potsdam 


R.D. Irving, 1876. 


ia Se 
Westport 


II 


one Preerie 


Midd let 


a Se ee 


Valley of Koshkonong Cr. 


ee 
(TELLLELTIPLETET PLETE ee 
VACPATET HTRTALLLTSLTUETTUCTTETTLTTU LTT TET TTL eg 


WILTALYD 


WHLED? 


A —— 
Peers (EC ET ULES PTD U ALLPORT OPTE 
UREA HTAMTHTRENMT MUTT 


a : 0 
Deerfield 


i z 
Middleton 


Cross Plains 


PLLTPEET 
ESremirnnren 


TAPPER 
Ciennntnnte ERE 


THE LOWER SILURIAN ROCKS. 601 


very even-bedded, close-textured, yellowish, limestone, which is much marked by dend- 
ritic manganese oxide, and contains the following fossils: Petraia corniculum, Stropho- 
mena alternata, a small Orthis, a Rhynconella, Cypricardites ventricosa, Trochonema 
umbilicata, Helicotoma planulata, and fragments of small orthoceratites. The fossils 
are casts only. 

The quarries on Sec. 23, Sun Prairie, show in all a thickness of about 20 feet, the 
upper layers of which are thin, shaly, and bluish in color, and appear to belong to the 
“Blue” beds, whilst below there are heavy regular layers of buff-colored limestone. 
Immediately beneath the shaly layers are found layers of a very close-textured, purplish 
brown, chonchoidal fracturing rock (698), carrying Columnaria alveolata. From the 
buff layers, the following fossils were obtained (697, 698): Petraia corniculum, Orthis 
trieenaria, Strophomena camerata, Cypricardites ventricosa, very large casts of the ex- 
terior of Trochonema umbilicata, Raphistoma lenticularis, a Muchisonia, Orthoceras 
vertebrale, Ortho.eras anellum, Gyroccras duplicostatum, n. sp., Oncoceras pandion, 
and crinoidal stems. A strong lime, hard to slack, is made here from the buff beds, but 
the stone is usv.d chiefly for building purposes. 

At the large quarries on the prairie, in the north half of Sec. 34, Bristol, are exposed 
of the Blue Jumestone about 8 feet, of the Buff about 10 feet. The Blue beds show a 
dark bluish-gray rock (703), with a flinty-textured matrix, in which are scattered numer- 
ous minute strings and patches of calcite. The layers of this rock are about one-half to 
there-fourths inch in thickness, very rough-surfaced, and show numerous obscure im- 
pressions of fossils, of which two brachiopods, Rhynconella and Strophomena, appear to 
be most abundant. Between these layers are very thin, regular, fragile, dark brown 
shaly layers, on which are fine, black, graptolite-like markings. The rough-surfaced 
blue layers contain: silica, 7.03; alumina, 2.21; carbonate of lime, 84.02; carbonate of 
magnesia, 5.83; iron peroxide, 0:83; iron protoxide, 0.39; water, 0.61 = 100.42. The 
Buff beds below are regular heavy layers of yellowish close-textured limestone, includ- 
ing some of a dark purplish brown, chonchoidal-fracturing rock, like that already men- 
tioned as seen on Sec. 14 of the town of Sun Prairie. The buff-colored rock (704), from 
directly below the junction with the Blue, contains: silica, 4.45; alumina, 2.08; carbon- 
ate of lime, 56.07; carbonate of magnesia, 35.32; iron peroxide, 0.69; iron protoxide, 
0.58; water, 0.46 = 99365. The usual fossil casts are found in the Buff beds, including 
fine ones of Cypricardites ventricosa and Gyroceras duplicostatum, 


Fig. 50. 


SEAS Abec2. 
Waodwards Juarri 


S. W. gx. oF Sxc. 2, NEARLY 
To THE Nort LINE or SEc. 3, BURKE. 


SxEction on A LINE 


YJorizontal scale 4 inches, 1 mile; vertical scale 1 inch, 200 feet. 


Fig. 50 represents a section obtained in the northern part of the town of Burke, 
showing the small thickness reached by the St. Peters and Lower Magnesian in this 
art of the county. ; 
a the small quarry on the N. W. qr. Sec. 35, in the same town, a 2 inch layer is 
crowded with impressions of the exterior, and casts of the interior, of the following fos- 
sils (694): Petraia Corniculum, Strophomena camerata, S. incrassata, Steptorhynchus 


602 GEOLOGY OF CENTRAL WISCONSIN. 


filitexta, S. deflecta, Orthis tricenaria, Rhynconella, n. sp., Cypricardites ventricosa, 
Raphistoma lenticularis, Pleurotomaria subconica, Trochonema umbilicata, Murchisonia 
bicincta, M. tricarinata, Orthoceras anellum, O. vertebrale. 

In the Catfish Valley, the Potsdam, Mendota, Madison and Lower Magnesian are 
frequently exposed, the last three being quarried at numerous places. A few important 
points only can be mentioned. O’Malley’s and Veerhusen’s quarries in Westport yield 
very handsome stone, and one quite different from the general run of the Lower Mag- 
nesian. O'Malley's quarry, 8. E. gr. §. E. gr. Sec. 10, shows the following section: 


1. Thin bedded to shaly yellow limestone. .......- 2.0 eee eee ee eee eee e eens *% a6 
2. Three heavier layers of the same ©... 00-0 see ee eee e cece ete e tence eres 2 6 
3. Broken yellow limestone with much odlitic chert (641) and geodic calcite 

(GLB) ota 5 tebe eet bate ata Siatalene rants. Sera een pos Gussie Shecernbg Seer eroial ee lady ese eis 4 
4. Very heavy layers— interstratified with two or three thin layers — of cream- 

colored, close, granular-textured limestone (640), containing 4.06 per 

cent, of argillaceous impurities........-. 00. cee ee cece e eee eee eens 10 


From the heavy layers of No. 4, one of which has a thickness of 24 inches, some 2,000 
to 3,000 cords have been removed, the stone having been chiefly used in the construction 
of the State Hospital for the Insane. Mr. Veerhusen’s quarry, N. E. qr. of the S. W. 
qr. Sec. 25, is on the top of a narrow ridge of Lower Magnesian, and has a face of 24 
feet, a large amount of stone having been removed. The following is the section, be- 


ginning above: 
Ft. In, 
1. Rough, brecciated, yellow, fine-granular limestone (629), containing 3.49 


per cent. of insoluble ingredients; bedding imdistinct.................. 8 
2. Very heavy layers, some 4-5 feet in thickness, of pale yellow, close-textured, 
granular limestone (626, 627, 628), which on solution leaves a large res- 
idue of fine gray sand, several determinations on specimens from dif- 
ferent parts of the face giving 12.14, 13.03, 20.59, 34.74, 35.63, and 40.78 


pericertes quarry layeren ss: sess He tens cede eee cee be § Siw alge ates 15 
3. Greenish sandy layer (62914); a specimen on solution left 41.17 per cent. 
Of Very Dne pray sand: 4. -ti04naweaew ayy taleusege 8 ¥oe 0083 Xo0 oes 1 


4, Thinner-bedded limestone, like No. 2, but finer-grained, of greenish tint, 
and profusely marked with dendritic oxide of manganese; below the 
base of the main quarry; thickness,.......... ee. ce ceeeec ec cceenceee 8 6 


The lowest layer is 39 feet above the base of the formation. No. 2 has yielded a 
very large amount of stone for the construction of the Insane Asylum. The stone is 
like that from O'Malley's quarry on Sec. 10, and should have much wider use than form- 
erly. It is 4 much handsomer stone, and endures weathering better than the sandstone 
used in Madison. The upper and less sandy layers at Veerhusen’s have been burned 
into a good hme, At Westport Station, near the center of Sec. 26, is a long railroad 
cutting’ through the western end of the ridge upon which the quarry just described is 


situated. The deepest part of the cut shows the following section: 


1. Lower Magnesian limestone (636); gray-and-yellow-mottled, porous, mode- Heat 


rately thin-bedded, the layers somewhat broken and displaced; con- 
tains 11.52 per cent. of argillaceous impurities; at base is a thin layer of 

white odlitic chert, and another of greensand; in all.................. 20 
2. Madison sandstone, including: thick-bedded, yellowish, fine-grained sand- 
stone (637), with only 2 per cent. of soluble ingredients, 19 feet; lighter 
colored sandstone, 2 feet 6 inches; and purely silicious, white sandstone, 

¢ often loose, and composed of much rolled quartz grains, 4 feet; in all.. 95 


llos 


THE LOWER SILURIAN ROCKS. 603 


The quarry on the north side of the mazsh, in the N. W. qr. of Sec. 12, Springfield, 
is on the Madison sandstone, whose upper luyers here are heavy, regular, buff-colored, 
contain over 40 per cent. of soluble ingredients, and make a good building stone, re- 
sembling that quarried at the same horizon ncar Madison. Heiny’s quarries, on the 
Lower Magnesian, N. W. qr. Sec. 35, Springfield, are quite extensive. They show the 
following section: 


Feet. 
1. Concretionary and brecciated yellow limestone.....2-20--2.sseceeeceeeceeeeee 5 
2. Heavily-bedded white layers with sineh chert, burnt for — a avtwarsinanaieint isis 10 
3. No exposure ...-- wid Simin esac aes sive oust yan en us oka due evade delpya tnactaactacGhecole’ cusuba taneous ante atm 20 


A, Trregoularly thin-bedded, porous, white-and-yellow-mottled limestone (648), with 
geodic cavities, many black dendritic markings, and 6.11 per cent. of msoluble 
INGTECCNt ws 26 66 shes ek ue as y lor se TES OLe Hee e ahaa DAE Cane wae aed & 15 


The lowest exposure is near the base of the formation. 

The Madison sandstone and overlying Lower Magnesian are finely exposed in a large 
quarry on the edge of the high land, 8. E. qr. Sec. 11, Middleton. The following 
section, taken here, is interesting as showing how the great Lower sandstone series 
graduates upward into the Lower Magnesian; the order is as usual a descending one: 


LOWER MAGNESIAN. 


- Ft. In. 
1. Very irreguiar layers, alternatingly thick and thin, of a brownish-gray, . 
close-textured, minutely-crystalline, cherty limestone (591), which leaves 
on solution 4.39 per cent. of a very fine, clayey residue; 7 feet below the 
top is a, marked concretionary layer, one foot thick..........-.-..+-+-- 18 4 


2. Brecciated layer of sandy, grayish limestone (592), containing 63.89 per 

cent. of fine gray quartz sand........ 60. cece ee eee tence tenet nee ee eee I as 
8. Thick layer of gray, flinty-textured limestone, with a thin, sandylayer attop 1 1 
4, Concretionary, cavity-bearing limestone (593), which leaves on solution 

11.03 per cent. of fine, grayish, aluminous residue; the cavities carry dol- 


omite crystals... 2.0.00. c cet e cece cece ence eee ere e eens et semeeenenes 4°94 
5. Yellowish calcareous-sandstone.......e see cece cece cece scene ae eee eeee .. 19 
6. Yellowish limestone, in places quite sandy........+-++e+seeeee eee cece 2 


7. Very close-textured, non-crystalline, yellowish limestone (594), containing 
9.19 per cent. of fine, aluminous, insoluble matter, and much marked by 


dendritic oxide of manganes@....-... 2 cece eee eect ee te eee ener ees Oo 30) 
8. Brownish, sandy, porous limestone (595, 652), carrying odlitic chert, numer- 
ous crystal-lined cavities, and containing 28.04 per cent. of sand....... 2 2 
9. Yellow-and-gray-mottled, rough-textured, conchoidal-fracturing limestone 
(596), containing 3.89 per cent. of aluminous impurities..........+++-- 1 
10. Oélitic chert layer (597; nearly pure quartz, only .01 per cent. being solu- 
PG iss ciccicneresese ee she ER AAA Nees Yb bug See GIN HAI ema nan cio ndeol de sey .. 6 


MADISON BEDS. 


11. Pure white, exceedingly fine sandstone (598, 651), composed of angular tc 
rolled grains of translucent quartz; often loose sand; the layer very ir- 
regular, swelling down and cutting off the layers below; in some places 
cutting off also the layers above; thickness varies from 7 inches to...... 1 

Light yellow, friable, fine-grained, dolomitic sandstone (599, 650), composed 
of rolled quartz grains embedded in a crystalline dolomitic matrix; the 
sand being 63.4 per cent. of the rock; the exact equivalents of the Mad- 
ison building-stone; thickness.......-.-+e+eeee seen erect etree reece 15 


on 


12 


4 
So 
a 
- 
5 
lo | aa 


604 GEOLOGY OF CENTRAL WISCONSIN. 


The following is the section at MacBride’s point, on the north shore of Lake Mendo- 
ta, N. W. qr. Sec. 1, Madison: 
Ft. Ia 


I. Heavy-bedded, jointed Mendota limestone (634), having a brown color, and 
close-grained, flinty matrix, and leaving on solution 15.05 per cent. of a 
fine sandy residue; layers run 2 to 4 feet in thickness; joints N. 87° W., 
used in construction of old capitol at Madison ......-.....eee seen ee 21 § 

Tl. Thin-laminated greensand layer 0.6... e eee e cece eee eee eee ee een e ees 1 

TI. Upper layers of Potsdam sandstone; fine-grained, light-greenish-tinted, 
calcareous sandstone, containing 15.5 per cent. of soluble ingredients; 
thin-bedded, alternate layers, different colors; some more calcareous 
layers weathering in relief; scolithus-bearing ........+0eeeeeeeeeeaes 31 


On the N. W. qr. Sec. 21, and the N. E. qr. See. 20, Madison, is a round isolated hill 
capped by the Lower Magnesian. The top of the hil is almost completely encircled by 
a large quarry which exposes the Lower portions of the Lower Magnesian and the upper 
part of the Madison sandstone. The following section includes the quarry face and the 
record of a well near by: 


LOWER MAGNESIAN, 


i 
1. Yellow, fine, granular, close textured limestone (607); thin bedded a 
shaly; some few layers near the top are burnt for lime..............-. 5 68 
2. Gray-and-yellow-mottled, porous limestone (603, 611), with large patches 
of rhombohedral calcite, much dendritic manganese oxide, and 4.1 per 


cent. insoluble matter; forming one layer -.........+.0. eee ener eeeee 2 
3. Thin-bedded to shaly yellow limestone, mostly quite sandy .............. 10 
4. Layer burnt for lime (606) and containing only 2.3 per cent. of insoluble 
ANBECAIONS Ss 354 cose dente elena et aeeen eee isc Golan e was aeiennaenes as 8 


5. Layer of odlitic chert (608); a milk-white material made up of little con- 
eretions 7y to 7; inch in diameter, which consist of minute rounded grains 
of limpid quartz encased in a milk-white powdery matrix; having the fol- 
lowing composition: silica, 98.01; alumina, 0.53; iron sesquioxide, 0.73; 
lime, 0.67; magnesia, 0,21==100.15; thickness, one inch to ........... .. 6 
MADISON, 


6. Greensand layer, consisting of a matrix of rounded quartz-grains and dark 
green grains of glauconite .,.... 6.6.0. eee eee e cece cence eee e eve 1 6 
7. Light buff-colored sandstone (604); in heavy uniform layers six inches to 
two feet in thickness; much used as a building stone in Madison: con- 
tains 10' per cent. of carbonates of lime and magnesia ................ 12 
8. Light-colored sandstone, similar to the foregoing but less firm and regular; 


in the lowest portions at the base of the quarry a loose white sand... 5 8 
9. Unexposed, below the quarry base... 1.0... 0c. cece cece eee ee cee cerns 5 
10. Soft red and brown sandstone in well ....-..... 000. cece eee c ence eceee 14 
MENDOTA 
11. Hard yellow limestone, in well... ....... 6c. e cece cece eee e nee ceetevees 80 
POTSDAM. 
12 Soft greenish sandstone, in well............. ccc cece cece cece cece cece ee 20 
107 


The building stone of these quarries is much sought for. It is obtained also from 
quarries across a small valley, on the N. W. qr., Sec. 21. It was formerly worked to 


THE LOWER SILURIAN ROCKS. 605 


considerable extent on the side of the hill on sections 17 and 18, and beyond doubt is to 
be found in the neighboring country at many other fovorably located points. This is a 
matter of some importance, since in the present quarries the stripping has become a 
heavy expense. 

At Madison, the Mendota is exposed in several small railroad cuttings (622) on the 
north side of Sec. 22. On the 8. W. qr. Sec. 23, on the point of a low ridge projecting into 
the mazsh, is a quarry of some size, showing the lower 10 feet of the Mendota limestone. 
The upper layers are thin, the lower heavier, and all very irregular. The rock (618) is 
a dark yellow to brownish, rough-textured, concretionary limestone, containing many 
red patches of iron oxide, which proceeds, apparently, from the oxidation of pyrite. The 
composition is: silica, 4.18; alumina, 2.17; iron peroxide, 1.45; carbonate of lime, 55.68; 
carbonate of magnesia, 35.52; water, 0.58=100.58, Greensand in scattering grains, and 
light green earthy patches are seen throughout, whilst a regular greensand layer (612) 
at the bottom of the quarry marks the base of the formation. Towards the side of the 
ridge the limestone layers have an inclined position due to undermining. This quarry 
was one of the first points at which the Mendota was recognized, and may be regardeci 
as typical of the lower part of the formation. The rock has many points in common 
with the Lower Magnesian, being quite as free from sand as that rock. 

The Artesian-boring in the Capitol park at Madison has a depth of 1,015 feet, pene- 
trating in its course Glacial Drift, the Potsdam sandstone, and 200 feet of the Archean 
rocks. The water in the well comes within some 60-70 feet of the surface, from where 
it is pumped for use in the boilers at the Capitol and for drinking purposes. It is re- 
garded as a ‘‘mineral’’ water, but is not one, being freer trom solid ingredients than 
ordinary well water, and containing nothing unusual except a small quantity of iron 
bicarbonate, the iron of which, on exposure to the air, peroxidizes, and produces a 
brownish sediment. A record of this boring has already been given in the annual re- 
port of Dr. Lapham, page 50; the greenish mineral from the rock at the bottom of 
the well is, however, probably not prehnite, as there given. The Artesian boring at the 
Milwaukee and St. Paul depot begins at a level 74 feet below the top of the boring in 
the Capitol park, and brings water to within 7 fect of the surface. The following is 


an abbreviated register of this boring: 
, Feet. 
Drift: sand and clay, with bowlders; the lower part nearly all loose sand, so that 


it is difficult to tell where the drift ends and the underlying sandrock be- 

SINS? BUGUE wcaiecwrdasin aahauNe ows OIe ewe tede we ahd Va aadee bs 70 
Potsdam sandstone: specimens from depths of 200, 250, 290, 850, 360, 380 and 

390 fect. show very fine, white quartz sand, stained here and there with 

deep brown points of iron oxide, and entirely non-calcareous; some of the 

sand is a little coarser, and «ll as seen under the microscope is made up of 

very much rolled grains, the larger ones of which are almost wholly spher- 

ical. Specimens from 600 and 680 feet are also of limpid quartz, but the 

grains are very much coarser and less rounded. The lowest layer of the 

formation struck is soft red shale, like that found in the Capitol well. 


Thickness in all, about.....0 6... cece eee cere eee cere tenn eee e ne ees 665 
Archean: dark colored rock, like that in the Capitol well ...-.....-+eseeeeees 50 
Depth of boring.......--- edi aden s Ghd eae COTS SEAT AN Gee 785 


The lower layers of the Madison sandstone are quarried on the S. E. qr. Sec. 28, 
Madison, on the south shore of Lake Wingra, and the same rock is finely exposed (614, 
617) with a thickness of 23 feet, largely pure white sand, and overlaid by 17 feet of non- 
arenaceous thin-bedded Lower Magnesian, in the railroad cutting, S. E. qr. Sec. 35. 
About 35 feet below the bottom of this cut, 10 feet of Mendota is exposed on the. 


606 GEOLOGY OF CENTRAL WISCONSIN. 


south shore of Lake Monona, near the §. E. corner of Sec. 26. On the south line of the 
town of Madison, Sec. 33, a large quarry on the Lower Magnesian shows the following, 


beginning above: Ft. In. 


1. Concretionary and irregularly bedded, yellowish-gray limestone ...-.-++-es 10 
2. Chert layer; sometimes formmg a continuous nodular-surfaced layer, at 
others occurring in a row of separate nodules; internally, the chert 
(644) is brown-and-white-banded, and jaspery; externally it has a soft, 
white, silicious coating ..... a bhadeuuidareean, Guanes ae Meee ese’: -- 3 
3. Compact, heavily bedded, flinty-textured, gray limestone (644) containing a 
few geodic cavities lined with dolomitic crystals; composed of silica, 
1.09; alumina, 0.44; iron peroxide, 0.43; iron protoxide, 0.63; lime 
carbonate, 66.82; magnesia carbonate, 30.40; water, 0.35==100.16; thick- 
PCRS. vrsvtomnbarerdngorsvaierd GRR OA Hid GRRE weiner ana ewe tae eUEE Che eae Be 2 
4. Chert layer, like No. 2... ...cecee ete e cece ee eee eee ee creer ene teenies ua 2 
5. Very heavily bedded limestone, like No. 1...---.-ee- ee cee eee e reece eres 5 


Throughout the quarry there is a marked local dip of 10° to 15° southward. The 
quarries have been opened for 20 years, the stone being used altogether for burning into 
lime, of which about 20,000 bushels are made annually in two large kilns. 

On the west shore of Lake Kegonsa, near the center of Sec. 26, Dunn, a large ex- 
posure shows the following: 


Feet. 

J. White sandstone with brownish stains... 2.0.0.2 esse eee eee e eee eee e eee es 1 

TI. Greensand layer .eccscccec cee eens eee tae k ede ee eet nents ete e edie ence 2 
JII. Light-colored, soft, thin-bedded, calcareous sandy layers, with specks of green- 

sand and geodic calcite... 2.6... ee ence ence cence eee e ete teen ees 1 

IV. Whitish layer, more calcareous than the preceding. ........-4+6..eee seen 2 


V. Heavily-bedded, light yellowish sandstone (693); fine-grained, firm, ncazly 
one-half soluble, the residue made up of angular to subangular white sand; 


in parts cross-laminated. 0... 06. e eee e cree eee ee eee eee eee teens 12 
VI. Sandy, yellowish, fine-grained limestone.....-.. 6... ee reece eee e eee eens 12 
30 


The lowes$ layers are unmistakably Mendota, which is here much less sharply defined 
than usual from the Madison. One-half mile north, friable, brownish, entirely non- 
calcareous, Madison sandstone is seen on the hill side, corresponding to the uppermost 
layers of the foregoing section. A similar sandrock shows near the roadside on the 
north line of the N. W. qr. of Sec. 27, at the Town ‘House, on the center of the south 
line of Sec. 21, and in the field near the middle of the 8. E. qr. Sec. 21, the last named 
lying near to, and about 15 feet below, one of Lower Magnesian. All of these exposures 
appear to carry the Madison to an unusual thickness, 50 or 60 feet. : 

On the divide betweem the Catfish and Sugar river valleys, in Middleton, Verona, 
Fitchburg, Montrose and Oregon, the Trenton is the rock most commonly quarried, be- 
ing obtained from the tops of isolated ridges whose sides often show large exposures of 
the St. Peters. Amongst other quarries may be named those on the S. E. qr. See. 27 
(662, 663, 669), and the 8. E. qr. Sec. 35 (664, 665, 666), Middleton; the very large 
quarries on Secs. 7, 15 and 18, Fitchhurg; those on Secs. 18 and 26, Montrose; those on 
Secs. 4 and 24, Oregon; and those on Sees. 28 and 35, Rutland. All of these are in the 
Buff beds, generally close to the St. Peters. 

In the Sugar river valley and its branch valleys the Trenton is quarried at a few 
points, but the St. Peters makes very frequent natural exposures of large size. Cliffs 


‘THE LOWER SILURIAN ROCKS. 60T. 


and shelving ledges of brownish, friable St. Peter’s are frequent on the valley sides, and 
isolated bluffs and towers of the same rock are to be seen at several places within the 
valleys themselves. One of these towers, on the 8. W. qr. of the 8. E. qr. Sec. 11 
Primrose, known as the Devil’s Chimney, is circular in section, 60 feet high, 50 feet in 
diameter on the top and 40 feet at the bottom. The isolated bluff on the N. E. qr. of 
the 8. W. qr. of Sec. 28, Springdale, is 100 feet high, 100 yards in diameter at base and 
20 on top. 

On the Wisconsin river slope the exposures and quarries, which are numerous, are 
chiefly in the Potsdam, Mendota, Madison and Lower Magnesian. The Trenton is 
quarried, however, on the N. E. qr. of Sec. 18, Middleton, at the top of a high bluff, 
showing 90 feet of St. Peters (658) as represented in Fig. 51. 


Fre. 51. 


SIAN S eiaiaial 
BUEE Limestone. ie TED 


Sr PETERS Sandstone i os" 


SF WE P6% SectionS 


YONI PF ALE 
MACNESIAN Limestone nad 
Black Earth Creek | 


ge 

3 —— 
oid MADISON Jiendstone——s 
A Limestone oe ES 


SEcTION AcRoss THE VALLEY oF BLack Eartu CREEK. 


Vertical scale 200 feet to the inch. Horizontalscale 400 feet to the inch. 


The Trenton at this place (659, 660, 661) contains numerous casts of the following 
fossils: Petraia corniculum, Strophomena, Cypricardites ventricoss Raphistoma lenticu- 
lave, Trochonema umbilicata, Murchisonia bicincta, M. tricarinata, Pleurotomaria Na- 
soni, Oncoceras pandion, and Orthoceras anellum. The Trenton shows also in a small 
quarry at the top of the bluff on the N. W. qr. of Sec. 28, Berry, far away from any 
other Trenton area. 


MAP OF PART OF WISCONSIN 
designed to show the main tacs with. regard to the distribution of the 


and other 
QUATERNARY DEPOSITS. 


Yl SAG ARSENE 


GLACIAL DRIFT 


PLATE, XXVA. 


- 
- 


VW vee 
KA 


rN 
— 
Ado 


SS 


of 


: 
L) 


RI 


Kel 


re 
PA 
YS 


a 
ae ey ae 


is 


6 
Pra 


ith 


>| Age 
ran 


Driftbearing Area Lacustrine (1 lays 


g 
gs 
§| 
4 | 
= | 
g° 

3h 
= 
S&S 
B 


Driftlimit and moraine,south of Town 5. atter Moses Strong and. 


Drifiless Area 


Py—> Clacial Striae 


mu Co 


Leia, & Bs 


THE GLACIAL DRIFT. 609 


Plate XXVI shows the boundary of the driftless region for the lar- 
ger, part of its extent in Wisconsin. This line lies chiefly in the. Cen- 
tral Wisconsin district, but for the four townships south of Dane 
county has been copied from the maps of Mr. Strong. Entering 
Dane county on the middle of the south line of Montrose, T. 5, R. 8 
E., it nearly coincides with Sugar river as far as the head of that 
stream in Oross Plains, T.7, R. 7 E. Along this portion of its 
course the heaviest drift deposits are several miles to the eastward of 
the boundary, which they gradually near to the northward. From 
the head of Sugar river the divide is crossed to Black Earth river, the 
northern side of which is followed into the towns of Black Earth and 
Mazomanie, T. 8, R.6 E. Thence, bending northward, and cross- 
ing the Wisconsin between Sauk City and the mouth of Honey creek, 
the line pursues a northerly course across Sauk Prairie to the foot of 
the Baraboo quartzite ranges, morainic drift occurring from half a 
mile to two or three miles east of it. On top of the quartzite ranges 
no drift is seen west of Devil’s Lake, in whose valley are, however, 
heavy doposits, and the line appears thus to make a slight bend east- 
ward. North of the ridge, however, it is further west again, for large 
heaps occur at Baraboo, and bowlders are to be seen two or three 
miles west of that place. 

Beyond the Baraboo, the line continues in a northeriy direction to 
the north line of Sauk county, where it bends out to the westward 
along the high ground that forms the rim of the sand plain of Juneau 
and Adams ‘counties, for granitic and other bowlders may be seen 
all along the road from Kilbourn to Mauston, as far as the N. W. qr. 
of Sec. 27, T. 14, R.5 E. Very soon, however, a sharp bend is made 
to the eastward again, the line following the inner edge of the high 
ground to the Wisconsin, above the Dalles, and, after crossing the 
river, in a curving direction through southeastern Adams county. 
Turning then northward, it lies a short distance west of the east line 
of that county, until its northern portion is reached, when, curving 
once more to the westward, it crosses the Wisconsin again near 
Grand Rapids, in Wood county. A sketch map of the Wisconsin 
driftless area, given by J. D. Whitney,’ includes all of Adams and 
the eastern part of Juneau counties within the drift-bearing area, 
and shows the limit altogether to the west of the Wisconsin. This 
portion of the state he does not, however, seem to have mapped from 
personal investigation. I have never seen any sign of glacial drift in 
the district specified, and, indeed, the numerous fragile sandstone 
peaks occurring within it preclude the idea that the glacial forces 

1 Geological Survey of Wisconsin, Vol. I. Albany, 1862. 
Wis. Sur. —39 


610 GEOLOGY OF CENTRAL WISCONSIN. 


could ever have acted there. Flanking the north side of the quartz- 
ite bluff at Necedah, in Juneau county, is a great bank of gravel and 
rounded bowlders, but these are wholly of quartzite, derived from the 
bluff itself, and must hence be regarded as the result of river or lake 
action upon the quartzite. Clay and sand deposits occur in much of 
Adams county, as, for instance, around Friendship, but are finely lam- 
inated, and appear to be due to deposition from expanded streams or 
lakes, being wholly without associated gravel. From southern to 
northern Adams, the drift limit, as marked by the loose materials of 
the surface, is for the most part directly along the edge of heavy mo- 
rainic heaps, with numerous bowlders. 

Westward from Grand Rapids, the drift limit is not always so well 
defined, but does not appear to be far from the line of the Green Bay 
and Minnesota railroad, as far as the crossing of Black river. From 
here it bends to the northeast, crossing the line of the West Wiscon- 
sin road some twelve miles southeast of Eau Claire. 

The nature of the topography of the driftless area, everywhere 
most patently the result of subaerial erosion exclusively, is even more 
striking proof that it has never been invaded by the glacial forces 
than is the absence of the drift material. Except in the level country 
of Adams, Juneau, and eastern Jackson counties, it is everywhere a 
region of narrow, ramifying valleys, and narrow, steep-sided, dividing 
ridges, whose directions are towards every point of the compass, and 
whose perfectly coinciding horizontal strata prove conclusively their 
erosive origin. A glance at the map of Plate XXVI, on which are 
accurately represented all but the very smallest streams, will serve to 
give an idea of this feature of the driftless area. Each one of the 
numerous streams shown has its own ravine, and the ravines are all 
in direct proportion to the relative sizes of the streams in them. This 
is well brought out by the colored geological maps of Areas D, E, G 
and H, in the Atlas. Since the several strata lie nearly horizontal, 
the colors representing them give really a close idea of the topography. 
The two first named maps include portions of both drift-bearing and 
driftless areas, and the different appearances of the geological outlines, 
stream and marsh directions, etc., on the east and west sides of the 
maps, are very instructive. It should be said that this difference is 
due, also, partly, but not mainly, to a change which takes place mid- 
way within the districts represented by these maps, from a nearly 
perfect east and west horizontality of the strata to a small, but grad- 
ually increasing, eastward descent. In this connection, reference 
should also be made to Mr. Strong’s excellent contour maps of the 
lead region. 


THE GLACIAL DRIFT. 611° 


In the central plain of Adams and Juneau counties, though the 
ramifying ridge-and-valley topography is wanting, no less indisputa-: 
ble topographical proof is at hand of the immunity of the region from 
the glacial action in past time; for, dotting the surface of the plain, 
we find the numerous sandstone towers that have been so often alluded 
to in this report. The fragile character of these peaks is sufficient 
evidence that they could never have stood in the path of a glacier. 

The altitude of the driftless area, as compared with the drift- 
bearing regions, becomes a matter of some importance in any attempt 
to explain the absence of the drift phenomena. It has been stated 
by some writers that the driftless area is higher than the drift- bearing, 
and was, consequently, not subjected to glacial invasion. It is true 
that an general the eastern half of the state is lower than the western, 
but from what follows it will be seen that farther than this the state- 
ment is inaccurate. From the south line of the state as far north as 
the head of Sugar river, in Cross Plains, the country west of the drift 
limit rises rapidly 200-400 feet. Just north of the head of Sugar 
river, the limit crosses high ground— the western extension of the 
high limestone and prairie belt of northern Dane and southern Colum- 
bia counties — and the altitudes east of the limit are as great as those 
to the west; whilst in passing from the head of the Catfish river west- 
ward, a glacier must have made an abrupt ascent of fully 300 feet. 
North of Black Earth river, the limit has the higher ground, by 200 
feet, on the east. Sauk prairie is crossed on a level, and though 
higher ground occurs west of the prairie, its topography and the ab- 
sence of drift show that the glacier never reached so far. Where the 
quartzite range north of Sauk Prairie is crossed by the limit, it is 
higher (850 feet above Lake Michigan) than any part of the driftless 
area except the Blue Mounds, whilst a few miles east a great develop- 
ment of bowlders and gravel is found on one of the highest portions 
of the range (900 to 950 feet altitude). From the Baraboo north to 
the Sauk county line, there appears to be no relation between the 
position of the limit and the altitude of the country. From the north 
line of Sauk county, in curving, as previously described, to the east- 
ward and northward around Adams county, the limit is on the very 
crest of the divide. From its position near the middle of the east 
line of Adams county, the country, for 40 miles to the west, is from 
100 to 200 feet lower. From the northwest part of Adams: county 
to the Wisconsin river the limit is in a level country; whilst from the 
Wisconsin westward the country north of it is everywhere much 
‘higher than that to the south, the rise northward continuing to within 
thirty miles of Lake Superior. 


612 GEOLOGY OF CENTRAL WISCONSIN. 


The surface features of the drift-bearing regions, so far as they 
are independendent of the rocky formations beneath, are in strong 
contrast with those of the driftless area. There is an almost entire 
absence of the narrow ridge-and-valley topography, or of very steep- 
sided valleys generally, the contours being everywhere more flowing. 
The difference is evidently due both to a different method of erosion 
and to the obliteration of abrupt changes of level by heavy deposi- 
tions of drift materials Another marked difference is noticed in the 
entire absence, east of the drift limit, of the fragile castellated out- 
liers that are found further west. Outliers do occur, though not 
abundantly, but are thick and of rounded contour, and more com- 
monly of limestone. Still another contrast is presented in the linear, 
and for considerable areas parallel, arrangement of the ridge, valley, 
marsh, and stream directions, and also of the outlines of the areas oc- 
cupied by the several formations, as compared with the ramifying 
arrangement of the driftless region. To these features of the drift- 
bearing districts are to be added the peculiar appearance due to round- 
ed hills and winding ridges of pebbles and sand, the abundance of 
circular and serpentine depressions without outlet, and often occupied 
by lakes of considerable size, and the omnipresent surface erratics — 
all of which receive especial attention below. 

The features thus enumerated are especially to be observed in that 
part of the state which lies east of the eastern boundary of the drift- 
less area, the region lying immediately north of its northern bound- 
ary, though showing in parts considerable quantities of drift material, 
having apparently not been subjected to so great glaciation. In much 
of the latter region the drift appears to be quite insignificant, and all 
surface irregularities as purely the result of subaerial agencies as in 
the driftless region itself. This is quite evident along both sides of 
the valley of the Wisconsin from Stevens Point to the north line of 
the district, and along the valleys of its principal western tributaries. 
All along the line of the Wisconsin Valley Railroad, between Knowl- 
ton and Grand Rapids, wherever the least cutting is made the rock 
is Jaid bare. Farther west, on the divide between the Yellow and 
Black rivers, in Clark and western Wood counties, there is a consid- 
erable thickness of drift material, which, however, presents none of 
the heaped up appearance characteristic of the more eastern drift- 
bearing regions. 

The linear topography above mentioned is generally found best 
marked in the regions east of the belt along which the drift materials have 
their most marked morainic development. As shown hereafter, this 
helt lies usually not far east from the western limit of the drift region. 


PLATE, XXVIA 


GEOLOGICAL MAP 
of the 
FOUR LARE COUNTRY of DAN COUNTY 
designed toshow the 
DIRECTIONS and EFFECTS of the GLACLAL MOVE MENT 


R.D leving 
1876. 


ii] 


ea | J 


ne 
tadison Mendota Beds Potsdam Sandstone 


St. Peters Sainddstonil LowerMagnesian himestont, 3 
GlacialStriae 


Trenton kimestone 
Direction of glacial movement 


Tt Miawat ane biti A Eon Ca 


THE GLACIAL DRIFT. 613 


In the Four Lake Country of Dane county the linear arrangement 
is finely marked, its directions coinciding with the directions of the 
glacial strive on the underlying rocks. Lakes Mendota and Monona, 
and Lake Waubesa, in part, lie in N.E.—S.W. valleys, the first 
named occupying two such valleys, which are partly separated by the 
rock ridge of Picnic and MacBride’s points. The valley of Lake Mo- 
nona extends several miles to the southeastward beyond the lakes, 
preserving its direction, which, like that of the two valleys of Lake 
Mendota, is about 8. 57° E., or parallel to the direction of the stri 
to be seen at the large quarries west of Madison. Numerous other 
similar valleys of varying size are to be seen in the same country, 
some occupied by marshes or streams, others entirely dry. Narrow 
detached ridges, lines of marsh, and the outlines of the formations 
show the same arrangement, and the same coincidence with the di- 
rections of the strie. 

Plate XXVI_ A is a geological map of the Four Lake Country, and 
is designed to show especially how the areas of the several formations 
have been carved out by the glacial forces; since the formations lie 
one above the other nearly horizontally, the map is also to some ex- 
tent a topographical one. It gives also the directions of the strie 
observed at different points, and the lines along which they indicate 
the glacial movement to have taken place. It will be observed that 
the glacial strie vary in direction from.due south at the southeast 
corner of ‘the map to nearly west at its northwest corner, and that 
the linear outlines of the formation areas, lake valleys, etc., keep pace 
with this change in direction. The Atlas map of Area D, which 
shows also the marsh and stream directions, etc , and is on a larger scale, 
as well as more accurately drawn, brings this interesting relation out 
even more strikingly. 

It would be instructive to describe in some detail the different 
lincar valleys, ridges and outlines of this district, tracing their vary- 
ing directions, but the space at command forbids this. It may be 
mentioned that in the town of Springfield a single narrow valley, 
carved out in the Lower Magnesian to a depth of 100 feet, is to be 
observed curving gradually westward to correspond with a slight 
change in the direction of the strise on its sides. 

Northwestern Dane and eastern Columbia counties are level com- 
pared with the district just described, but the linear arrangement is 
very plainly marked in lines of marsh, streams and geological out- 
lines, as will be seen readily from an inspection of the maps of areas 
D. and E. Fig. 52 gives the shape of the area of Trenton limestone 
which occupies the towns of York and Columbus, extending also into 


614 GEOLOGY OF CENTRAL WISCONSIN. 


adjoining towns on the east and west. A number of short parallel 
ridges are to be seen in the same region, some of which are rock, and 
others either altogether of drift or at least with a core only of rock. 
Roches moutonees, so characteristic of all glaciated regions where 
the underlying formation is of the hard crystalline rocks, are not en- 
tirely wanting in Central Wisconsin. The bald and smooth rounded 
summits of quartzite so conspicuous on the high bluffs of Caledonia, 
Columbia county, show the structure finely. ‘Thess summits have a 
direction but little south of west, coinciding with the directions of 
of the strie upon them. The scattering knobs of granite and por- 


Fie. 52. 


Cc OLUMB TA 3 COLUMBUS 


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COUNTY 


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TIZNREIE) TISNRXIIE. 


OUTLINE OF AN AREA OF TRENTON LIMESTONE NEAR CoLUMBUS. 
Scale 4 miles to 1 inch. 


phyry which rise through the Potsdam sandstone in Columbia, Mar- 
quette, Waushara and Green Lake counties are all distinctly “sheep’s 
backs.” The main Archean region of Central Wisconsin, stretching 
westward from the Wisconsin to Black river, does not show any dis- 
tinct “roches moutonées,” it being to the west of the region of 
greatest glaciation. Jurther east, in Shawano and adjoining counties, 
these shapes would be expected. The Silurian strata of Central Wis- 
consin are either too fragile or too susceptible to the solving action 
of the smospherie waters, to have received or retained aie “roche 
moutonée”’ shape. 


THE GLACIAL DRIFT. 615 


Drift hills and ridges occur over all of the drift-bearing area of 
Central Wisconsin. In the region north of the east and west drift 
limit, in Marathon, Wood, and Clark counties, they do not, however, 
show any distinct morainic character; but in Dane, Sauk, Columbia, 
eastern Adams, Marquette, Green Lake, Waushara, Waupaca and 
Portage counties, they show this character in a marked degree. More- 
over, there is, in these counties, a certain belt of country, the western 
border of which is never very far from the eastern edge of the drift- 
less area, in which the “knobby” drift hills reach an unusual de- 
velopment, the drift materiais are thicker than elsewhere, and the 
surface of the country is dotted with circular or winding depressions, 
without outlet, of very varying size, and often occupied by ponds or 
lakes. To these depressions, in certain other parts of Wisconsin, 
where they are to be recognized on a still larger scale, the name of 
“potash kettles”? has been applied, in allusion to their common shape; 
and the belt of country in which they occur has been designated as 
the “ Potash Kettle Range,” or, more simply, the “Kettle Range.” 
These latter names have heretofore been applied especially to a 
narrow and very marked range which follows the divide between 
the valley of Lake Michigan and that in which lie Green Bay, 
Lake Winnebago, and the head waters of Rock river. Prof. 
Chamberlin has traced this belt southward to the northeastern part of 
Rock county, where he finds it bifurcating, one branch running south- 
eastward into Lllinois, whilst the other, curving west and northwest, 
enters the Central Wisconsin district on the south line of Dane 
county, in the towns of Rutland and Dunkirk. 

From the south line of Dane county northward, the “ Kettle Range” 
is now recognized for the first time, having been traced for a distance 
of over 120 miles, as far as the line of the Wisconsin Central Rail- 
road, in Portage and Waupaca counties; beyond which it is known 
to extend until it becomes merged into the great accumulations of - 
morainie drift which stretch from the head waters of the Wolf and 
Oconto rivers westward, over a large part of the Archean region of 
the north part of the state. The Central Wisconsin “ Kettle Range ” 
reaches in parts a much greater width than that of the eastern part of 
the state, and its inner edge is not so well defined. These differences, 
however, admit of a satisfactory explanation. Plate XXVI shows 
the position of the Central Wisconsin Range, whose course and char- 
acter are described in more detail in what follows. 

Beginning on the south, we find, in the towns of Rutland, T. 5, R. 
10 E., western Dunkirk, T. 5, R.11 E., and northeastern Oregon, 
T. 5, R. 9 E., a considerable development of knolls and ridges of 


616 GEOLOGY OF CENTRAL WISCONSIN. 


gravel, with a number of depressions occupied by small lakes, one of 
which, on See. 8, T. 5, R. 10 E.,is amile inlength. The belt in these 
towns has a width of about eight miles, and a course west of north. 
In southwestern Dunn, T. 6, R. 10 E., and Fitchburg, T. 6, R. 9 E,, 
a bow is made to the westward, the convex side of which reaches the 
northwest part of Oregon, where knolls and large well marked dry 
kettles are to be seen, and the width is not more than from 4 to 6 
miles. In southwestern Madison, T. 7,R. 9 E., the inner edge of the 
belt reaches the western ends of Lakes Monona and Mendota, where 
are finely marked mammillary knolls, rising 50 to 75 feet above the 
lakes, and arranged in lines transverse to the axes of the lake valleys. 
The western side of this part of the belt is on the high ground of 
Middleton prairie, where kettles and knolls are to be seen at an ele- 
vation of 300 and more feet above the Madison lakes. The same is 
true of the low ground of northeastern Middleton, where is quite a 
cluster of water-filled kettles. From Middleton the range passes into 
Springfield, T. 10, R. 8 E., where the best development is in the 
northwest corner, and the width is some four miles. The high divide 
between the Wisconsin and Catfish rivers is crossed in the adjoining 
portions of Springfield, Dane, T. 11, R. 8 E., Berry, T. 10, R. 7 E., 
and Roxbury, T. 11, R. 7 E. In Roxbury the belt descends abrupt- 
ly 200 feet into the low ground of the valley of the Wisconsin. Hand- 
somely shaped and deep kcttles are seen in Roxbury, on Sections 8, 9 
and 16 in a low area, surrounded by eleven entirely isolated rock 
bluffs, and two quite large kettle lakes are found on the north side of 
the town. Columbia county is entered in the town of West Point, 
T. 12, R. 7 E., where the same characters as observed in Roxbury 
are continued. 

The Kettle Range crosses the Wisconsin river in the northern part 
of the town of West Point, and continuing northward along the east 
‘side of Sauk prairie, reaches the foot of the Baraboo bluffs in T. 11, 
R. 6 E., and T. 11, R. 7 E., Sauk county. On top of the bluffs im- 
mediately north of here it is not well marked, but in the gorge in 
which lies Devil’s Lake, and which makes a complete cut through the 
range, are very large accumulations of drift materials. The lake it- 
self really oceupies a kettle depression, being held in position by im- 
mense heaps of entirely unmodified drift at each extremity. These 
hills rise over 100 feet above the surface of the lake, the southern one 
falling off on the side away from the lake to over 150 feet, and tho 
northern one fully 100 feet, below its level. The thickness of the 
drift in the gorge must be nearly, if not more than, #00 feet. It has 
been shown on a previous page, that in this gorge we have, in all 


THE GLACIAL DRIFT. 617 


probability, an ancient erosion channel of the Wisconsin river, whieh, 
becoming blocked during the glacial times, was never after regained. 
The Devil’s Lake drift appears to lie on the western edge of the Ket- 
tle Range, no marked development of which is to be seen on top of 
the bluff for two miles east, when knolls of limestone, pebbles, and 
erraties of large size, are met with at the greatest elevations. 
| Northward from Devil’s Lake the Range traverses the Baraboo 
valley —in which large heaps of unmoditied drift occur near the vil- 
lage of the same name— and passing thence through northern Sauk 
county, crosses the Wisconsin into northwestern Columbia (Newport 
and Lewiston), and southeastern Adams. Here begins the great de- 
velopment of kettles, both dry and lake-filled, which is continued 
northward —the width of the whole range at the same time greatly: 
expanding —through northwestern and northern Marquette, Wau- 
shara, eastern Portage, and western Waupaca counties, to the line of 
the Wisconsin Central railroad, and for an indefinite distance in the 
less settled and unsettled regions beyond. In Waushara county, the 
Range has attained a width of fully five and twenty miles, the kettles, 
lakes, knolls and ridges lying thickly spread over the whole surface. 
As instances of finely marked kettles, may be mentioned those that 
occur very numerously over the town of Springfield, Marquette 
county, and in the eastern part of Lincoln, Adams county. These 
are for the most part dry, often quite perfectly circular, 50 feet in 
depth and 500 feet in width at top. They occur quite up to the edge 
of the driftless area, and within a mile of one of the fragile sandstone 
towers of that district— Pilot Knob. The elevation above Lake; 
Michigan is 550 feet. Excellent illustrations of lake-filled kettles 
are to be found in the very numerous lakes of the towns of Marion, 
Mount Morris, and Springwater, Waushara county. Some of these 
are of quite large size, as, for instance, Silver lake, near Wautoma, 
which is over a mile in length. They lie quite often in deep depres- 
sions, the water level not unfrequently standing at 25 to 40 feet below 
the top of the banks, which are wholly of gravel, and very steep, in 
some cases almost perpendicular. Two or more lakes commonly 
occur close together, the bank between them having a width on top 
scarcely enough for a wagon road, and a steep descent to the water 
on either side. This is finely shown in the case of Silver Lake, al- 
ready cited, and the nearly as large and partly peat-filled lake imme- 
diately north of it. The average elevation of the country in which 
all of these lakes lie is about 400 feet, and the country between them 
is everywhere pitted with smaller dry kettles. 

Further west, in Waushara county, in the towns of Coloma, Rich- 


618 GEOLOGY OF CENTRAL WISCONSIN. 


ford, Deerfield and Rose, is a belt of greater altitude, 550 to consid- 
erably over 600 feet above Lake Michigan. Here the lakes are less 
abundant, the drift taking on rather the character of ridges and knolls, 
though tortuous dry kettles are frequent. This ridge region is the 
divide between the waters of the Fox and Wisconsin rivers, and the 
drift depositions within it seem to have suffered little modification 
since their first formation. The roads running eastward from Colo- 
ma, on Burr Oak prairie, pass over parts of this great morainic heap 
where its structure and nature are seen to great advantage. 

For further ideas as to the Kettle Range, its position, varying 
width, and great numbers of lakes, as compared with the other parts 
of the state, reference should be made to Plate XX VI. The lakes on 
this plate are all, except mill ponds, that are given on the township 
plats of the region mapped, and are accurately placed, although the 
map is of so sinall scale. No doubt, others, not on the plats, occur in 
considerable numbers. 

The materials of the drift are bowlders, gravel, sand and clay. 
Bowlders are scattered thickly over the whole surface of the drift 
region. Nearly all are of some sort of crystalline rock, sandstone oc- 
curring very rarely, and limestone —- except as large sized pebbles — 
still more rarely. Of the crystalline rock bowlders, those of gneiss 
of some form or other greatly predominate, making up 50 to 75 per 
cent. of all. Nextin abundance to the true gneiss bowlders, are those 
of some form of brown-weathering, hornblendic rock, which is gen- 
erally syenite, and nearly always gneissoid in texture. Of 80 erratics 
counted within a few rods along the lake shore of the University farm 
at Madison, 44 were gneiss, 15 gneissoid syenite, 9 granite, 8 diorite, 
2 red porphyry, 2 quartzite, 2 sandstone, 1 red felsite, 1 granulite 
and 1 fine-grained slate. Whilst other rocks are often included, these 
numbers express, in a general way, what is true for the whole region. 
The gneiss bowlders vary much in mineralogical composition and 
closeness of grain, but are nearly always very distinctly laminated, 
and often much contorted. Occasionally they run into mica slates on 
the one hand, and gneissoid granite on the other. The granite 
bowlders vary also, but pink orthoclase granites are most common. 
All over the region, from Dane northward to Waushara, and prob- 
ably far beyond, red porphyry and compact red felsite bowlders are 
very noticeable from their bright red color, although forming only a 
small proportion of the whole number of erratics. They include 
kinds in which there is a compact red felsitic matrix, with dissemi- 
nated hyaline and amygdaloidal quartz; others in which both quartz, 
and felspar are porphyritic; others in which, in addition to these, the 


THE GLACIAL DRIFT. 619 


red matrix itself develops large crystalline faces; and still others in 
which the aphanitic matrix constitutes the whole rock. 

Quartzite bowlders are not at all common except inone or two lim- 
ited districts. One of these is in eastern Dane county, in the towns 
of Medina and Deerfield, where they are abundant, and associated 
with bowlders of conglomerate, both having beyond doubt come from 
a mound of quartzite a few miles northeast in Dodge county. It 
might be expected that the Baraboo quartzite ranges would have had 
their rock scattered very widely in the country to the southward, but 
this is not the case. In the Baraboo valley, and still more in the 
country immediately south of the ranges, quartzite bowlders of large 
size are very abundant. Further south they occur sparingly as far 
as the region about Lodi, including talcose quartz-slate, also undoubt- 
edly from the Baraboo ranges. Still further south they are more no- 
ticeable for their absence than their presence. It will be seen that 
this rather unexpected fact admits of a very satisfactory explanation. 
Sandstone bowlders are rare, not because sandstone is not abundant 
in the regions over, which the drift movement took place, but because of 
the very friable nature of the rock. Those sandstone bowlders that are 
found are always either somewhat quartzitic, or, as is more frequent- 
ly the case, are rendered hard by a large amount of cementing brown 
iron oxide. Amongst the smaller materials of the drift are sometimes 
found hard ferruginous concretions which are recognized as coming 
from the great sandstone region of the heart of the state. That large 
limestone bowlders should be so very rare appears to be due to the 
ease with which that rock is worn into smaller sizes. 

One of the most interesting substances found in the drift, though 
hardly attaining the size of a bowlder, is the native copper, which is 
found in fragments widely scattered over the northwest, from Ohio to 
Minnesota. These native copper fragments are far more abundant 
in Wisconsin than elsewhere, and far more abundant there than is 
commonly supposed. Specimens weighing from a few ounces up to 
30, 40, and even 50 pounds, are constantly found in digging. The 
late Dr. Lapham informed me that the coppersmiths in Milwaukee 
purchased from finders yearly several hundred pounds of this copper. 
Ancient implements of copper have been found very abundantly in 
Wisconsin, the largest collection of such relies in the world now being 
in possession of the State Historical Society at Madison. it has been 
argued that these implements prove a high degree of civilization for 
the races that occupied the northern United States in remote times, 
since copper smelting is an art unknown to the more barbarous peo- 
ples. It is evident enough, however, that there is a direct connection 


620 GEOLOGY OF CENTRAL WISCONSIN. 


between the abundance of copper implements, and the abundance of 
drift copper fragments, which in ancient times were probably much 
more plenty on the surface than now, and which by pounding could 
yield any and all of the implements ever found. ven a simple melt- 
ing down was unnecessary, and is directly disproved by the occur- 
rence on the tools of unalloyed silver. Some of the copper for these 
ancient implements may have been obtained directly from its home 
in the rock, on the shores of Lake Superior, but this required, of 
course, no more smelting than the drift fragments. 

In size the bowlders vary much, but there is generally a marked 
break in size between them and the “pebbles,” the latter being pre- 
dominatingly of limestone, the former of crystalline rocks of various 
kinds. In general the largest bowlders are found farther north. In 
the southern part of the district the larger ones run, commonly, from 
two to four feet in diameter, rarely exceeding the latter tigure, thongh 
occasionally running to as much as 10 feet in one dimension. In 
Wanshara county, especially on the eastern flank of the Kettle Range, 
bowlders 5 to 10 feet in diameter are very plenty, occurring sometimes 
in thick clusters, as on the hill immediately north of the village of 
Poysippi, and in several other places in the neighborhood, where many 
of one kind are found, giving rise to some doubt as to the possible ex- 
istence of the rockin place. The largest bowlder observed anywhiere in 
the district lies at the edge of a wood on the 8. E. qr. of See. 16, T. 1s, 
RR. 11 E., Waushara county. It is a red granite, sharp-angled, 134 
feet high, 30 feet long, and 22 wide, measures 110 feet in circumfer- 
ence, is buried in its lower part to an unknown extent, and came frum 
a large outcrop about four miles east. In shape, the smaller bowlders 
are often very much rounded, the angularity increasing with the size, 
but depending also much upon composition, hornblendice bowlders al- 
ways showing more rounding. Scratched and polished bowlders are 
often seen, but do not form any large proportion, and are generally of 
the harder and less destructible rocks, such as quartziteand granite. 

With regard to the distribution of bowlders, it may be said that, 
whilst scattered widely over the whole region, they are more plenty 
in the northern than in the southern portions of the district, and 
are especially numerous along the inner (eastern) edge of the Ket- 
tle Range. The greatest development of bowlders noticed in Cen- 
tral Wisconsin was in eastern Waushara county, and in the adjoin- 
ing portions of Portage and Waupaca. North of the village of 
Poysippi, as already stated, the hill is thickly studded with immense 
bowlders of a coarse, knotty gneiss, composed chiefly of black mica 
and pink felspar. In the town of Rose, T. 20, R. 10 E., the slope 


THE GLACIAL DRIFT, 621 


eastward from the high prairie of the next town to the west is strewn 
with immense bowlders ina very striking manner, and the same thing 
is to be observed twelve to fifteen miles further north, along the lines 
of the Wisconsin Central and Green Bay and Minnesota railroads, 
east of Amherst Junction. Clusters of bowlders are very common, 
even much further south, as in the central part of the town of Mar- 
cellon, Columbia county, and in the 8. E. qr. of Sec. 3, Deerfield, 
Dane county, where the bowlders are scarcely more than ten feet 
apart, over an area of some 10 to 15 acres. When these clusters: oc- 
cur, they are very apt to be mostly of one kind. Altitude has evi- 
dently had no influence whatever on the distribution of bowlders, since 
they are found on the highest and lowest parts of the country, indif- 
ferently. East of Devil’s Lake, in the towns of Greenfield and Mer- 
rimack, they are found in abundance and of large size on the highest 
est portion of the Baraboo bluffs, at altitudes of over 900 feet above 
Lake Michigan. Bowlders are found, also, on the tops of all the iso- 
lated bluffs that occur within the drift-bearing area. Very large 
hornblendic erratics, for instance, are to be seen on the very summit 
of the limestone bluff of the northwestern part of the town of Spring- 
field, Marquette county. This bluff lies on the top of the divide be- 
tween the waters of the Fox and Wisconsin rivers, has a height above 
its base of 200 feet, and a total altitude of 780 feet above Lake Mich- 
igan. It lies on the western edge of the Kettle Range, and a mile or 
two west, in a country 200 to 250 feet lower, the drift has ceased alto- 
gether. 

Gravel makes up a large part of the drift accumulations, though not 
so great a proportion as the sand. Two general kinds of gravel may 
be noted, the coarse and the fine, the former occurring more especially 
in those regions where the drift appears to take on a true morainic 
character, forming knolls and ridges, and the sides of many of the 
depressions of the Kettle Range, whilst the finer gravel is met with 
commonly in the valleys of streams, or wherever a distinct stratified 
arrangement of the loose materials is perceptible. The coarse gravel 
is for the most part of limestone pebbles, with which are mingled 
some pebbles of white chert, and some of various crystalline rocks, 
which increase in quantity towards the north. The ordinary limestone 
pebbles are of a white color, run from three or four to eight or ten 
inches in diameter, are commonly oblong in shape, much rounded at 
the ends, and often have one or two sides smoothed and striated. Not 
unfrequently fossils are contained, indicating the origin of the peb- 
bles, which is also to be inferred from their lithological characters. 
The coarse unstratified gravel is widely distributed over all the region 


622 GEOLOGY OF CENTRAL WISCONSIN. 


east of the drift limit and south of the line of the Wisconsin Central 
railroad, in Portage and Waupaca counties, and also to an indefinite 
distance further north. It is most abundant in the Kettle Range it- 
self, but is not entirely restricted to it. Even northward, into the 
region of the Archean rocks, the gravel is partly of limestone peb- 
bles, which have been brought from the limestone formations to the 
eastward. In the region north of the driftless area and west of the 
Kettle Range —ineluding the valley of the Wisconsin as far north 
as the northern line of Marathon county, and the country lying be- 
tween the Wisconsin and Black’ rivers, in northern Wood, and in 
Marathon and Clark counties — whilst erratics are often seen, some- 
times in clusters of very large bowlders, the coarse limestone gravel 
appears wholly wanting. The fine gravel consists, more largely than 
the coarse, of pebbles of quartz and various crystalline rocks. It is 
to be seen, finely stratified, in the drift of stream valleys. and in some 
places far away from the streams, as, for instance, on the divide be- 
tween Black and Yellow rivers, where it occurs interstratified with 
sand and clay to a thickness of over 100 feet. 

Sand appears to make up by far the largest part of the drift de- 
posits. Itis commonly light-colored and purely silicious, but is often 
mingled with more or less clayey material, both when in the plainly 
stratified and the more or less unstratified conditions. Occasionally 
itis stained brown with hydrous iron-oxide, and when stratified alter- 
nates in different colored bands. The explanation of the large pre- 
ponderance of sand over clay in the Central Wisconsin drift will ap- 
pear hereafter. 

Clay occurs, as already said, to a considerable extent mingled with 
the sand, over which it sometimes preponderates greaily, forming a 
firm, tenacious clay, which is stuck full of seratched and polished peb- 
bles and bowlders, and appears to be identical with the “ till’? of the 
Scotch geologists. Such a clay, however, is not often to be seen. 
Something like it appears in the heaps that lie on the high prairies 
of northern Dane and southern Columbia, but the only places where 
an apparently truce till has been noticed are in the vicinity of Devil’s 
Lake, for a better understanding of whose position reference should 
be made to Plate XIX, and the descriptions accompanying it. The 
lake lies in a perpendicularly walled gorge, 500 to 600 feet deep, 
which passes entirely through the main quartzite range of the Bara- 
boo. This gorge is about three-quarters of a mile in width, and be- 
tween three anda half and four miles in length. At the northern 
end its course is nearly due north and south for over a mile, when it 
turns nearly at right angles, and runs for the rest of its length but 


THE GLACIAL DRIFT. 623 


little south of east. Devil’s Lake lies in the north and south portion 
of the gorge. At its northern end a hill of drift rises abruptly from 
the water toa height of 100 feet, falling on Aas further side as ab- 
ruptly over 200 feet to the Baraboo river. A short distance beyond 
the southern end of the lake a similar hill chokes the gorge from side 
to side, rising 100 feet from the lake level, and on the eastern side 
sinking rapidly until at its eastern end the bottom of the gorge is 
full 150 feet below the lake. Through this hill a deep cutting is 
made for the Chicago and Northwestern Railroad. The sides of -the 
cutting show no sign of stratification, but only a sandy tenacious clay 
with numerous scratched pebbles and bowlders, the latter inclnding 
the usual kinds of crystalline rocks, but also a number of quartzite, 
some of which are much smoothed and striated. The large drift cut- 
ting near Baraboo shows something the same sort of material, which 
is, however, much more sandy, and has traces of a crude stratification. 
It is quite probable that till-like clays occur somewhat widely in the 
region of the Kettle Range, but the rare cuttings make this conject- 
ural only. In southeastern Adams county, in the region about Big 
Spring, quite a large area occurs in which the surface material is a 
red tenacious clay. No cutting was seen in this clay, and its exact 
relations and structure are doubtful. 

Stratified clays, often fine-laminated, are found in the valleys of 
most of the streams in the southern part -of the Central Wiscon- 
sin district, where they are interstratified with fine gravel and 
sand, and are often utilized for making brick. Such clays are found 
at a number of places in the Catfish Valley, as, for instance, in the 
vicinity of Madison, at Oregon, at Stoughton, etc., at times yielding 
a pure white or cream colored brick, at others, an ordinary red brick. 
The following analysis is of one of the latter kind, from a pit in the 
valley through which the Milwaukee & St. Paul mulened passes, on 
the S. E. qr. of Sec. 17, T. 7, R. 9 E., about one mile west of the 
University at Madison: silica, 75.80; alumina, 11.07; iron peroxide, 
3.53; iron protoxide, 0.31; lime, 1.84; magnesia, 0.08; carbonic di- 
oxide, 1.09; potassa, 1.14; ad, 0.40; water, 1.54; hyg roxonpte moist- 
ure, 2.16=99.56. 

These clays contain occasionally small pebbles of limestone which, 
on being baked in the middle of the brick w ill subsequently “slack ”’ 
and cause it to burst open. The clays that produce the light or 
cream-colored brick contain not unfrequently as much iron as the 
ordinary red clays, but are very much more calcareous, resembling in 
this regard the famous Milwaukee brick clay. 

The different behaviours of these two classes of clay under heat is 


624 GEOLOGY OF CENTRAL WISCONSIN. 


evidently due largely to the difference in amount of lime and magne- 
sium carbonates, but is not well understood. 

An attempt to study ont the system of arrangement of the drift 
materials meets with no little difficulty from the rarity of natural 
or artificial sections. Enough information can, however, be obtained 
from the few sections that do occur, and from records of well-borings, 
to show plainly enough the existence of the two classes of material, 
the unstratified and stratitied. The unstratified condition character- 
izes always the moraine-like heaps of limestone pebbles, and is in 
general the condition of the materials occurring on high land, and ail 
along the Kettle Range, where, however, there is often visible, in the 
sand, a rude sort of bedding, not due to aqueous action, but indicat- 
ing merely a gradual growth of the deposits. The knobby hills, 
when not formed of limestone pebbles, are often made up of layers of 
sand conforming roughly to the outlines of the hills. 

Stratified drift is to be seen in the valleys of streams, as also in 
many not now occupied by streams. A iew instances will serve to 
give an idea of what isa general truth. About a mile east of the 
Wisconsin, on the side of the road from the village of Knowlton, 
Marathon county, to the railroad bridge, finely stratified sand and 
gravel may be seen, at an elevation of over 50 feet above the river. 
The pebbles are all small, much rounded, and consist predominatingly 
of granite, with some diorite, quartz, etc, and no limestone. At 
Montello, Marquette county, in the immediate vicinity of the Fox 
river, flowing wells are obtained from what appears to be strati- 
fied drift. The wells are 50 to 90 feet deep, and pass through a 
series of layers of sand, gravel, and clay, the gravel layers at differ- 
ent horizons yielding water. A number of railnond cuttings in the 
vicinity of Madison, and to the southward along the Catfish valley, 
show finely stratified drift, one of the best points being at Stoughton 
depot, where a bank 25 feet high shows very regular layers, three 
to four inches thick, of alternating sand and gravel. On the opposite 
side of the Catfish, at a lower level, the following alternation occurs: 


Feet. Inches. 


POM nis. paroceatsnem avert e mace aopemine a ee wacine oieG amine aoa ats 1 
Bineigrayel .sicsunisatcuont is enniuites Seen ce oes aus eee wees 4 
Cross-lintinated sand .uisesceneuee veae eves so Deaw eae sa case oe aon 4 is 
Mineisravel si? sia dedee ve ways sev ek eaees oe ope dade saaswrnuen 1 6 
Cross-laminated sand ......... cece eeecee cess eneee cecueaseeue 3 et 
Horizontally laminated sand.......... 0c. c cece ec ce cc ee ereeaseee 2 2 
White brick clay to river level ...........ceneee Mai iaden Cees 15 


S| 
lo | 


THE GLACIAL DRIFT. 62% 


Of the total amount of the drift materials, it is difficult to make 
a satisfactory estimate, since the thickness is so very variable. The 
greatest amount of material appears to be in the region of the Kettle 
Range, and especially in that part of it that occupies Waushara and 
the adjoining counties. Wells in the town of Oasis, Waushara county, 
are sunk 140 to 150 feet, without striking rock. The drift hills of the 
Devil’s Lake gorge, described a short distance back, are fully 200 feet 
thick, and may reach 300. The drift hill on the University grounds, 
Madison, where the President's house stands, is 107 feet thick to the 
lake level, 122 feet to rock. The Artesian well at the Capitol Park, 
Madison, is 180 feet in drift. But the distinctly stratified drift has 
often also a considerable thickness. It is frequently the case that in 
valleys, wells sunk close to the rocky side hills will pass through 50 to 
100 feet of stratified gravel, sand and clay. Nearly all the valleys have 
their rock bottoms far below their present surfaces, whilst there are 
even evidences of entirely obliterated valleys. On the high prairie 
of Arlington, which is nearly everywhere underlaid, at a shallow 
depth, by the Lower Magnesian, wells sunk within a few rods of a 
ledge of St. Peters sandstone, on the S. E. qr., Sec. 28, pass through 
over 100 feet of loose materials. Even on the summit of the divid- 
ing ridge between Black and Yellow rivers, apparently stratified drift 
has a thickness of over 100 feet. In all of the drift-bearing region, 
wells commonly pass through 10 to 15 feet of drift-before striking 
rock, and it is probably far within the truth to say that the drift 
materials are equal toa layer 50 to 60 feet thick, spread over the 
whole drift-bearing area. : 

Three kinds of evidence are available with regard to the direetions 
of the glacial movement: the courses of the strise and grooves on 
the underlying rocks; the directions of the lines of glacial erosion; 
and the directions of travel of erratics of known origin. 

The rocks underlying the drift quite often show polishing, 
stri@, and grooves, but these markings have not remained over a 
large portion of the region, either on account of the exceedingly 
friable nature of the rock on which they have been made, or, if the 
rock be limestone, because this has suffered from the dissolving action 
of carbonated water. Moreover, over great areas, the drift conceals 
the rock basement. The markings observed are most commonly on 
limestone, which is frequently planed and scratched in a beautiful 
manner. One observation only has been made on sandstone, and this 
where the sandstone was unusually hard. The only Archean rocks 
on which the markings have been observed, are those of some of the 
isolated areas within the region of the Potsdam sandstone. In the 

Wis. Sur. — 40, 


626 GEOLOGY OF CENTRAL WISCONSIN. 


main Archean region of the district, no marked evidence of glacia- 
tion has been observed. The following is a tabulation of the obser- 
vations made: 


DIRECTIONS, ETC., OF GLACIAL STRIZ AND FURROWS. 


RS YSSiT| R. County. |Directions!} Kind of Rock. Remarks. 
1S W|14| 5/12 E) Dane...... 8. 35° E. | Trenton Limestone] Striations, 1 set only. 
2INW/]35| 6/12 BE] Dane...... 8. 5° W. | Buff Limestone...| Striations, 1 set only. 
SNWi14) 8/11 E} Dane...... 8. 19° W. | Buff Limestone...|} Striations. Fainter 
lines crossing at 
small angles. 
4|NW{17| 7/10 HE} Dane...... 8. 47° W. | Buff Limestone...| Striations. Fainter 
strie S. 40° W. 
5SINW)21] 7}9E} Dane ..... 8. 57° W. | Lower Magnesian.| Striations, 1 set only. 
6| SE {14} 8) SE] Dane...... S. 73° W. | Lower Magnesian.| Striations, 1 set only. 
7|NE/15] 8} SE} Dane...... 8. 81° W. | Lower Magnesian.] Striations, 1 set only. 
8] SE /23/10)8 E| Columbia...} West. | Lower Magnesian.| Striations. Fainter 
lines 8. 85° W. 
9}NE| 2/11/6E| Sauk....... 8. 65° W. | Potsdam sandstone} Grooves very mark- 


edly parallel, on the 
“stossed"’ end of a 
ridge. 

10INW)26|f2} 7 E} Sauk ...... 8. 85° W. | Archean Quartzite] Grooves, and fine 
striations, with glas- 
sy polished surtace. 

7E| Sauk... .. 8. 50° W. | Lower Magnesian.| Striations. 

12) NE /26/12}8 E| Columbia ..| 8. 85° W. | Archean Quartzite] Furrows 1' 6" wide, 
1"-2" deep; striations 
in same direction. 


13) SE | 3/10/12 E} Columbia . .|8. 47.5° W.| Lower Magnesian.| Striations. 
14} SE | 1/13/12 E) Columbia . .| 8. 63° W. | Lower Magnesian | Striations, 1 set only. 
15] NE} 2)17]/11 E] Green Lake] 8. 68° W. | Quartz-porphyry...| Striations, very close, 


: parallel, with pol- 
| ished surface. 


The linear topography, seen in lines of marsh, in the directions of 
streams, valleys, narrow ridges, and lakes, and in the outlines of the 
areas of the geological formations, has been described before, as char- 
acterizing especially the region of Dane and Columbia counties; and 
the bearings of these lines have been shown to coincide with the bear- 
ings of the glacial strix. A very brief examination of the table just 
given, together with Plates XXVI and XXVI A of this volume, and 
the Atlas Plates of Areas D and E will serve to show the following 
interesting facts. Beginning on the southeast, in the towns of Albion 
and Pleasant Springs, and following a curving course northwestward 
to the country about Lodi in Columbia county, we find the glacial 
striee and the linear formation outlines, stream, lake, and marsh direc- 
tions, ete., undergoing a gradual but steady change from a nearly due 
south direction to one as nearly due west, and we find this westerly 
direction continued further northward into the country of the Baraboo 


1 Trae bearings. 


THE GLACIAL DRIFT. 627 


ranges. Moreover, in this change of direction a constant position is 
maintained at right angles to the curving course of the Kettle Range. 
The southeast bearing observed in Albion is an exception to this state- 
ment, but this direction is evidently merely a local one, since in the 
country immediately east, as I am informed by Prof. Chamberlin, a 
constant direction to the south or a little west of south is observed. 
Other exceptions appear in two bearings observed in the country 
about Baraboo, but these are from places in the valley between the 
two quartzite ranges, and are evidently due, in some way, to their in- 
fluence. In going northward through the eastern parts of Columbia 
and Dane counties, though some increase in westing is seen, the gen- 
eral directions are more nearly southwest. The outline of an area of 
Trenton limestone that occurs in the adjoining corners of Dane, Co- 
lumbia and Dodge counties has been given in Fig. 54. North of 
Columbia county the linear topography continues into Green Lake 
county, but further west is not marked, nor are striz often to be ob- 
served. 

In considering the origin and directions of travel of the erratics 
and pebbles of the drift, we notice at once two classes of these mate- 
rials, those that have been carried but short distances comparatively, 
and whose exact place of origin may often be ascertained; and these 
that have traveled all the way from the Lake Superior country, and 
whose homes can generally be only roughly guessed at. It is from 
the first class of bowlders that we can get our best ideas of the direc- 
tions of the drift movement, not only because of the certainty of their 
places of origin, but because they have probably moved in more direct 
lines than those that have come from great distances. The following 
are a few facts in regard to the first class of erratics: In the eastern 
sections of the town of Deerfield, T. 7, R. 12 E., Dane county, are 
many bowlders of a bluish-gray, flinty quartzite. associated with 
others of a coarse quartzite conglomerate, both having evidently come 
from the mounds of Archean quartzite that rise through the St. 
Peters sandstone on Sces. 34, 35 and 36 of the town of Portland, T. 
9, R. 13 E., Dodge connty. The distance traveled is from 9 to 14 
miles, and the direction of travel S. 25°-30° W., coinciding closely 
with the directions of the topographical lines. On the top of the hill 
just west of the depot at Lodi, Columbia county, S. E. qr. of the N. W. 
qr. of Sec. 27, T. 10, R. 8 E.,is a bowlder some eight feet high, of hard, 
brownish sandstone, having a vitrified or quartzitic weathered crust. 
Four to six miles due east, on top of the high prairie of Arlington, 
are five small patches of St. Peters sandstone, the rock of which has 
characters exactly resembling those of the bowlder at Lodi. Midway 


628 GEOLOGY OF CENTRAL WISCONSIN. 


between the bowlder and its parent rock, on top of Kingsley’s bluff, 
near the southeast corner of Sec. 23, the Lower Magnesian is observed 
polished and striated in a due west direction. Several of the valleys 
of southern Lodi coincide with this direction. It has been stated as 
a peculiar fact that bowlders of the quartzite that make up the Bara- 
boo ranges are not found, except sparingly, to any distance south of 
these ranges, although of large size and abundant on both flanks of 
the main range, and even on its higher portions, as also in the Devil’s 
Lake gorge, and in the valley between the two ranges. The explana- 
tion evidently lies in the fact that the east and west trend of the 
quartzite blufts has coincided with the direction of the drift move- 
ment, which is proved to have been nearly due west by the bearings 
of the grooves and strise observed. The little southing that appears 
in these bearings would not carry the bowlders any distance south 
before reaching the eastern limit of the driftless region. Bowlders 
of dark colored quartz-porphyry are found along the road between 
Montello and Kingston, Marquette county, having traveled 4 to 5 
miles a little south of east from the large outerops on Secs. 2 and 3, 
T. 15, R. 11 HE. In the eastern part of the town of Marion, T. 18, R. 
11 E., Waushara county, are several mounds of granite, and in the 
country for several miles to the west and south of west, bowlders of 
the same rock are abundant. One of these, of extraordinarily great 
size, and already mentioned as occurring on the 8. E. qr. of See. 16, 
has traveled in a direction of about W. 10° S., three miles from the 
outerop on the east line of Sec. 12. A number of angular bowlders 
of Lower Magnesian limestone on the S. E. qr., See. 13, T. 17, R. 7 
E., Adams county, have been carried in a similar direction from the 
isolated limestone bluffs on Sees. 5 and 7, T. 17, R. 8 E., Marquetto 
county. A large bowlder, 30.5 feet in cireumference, of very coarso 
granite, with large surfaces of brilliant felspar, rests on top of the 
hill at Waupaca, Waupaca county, having been brought eight miles 
from a mound-like outerop of the same rock on Sec. 32, T. 23, I. 12 
E., in a direction of about 8. 60° W. 

But these bowlders, whose origin is so near their present positions, 
are but few in number, compared with those that have come from 
great distances. Most of the latter have been brought from points 
100 to 300 miles to the north, and possibly from places still further 
north. It appears probable that the region of the northern peninsula 
of Michigan has afforded a large proportion of them, though it is 
quite possible that many have come from the north shore of Lake 
Superior. The native copper fragments we may suppose to have been 
chiefly brought from Keweenaw Point, for a distance of 300 miles 


THE GLACIAL DRIFT. 629 


and over. The several kinds of red porphyry erraties are of very 
doubtful origin. No such rock occurs in the Huronian or Lauren- 
tian of North Wisconsin or Michigan, nor ain I aware that any oc- 
curs in the Copper series of Lake Superior, except in the state of 
conglomerate pebbles, which have evidently been derived from an 
older series. The limestone pebbles of the drift have come. from all 
the Silurian limestones of eastern Wisconsin, the Galena and Niag- 
ara formations having furnished the larger part. These formations 
extend in continuous belts from the south to the north line of the 
state, so that it is not often possible to say in what direction the peb- 
bles have come. 

The origin of the sand and clay of the drift may be considered 
in the same connection, though not affording more than a general 
idea as to the direction of the drift movement. The great prepon- 
derance of sand over the other drift materials, in much of Central 
Wisconsin, is without doubt to be attributed to the great surface 
spread of the friable Potsdam sandstone in the region over which the 
drift has passed. Sand is, however, also found forming most of the 
drift even far north in the Archean district, where it is sometimes in 
quantity sufficient to produce sand barrens. This fact may be regarded 
as proving a much greater surface extent north and east in the 
Archeean area of the sandstone formation in preglacial times. The 
clay has come partly, perhaps, from the limestone formations, and 
partly from the kaolinization of felspathic erratics, but its principal 
source would seem to have been the previously kaolinized granites 
and gneisses of the Archean region. It is well known that in all 
southern regions where the drift phenomena are unknown, as for in- 
stance along the Plue Ridge from Virginia to Alabama, and in Bra- 
zil, the felspathie crystalline rocks are found rotted to great depths. 
Hunt has drawn attention to the fact that in the region of the Blue 
Ridge this ceases to he the case north of the southern limit of the 
glacial drift, whose deposits lie upon the hard, unaltered, and often 
polished rock surface, and has inferred the removal of the softened 
rock by the glacial forces. ‘In that small portion of the Archean 
region of Wisconsin, in which the drift is insignificant or wanting 
entirely —as along the valley of the Wisconsin south of Stevens 
Point, and along Black river south of the crossing of the Green Bay 
road — decomposed and kaolinized gneiss and granite occur. Over 
the rest of the Archzean region, on the contrary, the drift rests directly 
upon the unchanged rock. 

No fossils of any kind have ever come to my attention as occurring 
in the drift deposits of Central Wisconsin. 


630 GEOLOGY OF CENTRAL WISCONSIN. 


The economic contents of the drift are of considerable importance. 
In many regions of the state where other limestones are either absent 
or yield only an inferior lime, the pebbles of the drift are profitably 
burnt. They yield often an excellent white lime, as, for instance, at 
several points on the Baraboo ranges, and in the sand region of Mar- 
quette and Waushara counties. The sand and gravel of the drift are 
everywhere put to use for the ordinary purposes. The gravel is occa- 
sionally transported far into the driftless region for railroad ballast- 
ing. The stratified clays of the drift are everywhere used for brick- 
making, yielding often, as at Stoughton and Oregon, in Dane county, 
a cream-colored brick fully equal to the “ Milwaukee brick.” 

The facts given in the foregoing pages will warrant a few briefly 
stated theoretical conclusions: 

(1) The drift of Central Wisconsin és true glacier drift; as is 
well shown by facts similar to those that are appealed to as proof of 
the same thing in other glaciated regions, viz.: the unstratified nature 
of the drift materials, except in stream valleys; the frequent moraine- 
like drift hills and ridges; the absence of fossils, marine or otherwise; 
the abundance of well rounded, scratched, and polished bowlders; the 
existence of a “till” with its striated pebbles; the polished, striated 
and grooved condition of the underlying rock surface; the linear and 
parallel erosion outlines; and the entire lack of any evidence of such a 
submergence of the region as would be necessary for the working of 
any other distributor of loose materials than a glacier. Moreover, in 
this special case, there is positive evidence that no such submergence 
ever did take place. This evidence is found in the sharply defined 
character and position of the drift limit, which pays no attention what- 
ever to the topography of the country it traverses, having the higher 
ground now on one side, now on the other, and crossing the highest 
ridges and lowest valleys indifferently. Only a glacier could have 
ceased its action along such a line. Jad the drift materials been 
spread by floating bergs, the sea in which these were borne would 
never have ceased along such an abrupt line, and, moreover, any sea 
which was deep enough to have floated icebergs over the higher por- 
tions of the Baraboo ranges would have carried them westward unin- 
terruptedly to the Mississippi river. 

(2) The Kettle Range of Central Wisconsin is a continuous ter- 
minal and lateral moraine. The mere fact of the existence of such 
a distinct and continuous belt of unstratified and moraine-like drift, 
which, in much of its course, lies along the edge of the driftless 
area, or, in other words, along the line on which the western foot of 
a glacier must long have stood, would go far towards proving the 


THE GLACIAL DRIFT. 631 


truth of this proposition, of which, however, a complete demonstra- 
tion appears to be at hand. In all the country just inside of the 
Kettle Range, we find that glacial strie, lines of glacial erosion, and 
lines of travel of erratics, all preserve a position at right angles to the 
course of the range, although that course veers in the southern part 
of the district from west to north. East of the Central Wisconsin 
district, as previously stated, the Kettle Range extends eastward and 
northeastward to the dividing ridge between the valley of Lake Mich- 
igan and the valley in which lie Green Bay, Lake Winnebago and the 
head waters of Rock river, and along this ridge northward into 
Green Bay peninsula. All along this part of its course, Prof. 
Chamberlin has found the glacial strie pointing east of south, and 
towards the Kettle Range, whilst along the middle of the Green Bay 
valley, he finds the strize directions parallel to the main axis of the 
valley, or a little west of south. On the west side of this great valley, 
and along the eastern border of the Central Wisconsin district, the 
strie trend about southwest, whilst still further west they gradually 
trend further to the west, becoming at last nearly due west, or at 
right angles to the western Kettle Range. 

We have then a most beautiful proof that at one time the Green 
Bay valley was occupied by a glacier, which was not merely part of a 
universal ice sheet, but a distinctly separate tongue from the great 
northern mass. The end of this glacier was long in northern Rock 
county, its eastern foot on the east Wisconsin divide, and its western 
on the summit of the divide between the Fox and Wisconsin river 
systems, as far south as southern Adams county, after which it crossed 
into the valley of the Wisconsin, and from that into the headwaters 
of the Catfish branch of Rock river, in the Dane county region. 
Whilst the main movement of the glacier coincides in direction with 
the valley which it followed, it spread out on both sides in fan-shape, 
creating immense lateral moraines. Peculiar circumstances caused 
the restriction of the eastern moraine to a narrow area, whilst that on 
the west, having no such restriction, spread out over a considerable 
width of country, the breadth of the moraine reaching in Waushara 
county as much as 25 miles. Of course this width of moraine must 
have been due to the alternate advance and retreat of the glacier foot. 
Such an advance and retreat appears moreover to be recorded in the 
long lines of narrow sinuous ridges, each marking perhaps the posi- 
tion of the glacier foot, or a portion of it, during a certain length of 
time. The intersecting of these winding ridges, which have no par- 
allelism at all with one another, appears to me to have been the main 
cause of the formation of the kettle depressions. Col. Whittlesey! 

1 Smithsonian Contributions to Knowledge. 


632 GEOLOGY OF CENTRAL WISCONSIN. 


has supposed that these owe their origin to the melting of ice masses 
included within the moraine materials, and this may possibly be true 
with regard to the more regularly circular kettles. 

The thickness of the great glacier we can only conjecture. It is 
easy to see, however, that it was at least a thousand feet, for it was 
able to accommodate itself to variations in altitude of many hundred 
feet. Morainic drift occurs on the summit of the Baraboo ranges 
over 900 feet above Lake Michigan, and on the immediately adjacent 
low ground 700 feet below. 

(3) Lhe Driftless Region of Wisconsin owes tts exestence, not to 
superior altitude, but to the fact that the glaciers were deflected 
from it by the influence of the valleys of Green Bay and Lake 
Superior. Some writers’ have thrown out the idea that the driftless 
area is one of present great altitude compared with the regions around 
it, and that by virtue of this altitude during the Glacial period it 
caused a splitting of the general ice sheet, itself escaping glaciation. 
This idea may have arisen from the fact that in the southern part of 
the area the district known as the “ Lead Region” has a considerable 
elevation; but the facts heretofore given have shown that in reality 
the driftless area is for the most part Jower than the drift-covered 
country immediately around; the greatcst development, for instance, 
of the western lateral moraine of the glacier of the Green Bay valley, 
having been on the very crown of the watershed between the Lake 
Michigan and Mississippi river slopes, whilst the driftless reyion is 
altogether on the last named slope. Moreover, to the north, towards 
Lake Superior, and to tlie west, in Minnesota, the whole country 
covered with drift materials lies at a much greater altitude. J. D. 
Whitney, in his report on the lead region of Wisconsin, favors the 
idea that the driftless district stood, during the glacial times, at a 
much greater relative altitude than now, and so escaped glaciation. 
But it is evident that in order that this could have been the case, 
either (1) a break or bend in the strata must have taken place along 
the line of junction between driftless and drift-bearing regions; or 
else (2) the driftless region has since received a relatively vastly 
greater amount of denudation than the drift-bearing. That no break 
or bend ever took place along the line indicated is abundantly proven 
by the present perfect continuity of the strata on both sides of the 
line, the whole region of Central Wisconsin being in fact one in 
which faults of any kind are things absolutely unknown. That no 
sensible denudation has taken place in Wisconsin since the Glacial 
times, in either drift bearing or driftless areas, is as well proven by the 


1 See Geological Survey of Ohio, Vol. IT. 


THE GLACIAL DRIFT. 633 


intimate connection with one another of the systems of erosion of the 
two regions. The valley of Sugar river, for instance, with itsbranches, 
is throughout its course worn deeply into the underlying rocks; on 
its east side it contains morainic drift, proving that it was worn out 
before the Glacial period, whilst on the west it extends into the drift- 
Jess regions. 
| We are thus compelled to believe that during the Glacial period 
‘the region destitute of drift had the same altitude relatively to the 
surrounding country as at present. Before the Glacial period por- 
tions of the drift-bearing region may indeed have been somewhat 
higher, for in it a considerable amount of material must have been 
removed from one place to another, by the glacial forces. The only 
satisfactory explanation remaining then for the existence of the drift- 
less region is the one I have proposed. We have already seen that 
the extent of this region to the eastward was marked out by the west- 
ern foot of the glacier which followed the valley of Green Bay. That 
it was not invaded from the north is evidently due to the fact that the 
glacier or glaciers of that region were deflected to the westward by the 
influence of the valley of Lake Superior. The details of the movement 
for this northern country have not been worked out, but it is well known 
that what is probably the most remarkable and best preserved devel. 
opment of morainic drift in the United States exists on the water- 
shed south of Lake Superior. Here the drift attains a very great 
thickness, and the kettle depressions and small Jakes without outlet 
are even more numerous and characteristic than in other parts of the 
state. The watershed proper lies some 30-40 miles south of the lake, 
and 800 to 1200 feet above it, but the morainic drift extends 25 to 50 
miles further southward. On the east side of the state the drift of 
Lake Superior merges with that of central and eastern Wisconsin, 
whilst west of the western moraine of the Green Bay glacier, it dies 
out somewhat gradually, until 125 to 150 miles south of the lake the 
the drift limit is reached. Much of the country 25 to 75 miles north 
of the driftless region, though showing numerous erratics, is quite 
without any marked signs of glaciation; as, for instance, along the 
valley of the Wisconsin from Grand Rapids north to Wausau. Fur- 
ther west the drift extends more to the southward. The course of the 
Lake Superior glaciers conveyed them further and further southward 
as they moved westward. : 

Future investigations will undoubtedly bring out a close connec- 
tion between the structure of the Lake Superior valley and the glacial 
movements south of it. Even the facts now at hand seem to point 
toward some interesting conclusions. Projecting from the south 


634 GEOLOGY OF CENTRAL WISCONSIN. 


shore of Lake Superior, we find two great promontories, Keweenaw 
Point, and the Bayfield Peninsula. Both of these projections have a 
course somewhat transverse to the general trend of the lake, bearing 
some 30° south of west. Both have high central ridges or backbones, 
which rise 1,000 to 1,500 feet above the adjacent lake, and are made 
up of bedded igneous rocks, sandstones, and conglomerates of theCop- 
per Series. Both of these ridges continue far westward on the main- 
land, haying between them a valley, partly occupied by the lake, 
which is a true synclinal trough, the rocks of the two ridges dipping 
towards one another. North of the Bayfield Peninsula, and again 
south ot Keweenaw Point, we find two other valleys running in from 
the lake shore in the same direction. In all probability each one of 
these valleys has given direction toa glacier tongue. An inspection 
of a good map of the northern part of Wisconsin, Minnesota and 
Michigan will serve to show that the almost innumerable small lakes* 
of these regions are concentrated into three main groups, each group 
corresponding to a great development of morainic drift, and lying in 
the line of one of the three valleysjust indicated. I suppose that 
each of the lake groups is a moraine of the glacier which occupied 
the valley in whose line it lies. The main ice sheet coming from 
the north met, in the great trough of Lake Superior, over 2,000 feet in 
depth, an obstacle which it was never able to entirely overcome, and 
so reached further southward in small tongues composed perhaps of 
only the upper portions of the ice. These tongues being deflected 
westward by the rock structure of the country, and having their force 
mainly spent on climbing over the watershed, left the region further 
south untouched. The eastern part of the Lake Superior trough is 
not nearly so deep as the western, and the divide between Lake Su- 
perior and the two lakes south of it never attains any great altitude, 
so that here the ice mass, having at the same time perhaps a greater 
foree on account of its nearness to the head of the ice movement on 
the Laurentian highlands of Canada, was able to extend southward 
on a large scale, producing the glaciers of the Green Bay valley and 
of Lake Michigan. 

Although quite crude in its details, Iam convinced that the main 
points of the explanation thus offered for the existence of the drift- 
less region in the northwest will prove to be correct. To obtain a full 
elucidation of the subject, much must yet be done in the way of in- 
vestigation, not only in Wisconsin, but over all of Minnesota and the 
states south, in order that the details of the ice movement for the 
whole northwest may be fully understood. 


1 Far more numerous in reality than shown on the best maps. 


LACUSTRINE CLAYS— BOG IRON ORES. 6385 


(4.) The stratified drift of the valleys owes its structure and distri. 
bution to the water of the swollen streams and lakes that marked the 
time of melting of the glaciers. 

(5.) Lhe depth below the present surfuces of the rock valleys ap- 
pears to indicate a greater altitude of this part of the continent, du- 
ring the Glacial period, than at the present time. 


LACUSTRINE CLAYS. 


Extending inland from Lakes Michigan and Superior for many 
miles, and reaching elevations of several hundred feet above the lakes, 
are stratified beds of loose material, chiefly marly clays, with more 
or less sand, some gravel and a few bowlders. These are proved to 
be, with but little doubt, of lacustrine origin, by the manner in which 
they follow the shores of the lakes, and they register a depression of 
several hundred feet, corresponding to the period subsequent to the 
melting of the glaciers, when all the lakes and streams of the north- 
ern part of the United States were greatly expanded beyond their 
present limits, and the whole northern part of the continent stood at 
a lower level. 

In the Central Wisconsin district the lacustrine clays have only a 
small development, most of the district being either too high to have 
been reached by the lake depositions, or else lying behind the divid- 
ing ridges. The eastern towns of Waushara county, however, are 
underlaid by a considerable thickness of red clay belonging to this 
formation. The surface elevation of the country here is 160 to 200 
feet above Lake Michigan, and the clays 80 to 100 feet and over in 
depth, as shown by numerous Artesian well borings that yield a flow 
of water which is obtained from seams of gravel at different horizons 
in the clay. The clay of eastern Waushara county is part of a large 
clay area that extends up the Green Bay valley from Lake Michigan. 


BOG IRON ORES. 


The most recent formations of the Central Wisconsin district are 
the marsh deposits of peat and bog iron ore. The latter is found on 
a small scale underlying the peat of many marshes, and also oceur- 
ring at points not now marshes, but still showing signs of a marsh 
origin. The large marshes of Juneau, Wood and Portage counties 
have yielded the best indications of the existence of good bog ore, 
although the points at which any quantity can be seen. are few in 
number. 

At Necedah, Juneau county, immediately south of an isolated 
hill of Arehean quartzite, is a tongue of the great marsh that 


6386 GEOLOGY OF CENTRAL WISCONSIN. 


spreads widely over northwestern Juneau county and into the adjoin- 
ing counties of Jackson and Wood. Underneath the peat of this 
marsh tongue, and aloug the banks of a dry run east of the marsh, 
bog ore occurs in some quantity. The best ore is found on the 8. E. 
qr. of Sec. 24, T. 18, R. 3 E., on‘ land belonging to Mr. J. T. Kings- 
ton, where it lies at about 3 feet below the surface of the marsh, be- 
ing covered by peat and peaty marsh mud. It is seen in the bottom 
of a ditch for some 40 rods, and can be raised by the crowbar in large 
firm blocks. These are very porous, but between the pores show a 
dark brown, very hard, fibrous, silky-lustred limonite. Immediately 
over the hard ore, in places, is a sand or shot ore, composed of rolled 
grains of limonite. The thickness is reported at 23 feet. The fol- 
lowing analysis shows the composition of a sample (1356) averaged 
from a considerable quantity: silica, 8.52; alumina, 3.77; iron perox- 
ide, 71.40; manganese oxide, 0.27; lime, 0.58; magnesia, trace; phos- 
phoric acid, 0.21; sulphur, 0.02; organic matter, 1.62; water, 
13.46 = 99.85: metallic iron, 49.98. Following the stream south- 
ward into the N. E. qr. of See. 25, the ore grows much leaner, being 
mingled with sand (13564). The same sandy ore is seen along the 
side of a dry run on the N. W. qr. of Sec. 30, T. 18, R. 4 E., an aver- 
age sainple yielding only 16.09 per cent. of metallic iron. Mr. 
Kingston’s ore is certainly an excellent one, and the marsh is well 
worthy of further investigation. 

At Point Bass, Wood county, on the west bank of the Wisconsin 
river, near the center of Sec. 10, T. 21, R. 5 E., on land belonging to 
the Hon. Moses M. Strong, a porous bedded limonite is exposed in the 
river bank, 15 feet above the water. The exposure extends along for 
some 50 feet, and appears to be some 8 feet in thickness, the upper 
3 feet being a porous but quite pure ore, containing some 50 per 
cent. of metallic iron. Two hundred feet down stream a cutting into 
the river bank shows that the ore does not continue in that direction. 

At several points on the east bank of the Wisconsin, north of 
Grand Rapids, on Sec. 4, T. 22, R. 6 E., and See. 34, T. 23, R. 6 E., 
sinall openings show ore just like that described. At one of. these 
points, on Mr. McGrath’s land, the ore is seen with a thickness of 20 
inches, very evenly and thinly bedded, and extending over an area of 
about 75 feet square. The following analysis, made by Mr. Oliver 
Matthews, a student of the Metallurgical Department of the State 
University, shows the composition of an averaged sample: silica, 
4.81; alumina, 1.00; iron peroxide, 73.28; lime, 0.11; magnesia, 
0.25; sulphuric acid, 0.07; phosphoric acid, 0.10; organie matter, 
5.88; water, 14.24=—99.69: metallic iron, 51.26. 


APPENDIX — MICROSCOPIC LITHOLOGY. ° 637 


APPENDIX. 


MICROSCOPIC LITHOLOGY. 


BY CHARLES E. WRIGHT. 


(Nore. — The following descriptions are of a small number of crystalline rocks selected from ths 
large mass of material on hand, as mast difficult to determine, or as having a special importance. 
The numbers are the same as given in the body of the report, and the original specimens will be 
found in the survey collections, when distributed. A few of Mr. Wright’s descriptions have been 
made use of in the foregoing pages, but the descriptions of crystalline rocks there given are 
nearly always wholly my own. It is a matter of regret that the funds were not available for micro- 
scopic examination of a ful) suite of the Central Wisconsin rocks. R.D.I.] 


501. Silicious Hornblende-Schist. Huronran? Black river, Jackson county, 
north line Sec. 14, T. 21,R.4W. Light-greenish-black; very fine-grained; crystalline 
texture; conchoidal fracture; hard and compact. With the lens, minute grains of silica, 
are plainly visible, but the ingredient mincrals cannot be distinguished. Under the mi- 
croscope, in the polarized light, a thin section of the rock presents a very pretty field, 
and is composed of small fragments of amphibole, minute grains of quartz, and a few 
scattered leaves of chlorite. From the structure it is evident that the amphibole formed 
after the quartz, since the former encloses grains of the latter. 

757. Granite. Hurontan? Village of Montello, Marquette county, S. W. qr. 
Sec. 9, T. 15, R.10 E. Pale flesh-color, dotted with a few dark patches of mica. The 
facets of felspar are easily recognized. Traversing the specimen is a thin, light-green- 
ish seam of what appears to he epidote. Under the microscope, in the polarized light, 
the coarse fragments of orthoclase apparently constitute more than one-half the en- 
tire section. An occasional twin crystal of felspar after the Carlsbad form may. be 
seen. The grains of quartz are mostly very small and angular, and are trequently 
enclosed within the felspar. With a power of 500 diameters are visible, in the quartz, 
fluid inclusions; the absence, however, of any glass or stone-filled cavities will no doubt 
refer the rock to a metamorphic origin. 

758. Argillo-chloritic Schist. Huronran? Village of Montello, Marquette County, 
S. W.qr. Sec. 9, T. 15, R. 10 E. Grayish-green; fine-grained texture; partially decom- 
posed; cleaves readily into irregular plates; in the joints it is often ocherous; under the 
microscope the pale greenish leaves of chlorite are plainly visible; also minute grains of 


silica and a few scales of hematite. 


638 GEOLOGY OF CENTRAL WISCONSIN. 


766. Granite. Huronran? Near Spring Lake, Waushara county, N. E. gr. See. 
27, T. 18, R.11 E. Similar to 757 from Montello. The felspar is more or less decom- 
posed; but this is probably local or accidental. 

859 1-2. Hornblende Schist. Laurentran. Grand Rapids of the Wisconsin, 
Wood county, S. W. qr. Sec. 8, T. 22, R.6 £. Bright greenish-black sprinkled with gray; 
fine-grained, highly crystalline texture; conchoidal fracture; the fresh surface having a 
raspy feel; several specks of iron pyrites are strewn along the joints; under the microscope 
can be easily recognized the amphibole, and considerable orthoclase felspar; also angular 
grains of quartz and several fluid inclusions, or small liquid-filled cavities. The speci- 
men resembles the hornblende-schist of the Marquette iron district. 

897. Hornblende Rock. Laurentian. Little Bull Falls, Marathon county, See. 
29, T. 27, R.7 E. Dark grayish-green; medium to fine-grained, crystalline texture; un- 
even fracture and somewhat jointed. The mineral ingredieuts can not well be distin- 
guished with the lens. Under the microscope, however, the amphibole, and plain and 
striated fragments of felspar, are easily recognized; also, a little chlorite, and a few 
grains of quartz. 

898. Syenite. Laurentian. Little Bull Falls, Marathon county, Sec. 29, T. 27, 
R.7 E. Greyish-white, spotted with greenish-black; coarse-grained texture; the amphi- 
bole and felspar are plainly visible to the naked eye. Under the microscope the felspar 
appears to be somewhat altered, and a few of the crystals are striated. An occasional 
fragment of quartz may be seen; also a little chlorite. The former contains fluid in- 
clusions. 

398 a. Hornblende Rock. Laurentian. Little Bull Falls, Marathon county, Sec. 
29, T. 27, R. 7 EH. Greenish-black, mottled with grayish-white; medium to coarse- 
grained; uneven fracture; the felspar and amphibole are plainly visible. It resembles 
very much a diorite. Under the microscope, the essential minerals are easily recognized. 
The felspar, owing to the partial decomposition, presents a milky texture, which frc- 
quently renders it nearly opaque. The grains of quartz, however, are clear and limpid. 
The specimen, no doubt, is a coarser variety of 897. 

902. Silicious Chloritic Schist (provisional). Laurentian. Little Bull Falls, 
Marathon county, Sec. 29, T. 27, R. 7 E. Very dark greenish-gray, and slightly 
tinged with bluish-black; weathers to a light drab; fine-grained texture and schistoso 
structure. Under the microscope, the section appears composed of chlorite, small 
grains of silica, brownish leaves of mica, and a few fragments of amphibole. 

905. Chloritic Hornblende Rock. Laurentian. Little Bull Falls, Marathon 
county, Sec. 29, T. 27, R.7H. Greenish-black; aphanitic texture; very jointed and ap- 
parently schistose; weathers to a dirty drab. Under the microscope can be seen the am- 
phibole and quartz. The felspar is very much altered, but may be recognized by a mo- 
ment’s careful observation. Considerable chlorite is contained, also an occasional scale of 
mica. It is possible that this rock is a less altered variety of 902, and therefore passing 
into a silicious chloritic schist. 

907. Syenitic Granite. Laurentian. Big Bull Falls, Marathon county, Sec. 
26, 7. 29, R.7 E. Pinkish, speckled with greenish-black; medium-grained texture; 
rough, uneven fracture. The felspar is easily recognized. The amphibole and black 
mica are scarcely to be distinguished from each other, even with a strong lens. Under 
the microscope this similarity still exists, but the position of the optical bisectrix to the 
principal crystallographic axis in the hornblende readily separates it from the mica, 
The former, however, is in excess of the latter. The felspars are mostly twinned, after 
the Carlsbad form; some of them appear, in the polarized light, to be irregularly band- 
ed, which is probably duc to an unequal decomposition. Numerous angular grains of 
quartz are present. The rock is evidently metamorphic. 

908. Syenite. Laurentian. Big Bull ‘Falls, Marathon county, See. 26, T’. 29, 


APPENDIX — MICROSCOPIC LITHOLOGY. €39 


R.7E. Gray, thickly speckled with black; fine to medium-grained; rough, uneven 
fracture; the felspar and hornblende are plainly visible to the naked eye. Under the 
microscope, each of the above minerals is easily recognized. The felspar fragments 
are chiefly plain, though a few of them are beautifully striated in one direction. Very 
little quartz is contained. 

910. Syenite. Laurentian. Big Bull Falls, Marathon county, Sec. 85, T. 29, R. 
7E. Same as 908, but coarser grained, and some of the grains of quartz contain cavi- 
ties filled with a salt solution, out of which have crystallized small, transparent cubes of 
salt. The small bubble and crystals are easily distinguished from each other, even 
when the corners of the cube are rounded, by the difference of their refractive indices. 
Scarcely any motion is perceptible in the bubbles, even when heated to 130° C. 

915. Silicious Hornblende-Schist. Laurentian. West bank of Wisconsin 
river, north line Sec. 26, T. 29, R.7 E. Grayish-black; very fine-grained, arenaceous 
texture; jointed and irregular fracture. Under the microscope, in the polarized light, 
the section appears composcd of a silicious base, interspersed with fragments of am- 
phibole, felspar, and dark colored mica. The felspar is of two varieties, one in small 
striated fragments, and the other in large plain ones, which are very much altered, fre- 
quently so much so that only an indistinct outline remains. 

932. Chloro-Silicious-Schist (provisional). LaurrentTian. East Bank Wis- 
consin river, S.W. qr. Sec. 1, T. 29, R. 7 E. Grayish-green; aphanitic texture; 
conchoidal fracture; slightly banded. Under the microscope the greenish chloritic 
base is interspersed with small angular grains of felspar and silica. An occasional patch 
of calcite may be recognized. 

932a. Very Silicious Marble’ (provisional.) Laurentian. East bank Wis- 
consin river, S. W. qr. Sec. 1, T.29, R. 7 EB. Grayish-green; aphanitic texture; 
conchoidal fracture; slightly banded. A fragment thrown into acid effervesces briskly, 
for a time, without disintegrating. Under the microscope it presents an indefinite 
fringy base, strewn with small crystals of felspar, grains of quartz, and greenish leaves 
of chlorite. 

948. Chloro-Silicious-Schist (provisional). Laurentian. Falls of Big Rib river, 
Marathon county, N. E. qr. Sec. 28, T. 29, R. 5E. Resembles 932. Under the 
microscope the base of the rock is composed largely of decomposed crystals of felspar; 
scattered in this are numerous fragments of amphibole and leaves of chlorite. The rock 
is apparently an altered hornblende-schist. 

948a. Chloro-Silicious-Schist (provisional). Same place as 948, to which it is 
closely similar. 

950. Syenite. Laurentian. Falls of Big Rib river, Marathon county, N. E. qr. 
Sec. 28, T. 29, R. 5 E. Light-pinkish-gray, mixed with dark-gray and black; medi- 
um to coarse-grained, indefinite texture. A few crystal-facets of felspar may be recog- 
nized, but they are mostly too much altered to have preserved their cleavage. This 
altered condition is very apparent under the microscope, where the section appears 
thickly strewn with indistinct outlines of the altered crystals, though some are quite 
fresh. The amplibole is also somewhat changed. A few angular grains of quartz are 
present, and they sliow liquid inclusions. 

952. Granite. Laurentian. Falls of the Big Rib river, Marathon county, N. E. 
gr. Sec. 28, T. 29, R. 5 BE. Grayish-white, spotted with dark-green; medium-grained, 
With the loupe, small, glassy grains of quartz may be recognized. The felspar is so 
much decomposed that it shows but little signs of cleavage. Under the microscope the 
crystals of felspar are grayish and indistinctly outlined. .A grecnish chlorite is contained, 


1 This rock is merely a phase of the preceding one (932) most specimens of which show no 
eflervescence with acid. R. D. I. 


640 GEOLOGY OF CENTRAL WISCONSIN. 


which is very much altered. The grains of quartz appear angular, and contain numer- 
ous fluid inclusions. 

953. Chloritic Schist (provisional). LAURENTIAN. Falls of Big Rib river, N. 
E. qr. Sec. 28, T. 29, R. 5. E., Marathon county. Light and dark-green; talcose or 
chloritic texture; warped schistose structure. Hardness about 4. Under the microscope 
a section of the specimen appeais to consist largely of altered crystal fragments of fel- 
spar, and grains of quartz, scattered in a greenish chioritic base. The rock is probably a 
syenitic and hornblende schist ash. 

958. Talco-Mica-Schist. Arcuman. Cutting on the W. V. RB. R., three 
miles north of Junction City, Sec. 24, T. 25, R.6 E. Light drab; talcose texture on 
lamination planes and arenaceous across the grain; cleaves readily into irregular finely- 
ribbed plates; somewhat altered, and emits a strong clay odor when moistened. Under 
the microscope the light scales of tale are hardly distinguishable from those of mica, but 
the dark ones of the latter are more easily recognized. The section is composed largely 
of small angular grains of silica. The argillaceous odor is due to the numerous de- 
composed fragments of felspar. 

961. Caleareous Mica-Schist. ARcHaAN. Cutting on W.V.R. R., twoand a 
half miles north of Junction City. Sec. 26, T. 25, R. 6 E., Portage county. 
Dark-green; fine-grained texture. A fracture in the direction of the cleavage glistens 
with bright, dark greenish-black scales of mica. A lump thrown into acid effervesces 
briskly, leaving a friable mass. Under the microscope the crystals of calcite are striated 
showing thei usual proneness to twin. The angular grains of quartz and leaves of 
mica (biolite) are readily distinguished, also opaque crystal cubes of pyrites. The separ- 
ate mineral ingredients are arranged in bands or layers. 

962. Mica-Schist. Anciraan. From cutting on W.V. R. R., one and a half 
miles north from Junction City, Sec. 35, T. 25, R. 6 E.., Portage county. Light drab; 
fine-grained, arenaceous texture across the lamination; slightly shimmering along the 
schist planes. The minute scales of mica are hardly recognizable to the naked eye. 
Under the microscope, in the polarized light, a section of the specimen appears brightly 
colored with angular grains of silica. The base of the rock presents a dirty appearance, 
and scattered in it are the brownish leaves of mica and a few altered crystal fragments 
of felspar. 

963. Hornblende-Schist. Ancuaman. From a cutting on the W.V. R. R., 3% 
mile north of Junction City, Sec, 35, T'. 25,R.6 E., Portage county. Dark-green. It 
is somewhat altered and has a dirty lock. The single mineral ingredients can barely 
be recognized with the naked eye, but under the microscope are plainly visible the 
amphibole, quartz and mica, also a little chlorite. 

964. Hornblende-Schist. Arciman. From a cutting on the W.V.R.R., 71-2 
miles south from Junction City, north part of T. 23, R.6 E., Wood county. Dark 
grayish-green; fine-grained, crystalline-texture; schistose structure and jointed; 
weathers to a drab. Under the microscope it appears to consist mostly of amphi- 
bole. Several small grains of quartz are contained, also a little chlorite. 

968. Chloritic Rock. Anciaan. From east side of Wisconsin river, 5 miles 
south of Mosinee, L. 26, R.7 E., Marathon county. Grayish-green; aphanitic text- 
ture; very jointed and apparently schistose. Under the microscope the base of the sec- 
tion presents a moss-like microcrystalline structure, and scattered through it are highly 
altered crystals of felspar, which are usually very indistinct, only the faint outlines re- 
maining, With a power of 500 diameters the small pale-greenish leaves of chlorite are 
visible, also numerous minute particles of magnetite. 

970. Quartz-Porphyry. Aromaan. From the bed of Yellow river, 3 miles north 
of Dexterville, See.3, T. 22,R. 3 B., Wood county. Light pea-green; massive; resem- 
hles some of the quartzites. Several erystal-facets of felspar may be seen, also an occa- 


APPENDIX — MICROSCOPIC LITHOLOGY. 641 


sional small quartz crystal. Under the microscope a section of the specimen appears 
composed chiefly of felspar, with a few crystals of quartz scattered through it. The 
quartz resembles that contained in igneous rocks, since some of the crystals enclose, ap- 
pirently, portions of the matrix. Their richness, however, in fluid cavities, would no 
doubt preclude such a supposition. The felspar is somewhat altered and presents fre- 
quently afringy texture. A few spherulites of felspar so common to quartz-porphyries 
may be recognized. 

992. Felspathic-Schist (provisional). ARcHaman. Cutting on W.V.R.R., 3.7 
miles south of Knowlton, Sec. 12, T. 25, R. 6 E., Portage county. Grayish-drab; fine- 
graincd, indefinite texture. A few minute crystal-facets are visible; emits a strong day 
odor when breathed upon. Under the microscope the rock appears very felspathic, and 
some of the crystals are beautifully banded. Numerous small angular grains of quartz 
are contained, also brownish leaves of mica, and a fibrous mineral resembling talc. 

997. Actinolite-Schist. Ancuaan. Cutting on W.V.R. R., 8.7 miles south of 
Knowlton, Sec. 12, T. 25, R. 6 E., Portage county. Light-green, medium-grained, 
crystalline texture. The cleavage faccts of the actinolite are easily recognized. It is 
somewhat decomposed. Under the microscope the actinolite presents a reticulated 
structure; a little quartz, felspar and chlorite are contained. 

1003. Diorite. Arcuaman. From bed of Black river, Mormon Ripple, Sec. 3, T. 
22, R.3 W., Jackson county. Light-and-dark-green; weathers to a light-drab; me- 
dium-grained texture, with coarse crystals of amphibole strewn through the mass. 
Under the microscope the principal mineral ingredients appear to be amphibole and 
felspar; the latter is of two kinds, plain and striated. An occasional crystal fragment 
resembling augite is contained, also a little chlorite. 

1004. Quartzite. Arcuman. From bed of Black river, Mormon Ripple, Sec. 3, 
T. 22, R. 3 W., Jackson county. Light reddish-gray, with streaks of dark-green; 
quartzose, vitreous texture. Under the microscope appears, in addition to the quartz, a 
considerable number of slightly altered crystals of orthoclase and grecnish leaves of 
mica or possibly chlorite, though they are apparently the former, since they are strongly 
dichroitic. 

1005. Felspathic Quartzite, or Granite. Arncnaan. From bed of Black river, 
at Mormon Ripple, Sec. 3, T. 22, R. 3 W., Jackson county. Flesh color; medium- 
grained texture. On a fresh fracture may be seen numerous bright cleavage facets of 
felspar. Under the microscope the felspar and quartz appear to be about equally di- 
vided. The former are mostly plain crystals, and the latter enclose numerous fluid 
cavities. 

1007. Micaceous Schist. Arcuaman. From the bed of Black river, at Mormon 
Ripple, Sec. 8, T. 22, Rh. 3 W., Jackson county. Drab; fine-grained, arenaccous texture; 
somewhat decomposed and emits a strong clay odor when moistened. Under the mi- 
croscope a section of the specimen appeazs to consist largely of altered brownish frag- 
ments, resembling mica. Scattered in the base are numerous small angular grains of 
silica. 

1008. Granite. Arcm#an. From bed of Black river, at Black River Falls, 
Sec, 15, T. 21, R.4 W., Jackson county. Flesh-color, spotted with dark-green; medium- 
grained texture. The crystal-facets of felspar and grains of quartz are plainly visible 
to the naked eye. Under the microscope the felspar appears to be more largely con- 
tained than the quartz. But little mica is present. 

1412. Quartz-Porphyry. Hurontan? Pine Bluff, N. W. qr. of the N. E. qr. 
of Sec. 2, T. 17, R.11 E., Green Lake county. Cxayish-white; fine-grained texture, 
and porphyritic with glassy crystals of felspar, which resemble sanadin. Under the 
microscope, the specimen seems to be an intimate mixture of felspar and quartz. Some 
of the felspar crystals have an appearance as if, after they were formed, they had been 

Wis. Sur. —41 


642 GEOLOGY OF CENTRAL WISCONSIN. 


partially dissolved, or replaced in part by crystalized silica; the latter presenting in the 
polarized light colored patches which have frequently their crystallographic axes all 
lying in the same direction. On the other hand, many of the quartz grains enclose crys- 
tals of felspar, but these may be instances where the felspathic material has been 
almost entirely replaced by the silica. The quartz resembles vein quartz and contains a 
few fluid inclusions. 

1430. Quartz-Porphyry. Huronran? From head of Lake Buffalo, N. E. qr. 
of Sec. 8, T. 14, R.9, E., Marquette county. Dark reddish-brown; porphyritic texture. 
The cleavage facets of the felspar are the only mineral ingredients that can be recog- 
nized by the naked eye. With the microscope, the base presents a semi-granular moss- 
like texture, in which are strewn a few crystals of orthoclase and quartz, also numerous 
small crystal grains of magnetite. To the latter is due the dark color of the rock. 


Tit Miracamer in Luria XP 


VIEW OF BLUFF OF GALENA LIMESTONE, 


Near Gassville on the Mississippi. 


PART IV. 


—___ 


GEOLOGY AND TOPOGRAPHY 


OF 


THE LEAD REGION. 


‘BY MOSES STRONG. 


GEOLOGY AND TOPOGRAPHY! 


OF 


THE LEAD REGION, 


CHAPTER L 
INTRODUCTORY AND HISTORICAL. ' 


Survey of 1873. In accordance with my instructions received 
from the late Dr. I. A. Lapham, in May, 1873, to make a survey of 
two lines, with sections of the strata; one north and south, and the 
other east and west, crossing at or near Mineral Point, work was com- 
menced on the 5th of June, 1873, at Scales Mound, IIl., as being 
near the southern boundary of the Lead region. 

The territory examined during the year 1873 is as follows: Town 
29 N., ranges 2 and 3 E., in the state of Illinois; towns 1 to 13 inclusive, 
in ranges 2 and 3 E., in the state of Wisconsin; towns 4 and 5, on 
ranges 1 to 6 W., to the Mississippi river; towns 4 and 5, on ranges 
1, 2, 83,4 and 5 E.; towns 6, 7, 8 and 9, on ranges 5 and 6 E., to the 
Wisconsin river, being in all an area of about 50 townships. 

Explorations were chiefly confined to the territory already men- 
tioned; departures were, however, occasionally made for the purpose 
of visiting localities of geological interest or mineralogical import- 
ance. In order to complete the survey of so large a tract of country, 
it was necessary to traverse an average area of twelve square miles 
per day. Such an amount precluded anything more than a careful 
examination of the more important localities, and a general inspection 
of the rest. 

The advantages of this plan of operations were numerous, but 
chiefly these: that by the examination of a tract of country twelve 
miles in width, passing through the center of Grant, Iowa and La 
Fayette counties, a large and comprehensive view of the entire Lead 
region was secured, so far as its general features were concerned; the 


646 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


details of which, belonging to each separate locality, could be more 
easily and intelligently obtained in the progress of the survey of 
this and the succeeding year. Further, it was necessary for topo- 
graphical purposes to ascertain the elevation of numerous points, 
which should be readily accessible to the various parts of the region, 
as will be more fully explained under the subject of Barometrical 
Observations. 

The greater part of the summer of 1873 was devoted to these pur- 
poses, and spent within the confines of the Lead region, with the 
exception of the latter part of July, and two weeks in August, which 
were passed in the counties of Sauk and Richland, in the examination 
of the Potsdam and Lower Magnesian formations, and the iron ore 
deposits incidental thereto. 

Survey of 1874. The territory examined in that year was as fol- 
lows: 


xn 
nee) 
' 


Towns 
“ce 


NA 
1 
' 


1 

2 

“ oy) 
6c 3; 
1 

1 

1 


“ce 


Qe coe 
rinssss 
Ree Oe 


“cc 


' BUR RDO DED 


“ 


The townships here enumerated comprise the northern and south- 
ern parts of Grant county, the eastern and western parts of La Fayette 
county, the western part of Iowa county, and that part of it which is 
drained by Mill creek, the whole of Green county, the western part 
of Richland county, and some parts of Vernon, Monroe and Jackson 
counties. 

The field work was commenced on the 14th of May, 1874, nearly 
three weeks earlier than in 1873. The total area examined is equal 
to sixty-six full townships, being an increase of sixteen over the pre- 
vious year. 

The first examinations were made in the vicinity of Cassville, pro- 
ceeding eastward from there to the eastern boundary of Green county, 
and visiting successively all the mining districts and individual 
mines, of which a full report will be found in chapter IV. After 
exainining the Mill creek district, the survey next proceeded to range 
two west, north of the Wisconsin river, including the valley of Knapp 
creek and the upper Kickapoo, and as far Tonle as the Green Bay & 
Minnesota railroad. Finally returning from there, the northeastern 
part of Iowa, and the northern part of Grant counties were examined, 
together with that part of the valley of the Wisconsin which lies 
south of the river. — 


INTRODUCTORY AND HISTORICAL. 647 


Previous Publications and Surveys. The firat geological survey 
embraced the extensive district lying between the Missouri river and 
Red river of the North, and included the upper part of the valley of 
the Mississippi and the mining districts adjacent to that river. It 
was undertaken in 1834, and completed in 1835, by the general gov- 
ernment, and placed in charge of G. W. Featherstonhaugh. 

The next survey was also instituted by the general government, 
and placed under the direction of Dr. D. D. Owen, in the fall of 
1839, and completed by him in the same year; its object being to as- 
certain the geographical position of the Lead region and its value as 
mineral land. Dr. Owen was afterward engaged in the geological 
survey of the Chippewa Land District, during 1847-8, of which he 
published a final report in 1851, accompanied by a general geological 
map. The exploration of so large a district did not admit of a mi- 
nute examination of any particular part: thus, the space devoted to 
the southwestern part of the state, and lying south of the Wisconsin 
river, is comprised in about twenty pages of chapter I. 

The next geological survey was undertaken under the auspices of the 
state, in 1853, and placed in charge of Prof. E. Daniels, who published 
in 1854 a pamphlet concerning the Lead region. He was then suc- 
ceeded by Dr. J. G. Percival, who held the pusition of State Geolo- 
gist, until his death, in May, 1856. He published two reports of 
about 100 pages cach, which contain much valuable information, and 
bear evidence of the careful research which always distinguished his 
work. 

To complete the survey interrupted by the death of Dr. Percival, 
Profs. James Hall, E.8. Carr and E. Daniels were appointed; and, in 
1858, Prof. Daniels published a report of about 60 pages, on the iron 
ores of Wisconsin. This was succeeded by the report of Profs. Hall 
and Whitney, in January, 1362. This was by far the largest report 
that had been published concerning the Lead region. It comprised 
about 450 pages, of which 300 were devoted to that district. This 
report was accompanied by a crevice map of the mineral ranges, and 
a general geological map of the Lead region. The latter, so far as it 
was made from.personal observation, was quite correct; but it still left 
much to be desired in this department; which deficiencies, it is be- 
lieved, have been supplied by the present survey. 

For ten years the Geological survey was discontinued. The next, 
being the examinations of Rev. John Murrish, of which he published 
a report in 1872, in a pamphlet of sixty-five pages. 

Topographical and Geological Maps and Sections. A great deal 
of time has been devoted to the construction of the maps accompanying 


648 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


the report, so as to represent the topographical features of the country 
vith accuracy. The topographical maps herewith published embrace 
all the Lead region. They comprise the country lying south of 
town six, and extending from the Mississippi river eastward, to the 
line between Rock and Green counties, with the exception of town 
five in ranges 4, 5, 6, 7,8 and 9 E. The maps are made on the scale 
of one inch to the mile, and exhibit by contour lines, fifty feet apart 
(vertically), the elevation of any point above the level of the sea. The 
elevation of any point not on these lines must be determined by its 
relative distance from the two contour lines between which it lies. 
In addition to this feature (not found on any other map), a complete 
road-map is presented; alsoa map of the streams and dry ravines, 
many of the smaller streams having become dry since the original gov- 
ernment survey of the country was made. Again, from an inspection 
of these maps, can be seen the rise of the various streams, and the 
height of the dividing ridges. This is also of special value in respect 
to railroad surveys, when the amount of time and money is consid- 
ered, which is annually spent in ascertaining these points. It is be- 
leived that a tolerably correct idea of the practicability or impractic- 
ability of any contemplated route can be obtained by reference to 
these elevations, and thus a vast amount of preliminary surveying 
may be dispensed with. 

One of the principal objects of the field-work has been the careful 
delineation of the geology of all parts of the country, and its correct 
representation on the colored maps which accompany the reports. In 
addition to the general geological maps of the state drawn on a scale 
of three miles to the inch, the geology of the Lead region has also 
been placed upon the topographical maps. The effect of this is to 
show the dip and thickness of the strata and “ the exact position of 
the mining ground at each locality.” The great extent of country 
which has been examined and mapped, together with the time and 
means which admitted of only a general survey, in which the contour 
lines, both geological and topographical, could, be sketched only by 
the eye, preclude that accuracy which is attainable only with the tran- 
sit and level. For such imperfections and inaccuracies as may be 
found to exist in the maps, these circumstances must be our apology 
and explanation. 

The geological sections accompanying the maps are chiefly valuable 
as showing the “ dip, number, magnitude, order and relative position 
of the various strata,’ as well as the amount of denudation to which 
the conntry has been subjected. They are located as far as possible 


IFTRODUCTORY AND HISTORICAL. 649 


in the general direction of the dip, in order to show the structure, ar- 
rangement and irregularities of the strata. 

Barometrical Observations. Considerable time has been devoted 
to ascertaining the relative heights of different parts of the country, 
for the purpose of ascertaining the amount of denudation, and pre- 
paratory to making geological sections. These observations con- 
sumed a great deal of time, and were made with much care; the plan 
followed being as follows: A series of repeated observations were 
made at points about half a mile apart, from the Illinois Central rail- 
road at Seales Mound, to Calamine, on the Mineral Point railroad, and 
from there to Mineral Point. A similar series was then carried from 
there to Lone Rock, on the Chicago, Milwaukee and St. Paul railroad, 
and from there to Lavalle, on the Chicago and Northwestern railway. 
In the same manner a series was carried from Mineral Point through 
Lancaster, to Glenhaven, on: the Mississippi river, and from Mineral 
Point east, to Moscow, and thence north, over the Blue Mounds, to 
Mazomanie; and also from Moscow to Oregon, on the Chicago and 
Northwestern railway. Starting from these known elevations, re- 
peated observations were taken; and the mean of several series of 
elevations, differing but little from each other, was assumed -to be 
approximately correct. Then, from the various points on those lines, 
series of lines were traveled over, embracing observations in all the 
accessible points in the Lead region. 

The instrument used was a three-inch aneroid barometer, imported 
by Wm. J. Young & Sons, of Philadelphia; a very delicate instru- 
ment, and one which indicated differences of elevation with great 
readiness and accuracy. The accuracy and value of barometrical ob- 
servations depend greatly on the state of the weather at the time they 
are made. The summer seasons have been, as a. general thing, quite 
favorable for such observations, and in cases where it was not, allow- 
ance has been made in computing the elevations. They may be con- 
sidered as correct within a few feet. For the extent of this part of 
the work the reader is referred to the topographical maps, which 
show what has been done much better than it can be described. 

The value of a work of this kind is incalculable. By means of the 
elevations obtained, we are readily enabled to make sections of any 
part of the country, in any direction; showing the geological position 
of the strata, with their dip, thickness, and the amount of denudation 
at any particular locality. In mining localities this is especially val- 
uable. It shows the position of the strata and openings, with their 
dip; the elevation of the neighboring streams, and the practicability 
of drainage, by means of levels; the depth to which shafts must be 


650 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


sunk from any point on the surface, to reach any particular stratum. 
All these things, and many others of like nature are most readily 
shown by sections, and these sections cannot be made without eleva- 


tions. 


For particular elevations of streams, roads, hills, section lines, 


mining grounds, strata, outcrops, 
accompanying this report. From 


ete., reference is made to the maps 
them a few are selected, of general 


importance, as being well known localities: 


ELEVATIONS ELEVATIONS 
ABOVE ABOVE 
Locatiry. -_-__— Locauiry. 

The Lake The Lake 

Sea. Mich. Sea Mich 
Wyalusing ............4 611 33 | Benton .........eeeeee eee 878 300 
Glen Haven, P. O.......-. 606 28 | New Diggings.......-..- 792 214 
Cassville... 2.2... 00000 ee 608 30 | White Oak Springs....... 928 350 
North Andover........+.- 838 260 | Shullsburg, school house .. 1018 440 
Bloomington........-..+. 905 B27 | Tain en s.ica-discreaiare ccs are 4% 1078 500 
Patch Grove ..........065 1060 498 | Union Mills.. .........-- 798 220 
Mount Hope...........-. 1076 498 | Kings Mills.............. 723 145 
Little Grant .........-..- R28 250 | Dodgeville, court house ... 1109 531 
Beetowii sinc cincnsaaceuees 762 184 | Mineral Point, depot...... 935 357 
POLOSbe sia ssh eeaeree ees 782 204 | Calamine, depot.......... 812 234 
British Hollow ........... 865 287 | Darlington, depot......... 802 224 
Rockville .............005 926 348°| Gratiot, depot ............ 783 205 
Hurricane Grove.......... 941 B63. | Mayvebtes.ccnssvieais, yaa ier a 1053 475 
Lancaster, court house .... 1080 502 | Adamsville ......-...-.05 878 300 
Mount Ida j 590 | West Blue Mound. .+. 1729 1151 
Homer P. O 400 | Blanchardville ........... 758 180 
Fennimore. . 990 | Wl Ota esas caster eparaasteronness 996 418 
Liberty Ridg DOG) Martin 5 sseaiayssisciararte waiedes 865 287 
Annaton....c.c.csecsanees QL, | OA MIG ccsis: nisia se ssenere oe. 3.4 ca.cvepe 859 281 
Ellenboro’..............-. TV, | Averyle susie sycersanceseless 808 230 
Dickeyville : 856 | Jordan .-....-..0-esee eee 858 280 
Jamestown, P.Q......... 912 B04) Willetts ss eiss cele Maes 888 310 
Fairplay, P.U............ 798 220 | Farmers Grove .........-- 1118 540 
Sinsinawa Academy...... 926 B48 | Bem vice wisive cwwwdaevcee 1078 500 
Hazel Green ............. 938 O60)| PeMy side <3 orabangesose 1088 460 
St ROse.3 352 eek aoe ekeaeen 994 416 | New Glarus, P. O......... 968 890 
Big PBC. ponding ecstasy 817 239 | Monticello.............05 858 280 
Platteville, P.O. ...... 00. 835 257 | Monroe, court house....... 1018 440 
Washburn .......+.... 00. 841 263:| Carn) es sete a 'sies saaseadeds 935 857 
New California........... 989 411] Twin Grove.............. 988 410 
MOnUfOrbisececnc oe deg 5 eee 1093 OL: | Urea cies asa itwenneuvan oes 821 248 
Castle Rock.. ....-...+... 847 269 | Sylvester ..........cc0008 865 287 
Highland, P,O........... 1161 583 | Dayton...... Lae Haas wee 818 240 
Cross Plains (lowa Co.).... 1198 620 | Brooklyn ................ 978 400 
Miflitie.. 3-6 oo caeacuten « 868 290 | Attica, P.O..... 0... ee 828 250 
West Platte Mound....... 1272 694 | Albany........... ce eee 818 240 
ag ak Shel Beacdes & hoaw aaivese ce an ea ee eee 798 220 

POV Goce bsuenad teense y BIC aan serosseemiesti sane tanive 

Meeker Grove..........4- 835 257 ? ae on 


The following elevations of stations have been furnished by the 


Chicago, Milwaukee and St. Paul 


Railroad Company, and’were used 


as a basis of some of the barometrical observations: 


INTRODUCTORY AND HISTORICAL. 651 


Elevation Above Lake 
above Sea. Michigan. 


Black Marth ssiwiniwewew ves veeese se eeas ies seuwane ans 810 232 
Mazomanie .......seeeeees (ccsvegiacs-oeuh'e.2and aavavdunsee etna 173 195 
ATEN Bis sever dia enue aneatale irs ois v's stewie 4 alate winsteenatranros nae 732 154 
Spring Green. sa sca sis estes essa wianeecdy woe neeiaes 722 144 
Lone Rock sewvsswasics te savy 0.5445 58 4004 aot tees 704 126 
VOCE ese 51a Rissa aehatere Geacre es ae near olarak SLRS Oro era TE. ott 695 117 
MISCO dai: is iccasacacestveid eaatelewieiedieekeateare sioueeinis eles ieiese'e' 687 109 
Boscobel eica snes lads eld sleet watin wanahar elt eed 667 89 
‘Wauzekacs: stews cso ovecsws Sits RTEES ESET S Ves 638 60 
Praiie dit Chiew sss ovieaccciacie tiene wie ca aia ciel ca de ore ase aie 619 41 


Finally, it may be said of the elevations, that they are by far the 
most important and valuable part of the work, inasmuch as they form 
the ground-work of the whole, and we are entirely dependent on them 
for definite results. They have been made and computed with the 
utmost accuracy and care. Lastly, they comprise that portion of the 
work, which, from its nature, consumes the most time, and makes the 
least outward show. 

In conclusion, I desire to express my thanks for the hearty co- 
operation which the survey has met at the hands of the citizens of the 
Lead region, who have willingly furnished all desired information 
and statistics, often at no small inconvenience to themselves. 

My thanks are also due to Mr. Allan D. Conover, of Madison, my 
assistant during the year 1873; to Mr. George Haven, of Minneapolis, 
Minn., my assistant during the years 1874-1875, who, by the careful 
discharge of their duties in the field, have contributed materially to 
the completeness of the work. 


652 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


CHAPTER IL 
TOPOGRAPHY AND SURFACE GEOLOGY. 


TOPOGRAPHY. 


General Features of the Country. Unlike most regions which 
nature has selected for the reception of metallic ores and useful min- 
erals, the Lead region bears no evidences of any sudden disturbances, 
or violent action of physical forces. The effects produced by igneous 
and eruptive agencies are wanting. Faults and dislocations of strata 
are nowhere found. The only irregularities are slight upheavals, or 
bending of the strata (and these never of great extent), producing 
changes of but a few feet from the normal dip. 

Between the geological condition and the general surface contour 
of the country, there is no direct correlation. The existence of a hill 
or a valley on the surface is not due to a subterranean elevation or 
depression of the surface, as is by many supposed, and whatever irreg- 
ularities exist, must be chiefly attributed to the milder natural agen- 
cies now constantly at work; such as running water, frost, winds, etce., 
acting through an immensely long period of time. 

Drainage. The most marked and persistent feature of the Lead 
region is the long dividing ridge, or watershed, which, commencing 
near Madison, continues almost directly west to the Blue Mounds, a dis- 
tance of about twenty miles. Tere it takes a slight bend to the south- 
west for fifteen miles, until it reaches Dodgeville, where it resumes its 
westerly course until it terminates in the bluffs at the confluence of the 
Wisconsin and Mississippi rivers; its total length is about 85 miles. 
Two points are noticeable; one is, its general uniform directness of 
outline (it being subject to but few and unimportant flexures); and 
the other is its parallelism with the Wisconsin river, so long as the 
latter holds an approximately westerly course; the summit of the 
ridge being always about fifteen miles from the river. 

The divide maintains an average elevation of about six hundred 
feet above Lake Michigan, and is seldom less than five, or more than 
seven hundred, except at the Blue Mounds, where it gradually rises east 


PLATE, XXVII 


OUTLINE MAP 
of the 
LEAD REGION 
hahrbtting the Dratiiage and the 
Distribration of Prawrte card Forest. 


iyisérele wee: Ne 
J 


I an 


PROM 


ae 


Tee 


vate 


Tun Mawauier Live &ExGn.Cn 


TOPOGRAPHY. 653 


and west, for several miles, until it attains an elevation at the west 
mound of 1,151 feet. This, however, is an extreme case, and, in fact, the 
only marked exception to its general level. In the town of Mount 
Hope, a slight decrease of elevation commences, and continues to the 
western end of the divide, where the elevation is about 430 feet, at a 
point within a mile of both the Mississippi and Wisconsin rivers. 
There are, also, two main branches or subdivisious of the watershed; 
of these, the western is the ridge which separates the waters that flow 
into the Platte and Fever rivers, from those which flow into the F'eca- 
tonica. It leaves the main divide in the town of Wingville, and pas- 
sing through the townships of Belmont and Shullsburg, in a south- 
easterly direction, passes out of the state in the town of Monticello. 
This ridge is not so conspicuous as the main watershed, eithe: for 
the directness of its course, or the uniformity of its elevation. The 
most conspicuous points on it are the Platte Mounds, which appear 
from a distance to be very high, but are in reality only relatively so, 
their actual elevation being only about seven hundred feet above 
Lake Michigan. The ridge appears to slope somewhat, in its ap- 
proach to Illinois, its average elevation there being about 500 feet. 

The easterly subdivision is that which separates the waters of the 
Pecatonica and Sugar rivers. It may be said to begin at the Blue 
Mounds, or a couple of miles east of them, and pursuing quite a de- 
vious course through the townships of Primrose, Washington and 
Monroe, it crosses the state line in the town of Jefferson. This ridge 
is characterized by a much greater want of uniformity in its general 
course, and by its very irregular elevation. It is much narrower than 
either of the others, more abrupt in its slopes, and contains quite a 
large number of hills and low places, especially in the towns of Prim- 
rose, Perry, York, and New Glarus, in which towns the streams head 
within comparatively short distances of each other, on opposite sides 
of the watershed. 

These are the principal elevations of the country affecting the drain- 
age; there are, of course, many minor ones, such as the divides be- 
tween the Grant and Platte rivers, or the several branches of the Pec- 
atonica; they are, however, merely subordinate ridges, and are but 
the details of the general plan. 

Streams. Having thus given a general outline view of the sys- 
tem of watersheds, a few remarks on the rivers and drainage of the 
Lead region are necessary to supplement them. As a preliminary 
remark, it is well to bear in mind, that their present situation was 
probably never modified or influenced by drift or glacial agencies; the 
evidence being insufficient to prove that there ever was any drift de- 


65+ GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


posited in the Lead region, the probabilities being rather to the con- 
trary. Premising this, it follows, that the location of streams must 
have depended on the natural configuration of the country, and the 
superior advantages of certain strata in certain positions, predisposing 
them to become the beds of streams. Other things being equal, sur- 
face waters would naturally form a channel first in the more soft and 
easily erosible strata lying along the line of strike of some soft for- 
mation, and would cause a river to conform its first channel to its out- 
cropping edge! Simultaneously its tributaries would shape their 
channels, approximately at right angles to the river, under the follow- 
ing conditions: when the general slope and drainage of the country 
is not contrary to the geological dip of the formations; which, in the 
Lead region, does not appear ever to have been the case. The trib- 
utaries on one side of the river thus formed would conform them- 
selves to the natural dip of the underlying strata, sloping toward the 
main river, and would be found wherever there were depressions, or 
irregularities in the surface, suitable to their formation. These would 
at their inception approximate to their final length and course, and 
future changes in them would be confined to the deeper erosion of 
their beds, and widening of their valleys; the formation of lateral 
branches; the division of the head of the stream into several smaller 
sources, and finally, the gradual recession of all the subordinate parts. 

With the tributaries on the other side of the principal river, a dif- 
ferent order would prevail, as regards their position and growth. 
They would at first be the merest rivulets, and increase only from ero- 
sion; and their beds would lie across the edges of the strata. Thére 
would be only a very limited extent of country tributary to the river 
on this side; the great volume of its water being derived from the 
tributaries of the other side. The dividing ridge would thus be very 
near the river, and a second set of long streams, tributary to some 
other river, would here take their rise and flow away. 

In the process of time, the main river would slowly cut its way 
through the soft formation, in which it had its original bed, into 
and through those which underlaid it. This might at first be accom- 
panied by a slight recession parallel to the line of strike; such a 
movement, however, could not be of long duration, but would become 
less as the valley became deeper; because any such recession would 
necessitate the removal of all the overlying formations. Finally the 
small streams flowing across the strata would cut their valley back 
from the river; the dividing ridge would recede, and their sources 
would, from the position of the strata, be in steep and precipitous ra- 


‘See Report of Board of Regents of the University of Minnesota. for 1279, pp. 46 and 47. 


TOPOGRAPHY. 655 


vines. Such, in brief, appears to be the theory of the formation of 
streams in the Lead region. Its application is easy, and would be as 
follows: : 

The Wisconsin river from Mazomanie, to its mouth near Prairie 
du Chien, is the most conspicuous example and illustration of the 
foregoing remarks. 

Although the surface of the country, in its present condition, does 
not permit the accurate delineation of the former lines of outerop, of 
the paleozoic formations; yet a sufficient number of outliers remain, 
to show us that they must once have covered the country, far north 
of where they are at present found. ~The existence of Niagara lime- 
stone, in a thickness of about one hundred and forty feet at the Platte 
Mounds, and probably the full thickness of the formation at the Blue 
Mounds, warrants us in supposing that the former outcrop of the un- 
derlying Cincinnati group was at least as far north as the present bed 
of the Wisconsin river. 

The valley now occupied by the river, from Mazomanie to Blue 
river, is very nearly that of the present line of strike of the Lower 
Silurian formation, and, although from there the strike of the lower 
members (of which outliers still remain) appears to bear rather more 
to the northward, yet, observations on the dip of the Cincinnati group, 
in such occasional outliers as remain, lead me to believe that its origi- 
nal strike was approximately in a southwesterly direction, from Blue 
river to the Mississippi. 

Assuming, then, that the Cincinnati group once had its northern 
outerop where the river now runs, or in a line parallel to it, in that 
vicinity, the surface waters would easily erode a channel in the soft 
and friable shales which, to a great extent, compose this formation. 

In fine, the whole process of formation previously described would 
take place. On the north side it had, as now, its principal tributary 
streams, the Kickapoo, Knapp creek, Eagle river, Pine river and Bear 
creek, in their present localities, and approximately their present 
length. On the south of the river, however, the principal watershed, 
already referred to, was probably quite near the river, from which 
position it has receded to the place it now oceupies. The Green river, 
Blue river, Otter, Mill and Blue Mound creeks were small and insig- 
nificant streams; which, by the gradual process of erosion, have in- 
creased to their present size and length; but even now, are small when 
compared to the northern tributaries. 

A further effect was to shorten the Grant, Platte, and Pecatonica 
rivers, by the gradual southwesterly recession of the watershed, and 
the lowering of the latter by the denudation of the Niagara limestone 


656 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


and Cincinnati groups; except in such localities as were protected by 
a superior hardness of some part of the formation, as in the case of 
the Blue Mounds. ‘ 

The result of the denudation has been to divide the country into 
two parts, each differing widely from the other in its topographical 
features. The streams flowing southward from the watershed have 
eroded the country into gently undulating slopes. This is probably 
due to the direction of the streams conforming in a measure to the 
dip of the strata. Abrupt cliffs and steep ravines are the exception, 
and not the rule, never being found in the immediate neighborhood 
of the watershed, but rather confined to the small lateral branches. 
On the other hand, to the north of the watershed, the panorama of 
bluffs and precipitous ravines is almost mountainous in its aspect. 
In fact, nothing can be more striking than the contrast which pre- 
sents itself, from certain points on the divide, in looking from north 
to south. In nearly all of the ravines leading northward, the fall of 
the first quarter of a mile is not less than one hundred feet; and, in 
general, it is true of the streams flowing northward, that three- 
quarters of the fall takes place in the first quarter of the distance 
from their sources to their mouth. 

It seems not improbable that these sudden declivities are due to the 
streams flowing over the edges of the strata, rather than lengthwise 
along their dip. Again, the streams flowing to the southward become 
comparatively sluggish in their course, as soon as they cease to be 
brooks. They have usually a soft muddy bottom, while those tributary 
to the Wisconsin are clear and rapid streams, flowing over a saudy 
or gravelly bottom, their valleys being narrow and their sides very 
steep. 

The streams tributary to the Platte, Grant and Pecatonica rivers do 
not exhibit any marked characteristics on one side that are not shared 
equally by the other. It may be remarked, however, that the short 
streams, which flow into the Mississippi river, present much the same 
topographical characteristics as are seen in the southern tributaries 
of the Wisconsin, narrow and deep ravines and valleys, being ap- 
parently the rule in the western part of Grant county. 

The Platte river is frequently found inclosed by hills which are 
gently sloping on one side, and quite precipitous on the other. This 
is especially noticeable near its mouth. The river in such cases soems 
to have encroached on one side of the valley for a long period of 
time, producing a cliff exposure of Lower Magnesian near the river, 
and a steep bank of St. Peters, capped with a more retreating slope of 
the Trenton, as shown in the following section. [See Fig. 1.] 


TOPOGRAPHY. 657 


In this connection may be noticed the diminution of water in the 
Lead region since the early mining times. In comparing the streams 
at present with those recorded in the government surveys, it will be 
fornd that many of the smaller ones are entirely dry, and others 
nearly so. Numerous springs, which formerly furnished an abund- 
ant supply of water, are now dry, and have been replaced by wells, 
sunk to obtain water from a deeper stratum. 


Fie. 1. 


GENERAL SECTION OF PLaTTe RivER VALLEY. 


1. Trenton Limestone. 2. St. Peters Sandstone. 3. Lower Magnesian Limestone. 


In T. 5, R. 6 W., are several streams flowing into the Mississippi 
river, which present some curious features in common. They vary in 
length from three to five miles, and take their rise in the Trenton 
limestone. They occupy quite long and narrow valleys of erosion, 
and their dry beds may be distinctly traced in them. They are quite 
large streams, and continue increasing in size for a mile or two from 
their sources, until they reach certain beds of the Lower Magnesian 
formation, when they gradually disappear. 

The large streams of the Lead region contain a much smaller 
amount of water than heretofore. Several places were seen where 
old mills, formerly operated by water-power, had been abandoned, on 
account of a diminishing and final failure of the supply. 

The diminution is not confined to surface water, springs, streams 
and the like, but is true, to a greater or less extent, of all the mining - 
ground of the region. In many instances this circumstance alone has 
led to the reopening and profitable working of mines which years 
ago were abandoned on account of water, with ore “going down” in 
the crevices. 

It is probable that cultivation of the land is the chief cause of this 
decrease, as a much greater amount of surface is thus exposed, and 
evaporation takes place more rapidly and in larger quantities. Re- 
moval of the timber is, without doubt, another cause of this decrease. 
The soil of the timbered land contains more moisture than that of the 
prairie; and in all countries, the removal of the timber has always 
been followed by a marked decrease of the water supply. This was 

Wis. Sur. — 42 


658 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


notably the case in the Hartz mountains, of Prussia, after the fir and 
hemlock forests were removed. When the mountain sides were again 
planted with the indigenous trees, by order of the government, their 
growth was found to be attended by an increase of water in the 
streams and springs. 

Springs and Wells. The Lead region is one of the best watered 
tracts of country in the state. Springs are very numerous, both about 
the sources of the streams and frequently in their banks. They aro 
found in all the geological formations, but with the greatest frequency, 
and of the largest size, between the bottom of the Galena limestone 
and the top of the St. Peters sandstone. Such springs are usually 
found flowing along the surface of some layer of clay, and finding a 
vent in the outcrop of an opening. The clay “openings” most favor- 
able to their formation are, the “ Upper Pipe Clay opening,” situated 
on the top of the Blue or Trenton limestone, and separating it from 
the Galena limestone; the “Glass Rock opening,” separating the 
Blue and underlying Buff limestone; and the “Lower Pipe Clay 
opening,” situated in the lower part of the Buff limestone; the latter 
however, does not seem to be so persistent a bed as the other two. 
Springs are by no means confined to these three openings, but occur 
in many of the beds of the Galena limestone, as well as in the lower 
formations; usually, however, flowing over an impervious bed of clay, 
or some layer of rock too compact to admit of the passage of water 
through it. 

Tn this connection it is desired to call attention to the springs sit- 
uated about 150 feet below the summit of the west Blue Mound. 
They have been attributed by many persons to thermal, igneous, and 
other deep-seated agencies, and by some to hydrostatic pressure. The 
following facts are offered in regard to these springs: (1) They are 
found at intervals on all sides of the mound, at a uniform elevation, 
either as springs or low wet ground, and always on the surface of a 
stratum of clay impervious to water. (2) They flow most abundantly 
during and after rainy seasons, and in summer are frequently nearly 
dry. (8) They are surmounted by the cap of the mound, which is al- 
most a solid mass of flint, and presents a surface of about 100 acres 
as a watershed. The annual rainfall in the Lead region is about 30 
inches, of which about one-quarter is removed by evaporation and the 
requirements of vegetation, while the remainder finds its way to the 
springs and streams. On the one hundred acres lying above the 
springs, there fall annually 10,890,000 cubic feet of water, of which 
three-quarters, or 8,167,500 cubic feet pass out through these springs, 
which seems amply sufficient to supply them. (4) The temperature 


TOPOGRAPHY. 659 


of the Blue Mound springs is the same as that of all other springs in 
the Lead region, which is about the mean temperature of the earth 
through which they flow. Were they thermal springs, or of igneous 
origin, we should expect to find at least some lingering traces of heat, 
to show us from whence they came. In view of these facts, it seems 
more logical to look for their origin in the natural and selfevident 
causes presented, than to attribute them to more complex conditions, 
imperfectly understood. 
Fie. 2. 


SKETCH OF THE UPPER Part oF THE BLUE Mounps. 


1, Flinty cap of the West Mound; 2, Horizon of the springs; 3, Niagara limestone; 4, Cincinnati 
group; 5, Galena limestone. 


{nm such portions of the country as are not liberally supplied by 
nature with springs, water is easily and abundantly obtained by 
means of wells. Their average depth is about twenty-five feet; this, 
however, depends chiefly on the locality in which they are sunk, those 
on the ridges and prairies being deeper than the rest. Round wells, 
of four or five feet diameter, are usually sunk for shallow depths, 
sometimes being as deep as sixty feet. Wells are sometimes obtained 
by drilling; such borings being chiefly confined to the prairie, and 
seldom exceeding sixty feet in depth. They are then furnished with 
a windmill pump, and supply an abundance of clear water for stock 
and farm purposes. 

Nearly all the water in the Lead region, whether in springs or 
wells, holds in solution a small portion of lime and magnesia, and 
a still smaller quantity of sodium, iron, alumina, and silica. The 
presence of these salts usnally gives the water what, is called a hard 
taste which is more noticeable in the limestone than in the sandstone 
springs, and not infrequently induces persons to believe them pos- 
sessed of medical properties. 

The following analysis, which is believed to be a fair sample of the 
quality of the water in-the springs and wells of the Lead region, is in- 
serted to show the small amount of foreign substances which they con, 
tain. The well is situated on the N. E. qr. of Sec. 9, T. 2, R. 9 E., a short 
distance northwest of the city of Brodhead, on the farm of Mr. Freder- 
ick Gomber. It was sunk to a depth of about thirty feet, of which 


660 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


the lower part (probably about ten feet) was sunk in the Lower Mag- 
nesian limestone, the rest being in the St. Peters sandstone. 

The following analysis of the water, by Dr. Gustavus Bode, of Mil- 
waukee, was furnished by Mr. Gomber: 

One gallon U. 8. standard measure contains of solid salts, 13.2720 
grains, consisting of: 


Chloride of sodium........ cece cece eter er eee teen et en anaes 0.3248 grains. 
Sulphate of soda......-.eeeee ee cee e cere ee etter tee eee ees 0.1792 =‘ 
Bicarbonate of soda....... cece ese e eee n eee e eee ene teen eeeee 0.0280 ‘ 
Bicarbonateok Hine. vccshes edhe once y eee cals puis creettoe een 6.6584 “ 
Bicarbonate of magnesia. ... cesses eee e ee eee eee eee eee eee 4.8552“ 
Bicarbonatevol iwoncsdrys nowat eee teatce sacs ees Aenea 0.2296 * 
VARTA LIVE Se e6d ease @ ga Swi eee Gaeta a acon de ne eta coums uct 0.1288 =“ 
STiethas use hae HOAs Heke DIRE emer as aS LOT Qabades 0.6888 ‘ 
Organic matter... 0.6... c esis eee eect teeter ene oe 0.1792 =“ 
MESES sc tissho ede seam iheatoneindenR tae eae Nei 13.2720 grs 


Dr. Bode remarks of this well as follows: “The total amount of 
salts is small in comparison with other waters. The salts themselves 
are the same as those in the Waukesha water, and in the same com- 
bination. If the operation of this water depends on the absence of 
sulphuric acid, and its containing bicarbonates, so the same good and 
healing results may be expected from your spring.” 

Prairie and Forest. The prairie area of the Lead region is com- 
paratively small, and seems to be chiefly a continuation of the great 
prairies of Illinois. The most extensive prairie is that found in the 
southern part of Grant and La Fayette counties, comprising the town- 
ships of Jamestown, Hazel Green, Benton, New Diggings, Shulls- 
burg, Seymour, Monticello and Gratiot. From this there is a branch 
extending in a northwestern direction (corresponding to the eastern 
subdivision of the watershed previously alluded to), until it unites 
with the main watershed; here it branches to the east and west. The 
western extension forms a prairie in the towns of Glen Haven, Patch 
Grove, Little Grant, and some parts of Fennimore and Wingville. 
The eastern prairie follows the main divide already described, the 
prairie being from six to ten miles in width. 

Between the east and west branches of the Pecatonica, there is a 
prairie, including most of the towns of Fayette, Waldwick and Wiota. 
In Green county the principal prairie is found in the towns of Mon- 
roe, Clarno, Sylvester and Washington. 

This, in substance, is the prairie land of the Lead region, although 
there exist small isolated patches of timber, in the area already de- 
scribed, as well as small prairies, or openings, in the remainder of the 


TOPOGRAPHY. . 661 


region, not included in the prairie area, and which is mostly timbered 
land. The original area of prairie appears, from the government 
surveys, to have been somewhat greater. At the present time, the 
original forests of large timber have been mostly cut down, except 
about the Wisconsin river bluffs, such timber as is now found, being 
a second growth, of black, white and burr, oaks, maple, hickory, poplar 
and elm, the trees being of small size, seldom more than a foot in di- 
ameter. 

Mounds. The nearest approach to mountains in the Lead region 
are the Platte Mounds in La Fayette county; the Blue Mounds in 
Dane and Iowa counties, and the Sinsinawa Mound in Grant coun- 
ty. The former are three in number, about a mile apart, the mid- 
dle one being very sinall in comparison with the other two. The 
east and west mounds are about the same elevation, and are capped 
with a very hard Niagara limestone to which they doubtless owe 
their preservation, in the general denudation of the surrounding 
country. The ground slopes away from them so gently, and blends 
so gradually with the surrounding high land, that it is impossible to 
define exactly where the mound proper begins. 


Fie. 3. 


ye 


ae Be 


West Mound =—i:ttle Mound == TFust Mound 


SKETCH OF THE PLATTE Mounps. 


= A == a e=F 


1 Niagara limestone; 2 Cincinnati group. 


The Blue Mounds are two in number; one being in Iowa county, 
and the other in Dane. The*top of the west mound (which is the 
higher of the two) consists of over a hundred feet of very hard flinty 
rock, somewhat resembling quartzite; below this is the Niagara lime- 
stone. This cap of quartz rock seems to have been removed from the 
east mound; the top of which is a flat table land under cultivation. 
These mounds are very conspicuous, and can be seen from any mod- 
erately high land in the Lead region. 

The Sinsinawa Mound is also a very conspicuous object, in the 
southern part of Grant county, near the village of Fairplay. It is 
composed, for the most part, of the Cincinnati group, capped with a 
small amount of Niagara limestone. 

Sinks. Very remarkable features in the vicinity of the Blue 
Mounds are the numerous sink holes found near their base, and fre- 
quently quite high up on their sides. These sinks are usually in 
groups of three or four, and invariably in nearly an east and west 


662 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


line. One group is near the former residence of Ebenezer Brigham, 
at the foot of the East Blue Mound, in the 8S. W. qr. of Sec. 5, T. 6, 
R.6E. There are about a dozen of them, nearly round, varying in 
diameter from ten to twenty feet, and about five feet deep, all ina 
line, bearing about 10° north of west. At the West Blue Mound 
there are several lines of them, about the base and side of the mound. 
On the center line of Sec. 1, T. 6, R. 5 E. there is a well defined line 
of them, extending for about a quarter of a mile on each side of the 
center of the section. There is another range of them near the 
center of the 8S. W. qr. of Sec. 1, and a third line near the quarter 
post of Secs. 1 and 12. The largest of these sinks is an isolated one 
near the center of the 8. E. qr. of Sec. 1, which is as much as fifty 
feet in diameter, and twenty feet deep. In this one the wall rock of 
the fissure could be very plainly seen on the south side. From the 
circumstance of their direction and position coinciding with that of 
all the mineral crevices in the vicinity, and the fact that the ore is 
always found in large crevice openings, the inference seems to be that 
these sinks mark the line of large open crevices in the rock beneath 
them. It is also reasonable to suppose that the sinks along the cen- 
ter line of Sec. 1, T. 6, R. 5 E. are a continuation of those near the 
Brigham place, as they seem to point almost directly to one another. 
It is probable that the water, percolating through the earth into these 
crevices, has in process of time carried so much of the soil with it 
as to cause a falling in of the surface, leaving the sinks as the result. 
In view of the vast quantity of ore which has in former times been 
obtained from the crevice openings in this locality, it would seem to 
be worth while to prospect some of these sinks; but nothing of tho 
kind has ever been done. 

Sinks do not appear to be confined to the Galena limestone, but 
seem to be quite as frequent at the Blue Mounds in the Niagara 
formation. They have been observed in many other localities in the 
Lead region. The following are cited, to show their occurrence in 
the several formations. On the S. E. qr. of Sec. 14, T. 5, R. 2 W., 
are three, situated in a triangular form, in the St. Peters sandstono. 
This is somewhat exceptional, as the sink holes are usually confined 
to the limestone formations. On the S. hf. of Sec. 11, T. 6, R. 4 E, 
are several of these sink holes, from eight to twelve feet deep. 

The largest one noticed ‘is situated on the summit of the ridge, on 
the S. E. qr. of Sec. 29, T. 6, R.2 E. It lies in the Galena limestone, 
and is about 200 feet long, by 100 wide, and about twenty feet deep. 


SURFACE GEOLOGY. 668 


SURFACE GEOLOGY. 


Soil and Subsoil. The quality of the soil of the Lead region is 
- chiefly dependent on the character of the subjacent formations. The 
subsoil appears to be derived directly from the decay and disintegra- 
tion of the strata, of which it is the residuum. South of the princi- 
pal watershed, the subsoil is clay, almost without exception, having 
a thickness of from three to six feet, depending on the configuration 
of the underlying rock formation. This is the average thickness, on 
comparatively level land; on side hills it is usually much thinner, the 
greater part having been washed down into the valley below. The 
clay soils and subsoils appear to consist chiefly of those portions of 
the overlying Galena limestone, and earthy Cincinnati shales, which 
being insoluble in water, were not removed by the gradual process of 
denunation. 

The amount of lime, magnesia, and alkaline earths in the subsoil 
and soil, together with the vegetable mold in the latter, constitute a 
soil, which, in its virgin state, is unsurpassed for richness and fertil- 
ity. The number of successive wheat crops which have been raised, 
without regard to rotation, on some of our prairie farms, attest its 
native strength; as also the marked decline in fertility of the soil 
when this has been done, shows the inevitable retribution which fol- 
lows the practice. 

Exceptions to the clay soil, usually found in the country covered 

by the Galena limestone, are found in the eastern part of La Fayette, 
and frequently in Green county, where the soil is quite sandy, owing 
to the disintegration of calcareous sand layers frequently found there 
in that formation. <A few localities are cited below, where the sand 
was so abundant, that the formation might have been considered a 
sandstone, were it not for the occasional outcrops of Galena limestone 
in place. In the western part of the town of Jordan, T. 2, R.6E., 
in secs. 2, 11 and 14, the ridges have a great deal of sand contained 
in the soil. The roads are frequently sandy, similar to those ina 
sandstone formation. Lying entirely without the limits of the Drift, 
this circumstance led to a search for and discovery of the original 
beds. 
At the village of Martin, in the S. E. qr. of sec. 32, T. 1, R. 6 E., 
on the Pecatonica river, at the saw-mill, isa large stone quarry, of 
which the upper portion consists of Galena limestone in thin beds, 
containing considerable calcareous sand between the layers. This is 
the first locality where the sand was found in place. 

On the ridge near the quarter-post of 29 and 32, T. 2, R.6E., a 


664 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


great deal of sand was seen at an elevation of 150 feet above the top 
of the St. Peters; numerous concretions of iron were also found, sim- 
ilar to those usually found in the upper bed of that formation. East 
of the center of sec. 34, T. 3, R. 6 E., is another sandy ridge. 

The agencies of the glacial period do not appear to have had any- 
thing to do with transporting the component materials of the soil, 
and although a slight transportation has taken place, it is always 
merely local. For instance, in the valleys of the creeks which lie in 
the St. Peters sandstone, the soil is usually a rich clay loam, richer 
in fact than that of the adjacent ridges, because the best parts of the 
upland soils have been washed down, and distributed over the surface 
of the valley. 

A similar transportation may be observed in passing up any long, 
and moderately steep hill, which includes several formations; such 
hills being very common north of the principal watershed. Let us 
suppose one, whose summit is composed of Galena limestone, and 
whose base lies in the Lower Magnesian. Scattered about the base- 
will be seen many loose pieces of Lower Magnesian limestone, mixed 
with less numerous bowlders of St. Peters sandstone; still less nu- 
merous and smaller pieces of the Buff and Blue (Trenton) limestone, 
while fragments of the Galena limestone will be comparatively rare. 
On ascending the hill and arriving at the St. Peters, fragments of 
Lower Magnesian will no longer be seen; while those of the upper 
formation will become larger and more numerous. On arriving at 
the Buff limestone, the fragments of St. Peters sandstone will also 
have disappeared, fragments of Blue limestone will be very numerous 
and easily recognized by their white color, and their general rounded 
and worn appearance. Qn reaching the summit of the hill, no frag- 
ments of stone will be found, except such as are derived from the 
subjacent Galena limestone. One prominent feature of the soil will 
be the prevalence of flints, which are nearly indestructible, and often 
form a large component part. From the arrangement of the surface 
soil and fragmentary rock, it is evident that the rock of any formation 
is never found above the level from which it was detached. 

Peat. While on the subject of surface soil and subsoil, it is de- 
sired to report two places in Green county which afford the only ap- 
proach to this useful article, which has been observed in the Lead 
region. The first is situated on Jordan creek, in the E. hf. of Sees. 
21 and 28, T. 2, R. 6 E., and comprises from one hundred and fifty to 
two hundred acres. The other locality is on the Little Sugar river, 
near the center of Sec. 11, T. 8, R.7 E. As the conditions under 
which they exist are similar, one description will serve for both. 


SURFACE GEOLOGY. 665 


The turf is underlaid by an impervious stratum of blue clay, which 
holds the water and nourishes a vegetable growth about four feet 
thick, which, in this section of the country, is known as peat. When 
cut and dried, it burns similarly to peat, but with so large a residuum 
of clay, sand and ashes, as to render it unfit for economic purposes. 

Brick Clay. Clay suitable for making brick is found in many 
parts of the Lead region. Among the localities are Lancaster, Min- 
eral Point and Platteville. The first has two yards in operation, and 
the latter has one, which commenced operations in the spring of 1874. 
The clay used is usually of a grayish-yellow color which becomes red 
on burning. It appears to have been formed in the same manner as 
other portions of the soil, as already described. 

In the Platteville yard an opportunity was found to see the process 
of manufacture. The clay is dug from an adjacent bank, some selec- 
tion being necessary. It is then run on small cars to the pug-mills 
(which are three in number) and ground with water, until it forms a 
homogeneous paste. After this comes the moulding into bricks, 
which are spread out on the floor of the yard, dried and piled in a 
kiln to burn. A kiln of these bricks takes about eight days to burn. 
It is estimated that about 8,000 bricks per day can be made in this 
yard. 

In the city of Monroe, in Green county, is a brick yard where two 
kinds of brick are made from the same kind of clay. One isa red 
brick, similar to all common red brick; tke other is a cream-colored 
brick, of very handsome appearance, closely resembling the Milwaukee 
brick. From the latter, many of the handsomest buildings in Monroe 
are constructed. The difference in color is due to the difference in 
burning, the red color being caused by a greater and long continued 
heat. 

The origin of the clay of which the brick are made is a matter of 
some doubt. It does not have exactly the appearance of a drift clay; 
and if not, its situation indicates that it must have undergone some 
subsequent reirrangement. 

Glacial Drift. As has been before intimated, the Lead region is 
a driftless tract of country; not a single bowlder, pebble or clay of . 
foreign origin being found in its limits, except in three or four 
isolated cases, which will be hereafter described. 

The northern boundary line of the driftless region lies far to the 
north of the Lead region. The eastern line was found in Green 
county, and traced out with all possible accuracy. For a particular 
description of it, reference is made to the geological maps; in brief, 
however, it is as follows: It commences on the west side of the Pec- 


666 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


atonica river, crossing the state line at the southwest corner of the 
town of Cadiz. From here it proceeds almost in a straight line to the 
city of Monroe. Thence north, it runs along the divide between the 
Pecatonica and Sugar rivers, until about two miles south of New 
Glarus, where it takes a northeasterly course, and passes out of the 
county about a mile west of Belleville. The course thus indicated is 
its present line as shown by erratic bowlders lying upon the surface. 
If the drift deposits originally extended farther westward, no trace 
thereof now remains. Hast of the line described, bowlders are found 
in all parts of the county, with more or less frequency. The boun- 
dary line, where bowlders are now found, does not appear to conform 
at all to the surface features, but crosses the valleys of the streams, 
and the ridges between them, with equal impartiality. 

The different kinds of rock found in the drift are so numerous that 
it would require quite a catalogue to enumerate them all. It will be 
sufficient to state that the great bulk of them are granitic, metamor- 
phic, or trappean; the most frequent being varieties of granite and 
gneiss, and next to them the trappean rocks; chloritic rocks, and those 
of a schistoze structure, are also quite numerous. 

In addition to these there are, in certain places, beds of gravel, sand 
and clay. The distribution of the bowlders does not appear to be 
very regular in Green county, in fact, the whole of the county verges 
so near the western boundary of the drift, that comparatively small 
deposits were made here, which are quite insufficient to exemplify any 
general laws of distribution. No difference could be seen in their 
frequency, between the eastern line of the county and the western line 
of the drift. 

The bowlders are of various sizes, from a few inches to two or three 
feet in diameter, and are always rounded and worn smooth. They are 
frequently found quite numerous in one place, and then scattered 
along at very distant intervals, on the same kind of ground, but do 
not exhibit any distinctive morainie appearance. 

Gravel beds are not very frequent, although they are found in sev- 
eral places in Green county. There is one situated very near the 
boundary of the drift, on the N. W. qr. of See. 4, T. 1, R.7 E., where 
there is a bed of gravel about eight feet thick, underlaid by a bed of 
stratified sand and clay about four feet in thickness. This sand is 
very fine, and has just enough clay mixed with it to make a good ar- 
ticle of moulding sand for iron foundries; it would give a fine impres- 
sion, and make a smooth casting. A similar bed was found about 
two miles east of the preceding, in the S. W. qr. of See. 2, T. 1, R. 
7 E., where the drift sand and gravel have accumulated to a thickness 


PLATE, XXIX 


“YIU | = Tf OOF FPIIS:"F-43,1, — PINUITUTI UITPIIS 


EDUC PHOT $2 1949 T yuopspuDg reer 
EFFI] OPAL yy 
7 vUuojsauNT Duswyg 8 a z 
Pp Re oa Sis as ee 5 re 
= a > : 
SS 


fimdany >) 
uM 


DAHOMLOD 


Ed 
z 
§ 
3 
a 
= 
g 
ag 


4180} 


appahiagarg 


uoynprua ayy GiUpaoys:IULT 22716 BY} 0} LAAT Y UISUOISHY AYs JO Yynout ayy qo Tdadississyy 
ayy woLy Sindy PUP So9}oy'UMOIIT JO SITAISIT Bunny ayy YGnosyy U0HIaS 


TUOISIULT UMSIUBDY LaAscory 


FUGISPUYS S4ITAT "IS 


‘wT Uoruany, 


yaasy Moa 
UMP ) 


AIA PUDAD 


PUOPSIUUT WUaTOU 


Ht 


wfaa.t,) PruDy 


waary iddssissyyyy 


Toe Muaawariinn Lento & bee Ca 


SURFACE GEOLOGY. 667 


of about twelve feet. A large amount of it has been utilized for 
railroad ballast. A third bed, like the other two, was observed on 
the N. E. qr. of Sec. 9, T. 1, R. 7 E., also several others in various 
portions of the county. Those already described will serve as sam- 
ples of all. 

The amount of drift clay in Green county is comparatively small, 
it probably having.been dissolved out and washed away from the 
greater portion of the surface. It was only observed in one place, in the 
N. W. qr. of Sec. 25, T. 3, R. 7 E., where a well had been sunk in 
the drift. There was here a thickness of about twenty feet of slate- 
colored clay, full of small pebbles. 

Outside of Green county, the indications of drift observed were so 
few and uncertain, that it seems scarcely proper to attribute them to 
glacial agencies, and, on the other hand, there is great difficulty in 
accounting for them in any other manner. They are briefly as fol- 
lows: 

Prof. Whitney describes, on page 137 of the report of 1862, a group 
of loose blocks of sandstone, which are situated as he represents them 
in his wood cut. It.is referred to in this connection, because I de- 
sire to report with it two similar deposits, which have been observed. 
The first is situated on the road from Mineral Point to Dodgeville, 
on the S. E. qr. of Sec. 9, T. 5, R. 3 E, as much as three miles from 
any outcrop of the St. Peters sandstone. The bowlders are from one 
to two feet in diameter, and lie scattered along the road, and in the 
adjacent fields, on the south slope of the hill. The bowlders are none 
of them very large, and it is not impossible that they were hauled 
there, although it is difficult to understand for what purpose. There 
are not now, nor have there ever been any houses near them. 

The second locality is on the N. E. qr. of Sec. 5, T. 1, R. 2 E., on 
the ridge between the Strickland and Myers branches. There are 
here quite a number of blocks of St. Peters sandstone lying on the 
summit of the ridge. The blocks are of various sizes, some of them 
weighing several tons. These bowlders are more distant from any 
outerop of sandstone than either of the others; the nearest being at 
 Cook’s,”’ about five miles to the northwest, in Sec. 22, T. 2, R. 1 E. 
It is somewhat singular that these isolated bowlders should always be 
of sandstone. These several instances have been cited as quite remark- 
able and singular exceptions to the general driftless character of the 
Lead region, although we have no very plausible theory to account for 


their origin. 


668 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


OFA PTE, 117. 
GEOLOGICAL FORMATIONS. 


POTSDAM SANDSTONE. 


Geographical Boundaries. South of the Wisconsin river it is 
found as the bed rock of Otter, Mill and Blue Mounds creeks, and 
their various tributaries, as far south as town 7, on the various ranges. 
Here it disappears, owing to the southerly dip of the formation, and 
the sudden rise of the country to the south. The valley of the Wis- 
consin river also lies in this formation, forming a very level plain 
from two to three miles wide, and extending from Sank City toa 
point about four miles above the mouth of the river. Good natural 
exposures are seen in the bluffs on each side of the river, in which the 
various strata may be traced uninterruptedly for miles. 

The greatest exposed thickness is seen in the valley of the Wiscon- 
sin river, where it is about 300 feet from the water to the bottom of 
the Lower Magnesian limestone. Examinations north of the Wiscon- 
sin river make the entire thickness of the formation about 1,000 feet. 

Lithological Characteristics. The following section, taken from a 
bluff about three miles northwest of Lone Rock, in the N. E. qr. of 
Sec. 34, T. 9, R. 2 E., will serve as a general guide to the formation: 


A. Lower Magnesian Limestone. 
1, Irregularly-bedded, white and yellowish Lower Magnesian limestone, con- Ft. In. 


HATING TO) HIPS a orere sss Ash aie dh Ga Sonrertoensinsy “Gdn MELE a AIA EMA coe aie ine ue 60 
2. Transition beds of arenaceous limestone, in which rounded grains of sand 
are cemented together by limestone..... -.-.. eee cee cece eee eee e es 5 


B. Potsdam Sandstone. 
3. Sandstone, white, very heavy-bedded, containing at the bottom occasional 


horizontal seams of lime. Friable .......... 0 ccc c cc cece ene eee eee 45 
4. Thin-bedded, earthy, straw-yellow shales, containing Dicellocephalus and 
LinGQildc vee evheie ieee desea ede ioe 8 R08) eRe ed REN S Tae AR eee 45... 
5. Very finely laminated blue shale......... 0.0. cee ee cece ee eee tence ee eee aie 
6. Thin-bedded, yellow, argillaceous limestone .............. 0. cece ee eee Dee 
Ts Harthy miaterialsccccunecasea wa Sab soaeereh i ied Ga peybe ben saeeatesd 4, 13 
8. Very hard and compact brown limestone, building stone ................ 4 
9. Thin-bedded gray limestone, building stone .......... 0. ce eee eee neces 9 
10. Yellow and white friable sandstone, to the valley, mostly unexposed, cov- 
ered. by slope Of Hill... ccs ey ccna eee sistenendenbaviemee elena’ eua ex 190 


Gidea. gach paeehadomnaisn cams ccianl Ge uaaleas A 360 6 


PLATE, XXX] 


WULT VW O09 YPTEOY [Eee PaAMUTIPI9. WOT II. 


: UPDIYIUE FYOTIO [IAI T 


HODIGIDE TYAT FP PIATT 


AUOSPUDES MEPS] RL 


: 


Sate eG 


a 
ie 5 Rl nae aoe 
a > z 
§ ws YC oreapso aia, EISIH DY AINA T 
5 AN 
8 aX ET 3 pee ae ee 
= 2 al as ue TyTN Wa ; 
: ely 6 ee SEEITT OPT ve 4 
q D = se aS PHO OMPEP mms, ig eee aK. 
i ee gee a ee : = e 
= N = 
= N 
: § 3 
N tS N 
N .. ~ 
N 8 > 
a x. 
3 
Ne 


Wonepnusd oti SULMOYS' JaATy UlsUODETAA oT oy SUIT OWUIY ayy Wogy 
HiYfod [Pau pue Uo Usedg [aZeY JO spiiystq SULUY 97 YSnN0aM uoyosag 


ss LanoT i 
yp ppsruliy(y te SIUBOL ee eee aa ta ee 
guagysrtty T ee aetna Oe TUOISPUDSY SLIVIL w 


Lipps CS see oy 
- FLO ISPUULT UOFUILT, 2 3 
ae fee a et AF w\/ 


} 

ie 
el: 
A 


a aeons A N 
ceees!, © i 8 “~~ 8g > 
/ > 2. Nw z y a 
i ~~ 8 N Q by 
ao a N § . q N 
5 3 s : : 
Q 8 > * 
3 ; 
Ss 
* 


> 
x 

: 
N 
> 
Ni 
S 


PMaPUTT PUAVD 
i adr XA N 
8 

S 5 & 
by & 
; <  & 
= iS NI 
$ y 


Tae Muaravker Litno.& EwonCo. 


GEOLOGICAL FORMATIONS. 669 


The beds mentioned under Nos. 8 and 9 change to a yellow, arena- 
ceous limestone, which is extensively quarried for building stone at 
Mazomanie, Black Earth and other towns in the vicinity. It is easily 
quarried and dressed, and makes a good and durable building stone, 
which does not undergo much change on exposure to the weather. 
The sandstone is but little used for building stone, as it is too friable. 

The sandstone beds of the Potsdam are usually composed of a very 
soft and friable sand, frequently crumbling readily between the fin- 
gers, especially if it is white. The upper beds are more frequently 
white than the others, although white beds are not uncommon in all 
parts of the formation. In general, the lower beds are yellow or 
brownish in color. The great inequality in the hardness of the sev- 
eral strata of the Potsdam is frequently the cause of the formation of 
terraces by erosion, which are often a conspicuous feature of the 
valleys in the vicinity of the Wisconsin river. The following section 
of a hill near Lumberville, on the Wisconsin, illustrates their ap- 


pearance. 
Fie 4. 


40", 30° , 50" 


420", 20°, 40" 


- 


#0 


a 


SkeTou oF A TERRACED Hitt NEAR LUMBERVILLE. 


1. Lower Magnesian Limestone. 2. White Potsdam Sandstone. 3. Fossiliferous Shales. 
‘ 4and 5. Dolomitic Beds. 6 and 7%. Dark-colored Sandstone. 


South of the Wisconsin river, about the head-waters of Blue 
Mounds ercek, and Mill creek, the upper bed of the Potsdam consists 
of ared and very ferruginous sandstone, often containing seams of 
iron ore, and iron concretions. The coloring matter appears to be 
partially soluble, and, becoming washed out by the rain, colors the 
-goil in some places to aconsiderable extent. It is quite conspicuous 
at Mr. Ruggles’ farm, on the road from Dodgeville to Arena. It 


670 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


was found in a tract of land about six miles long, east and west, and 
about five miles wide, north and south. Another locality where it is 
very conspicuous is near the center of Sec. 17, T.7,R. 4 E. Ina 
ditch by the side of the road, it appears as a very dark-red sandstone, 
streaked occasionally with yellow, and overlaid by a dark-brown, 
earthy, ferruginous shale. 

Along the road for some distance above this outcrop, there is a 
sandstone containing seams of iron ore. The formation appeared to 
be about sixty feet thick and unfossiliferous. The country here is so 
deeply covered with fallen rock, from the overlying formations, that 
it is difficult to deterinine the precise horizon of the different beds. 
The same beds were traced out to the N. W. qr. of Sec. 7, T. 7, R. 4 
E., where they present the same appearances. In each of these local- 
ities, the thickness of the overlying Lower Magnesian does not exceed 
100 feet. 

From the results of certain experiments instituted upon the shales 
designated in the section as No. 4, we are inclined to think they 
would make a tolerable quality of hydraulic lime, although they are 
not sufficiently quick-setting to make a good hydraulic cement. 

It will be seen from an inspection of the foregoing section, that no 
sandstone is included in the Lower Magnesian formation which ex- 
tends to B. Some geologists, however, place the line dividing the 
two formations between the beds numbered nine and ten under B in 
the section, p. 668, thus including the Diccllocephalus shales and lime- 
stones, as well as the upper bed of sandstone, in the Lower Magne- 
sian formation, and beginning the Potsdam with the bed numbered 
ten. If this arrangement were adopted, the Lower Magnesian would 
sum upas follows: Limestone above the sandstone bed No. 3 of the 
section, full thickness, 250 feet; sandstone, 45 feet; shales and lime- 
stone, 61 feet, making a total of 356 feet, which is much greater than 
has heretofore been attributed to the formation. On the whole, it has 
seemed best, on paleontological grounds, for the sake of perspicuity, 
and to avoid confusion in comparison with other reports, to respect 
the old landmarks of subdivision, especially as bed No. 4 contains 
the characteristic Potsdam fossils. , 

Paleontology. The fossil remains of this formation seem to be 
chiefly confined to the calcareous strata and argillaceous shales, de- 
scribed under numbers 4 and 6 of the foregoing section, the most 
productive being those which immediately overlie the limestone 
quarry rock, All the quarries from Black Earth to Boscobel were 
examined, and, in all, more or less specimens were found. The re- 
mains consist chiefly of Lingula aurora and Dicellocephelus Minne- 


GEOLOGICAL FORMATIONS. 671 


sotensis, the former being quite small, and usually having the shell 
remaining; sometimes, however, the shells have been ground up so 
that only a few fragments are found, disseminated through the shales. 
The trilobites are seldom or never found entire, but usually the 
cephalic portion, the pygidium, or still smaller fragments. The vari- 
ous sandstone beds of the Potsdam are usually unfossiliferous. The 
upper bed of sandstone seldom contains anything but Scolithus, which 
in some localities is very numerous. This fossil is also frequently 
found in all the sandstone beds. 


LOWER MAGNESIAN LIMESTONE. 


Geographical Boundaries. South of the Wisconsin river and 
north of the main watershed, it occupies a tract of land lying about 
the heads of all the smaller tributary streams, although seldom found 
so far back as their springs. Passing down any of the streams, such 
as Otter creek or Mill creek, we gradually pass below its surface; and 
its outcrops are seen gradually higher in the hills, until, on reaching 
the Wisconsin river, it forms the cap of all the bluffs from Sauk 
City to Boscobel, usually appearing in bold and rugged cliffs, lend- 
ing a very picturesque effect to the scenery of the river, It forms 
also the valley of the Wisconsin for about four miles above its mouth, 
and the valley of the Mississippi as far south as Glen Haven, where 
it passes beneath the surface. Passing south of-the divide which 
separates the waters which flow into the Wisconsin from the Pecato- 
nica, it is found in the branches of the latter stream, as far north as 
the north line of town 5 in ranges 5 and 6 E. Proceeding westward, 
it is not again encountered until the Platte and Grant rivers are 
reached, where it is found as the bed-rock of those streams, and in 
T 5, R. 3 W., it covers a large portion of the township. 

In Green county, there is but one exposure of the formation. It 
is in the valley of the Sugar river, about three miles above Brodhead. 
It commences a short distance north of the center of Sec. 15, T. 2, R. 
9 E., where it has a width of about half a mile. In passing into town 
three, it widens to nearly two miles. It then becomes narrower, at- 
tains its greatest elevation above the river at Albany, and finally dis- 
appears beneath the surface of the river about a mile and a half above 
that village. 

Lithological Characteristics. After passing through the transi- 
tion beds separating it from the. Potsdam sandstone, it assumes all 
the qualities characterizing dolomite. It is very hard, compact, and 
close-grained, of a grayish-white color. Beds of flint or chert are 


672 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


contained in all the strata, irrespective of geological position, differ- 
ing however considerably from the flint found in the Galena lime- 
stone, in that they are more regularly segregated, forming layers by 
themselves, and are not so promiscuously distributed through the 
formation. 

The flint of the Lower Magnesian limestone is much whiter and 
more liable to decomposition than that of the Galena. There are 
also frequent geodes and cavities lined with drusy quartz-crystals, 
which have never been seen in the Galena limestone, but are very 
adundant in the Lower Magnesian. The erystals are of many colors, 
white, yellow and rose color predominating, and often affording beau- 
tiful cabinet specimens. 

A good general idea of the formation may be obtained from the 
following descriptive section, taken from a bluff at the mouth of 
Green river, on the Wisconsin, situated on the N. W. qr. of Sec. 22, 
T. 7, R.4 W. Upon the summit of the bluff, there was considerable 
sandstone scattered about, although none could be found in place. It 
was found in place on the other side of Green river at about the same 
clevation, consequently we may assume that the top of the blutf is 
quite near the top of the formation: 

A. Lower Magnesian Limesione. 
1. Slope of hill (to top of vertical cliff) composed of heavy-bedded, ito 


Magnesian limestone; stratification quite regular, contains no flints; good 
bilding stone ce vcasce enee-riie ccm emai eve Heyes geeg pata Ree ee ear nel ae 23 


2. Hard, compact, heavy-bedded, light-colored limestone, lines of stratification not 
distinct; full of irregular masses of flint, which compose about half of the 
bed; exposed in a vertical cliff. 0.6.6... cece eee e cee een e teen eens 33 
3. Slope of hill covering limestone, not well exposed.........-.+++-. eee eee seey 23 
4, Coarse-grained limestone, weathering irregularly on exposed surfaces, contain- 
ing a few flints disseminated through it, and occasional druses of quartz...... 7 
5. Gray limestone, very hard and compact, regularly stratified, beds from one to 
two feet thick, containing no flints.<.c+scessciesiee gee eeeeeuear dienees ee 29 
6. Crystalline, gray, magnesian limestone, with a few flints irregularly cissemin- 
ated; beds two feet thick ..... Pe er rea ee er 9 
7. Hard, light-colored limestone, crystalline in texture, weathering but little on 
exposure; beds about three feet thick; contains no flints...............005 46 
8. Fine-grained, straw-colored, slightly arenaceous, magnesian limestone; beds 
about one foot thick; stratification quite regular ......... er ee 20 
9. Trregularly bedded, dolomitic limestone, has sometimes an odlitic structure.... 26 
10. Yellow, arenaceous limestone, transition beds. The sand appears in rounded 


rains, separate from one another, and cemented together with lime; strati- 
ication indistinctly marked ..........-csceccecseesenveeeeneteceneeenens 23 


B. Potsdam Sandstone. 


11. Hard and compact sandstone, in beds from two to four feet thick, unfossiliferous, 20 

12. Very coarse-grained, yellow sandstone, weathering in rounded masses; exhibits 
cross lines of deposition; is very soft and friable..... 2.6... eee e eee e eee 18 

13. Slope of hill probably covering sandstone «1.6... 6... cece ee eee Risicieadve Mate 

14. Steep slope of hill to water in Wisconsin river; this is probably the place of the 
shaly, argillaceous layers ..... 6). esse cence cee eee neces iewesee ew genaes 


Total thickness from water to top of the bluff........ sie emie nh Chie eese eee E 
Total thickness of Lower Magnesian exposed.........00008 errr 


GEOLOGICAL FORMATIONS. 673 


The Lower Magnesian is a formation of extremely variable thick- 
ness; the greatest known in the Lead region, is about 250 feet; this, 
however, is seldom seen. The country in the vicinity of the above 
section, and Sec. 20, of T.11, R. 2 W., are two instances where the full 

‘thickness prevails. In ranges 4 and 6 E., south of the river, the forma- 

tion is frequently as thin as one hundred feet, in some localities, and 
‘in others, only two or three miles distant, it will attain double that 
thickness. These sudden variations in thickness are due to an un- 
conformability between the Lower Magnesian and the St Peters 
sandstone, discovered by Prof. T. C. Chamberlin, and described in 
another part of this report. 

The only change from limestone that was observed was some lay- 

ers consisting of a very fine calcareous shale’ with some arenaceous 
layers and earthy matter interlaminated, about three feet in thick- 
ness, which were noticed in 
the valley of Grant river, in 
the N. W. qr. of Sec. 42, T. 
4,R.4W. They were also 
seen on Pigeon creek, near 
the center of section 24, in 
the same township; also in 
the quarry at Reese’s Mill, 
in the N. E. qr. of Sec. 34, 
T.4, R. 4 E., in nearly the 
same geological position, 
near the top of the forma- 
tion. 

They were not found oc- 
cupying this position in 


Fre. 5, 


SrcTION oF CALCAREOUS AND ARENACEOUS SHALES AT other localities. Their pres- 
Guan Eat: ence is due, probably, to 


1. St. Peters sandstone. 2. Turfed siope. 3. Lime- % 
stone bed. 4. Calcareous shales. 5. Limestone bed. 6. local causes alone, and they 


Calcareous and arenaceous shales. 7%. LowerMagnesian Cannot be considered as 


ee constituent beds of the for- 
'The following is an analysis of the calcareous shales, by Mr. E. T. Sweet: 

SiGe cccaieivet eos aie Rae Veiwetenie wees ade ees eae s re 17.03 
SAT aT aie eoiesd eee GG Badaee Gua RHE Shere anaes eioaeta s Deen eee A ae Eee 3.56 
Sesquioxide of Ion ..... este cece ete ence eee eee e tenet ene ee tee 1.51 
Casborate of dimers cavoctawnsdnees vee ciless cegechenvune- a seustes 42.14 
Carbonate of magnesia... 2... ccc cccc cece eee ce eect eter ne eenee tee 34.56 
Wiaiteisid cca ciaretee toh ore asda sora igs Groce aioe aperodaGidueuin hace mien RMR DAS OH 1.28 

100.08 


674 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


mation. About a quarter of a mile east of the preceding locality, on 
the opposite side of Grant river, some of the thin layers of the 
Lower Magnesian are slightly folded and bent, and are underlaid 
by other and heavier beds which are undisturbed. Their horizon 
is a little higher than the arenaceous shales, probably near No. 
2 or 3 of the preceding section. These flexures are probably due 
to a slight lateral or horizontal pressure, exerted during the so- 
lidification of the rock, which either did not extend to the under- 


lying layers, or eee 
which, by _ their 

greater compactness, &, 
they were able to Uh. 


7 


resist. The level 
upper surface of the 
lower beds (4), ex- 


cludes the idea of 
unconformability. 
Fig. 6 is a section . pe tite Silse 4 


taken at this locality. 
At the Welsh Mill, Granz 
Hiver 
in Iowa county, a 


short distance north 
SEoTION or CuRVED Srrara AT GRaNtT RIVER. 


of the quarter post 
1. St. Peters sandstone. 2. Slope of hill unexposed. 3. Curved 
of Secs. 18 and 19, strata of limestone. 4. Heavy-bedded limestone. 5. Slope of hill 


T. 4, R. 2 E,, is q "mexposed. 
somewhat anomalous occurrence of the Lower Magnesian, as shown 
in Fig. 7. 


Fie. 7. 


Sgetco or Lowrr Magnusran LIMESTONE AT THE WELSH Mx. 
1. Quarry. 2 Curved strata of limestone. 8. West branch of Pecatonica. 


The Lower Magnesian appears here on the south side of the stream, 
for a distance of about a quarter of a mile. It seems to have under- 
gone a slight upheaval subsequent to its deposition. The stream 


GEOLOGICAL FORMATIONS. 675 


flowing over the sloping beds of the formation has here a consider- 
able fall, which has been utilized as a water power. 

Paleontology. The Lower Magnesian limestone is characterized 
by the extreme rarity of its organic remains. Indeed, it is believed, 
that up to the period of this survey, no fossils whatever have been 
reported from the formation in this portion of the state. During the 
summer of 1873, several places were discovered which establish their 
existence beyond a doubt. The fossils are usually found imbedded in 
the drusy quartz, with which the formation abounds, and usually in 
the form of casts. Some, however, have been found in the limestone. 

From several localities, the following are selected, because fossils 
are more readily found there than elsewhere: 

(1) The 8. W. qr. of the 8. W. qr. of Sec. 4, T. 5, R. 5 E.,on the 
southwestern slope of the hill near the creek. 

(2) The 8S. W. qr. of Sec. 12, and the N. W. qr. of Sec. 13, T. 5, 
R. 4 W. 


ST. PETERS SANDSTONE. 


Geological Boundaries. The formation known by the above title 
in the geological reports of Iowa, Minnesota, Illinois and Wisconsin, 
was formerly frequently designated as the Upper Sandstone, in contra- 
distinction to the Lower. or Potsdam. It is thought best on account 
of uniformity, to adhere to the presentname. It is found in the val- 
leys of the Grant, Platte and Pecatonica rivers, and their tributaries; 
and in Green county, it forins the valley of the Sugar river and its 
branches, this valley being in many places as wide as that of the Mis- 
sissippi. North of the dividing ridge it is found about the head- 
waters of the streams which flow into the Wisconsin, having its 
northern outcrop usually within two or three miles of the river, and 
as far east as Boscobel, forming a portion of the bluffs which inclose 
the river valley. 

Lithological Characteristics. The formation differs from the 
Potsdam sandstone, in that it contains no beds of limestone or shales 
interstratified with it, but presents at any given locality a homogene- 
ous structure through its entire thickness. Its color varies from snow 
white, through all shades of yellow, to a very dark red, and in texture, 
from friable crumbling sand, to compact and fine-grained stone. Be- 
neath the microscope the particles of sand appear rounded and water- 
worn. The same color and texture usually exist through the entire 
thickness at any given place. 

The St. Peters formation frequently impresses upon the surface of 
the country an appearance of terraces, although no true terraces, such 


676 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


as are formed in river valleys by changes of level, have anywhere 
been observed. This is most readily seen in those districts where it 
becomes the surface rock over any extended portion of country. 
About the head waters of Grant river, in the towns of Fennimore, 
Lancaster and Mount Hope, the country is an undulating prairie, 
where the hills are sandstone, capped with a little Buff limestone, the 
greater part of that formation having been denuded. Here the St. 
Peters can be seen, its upper beds jutting out in low ledges, which 
may be traced by the eye continuously for long distances, about the 


heads and sides of the small valleys. 
Such exposures are very fre- 


quent in Green county, where, 
in addition to the continuous 
exposures, small hills are fre- 
quently seen, with flat tops, 
which have been denuded near- 
ly down to the St. Peters. The 
: accompanying sketch represents 
Sketou or A HILL IN THE Town OF MT, PLEAsaNT. a section of such an exposure, 
1. Soil and clay. 2. Buff limestone. 3. St. Peters and is taken from a tract of 

cuca country in the town of Mt. 
Pleasant, in Green county, lying about the little Sugar river. The 
characteristics are the cliff exposure at A, the steep slope of the 
hill from A to B, and the table land of Buff limestone covered with 
soil at C. 

The varying hardness of the upper bed of the St. Peters, some 
portions, especially the white, being quite soft and friable, and 
others nearly as hard as quartzite, due, perhaps, to its greater or less 
impregnation with iron, appears to have caused an unequal resistance 
to disintegration, which has resulted in the formation of Knobs, 
as they are called. They are isolated pillars of sandstone, which shoot 
up in picturesque castellated forms, frequently exposing the entire 
thickness of the formation, and forming very conspicuous objects in 
the landscape. They are chiefly found north of the dividing ridge, 
about the tributaries of the Wisconsin. The following are the most 
remarkable instances: 

(1) The Knobs, situated at the N. W. cor. of Sec. 21, T. 7, R. 4 
E. They are two conical hills of sandstone, forming the termination 
of a ridge extending out from the west. They exhibit the full thick- 
ness of the formation, which is here about 100 feet. 

(2) Castle Rock, situated in the southwest corner of the town of 
Blue River. There are here two very high and precipitous hills of 


Fie. 8. 


GEOLOGICAL FORMATIONS. ” 677 


sandstone, about 250 feet higher than the stream which flows along 
their base. 

(8) Pine Knob, on Otter creek, S. E. qr. Sec. 9, T. 7, R. 2 E. 

(4) Pompey’s Pillar, S. E. cor. Sec. 13, T. 7,R.1E. This is one 
of the most picturesque and precipitous of all. 

The peculiarity of the hardness of the upper beds has proved of 
great assistance in tracing the outlines of the formation, in determin- 
ing its thickness, and detecting irregularities in the surface contour. 

Ripple-marks on the sandstone were only found at one locality. It is 
at a quarry in the 8. W. qr. of Sec. 3, T. 2, R. 5 E., at the grist-mill 
near the mouth of Whiteside’s creek; the top of the sandstone being 
about 25 feet above the water. The sandstone is very irregularly 
bedded in thin layers, with many cross lines of deposition, and the 
upper beds contain many hollow concretions of iron and sand. The 
ripple-marks were very plainly seen on some of the layers by the side 
of the road, and were very regular, parallel and well-defined. 

The St. Peters sandstone differs very much in its thickness in dif- 
ferent localities,’ although this does not appear to be the case so much 
in the Lead region as near the northern outcrop of the formation, where 
it is in some places as thin as 40 feet, and in others, not more than a 
mile or two distant, it is 100, or even 150, feet thick, and seemingly 
depends on the varying thickness of the underlying Lower Magnesian 
limestone. The layers consist of subordinate parts of very various 
lamination, dipping in various directions. 

Many instances were seen of the varying thickness of Lower Mag- 
nesian and St. Peters sandstone,? from which the following are se- 
lected: 

(1) In the S. E. qr. of Sec 26, T. 8, R. 1 E., is a dry run in which 
the Potsdam is seen in outcropping cliffs; passing above the top of 
this, a clay soil sets in, which indicates the place of the Lower Mag-. 
nesian, although it is not seen. Next the St. Peters is seen in bold 
cliffs 120 feet high; the distance from the lower bed of the St. 
Peters to the top of the Potsdam being nowhere over 100 feet. 

(2) In the S. W. qr. of Sec. 13, T. 7, R. 4 W., the St. Peters has a 
thickness of 150 feet, of which the upper 15 feet consist of a soft, 
white, friable sand, in which the usnal concretions and impregnations 
of iron are wanting. This is underlaid by 20 fect of yellow sand- 
stone, and this again by a very dark red sandstone. 

(3) In the N. E. qr. of Sec. 29, T. 8, R. 2 W., the Lower Magnes- 
ian limestone is just 100 feet thick, and the St. Peters sandstone 


150 feet. 
1 See page 673. _ *See page 673. 


678 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


(4) In the S. E. qr. of Sec. 8, T. 7, R. 2 W., the ower Magnesian 
is 200 feet, and the St. Peters 100 feet thick, its upper surface being 
nearly horizontal; both formations appear to have about their average 
thickness. 

(5) In the S. E. qr. of Sec. 2, T. 6, R. 3 W., the sandstone is about 
70 feet thick, and the Trenton limestones about 50. 

There are several new localities which were examined in 1874, 
where slight upheavals of the formation appear to havé taken place. 
The most marked example of this, known as Red Rock, is situated in 
the valley of the Pecatonica, in T. 2, R. 4 E. The sandstone emerges 
from the river near the center of Sec. 20. It reaches it greatest ele- 
vation near the quarter-post of Secs. 17 and 18, where it has a thickness 
of over 100 feet, and disappears again below the river in the S. E. qr. 
of Sec. 7. The average width of the exposure is about half a mile. 
It also extends up the valley of a small creek as far as the center of 
Sec. 8. This exposure covers about one and a half square miles. The 
following section (Fig. 9) through the railroad cut at this place 
illustrates the upheaval: 


Fia. 9. 


: La 
- fe 


a Railroad wath 
L278 Embankment? : 


Lo = 


UrubavaL or Sr. Peters SANDSTONE Ar Rup Rock. 


In the northeast part of T. 3, R. 5 E., there is an upheaval of sand- 
stone, beginuing at the creek which flows nearly due west, south of 
Secs. 11 and 12. The disturbance continues north for some distance, 
as the whole ridge between this creek and the one next north of it 
lies in the sandstone as far north as the Pecatonica river, in T. 4, R. 5 
E. The thickness of the sandstone is here so great that it is hardly 
probable that it has its normal position. A third disturbance, and the 
last which will be cited, is in T. 2, R.6 E. The sandstone on the 
small branch in Sees. 35 and 36 slopes gently toward Skinner creek, 
which appears to lie in a slight depression or aynclinal valley. Pas- 
sing over the ridge between Skinner and Jordan creeks, a slight an- 
ticlinal ridge was discovered, by means of observations on the top of 


GEOLOGICAL FORMATIONS. 679 


the St. Peters, which was exposed in numerous small dry runs. The 
top of the formation was found to be thirty feet higher on the ridge 
than at either of the creeks. Although disturbances of this kind are 
extremely rare and infrequent, yet, in these instances the variations 
‘from the normal dip are too plain to be mistaken. : 

Ores and Minerals. The St. Peters sandstone has been carefully 
examined to find, if possible, any indication of openings, either ver- 
tical or flat, such as exist in the Galena limestone. No evidences 
were seen, except occasional vertical seams and fissures, which con- 
tained neither metallic matter, nor minerals and clay, such as are 
found in veins, and which probably have no connection with the vein 
system of the Galena limestone. The formation seems to be also per- 
fectly destitute of organic remains. 

The only indication of metal seen in this formation is the presence 
of small concretions of sandstone, cemented by a ferruginous sub- 
stance. This is due to the decomposition of iron pyrites or marcasite, 
as is proved by its existence in various stages of decay. These con- 
cretions are not confined to any particular part of the formation, but 
are much more abundant in the upper beds. They are frequently per- 
fectly spherical, and, when they occur iu the dark-colored sandstone, are 
often surrounded by a white ring, about half an inch in width, from 
which the coloring matter seems to have been absorbed. They have 
been noticed with more or less frequency in various places, but were 
found most abundantly in the road near the center of Sec 3, T. 1, R. 6 
E. Another place was observed where the concretions were wanting, 
and their place had been supplied by a different salt of iron; it was in 
the S. E. qr. of Sec. 25, T. 1, R. 9 E., at the junction of the Buff lime- 
stone and St. Peters, The lower bed of the former is full of irregular 
cavities, and small round holes about one-fourth of an inch in diameter. 
The upper bed of the sandstone is colored green by some salt of iron, 
and in it is a seam of greensand and ferruginous matter. It is a pe- 
culiarity of this formation that the stone hardens on exposure to the 
weather. In examining any natural exposure, it is found to consist 
of an outer indurated shell, and an inner and softer sandstone. This 
is a valuable quality, causing it to be easily quarried and dressed, and 
enabling it afterward to withstand the influences of the weather. In 
addition to this, it is easy to find almost any color that may be de- 
sired. Numerous quarries exist in the vicinity of Mineral Point, 
furnishing a white and yellowish-red stone, which is extensively used 
in that locality. 

Situated on Sec. 17, T. 2, R. 4 E., between the villages of Darling- 
ton and Riverside, on the line of the Mineral Point railroad, is the 


680 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


most extensive quarry that has been opened any where in this forma- 
tion. It is the property of Mr. Wm. T. Henry, of Mineral Point, by 
whom it was opened in the summer of 1872. The stone in this quarry 
is of two colors, both a very dark red, but one somewhat lighter in 
color than the other. It very closely resembles the Lake Superior 
sandstone in color, and is by far the handsomest building stone that 
has come under our observation in the Lead region. The railroad 
passes through the hill, so that the stone can be loaded directly from 
the quarry on the cars. 


TRENTON (BUFF AND BLUE) LIMESTONES. 


Geographical Boundaries. It will not be necessary to enter into 
a detailed description of the ground covered by this formation. It is 
sufficient to say that it is always found between the lowest bed of the 
Galena limestone and the top of the St. Peters sandstone, and having 
an average thickness of about fifty feet. 

Lithological Characteristics. The Blue is remarkable as being 
the purest limestone in the Lead region, and the nearest approach to 
the Trenton limestone of the eastern states, both in its lithological 
and paleontological characteristics. A very noticeable feature is its 
marked division into two parts; one very heavy-bedded, in layers of 
two or three feet thick, known as the glass rock, which constitutes the 
lower half; and the other, thin-bedded, in layers of two or three 
inches, graduating sometimes without much change into the thin- 
bedded Galena limestone above. It is at this point that the stratum 
of carbonaceous shale occurs, which is the line of demarkation between 
the Blue and Galena limestones, and as such, is an unfailing guide. 
It varies very much in its thickness, being from a quarter of an inch 
to a foot or more, but wherever a good exposure of the two formations 
is seen, it has uniformly been found. 

The carbonaceous shale attains its greatest thickness in the vicinity 
of Shullsburg. At the Oakland level on the S. W. qr. of See. 5, T. 
1, R. 2 E., it varies from one to two feet;? and at the grounds of the 


1The following is an analysis of this stone, by Mr. E. T. Sweet: 


Sildic ve cecee ss sevenae sac SENTRA Waals shan eled Gane dar eee an eaeme 96.74 
DV TIA VALI Lats <ctactsdosyous sauces pstndeena ter exsae aver iar alee Glas dine xine cite eae hehe val 
Sesquioxide: Of W0niissccadaotannisccwe ge) agence ekamimugesee eews 1.45 
Carooraite Of linia via siesiscva lanai waisracealor ornlnrceniahok Gee a enews eee 1.24 
Carbonate Gf Magneslaescissevsecnesdtcsentne waesee sew aracede ous 18 

100.382 


* Prof. W. W. Daniells, of Madison, has made the following analysis of the shale: 
carbonaceous matter, 43.60; carbonic acid, 0.88; water, 0.30. 


GEOLOGICAL FORMATIONS. 681 


Silverthorn mine on the N. E. qr. of Sec. 31, T. 2, R. 2 E, it has a 
thickness of seven feet,' affording in each of these loealities small but 
handsome crystals of Galenite, having smooth polished faces, which 
is but seldom the case with crystals of this mineral found at other lo- 
calities in the Lead region. . 

The following section taken from the Darlington quarry will give 
a good general idea of the formation. The quarry is situated on the 
N. E. qr. of Sec. 3, T. 2, R. 3 E.: 


Galena Limestone. 


r t. 
1. Soilarid loose rOtk hs anieiing cid nie se aes ou shea ea ae aiey Moet hee take ” se 
2. Yellowish, hard, compact dolomite, similar to the Buff on the surface, but 
not blue between the layers, evenly bedded in layers one foot thick..... 6 
3. Thin layers two to four inches thick..........ccceeeeee eee ce rece eeeeeee 5 
4. Carbonaceouis sb ale vs sjacscins,siate: sincera she sneiaic nin gis 8b ieiesdin ie Sinrt te Bia acd Busted ate OS gs 2 
Blue Limestone. 
5. Thin-bedded, very fossiliferous limestone, in layers from two to five inches 
CHIE seas araasenis Sakeialdodcns elon ae Ghuies oeate eset eae PEAR MTom ReaD EES 3. 6 
6. Heavy-bedded, dark blue limestone, very hard and compact, unfossiliferous 
except in the shaly partings between the beds*®..........esseeeeeeerees 12 
Buff Limestone. 
7. Heavy-bedded, light blue limestone, weathering to buff on exposure; beds 
from 4 to 6 feet thick, contains but few fossils, quarry rock........ wines; 82 
8. Thin-bedded, fossiliferous limestone, similar to preceding.........-.+.+++ 13 
9. Unexposed beneath bed of river not less than ......6--.es secre eereeeeee 10 .. 
Total thickness isncsvonsudokceanGeGaGers: Bik sess olols gaa veer eek ials 83 8 


The Blue limestone has here a thickness of fifteen feet and six 
six inches, and the Buff not less than fifty-five feet, which is remark- 
able as being much greater than was seen at any other point. Its ay- 
erage thickness does not exceed thirty feet. 


1 Also the following analysis of the Silverthorn shale: 

(1) Carbonaceous matter, 18.31; carbonic acid, 1.85; water, 0.40. 

(2) Carbonaceous matter, 15.76; carbonic acid, 0.60; water, 0.32. No. 1 of the Sil- 
verthorn shale was quite dark colored, while No, 2 was a light, ash-colored shale. 

The specimen from Oakland had been for several years exposed to the weather. 


2The following is an analysis, by Mr. E. T. Sweet, of the Glass rock from Mineral 
Point, corresponding to No. 6 of the above section: 


GiliG Bases ry teasinntnbeen. we men Ye oe oe NS A R8 date aa aig sae Hee eT 6.160 
AVI as 5 rosea mune tenn, (Sed dake sada O86 aie cc ete eeeee 2.260 
Sesquioxide Of WON. ... 6. cece cece cre ee eter eter e eee eee e ten eee one 950. 
Carbonate of line .ictscccscsecsneiae Saaveweseceas sage rae cies 85.540 
' Carbonate of magnesia.........ecseecee eee ees usdidedaeeie ategaes 8.930 
Water......... aie Baan hues aii anata ievelaie wea were cess eanee gh bya wee aca -930 
Phosphoric acid ....sseeesccseeeceseeeencenereeeenee teetene sees -055 


682 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


There exists at Mineral Point, at an elevation of about fifty feet 
above the upper surface of the Buff limestone, or quarry rock, a 
stratum of compact limestone several feet in thickness, which in color 
and texture closely resembles the lowest recognized Blue limestone, 
and contains Strophomena alternata, Leptana sericea, Bellerophon 
bilobatus, and some varieties of Orthis, all in great profusion, and all 
of them characteristic of the Blue limestone below. The strata 
which separate them are not exposed. 

It seems probable that this upper stratum may correspond to No. 
5 of the preceding section; that Nos. 6 and 7 are the unexposed beds 
at Mineral Point; and that Nos. 8 and 9 of the Darlington section 
represent the Blue and Buff limestones at Mineral Point. The rela- 
tions of the two principal fossiliferous strata are not, however, fully 
apparent in the Lead region, nor does the upper, one seem to be of 
constant occurrence, whereas the lower one is universally recognized 
in Iowa, La Fayette and Grant counties. 

East of range three east, the presence of the Blue limestone is no- 
where so clearly marked as west of this line. It is usually recog- 
nized by the outcropping of a quantity of highly fossiliferous frag- 
ments, scattered through the soil, having a worn and bleached appear- 
ance. East of range three the fossiliferous Blue limestone was not 
found. It is replaced by a yellowish limestone, containing but very 
few fossils, and in all respects similar to the Buff limestone. The 
thickness between the Galena limestone and. St. Peters sandstone 
remains as usual, about fifty feet. 

There are two exceptions to the foregoing general statement. <A 
short distance south of the center of sec. 18, T. 1, R. 6 E, the Blue 
limestone reappears in its full thickness, with all its characteristic 
fossils, but only covers a small area of ground. 

The second exception is situated in the town of Mt. Pleasant, in 
Green county, in the 8. E. qr. of See. 11, T. 3, R. 7 E. It is known 
as the Marble Quarry, so named on account of the fine polish which 
may be given to the stone. The Blue limestone has here the same 
thickness, both of the thin and thick beds, as in the western part of 
the Lead region. All the characteristic fossils are present, and in 
short, it presents all the usual lithological appearances. It appears 
to have been deposited in a basin-shaped depression, as the top of the 
St. Peters was found to be much lower here than any where in the 
vicinity. Although separated many miles from any other outcrop of 
the Blue limestone, it is evident that it was deposited under the same 
conditions, as in other localities. It has been used here for burning 
lime, of which it always makes a good article. Some small pieces 


GEOLOGICAL FORMATIONS. 683 


have been polished for paper weights, and other small ornaments. It 
takes a high polish, equal to marble, although large pieces cannot be 
obtained. 

One other bed has been observed, not mentioned in the descriptive 
section. It is the line of demarkation between the Buff limestone 
and St. Peters sandstone. It consists of a greenish blue clay, usually 
from one to two feet thick. The clay is very finely laminated, aud 
consists of argillaceous and calcareous matter. It might be valuable 
as a marl, were there not so much of the same constituent parts in 
the surrounding soil, as to make its application superfluous. It is 
not a bed of invariable occurrence, but it has been seen in so many 
localities, over a great extent of country, that it may be regarded as a 
constituent bed of the formation. 

Ores and Minerals. The Blue and Buff limestones are the low- 
est in which any ores are found in sufficient quantities to repay min- 
ing, and the northern and eastern parts of the region in the vicinity 
of Mineral Point, Linden, Dodgeville, Highland, Centerville, Mifflin, 
and the Crow Branch Diggings are the most remunerative. It is not 
to be inferred from this that the formation is barren in the southern 
and western parts, but rather that it lies so deep that it has not yet 
been reached in the present system of mining. 

Large bodies of lead ore have from time to time been taken from 
this formation, but it seems to be more especially productive of zine, 
both as carbonate and sulphnret. At present the zine furnished from 
the localities above mentioned is chiefly derived from it. For statis- 
tics of this product, the reader is referred to the latter part of this 
report, chapter IV. 

Organic remains are found in the greatest profusion, and in a very 
fine state of preservation, the rock in many places being entirely com- 
posed of them. In the Buff limestone they usually occur as casts. 
Without particularizing, reference is made to the general list. 


GALENA LIMESTONE. ! 


Geographical Boundaries. This formation is by far the most im- 
portant in respect to its metallic wealth of all which we have to con- 
sider. In it are contained all the mines of the southern and western 
parts of the Lead region, and whenever mining has been carried on 
in the underlying Trenton limestones, lead is usnally present in the 


overlying Galena. 

1In describing this formation the term ‘‘ Galena limestone,” used in other reports, has 
been adhered to in this, to prevent the confusion arising from several names for the same 
thing, although strictly speaking it is a dolomite. 


684 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


The Galena limestone is the prevailing surface rock in the Lead 
region. Its northern outcrop conforms closely to the main water- 
shed, being parallel to, and always within a few miles north of it. 
Its surface area is given as follows, for each range in the Lead region: 


Range 1 West, 176 sq. miles.| Range 1 East, -  — - 190 sq. miles. 
ae 2 ee dt a 137 ae “ec 2 oe om 179 a3 
“ce 38 “ec Pf R4 oh ac 3 “ = ce 189 “ce 
ins 4 “cc % O4 be oe 4 “ee 164 “ce 
ac 5 ec 108 “c“ oe 5 oe 103 “ce 
oe 6 ia) 7” 45 ae ee 6 oe 144 ee 
644 + 969 = 1,613. 969 


For a more particular exposition of the surface covered by this 
formation, reference is made to the maps accompanying this report. 

Lithological Characteristics. The Galena limestone is almost in- 
variably a very compact, hard, crystalline rock, of a yellowish gray 
color, with numerous small cavities, sometimes filled with a softer 
material, and sometimes lined with small crystals of calcite. The 
upper portion is usually thick-bedded and free from flints, the layers 
being from one to four feet thick, while the lower portion almost in- 
variably consists of several feet of layers from one to two inches thick. 
Good exposures of parts of this formation are frequently to be met 
with; it may be seen in cliffs and ledges on nearly all the streams in 
the Lead region. It always weathers irregularly in these natural ex- 
posures, leaving the surface full of small cavities due to the removal 
of the softer parts. : 

The formation is characterized by layers of flints which however 
are not constant in their occurrence in the same beds at different local- 
ities. In some places there are several beds of flints, which seem to 
be connected with the openings, and serve as a guide to them, while 
in others they are either entirely absent or occupying very different 
geological positions. The flints are sometimes found in separate 
layers, deposited conformably in the rock, and often in irregular 
pieces distributed through the strata. They seem to be confined 
principally to the middle and lower parts of the formation, although 
not entirely absent from any part. 

The general features of the formation will be more readily under- 
stood by reference to the following descriptive section taken from a 
bluff on the Mississippi river, situated on the S. E. qr. of Sec. 28, T. 
3, R. 5 W., where the Potosi road leaves the valley: 


1, Heavy-bedded, Galena limestone; hard and compact, showing a crystalline age 


ture; stratification very regular; good building stone, contains Receptaculites. 26 
2. Thin bedded, light yellow limestone, containing flints intercalated, and in layers 
hetwween the: beds ws sss 4a aisteg a cewaiie ad tase aang seeley aavosurteeg ace 6 


GEOLOGICAL FORMATIONS, 685 


3. Beds of limestone three to four feet thick, containing but few flints; good build- seer, 


Gah Rene aN ARS OS Cpe NSS Ree MEI a des og Dodd Saeed Ee 12 
4, Alternating layers of limestone and flints......... Sed than asigehansls aieslte Satan aaa 9 
5. Beds of limestone 18 inches thick, separated by layers of flint two inches thick.. 19 
6. Heavy-bedded limestone, layers two feet thick, containing numerous intercalated 
flints, very hard and compact; stratification quite regular .......... .....06 17 
7. Very close-grained limestone, in beds about four feet thick; good for building 
stones ‘Conbalnis NO Mints sissies eiomartaia aan neariears ener se eRe ae Ree 29 
8. Slope of the hill to water in the Mississippi river covering Galena limestone..... 91 
Total thickness 0625204) io se ears oon Pods Mine ENOO CROSS YeRAIAea Lewes 209 


The ground rises as it recedes from the bluff, so that there is prob- 
ably an unexposed thickness of at least 40 feet of Galena limestone 
above the top of the cliff. 

The Galena limestone is in many localities successfully quarried as 
a building stone. This is chiefly the case in the southern and western 
parts of the region, where the Buff limestone or St. Peters sandstone 
cannot be obtained. The chief objection to it is the frequency of 
cavities and soft places in it which render it difficult to dress, and 
cause it to weather irregularly. For foundations, or any work where 
beauty of finish is not the chief object, it is a good and durable stone. 

Paleontology. The organic remains of the Galena limestone are 
quite abundant, but do not exist in such profusion as in the Blue 
limestone. The characteristic fossil of the formation is the Recepta- 
culites Owen or lead coral, which is found indifferently in all parts 
of the formation. Next in frequency are the Streptelasma (Petraia) 
corniculum, and som: varieties ofsmall Orthis. The most infrequent 
is the Maclurea magna, which is found in the middle beds of the 
formation. In the upper beds the Lingula quadrataisquite frequent, 
and often found in a fine state of preservation. Other and more in- 
frequent fossils are the Plewrotomaria lenticularis, Bellerophon bil- 
obatus, Orthis biforata, and occasional Orthocerata. 


CINCINNATI GROUP. 


Geographical Boundaries. This formation was found to cover a 
much larger area of country than had previously been supposed. It 
appears in T. 1, R. 2 E., and has an area of about five square miles, 
contained in the following sections: 21, 22, 28, 24, 25, 26, 27, 28, 34, 
35 and 36. In T.1, R.3E,, it is found in Sees. 30 and 31, covering 
about one square mile. It does not occur north of T. 1, on ranges 2 
and 3 E. 

Near the corner of Secs. 22, 23, 26 and 27, T. 1, R. 2 E., the forma- 
tion attains an elevation of nearly 600 feet above Lake Michigan; and 


686 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


from here to Seales Mound village it forms a continuous chain of hills, 
among which the most noticeable is Charles Mound, which is the 
highest land in the state of Illinois. This mound is capped with 
about 50 feet of Niagara limestone, and in one place a quarry has 
been opened, from which specimens of the fossil /avosites favosa 
have been obtained. 

The average dip of the strata, in the vicinity of Scales mound is 
about 29 feet per mile in a southwesterly direction, with indications 
that it is not perfectly uniform but slightly undulating as represented in 


Fre. 10. 


SECTION FROM SCALES’ Mounp To THE STaTE LINE. 
1 Cinncinnati Group. 2 Galena Limestone. 


The Cincinnati group next appears about the Platte Mounds, in the 
southern part of T. 4, R.1 E, and the northern part of T. 3, R. 1 
E. InT.4,R.1 E., it is found in Sees. 31, 32, 38, 84, 35, 36, cov- 
ering an area of nearly three square miles, and reaching an elevation 
of 1,140 feet above the sea. 

The formation also exists in its full thickness at the Blue Mounds, 
but exposures of it either natural or artificial are seldom visible; 
some of the clay which characterizes the lower part of the formation 
was found on the Brigham farm at the East Mound. 

No exposure of this formation was found at these localities. Ina 
passing over the gradual slope of the mounds it is impossible to dis- 
tinguish any boundary line between the Cincinnati group and the un- 
derlying Galena limestone, such as is seen on the level table land 
south of Shullsburg, which has been formed by the denudation of the 
soft shales which the harder limestone has to a great extent escaped. 
The line of demarkation between the shales and the overlying Niag- 
ara limestone, is well defined at the West Platte Mound on all sides 
by the very marked change from the steep slope of the limestone to 
the comparatively gentle one of the shales. On the north side of 
this mound, ledges of the Niagara limestone may be seen in plave 
almost to the bottom of the formation. 

The Cincinnati group was also found covering about seven square 
miles of country, about the Sinsinawa Mound, in the following sec- 
tions: 1,12, 18, 14, 24, 25, 26, 35, 36, T. 1, 2. 2W. Secs. 6, 7, 8, 16, 
17, 18, 19, 20, 29, 30, 31, T. 1, R. 1 W., extending north from the 


GEOLOGICAL FORMATIONS. 687 


Sinsinawa Mound, as far as Jamestown. Nearly all the mines on 
the ridge north and east of Fairplay are sunk through the lower part 
of the Cincinnati group, and good specimens of WVucula fecunda 
may often be found in the dirt thrown out of the shallow holes, when 
the clay has not been covered again by the refuse of deeper workings. 

Lithological Characteristics. The strata of the Cincinnati group 
are very regularly and conformably deposited, and do not exhibit any 
indications of sudden and violent dislocations, faults, or uplifts. 

The lower beds of the formation are very finely laminated, and of 
a dark blue color, in many places becoming green and brown. The 
upper layers are of a yellowish color, and more or less calcareous and 
silicious. 

The lower and middle members of the group split readily and with 
a very smooth face, but the upper layers, though quite thin-bedded, 
present a rough and uneven appearance. This group nowhere presents 
beds of sufficiently thick and durable stone for building purposes. 
Only one place was noticed where an attempt had been made to quarry 
this rock; it had been abandoned as impracticable, after a small 
amount of work had been done. 

Where undisturbed, this group has a thickness of about 125 feet. 
This is the case only on the mounds, which are still capped with the 
Niagara limestone, as in all other places it has been more or less re- 
moved by denudation. 

There is nowhere a good natural exposure of the formation. The 
rocks throughout the group offer so little resistance to the weather 
that they do not appear in rugged cliffs, such as are seen in all the 
formations which underlie them, but usually in gently undulating 
hills. The best exposure is the one in the ent of the Illinois Central 
railroad, near Scales Mound Station, of which a very accurate section 
-has already been given in Prof. Hall’s report. It is much more aceu- 
rate than can now be obtained, as the weather has since then so de- 
composed the friable shales that only a few feet of the lower beds are 
now visible, as they were originally presented. Asa general guide 
to the formation, we take the liberty of reproducing it: 


Ft. In 
1. Greenish shale, with alternations of calcareous and silicious layers, a few 
inches in thickness ..-.- 0. ese esse eee eee e eter e teen ene e eee ene ee 7 8 
2. Green silico-calcareous and argillaceous shales ......------ ener ee eens ll 6 
3. A silico-caleareous or magnesian band ...-.--..++eeeeeeee cere eter reese ae. 4B 
4, Greenish shale as above ....-- secre eee ee cece cece e etter eee e teen teen nes 12 
5. Coneretionary layer, 1 to 3 inches....-..--..+e.eee sere eee e tree tees ee &8 
6. Shale with Lingulas.......e cece cee reece crete nee nett eee ene nes Go Ake 
7. A layer filled with a small Nucula, and known as the Nucula bed, 4 to 8 


inches . vec cecccccrseccrcenecer es eeeenn ee eeeneeeerensisen seen esate w“ 8 


688 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


8. A calcareous band cut by open joints or fissures, into which the materials of ¥¢. In. 


the layer above have penetrated.......... 0 cece cece cree eee e eee renee 4 

9. Dark olive shales, finely laminated and destitute of fossils.............. 3.4 
10. Nucula bed, similar to the above, 4 to 6 inches...-..-+.+eee seers eee eee . 6 
Total thicktiess exposed ....... cece cess ce seen rete eee e ence enone 42 ‘5 


A noticeable feature of the two Wucula beds, which are the lowest 
of the series, is that the floor of each is a thin seam of pyrites of a 
nodular and crystalline form which rests on the bed below. This 
was the only metalliferous indication noticed in the formation, and it 
did not seem to exist in great abundance. 

The beds of Galena limestone which underlie this formation are 
quite regularly stratified in beds about six inches thick. In the west 
end of the cut, the beds are perfectly horizontal on a course N. 55° W. 
On a course at right angles to this, the dip was found to be about 50 
feet per mile on a S. W. course. It is probable, however, that this is 
only a local dip. 

Nothing of a metallic nature was discovered in the formation, ex- 
cept a few small seams of marcasite in the lower beds. 

The best localities for obtaining fossils from this formation are on 
the sides of the mounds, where the water has partly removed the 
turf and soil, and formed gullies which are filled with broken frag- 
ments of the different beds. Among these may be mentioned the 
8. E. qr. of Sec. 22, T. 1, R. 2 E., near what is known as the Gratiot 
place. The lower beds abound with shells of the Wucula fecunda; 
the middle ones with Rhynchonella increbescens, Strophomena alter- 
nata, and stems of Chetetes. The upper beds contain a few Orthoce- 
rata, but they are infrequent. 

The lower beds of the Cincinnati group have been exposed in some 
old diggings in the N. E. qr. of sec. 2, T. 8, R. 1 E., on the road near 
the Burris place. Specimens of the Wucwla, and other shells charac- 
teristic of the lower beds were here found in great profusion and per- 
fection. 


BAA 


ney 


eS 


ea 


Tur Maavartcey, Leran.< Ewan Cnt 


VIEW OF BLUFFS ON THE MISSISSIPPI. 


THE LEAD REGION. 689 


CHAPTER IV. 
THE LEAD REGION. 


Boundaries and Area. In Wisconsin, the Lead region may be 
said to be bounded on the north by the northern outcrop of the Ga- 
lena limestone, running parallel to the main watershed from the Mis- 
sissippi to the Blue Mounds, as already described; on the west by the 
Mississippi river; on the south by the state line; on the east by 
Sugar river. These limits include all of the Lead region which has 
ever been productive, as well as much that has never as yet proved so. 
The area thus included which has been, or may hereafter become pro- 
ductive, is necessarily that of the Galena limestone, which is about 
1,776 square miles. 

Explanation of Mining Terms. For the enlightenment of the 
readers of this report, who are unfamiliar with mining terms, the 
following short explanation of expressions most frequently used in 
the Lead region is offered. 

Range. This is probably the most indefinite term in use, and at 
the same time, one which is universally applied. 1st. A range de- 
notes a single, or several parallel crevices, containing useful ores or 
minerals; vertical, or approximately so; seldom more than a few 
yards apart; sometimes, but not necessarily, connected by quartering 
crevices. Its length may vary from a few hundred feet to a quarter 
of a mile or more; in short, so far as the crevice or crevices have 
been connectedly traced, or there is a reasonable probability of such 
connection. Thus, different parts of the same range often have dif- 
ferent names given them before the connection between them is 
proved. This is a fruitful source of confusion. 2d. The term range 
is also applied to horizontal bodies of ore, of which there may he 
one, or several, superimposed upon one another; sometimes, but not 
necessarily separated by unproductive layers of rock, limited in 
length in the same way as a vertical range. 

Crevice. This term denotes a fissure in the rock, vertical or near- 
ly so, but a few inches in width, of indefinite length, which may or 
may not be filled with ores or minerals; when a crevice becomes very 
small, less than an inch in width, it is called a seam. 

Wis. Sur. —44 


690 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Vein, is aterm little used; it denotes the filling of ore and accom- 
panying minerals, or either, found in a crevice. 

Lode or Lead, are words usually substituted for vein; they are, 
however, generally applied to ore deposits found either in crevices or 
openings. 

Swither, a metalliferous crevice, making an angle with the prin- 
cipal vein or lode, sometimes called a quartering crevice. 

8 o’clock, 10 o’clock, etc, ranges whose course bears toward the 
sun at those hours of the day. 

Openings. They are of two kinds, vertical and horizontal. 1. 
Vertical openings are known as crevice openings, which are mere en- 
largements of the crevice in certain parts, these being sometimes co- 
extensive with the vein in length, and sometimes mere local enlarge- 
ments. There are in the same crevice frequently several openings, 
situated one above the other, separated by beds of unproductive rock. 
Crevices vary in width from one to several feet; when very wide and 
high, they are sometimes called tumbling openings. 2. Horizontal 
openings are large 
irregular spaces 
between the strata 
which contain the 
lode. Such open- 
- ings are usually 
- from one to four 
feet high, and are 
frequently super- 
imposed upon one- 
/== another, separated 
= by an unproduc- 
SEctIon or OpENtINGs (ideal), tive rock called a 


A, Crevice; B, Crevice opening; ©, Flat opening; D D, Flat openings ‘* cap.” The “cap” 
connected by E E, Pitching sheets; F, Pocket with ore. . 
of one opening be- 


Fie. 11. 


ing frequently the “floor” of the one above it. 

Pockets are small irregular cavities in the strata in which ore is 
frequently obtained. 

Chimneys are irregularly shaped vertical holes found in crevices; 
sometimes connecting openings, and at others extending from ‘the 
surface of the ground to some particular stratum of rock. 

Sheet. This is a term usually employed to designate a solid body 
of ore exclusive of other minerals which may fill a crevice or open- 
ing. A sheet is said to “pitch” when it inclines considerably from 
the perpendicular. 


‘ 


MINERALOGY. 691 


Gouge. This is the soft rock or clay frequently found between the 
sheet and adjacent wall-rock. 

Bar. The term denotes a band or belt of very hard and unpro- 
ductive rock, crossing the crevices and sheets. In crossing a bar all 
sheets become less productive, and are sometimes entirely lost, the 
crevices usually dwindling to mere seams. Their width varies from 
a few feet to many yards. 

Wash-dirt, is the name given to the small ore as it first comes 
from the mine, mixed with small pieces of rock and clay. 

Pipe-Clay. A light colored plastic clay frequently found in the 
openings and crevices. 

Drift. An underground gallery or roadway. 


MINERALOGY. 


There does not appeax to have been any absolute and unvarying order in which the 
minerals of the Lead region were deposited in the mines. The following conclusions 
are derived from the inspection of the ore as it occurs m place in the numerous mines 
visited, and from the examination of a great number of specimens; and it is assumed 
that when crystals of one mineral are coated or covered with another, the overly- 

. ing one is the more recent. The minerals appear to have been deposited in the follow- 
ing general order: oes 


SPHALERITE. 


ee iomeunrrennes 
Dotomire, CaLcrre. 


a pee} 
Pyrite, Marcastrg, CHALCOPYRITE. 
BaRirE. 


CALCITE. 


= 
es 
CERUSSITE, SMITHSONITE, MALACHITE, AZURITE. 


The order above given, however, is subject to very numerous and important excep- 

tions, and is more particularly applicable to crystallized specimens than to heavy ore de- 

* posits. Large bodies of ore frequently consist of galenite, sphalerite and pyrite, so 
mingled together that no order of deposition can be ascertained. ; 

In general it appears that the sulphurets of the metals were deposited first, and that 
the carbonates have been generally if not invariably derived from them. Carbonate of 
lead (cerussite), when found crystallized, always occurs in connection with galenite; and 
carbonate of zinc (Smithsonite) is so frequently found graduating into the sulphuret 
(sphalerite) as to leave but little doubt of its origin from that mineral. 

Jt seems not improbable that the formation of the carbonate of zine may even now 
be taking place in the ground to quite a large extent ; especially in such deposits as are 
not below the water level, or are only periodically submerged. Itis a well known 
fact that the Drybone diggings are usuaily comparatively free from water, and that 


. 


692 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


the zinc ore below the water level is usually blende (sphalerite) with but little admix- 
ture of the carbonate. As the level of the water in the ground becomes gradually lower, 
and it is a well known fact that it does, the atmosphere, together with surface water 
charged with carbonic acid, is permitted to act upon the blende, and a transformation 
from the sulphuret to the carbonate is the result. . 

The association of calcite with other minerals is such as to indicate that it must have 
been formed in crystals during at least two different periods. Stalactites of recent ori- 
gin are found in the mines, which on being fractured show a distinct crystalline struc- 
ture, and large planes of cleavage. 

The following is a list of the minerals known to occur in the Lead region, arranged 
according to the system adopted by Prof. Dana, in his Mineralogy: 

Sulphur. Native sulphur is found but seldom in the Lead region; its presence is 
usually due to the decomposition of iron pyrites. It is usually found in a pulverulent 
form. Some pieces weighing as much as an ounce were seen in a cabinet at Hazel 
Green, which are said to have been obtained from a small sheet in some of the Bun- 
come mines. It is said to be not uncommon in this vicinity. Other localities where it 
is found are, Mineral Point and the Crow Branch diggings. 

Bornite. Variegated or Purple Copper ore. Composition: copper 62.5; iron 13.8; 
sulphur 23.7. This is quite a rare mineral; a few pieces have been found in the copper 
diggings near Mineral Point; it has never been found here crystallized, but always mas- 
sive and in small pieces. 

Galenite. Composition: lead 86.6; sulphur 13.4. This is the only ore of lead found 
in sufficient quantities to be of economic value; it is universally known in the Lead re- 
gion as ‘‘mineral.”’ It frequently occurs in distinct crystals, either as a cube or some 
modification of it. Octahedral crystals are quite rare, but are occasionally found, espe- 
cially in the carbonaceous shale of the southern part of the region. Usually, however, 
galenite occurs massive, with a very distinct cleavage. Freshly broken surfaces have 
always a bright steel color, which speedily tarnishes on exposure. to the ai. 

Sphalerite. Blende or Black-jack. Composition: zine, 67; sulphur, 33. This is 
one of'the most abundant minerals in the Lead region, besides being of great economic 
value as an ore of zinc. It is almost invariably found as an associate vein-mineral in the 
horizontal deposits of Lead ore. It is usually found massive and compact, of a dark 
brown or black color, due to a small portion of iron contained in it, und more or less 
mixed with galenite. The Lead region has never afforded a perfect crystal of blende, 
although many specimens are found with small and impertect crystalline faces. The 
fractured surfaces of such specimens usually have a resinous luster. 

Pyrite. Composition: iron, 46.7; sulphur, 58.3. This is the most common vein- 
mineral found in the mines; it is universally met with in veins, lodes or other deposits 
of ore, and in many cases impregnates the rock when all other metals are absent. In 
crevices it frequently appears to have been the first mineral deposited. It is usually 
found massive, although handsome crystallized specimens are frequently obtained from 
the mines. In crystals it usually assumes some modification of the cube, the octahedron 
being quite frequent. It also occurs in radiated and reniform masses. It has never yet 
been considered of any economic value in the Lead region, and as it is so much mixed 
with rock, it is doubtful if it could be profitably separated, except by the natural process 
of disintegration, to which some varieties are liable when exposed to the air. The Crow 
Branch diggings and the Linden mines afford large quantities and good specimens of 
this mineral. 

Marcasite. Composition: iron, 46.7; sulphur, 53.3, or same as pyrite. The difference 
between this and the preceding is but slight, and chiefly due to crystalline structure; 
the former belonging to the monometric and the latter to the trimetric system. It is 
somewhat lighter colored than pyrite, and decomposes more readily in the air. It is 


MINERALOGY. 693 


quite a common vein-mineral and occurs in globular and cockscomb shapes. It is abund- 


ant in the New 


Diggings district. It is difficult to preserve specimens of this mineral 


longer than a few months. 


Chaleopyrit 


e. Composition: copper 34.6; iron, 30.5; sulphur 34.9. This is the 


principal ore of copper in the Lead region, and is most abundantly found in the vicinity 
of Mineral Point. 1t usually occurs massive, frequently mixed with pyrite; small and 
indastinct crystals are occasionally found. 


Hematite. 


Composition: iron, 70; oxygen, 30. Impure arenaceous varieties of this 


mineral frequently occur, nowhere, however, sufficiently rich or abundant to be of any 


economic value 
common as the 


. It seems to be chiefly due to the decomposition of pyrite, and is most 


ferruginous sandstone concretions in the upper beds of the St. Peters. 


It is also frequently found as ocher, with other vein-minerals, especially in the flat 


openings. 


Oxide of Manganese. A substance consisting of oxide of manganese with a little 
oxide of iron, zinc, and traces of magnesia according to an analysis of Dr. Bode of Mil- 
waukee, is found in crevices in the ‘Trenton limestone, in some diggings situated on 
Sec. 11, T.4,R.1E. The mineral is as light as cork, color brownish-black, submetallic 
luster and streak, soils readily, and is infusible. It is very soft, and does not occur 
erystallized. It has a structure in thin parallel layers resembling wood. 


Calamine. 
is of very rare 


Composition: silica, 25.0; oxide of zinc, 67.5; water, 7.5. This mineral 
occurrence in the Lead region. It is found in small, drusy crystals, 


coating Smithsonite. The crystals are very brittle, colorless, and have a vitreous lustre. 
It is found near Mineral Point. 

Barite. Composition: sulphuric acid, 34.33; baryta, 65.67. It occurs usually white 
and massive, but sometimes in lamellar and crested forms. The only place where it 
was found in distinct crystals was in the railroad cut at Scales Mound, where it occurs 
in small cavities, as small but very perfect transparent crystals, associated with dolo- 
mite and pyrite. It is not a very abundant mineral, but is found in several of the min- 
ing districts, especially Dodgeville and Mineral Point. The following is an analysis by 
Mr. E. T. Sweet, of a specimen from the 8. W. qr. of Sec. 6, T. 5, R.3 E., on Van 


Meter’s survey: 


Sihieai ns Seas esehe red ata bedi ntaed pe at ea wade suesauneo caine eve 2.24 
Alin aes 2 oh eoig sores Meee ew kas ook Se ete wae eels Ie sas arose .83 
Sésquidxideof Wott acseosseky sees veveeers tio say ees ceuleseameaveld s 77 
IWeatericc antic Gos Mois nd oak eRaMGagatne Riad aan Ska etatee tunes asses Trace 
Barite. sulphate seuicnya cranes doe cee spark dave pinue amended ne eielnee 95.27 
Lame, sulphates +: sesitwesyassaeas eyes cee see eee gia tangas saute 1.30 

100.41 

Anglesite. Composition: sulphuric acid 26.4; oxide of lead 73.6. Traces of this 


mineral are reported as occurring in some of the mining districts, but no specimens 
have as yet been obtained. It probably originates from the decomposit‘on of galenite. 

Calcite. Composition: carbonic acid 44; lime, 56. This is a vein-mineral common 
to all the deposits of ore whether in crevices or openings. It occurs crystallized in modified 


rhombohedrons 


and scalenohedrons. The variety known as Dog-tooth-spar is a very 


‘frequent form, especially in the Shullsburg and Linden districts which affords very hand- 


some cabinet specimens. The Mineral Point district affords handsome rhombohedrons, 


and the Linden 


mine affords handsome twin crystals of calcite set on sphalerite (blende). 


It also occurs there, rarely, as a pseudomorph after marcasite and has then a radiate or 


divergent form. 


Dolomite. Bitter Spar or Brown Spar. Composition: carbonate of lime and car- 


694 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


bonate of magnesia, in slightly varying but nearly equal proportions. It occurs occas- 
ionally in small rhombohedral crystals in cavities of the Galena limestone. The best lo- 
cality for obtaining cabinet specimens is in the railroad cut at Scales Mound. 

Smithsonite. Often improperly called Calamine. Composition: carbonic acid, 
$5.18; oxide of zinc, 64.81. This mineral, commonly known as Drybone, is one of 
the two ores of zinc found in the Lead region. It is found most extensively in the cen- 
tral and northern parts and usually in connection with blende. It crystallizes in 
rhombohedral forms; such specimens are, however, rare. It usully occurs massive, hav- 
ing a structure similar to partially decayed bone, from which it derives its common 
name. 

Pseudomorphs, of Smithsonite, after calcite, are sometimes formed. They occur as 
rhombohedrons, and in the various irregular shapes in which calcite occurs in the Lead 
region. Perfect crystals, in which the transformation from calcite to Smithsonite is 
complete, are very rare. It is much more common to find skeleton crystals, or those 
which have been formed by the deposition of a smooth, light-colored shell of Smithsonite, 
about a sixteenth of an inch thick, over all the exposed surface of the calcite, followed 
by a gradual removal of the crystal contained within the shell. The space within the 
shell is sometimes partially filled with Smithsonite, and frequently planes ave formed 
within, parallel to the cleavage planes of the original crystal. Pseudomorphs are also 
found in which the imperfect crystallization of sphalerite is very evident. Smithsonite 
is also found covering crystals of galenite, which are undecomposed. 

Cerussite. Composition: carbonic acid,16.5; oxide of lead, 83.5. Cerussite is occasion- 
ally fonnd in small pieces, but never in sufficient quantities to form an object of mining. 
It occurs in irregular rounded pieces of a yellowish color, exhibiting no crystalline 
structure. It has been found near Mineral Point, and in former years quite frequently 
at the diggings near Blue Mounds. 

Cerussite is found in small, irregular, translucent crystals of a white or light yellow 
color, in the mine of Messrs. Poad, Barrett & Tredinnick, near Linden. The specimens 
seen were large, cubic crystals of galenite coated with pyrite, the crystals of cerussite 
being formed on both of these minerals. The specimens indicate that the crystals of 
pyrite had been formed, and many of them broken before the formation of the cerussite. 

Hydrozincite. Composition: carbonic acid, 13.6; oxide of zinc, 75.3; water, 
11.1. This isa mineral of rare occurrence in the Lead region. It is found at Linden 
and Mineral Point as a white, finely crystalline, fibrous incrustation on Sinithsonite. 

Malachite. Composition: carbonic acid, 19.9; protoxide of copper, 71.9; water, 
8.2. It is occasionally found m small seams mixed with other ores of copper in the 
Mineral Point copper mines. Crystals or good cabinet specimens do not occur. 

Azurite. Composition: carbonic acid, 25.6; protoxide of copper, 69.2; water, 5.2. 
It occurs similar to malachite, massive and in seams associated with chalcopyrite. The 
Mineral Point mines aftord very beautiful cabinet specimens of small rhombohedral 
crystals of dark blue color. 


PRESENT CONDITION OF THE MINES IN THE VARIOUS DISTRICTS. 


dn this subdivision of the chapter, it is desired to present such information in regard 
to the individual mines as has been collected during the course of the survey up to the 
time when it became necessary to submit the manuscript for publication. This infor- 
mation has in many cases been procured under difficulties; owing sometimes to tem- 
porary suspension of mining operations, sometimes, but not often, to the reticence of 
owners, and sometimes to petty and vexatious hindrances which are best understood by 
those who have ever attempted to collect such information. It has been our aim per- 
sonally to inspect and visit all the mines of any consideralble magnitude, or possessing 


MINES — BEETOWN DISTRICT. 695 


any features of geological or mineralogical interest; and in nearly all cases the owners 
have been found ready to afford every facility for investigating and obtaining infor- 
mation. 

Mining is a business in which change is the rule and not the exception, it is therefore 
probable that some changes may have occurred since the commencement of the survey 
which are not here recorded, although it has been our aim to discover and incorporate 
them in the following report. The mines of the Lead region will be considered under 
separate districts, as, in tact, they are geographically distributed. 

The visitor in the Lead region will constantly hear the terms ‘‘ Brown rock,"’ ‘‘ Glass 
rock,’’ ‘‘ Pipe-clay opening,”’ etc., used by the miners to designate the different strata 
in which they work This would be an advantageous system, were it not vhat the sev- 
eral names are applied to widely different strata by persons in the several districts. The 
term ‘‘ Glass rock,” for instance, is indiscriminately applied to all the strata in the Buff, 
Blue and Galena limestones. The following section is given as a general guide in un- 
derstanding the relative position and thickness of the strata and openings, to which ref- 
erence will occasionally be made in the subsequent pages. The section, however, will 
not be found of universal application, but merely shows the strata as their position is 
now understood by the most intelligent and systematic miners. In practice, the most 
reliable plan for determining the geological position of an ore bed or mine is, to find the 
outcrop of some well defined horizon in the vicinity, and ascertain the distance of the 
bed or mine above or below it, after making due allowance for the dip. 

There are numerous openings occurring in all the upper and middle beds of the Galena 
limestone, none of which appear to be found regularly in all the districts. The section 
is, therefore, confined to the more persistent openings of the lower beds. 


Galena Limestone. 


Feet. 
Green rock.......... Saiurbaviehnerdtacad hore eaitta’h seine aid omnaane nals Spade 4 
Green rock opening....... 6c. ec ee ec ere teen eect e ete e ee eee enter ener ees 3 
Groen 10d vids ocetens A ohedeGee Meets AeieaumGuaid eae ee raes 12 
Brown rock... .. ccc e cee eee eect eeee Seri ateg Vise NOERS Dene HOES BOR bees 12 
Brown rock opening ..... 6 sce eee e cece eee eee e nent e ene teen eee ee 5 
Brown TOCkkswies Wee che hee Cae EMEA RIEU wacd Cmte hee A ee Es 8 

Buff and Blue Limestone 

Upper pipe clay opening... .. 6.2. eee e cece cece ee eee ee ene eee es 5 
Glass rock (Blue limestone)....- 60.2 sere reece ete eee teen nent eeeen es 25 
Glass rock opening. ..---eeeeee seer eee ee eet e etter e nent eee cnet ee 6 
Buff limestone. ...- 6c cece cece eee ee teen eee eee e teense eee e teen eeees 12 
Lower pipe clay opening...-+.+-+.-+eseeeeee vane a eataany ety vid gee cane 3 
Buff limestone. .... 0. eee ee cee eee eee eee eee tense ene e ee eeeerrete 10 
St. Peters sandstone........ sce cece cere eee tee en ee tenes ee eet eeees 


BEETOWN DISTRICT. 


This is the most westerly district in which any productive mines have been worked. 
In former years they were very productive, but have gradually become less so. There 
are several subdistricts, of which the principal ones are Beetown, Nip-and-Tuck, Mus-: 
calunge, and Hacketts. The diggings in the immediate vicinity of Beetown are situated 
north and east of the village, chiefly on Secs. 20 and 29 of T. 4, R. 4 W. There are 
here on the ridge about a dozen principal old ranges, all nearly parallel, and bearing a 
few degrees north of west. They vary from half a mile to a mile and a half in length, 
some of them extending easterly to the Grant diggings. There are no large organized 


696 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


companies at work on them, the principal product being by individual parties in small 
lots. Lead ore is usually found in this district in two principal openings, known as the 
12-foot opening and the 65-foot opening. The first is named trom the height of the 
opening which usually averages about 12 feet. The second derives its name from 65 
feet of unproductive rock which separate it from the first. 

The following parties are now or have recently been mining near Beetown: 

Brown Bros, & Birch. These diggings are situated in the Hull Hollow, about 
three-quarters of a mile south of the village. They were discovered in 1860 by Walters 
& Roberts, and were first worked in the twelve foot opening. 

There are three parallel east and west ranges situated about nine feet apart. They 
produce lead ore which is found in flat openings 414 feet high and 4% feet wide, lying 
about 7 feet above the 65-foot opening. The ore has been traced by a level 300 feet 
west from the discovery shaft. The depth at the working shaft is 60 feet; the greatest 
depth on the ridge will be 160 feet. Work was commenced in the winter of 1875-€, 
since which time the product has been 35,000 pounds. The prospects are considered 
good. 

Wilcox Diggings. N. hf. of S. E. qr. of Sec. 32, T. 4, R. 4, W. This ground has 
been recently bought by Messrs. Henry, Ross, Gundry & Toay, of Mineral Point, by 
whom it is now operated under the name of the Beetown Mine. 

Work was commenced here by Mr. Wilcox in 1868. <A level has been run in the 
ground 500 feet, underlying a flat sheet of blende and Smithsonite, which is in places 36 
inches thick. The sheet has been found to extend 80 feet north and south, and 180 feet 
east and west; its extreme limits are not yet known. On its south side, some copper 
ore has been found. The sheet lies in the upper pipe clay opening. 

About 22 feet above the sheet of zinc ores is one of Smithsonite and lead ore, 150 feet 
wide, whose length is unknown. It lies in flat and pitching sheets in the greenrock 
opening. 

The ground has produced lead ore to the value of $3,500; also, 45 tons of Smithsonite 
and 175 tons of blende. Four men are now employed here, and it is intended to work 
the mine to its full extent. Fig. 12 shows the position of the present workings. 


Fia. 12. 
a N 
a 
3 
= 
—_ x, 
De . 
4S *s 
Se 


ee pees ees 

SEER NOS a ee 
Works th the 

‘Greenrock Openin 

SORE 


S x 
Puan oF WORKINGS IN THE BEETOWN MINE. 


BS 


Some mining has also been done during this year (1876) on Sec. 27, on the east side 
of Grant river. The parties are as follows: 

Josiah Crossly & Co. Produced about 8,000 pounds of lead ore in the operations of 
one month. 

Crossly & Bass. Situated south of the preceding. Work was carried on for six 
months, and stopped by the owner of the land; 20,000 pounds of lead ore were produced. 

Wilcox &Sons. These parties have been working about a month on a new east and 
west range. The prospect is considered good. 


MINES — BEETOWN DISTRICT. 697 


Pigeon Diggings. 

They are situated on the north half of Sec. 20, T. 4, R. 3 W., and consist of several 
east and west ranges, in which the ore is found in flat openings in the ‘‘ Brown-rock "’. 
division of the Galena limestone. The ground is owned by Messrs. Barber, Dewey & 
Cox. There are about 50 men employed here, mining chiefly in the old workings, at a 
depth of 30 to 50 feet below the surtace. The annual product of the Pigeon diggings is 
about 250,000 pounds of lead ore. Mining is chiefly confined to the winter season. 

During the last year a sheet of Smithsonite was discovered on the 8. E. qr. of Sec. 19, 
which has produced 60 tons. 


Hacketts Diggings. 

These mines are situated on Sec. 17, T. 4,R.4 W. They have been idle for several 
years. Work has recently been resumed on them by the following parties: Hutch- 
croft & Pigg, and Whitehead & Co. They have now good paying mines in the 65-foot 
opening. The annual product is about 30,000 pounds. 

Nip and Tuck Diggings. 

Situated on the south half of Sec. 25, T. 4, R. 5 W. They consist of several east and 
west ranges, crossed by north and south ranges. Very little mining is now done here. 
The parties are Sillick & Co. and Roberts & Co. The annual product is about 20,000 
pounds. 

Musealunge Diggings. 

Situated on Sec. 26, T. 4, R.5 W. There are here numerous east and west ranges, 
from a quarter to a half a mile in length, lymg near Rattlesnake creek. More activity 
is displayed here in mining operations than anywhere else in the district, about half of 
the ore smelted in the Beetown furnace being obtained here. In addition to the east 
and west ranges already mentioned, there are a great number of small parallel crevices 
running nearly east and west, and crossed by various quartering ones, forming a perfect 
net-work of veins and crevices. The following parties are operating in this vicinity: 

Graham Mining Company. This is a Milwaukee company who own and work a 
large tract of ground comprising the west half of Sec. 26. The workings are all in the 
65-foot opening. The following section of the Dewey and Maiden shatt is given, which 


shows the position of strata from the top of the ridge downward: i 
cet. 

Soil and Chiys o. o.sor based nasteen seesees ans Aaiekeaaeeesdye 15 
Galena limestone... 1.6.0... cece cee ee cece EEE eee ee enters 38 
Tough, light rock, hard and flinty ....... 6. .eeee cece cence eee e teenies 2 
Opening from 5 to 12 feet high...... 0... cc cece cece cece een eee nen ees 12 
Hard rock with layers of flint..... . ....... evened eeayehaeeeasteavexd 65 
Opening (workings)........6.c cece cence cnet eee n eee nent ene enn es 13 
Galena limestone to top of Trenton..............2.005 sdboueetectrday inecig aeiake 35 
Dot al GHickness cw sige cages he od MODE Aa Rae KA wel Cer? 180 


The two openings are seen here to be separated by 65 feet of intervening barren rock. 
The ground is drained by a level, about three-quarters of a mile long, run on the ran- 
dom of the lower opening, at an expense of $20,000. It empties into one of the adja- 
cent branches of Rattlesnake creek. It could easily be drained to the top of the Blue 
limestone, by a level in the horizon of the Pipe-clay opening. 

A convenience in hoisting was noticed here which might profitably be adopted in other 
portions of the Lead region. A six-inch hole had been drilled from the surface to one 
of the drifts for purposes of ventilation. An Artesian well bucket was then put on, and 
all small stuff and wash-dirt was removed through the hole, thus saving a long and un- 


698 - GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


necessary transportation underground to the main shaft. The company has worked 
continuously here for many years, and now employs about fifteen men. The ground has 
been very productive; it produced in one year 1,300,000 pounds. Its average annual pro- 
duction for the last nine years is estimated at 300,000 pounds of lead ore. 

James Thomas & Co. This company has been working here for the last fifteen years. 
The ore isfound on an east and west range, in the 65-foot opening. The diggings are 
dry and from 150 to 160 feet deep. Four men are employed here. The average pro- 
duct is 150,000 pounds of lead ore per annum. The land is owned by Mr. Dewey. 

Hutcheroft & Thomas. Situated 450 feet south of the preceding, and connected 
with them underground. They are in the same opening as the preceding, and have 
been worked continuou:ly many years. During the last year they have been idle, hav- 
ing been sold by the parties who operated them. When worked, their annual product 
was 150,000 pounds. 

Hutchinson, Dewey & Co. Situated on the 8. E. qr. of Sec. 26, east of James Thom- 
as & Co., and on the same range and opening. This party has been working here since 
1869, and has now a very good prospect. The average depth below the surface is 160 

feet; in some cases it is 180 feet. They are 
ErGae connected with the Adkinson diggings by a 
quartering range. They have produced about 
30,000 pounds in the last three years. Three 
men are now employed. 

Adkinson Diggings. Situated a short dis- 


SSS 


tance east of the preceding and connected 
SESSEED with them. Access is gained to these diggings 
NESSES through a level about a quarter of a mile long, 


emptying into the valley of Rattlesnake creek. 
The level was run on a northeast crevice, 
which contamed a large amount of ore, and 
was frequently intersected with east and west 
ee Ten Renn er en CCR crevices, as represented in Fig. 13. These dig- 
QUARTERING Rane, ADKINSON Diacines. gings have been worked continuously during 
1. Northeast or quartering range; 2, 3, 4. East the last twenty years. During the last fifteen 
and west veins. years the annual product has been 150,000 

pounds of lead ore. Four mea are now employed here. 

Showalter & Payten. Situated a quarter of a mile southeast of the preceding, and 
near the south line of the Dewey land. These parties commenced two years since, and 
are now working an east and west range in the 65-foot opening. Two men are now 
working here, and the prospect is good. During the last two years the product has been 
70,000 pounds. 

Arthur & Co. Situated 200 feet south of the preceding, on Mr. Arthur's land, This 
is a new east and west range, discovered in the spring of 1876. A shaft has been sunk 
90 feet to the 65-foot opening, and a small amount of ore produced. The appearances 
in this new range are quite encouraging. 

Ritter & Bock. N. E. qr. Sec. 35, T. 4, R. 5 W. Situated on land owned by Mr. 
Ritter. This is a new east and west range, discovered in the summer of 1875. It is 
worked on the 65-foot level. It is regarded as a good prospect, and has already pro- 
duced 20,000 pounds. 

Loomis & Co. Situated on the land of the Graham Mining Co., in the southern 
part. This is also a new east and west range, discovered in August, 1876. It has pro- 
He ahout 12,000 pounds. The mine 1s now in a condition to yield 1,000 pounds per 

ay. 

The Lead ore in the Muscalunge mines occurs in direct contact with the wall rock, 


MINES— POTOSI DISTRICT. 699. 


usually in vertical sheets, and without any of the associate vein-minerals which are usu- 
ally found in the other mining districts. 


n 


POTOSI DISTRICT. 


Mining operations here are chiefly confined to the winter season, and furnish employ- 
ment to about twenty miners. 

The old ranges of the Potosi diggings are included in Secs. 33 and 34, T. 3, R. 3 W. 
Their general course is about N. 70° W., although some bear a few degrees more to 
the west, and some a few more to the north. They numbered about thirty in all, which. 
were considered as separate and distinct ranges; and in addition there were many 
smaller crevices not sufficiently important to constitute ranges by themselves. 

Among the more important were the Long, Wooley, Gillet, Gilmore, Smith, Polking- 
horn and Barbara, some of which were over a mile in length. 

The productive portion of these ranges is confined to the middle and lower portions of 
the Galena limestone, none of the crevices having as yet been proved as low as the 
Brown rock; the ore is usually found in sheets of varying thickness. 

Considerable irregularity exists in the form- 
ation of many of the crevices in the Potosi 
3: district, by which, they seem to split up 
in the lower beds of the limestone, forming 
key-rocks and divergent crevices. An instance: 
= in point was seen in the diggings of Mr. 
J Meredith, in the N. E. qr. of Sec. 33, about 
- 300 feet south of the old Wooley range, on- 
1% the summit of the ridge. 
* A shaft was sunk on the main crevice which 
continued without change for sixty fect from 
_ the surface. At this point a hard key-rock, 
:!F as it is called, was encountered, on which 


Fie. 14. 


Main Crerice and Shalt 


downward at an angle of about 45° for a 
distance of thirty feet. Here a vary hard and 
smooth floor was found on which the sheet 
was followed out by drifting, for a distance of 
one hundred and thirty feet without reaching 
the end. No appearance of openings was 
: - observed. These diggings were struck about 
Suotiox OF THe ‘Munepind MINE: six years ago (1870) and have produced since 
then about 420,000 Ibs. 


mw 
NY 
aN 
15 
ms fe 
8 
& 


Rockville Diggings. 


There are here a number of east and west ranges with flat openings, which have been 
worked with but little interruption since 1840, and now fumish employment to about 
twenty miners. Mining is chiefly confined to the winter season. The following parties 
are now operating here. 

Phillips & Walker. 8. W. qr. of 8. W. qr., Sec. 13, T. 3, R.3W. These parties 
are working a new east and west range, discovered by them in the summer of 1874. 
The ore is found at a depth of about 100 feet below the surface, in flat openings from 50- 
to 60 feet wide, whose length has not yet been ascertained. They have, however, been 
worked to a distance of 300 feet. The lead ore is found in what is known here as the 


700 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


second opening, which lies about 30 feet above the upper surface of the Bluc limestone. 
Their annual production is 30,000 lbs. : 

Dilger Mine. N. W. gr. of N. W. qr. Sec. 24. This is a new range discovered in 
January, 1876. The works are as yet confined to the first opening, which is here 30 feet 
above the second. It has produced during the past year 40,000 pounds. 

Hayward Range. 6. W. qr. Sec. 18. This range has been worked continuously 
every winter since its discovery in 1841, and has yielded in all between four and five 
million pounds. It is now worked by Messrs. Jackson & Calloway in the second open- 
ing, which is here from 30 to 40 feet wide. It produces about 100,000 pounds per an- 
num. 

Warfield Range. §. W. qr. Sec. 13. This range has been worked every winter 
during the last thirty years, and has produced about 2,000,000 pounds. It is now 
worked by Messrs. White & Dunn in the second opening, which is here from 30 to 40 
feet wide. Its annual product is about 100,000 pounds. 

Curnow and Pillow Range. §. W. qr. Sec. 13. This range has not been idle 
during the last thirty years, and is still productive. During the last fifteen years the 
range has produced over 100,000 pounds per annum. Messrs. Nichols & Stephens are 
now mining on it, and producing 20,000 pounds per annum. 

Emery and Davis Level. N. W. qr. of N. W. qr. Sec. 24. The level was com- 
menced in 185%, and is now 600 feet long, and drains the ground 1m its vicinity nearly 
as low as the second opening; its cost was about $20,000. The excavations here were 
of the nature of a quarry, several flat sheets of lead ore being found interstratified with 
the Galena limestone. While the level was in operation, the annual product was about 
100,000 pounds. The level drains the Langstaff and Willey ranges, which were discov- 
ered about thirty years ago, and have been worked continuously ever since. Most of 
the lead ore is obtained from the first opening; the annual product is 50,000 pounds. 
These ranges have been worked to the present water level, leaving sheets of ore from 
12 to 18 inches thick going down. The level should be run a few rods farther to con- 
nect with a north and south crevice; it would then probably drain all the ranges much 
cleeper. 

Stone & Bryhon. Situated near the N. W. corner of Sec. 1, T. 3, R. 3 W., on 
land owned by Mr. Stone, about three miles north of the village of Rockville. ‘The 
works are in the first opening, which is from eight to ten feet wide. They have been 
worked in the winter season during the last four years, producing annually between 
30,000 and 40,000 pounds. They were formerly worked by Mr. Grusham and were 
more productive. The mines are dry. 

Griswold Diggings. Situated about a quarter of a mile south of the preceding. 
These are dry diggings worked in the first opening, which is here about six feet high 
and from ten to thirty feet wide. They have been worked continuously during the last 
seven years, producing about 65,000 pounds per annum. 

Henry Gillilan’s Diggings. These diggings are situated about three miles south- 
east of Rockville, on the Platte river. They are dry diggings, and have been worked 
during tke last four years, in the first opening, which is here thirty feet wide and about 
six feet high. The annual product is 25,000 pounds. 


British Hollow Diggings. 


But little mining is now done in these mines. In the winter s2ason about twenty 
men are employed. The following parties are now mining here: 

J. Alderson’s Diggings. N. W. qr. Sec. 26, T. 3, R.3 W. They are situated on 
the Craig range in the village of British Hollow. This range was worked by a Cincin- 
nati company for three years; they abandoned it two years ago. This company 
produced about three million pounds during the time of their operations. Mr. Alder- 


MINES — FAIRPLAY DISTRICT. 701 


son commenced mining here again in July, 1876, with a steam pump, and has sunk four 
shafts. The workings are about 120 feet deep in the second opening, and in the third, 
which is about 25 feet below the second. The mine has not produced much yet, as the 
time has been mostly consumed in preliminary operations. 

Peak & Blair. N. W. qr. Sec. 26. These parties have also been working on the 
Craig range during the past summer (1876). They have a flat sheet of lead ore about 
five inches thick in the first opening, which here averages 20 feet in width. This range 
has been worked during the last forty years. The product of the present parties has 
been about 20,000 pounds. 


Dutch Hollow Diggings. 


They are situated on the north half of Sec. 36, T. 3, R. 3 W., about two anda half - 
miles east of Potosi. The following parties are now operating here: 

Dutch Hollow Level Company. Mining operations have been carried on here con- 
tinuously for the last six years, excavating a level on or near the upper surface of the 
Blue limestone. The level is now about half a mile long, and it is expected to reach the 
main shaft in about a month. When completed, the level will unwater all the Galena 
limestone above it, which is here about one hundred feet thick. Itis expected to un- 
water the Kendall, and many other old ranges in the vicinity, as deep as the third open- 
ing. The level is not producing much now. During the year 1872, it produced 60,000 
pounds. i 

Rup & Son. N. E. qr. Sec, 35. This party has been working during the last six 
months on a part of the Ziig range. The ore is found in the first opening, which is 
here about 15 feet wide. The production has been 150,000 pounds. 

Zug Diggings. This is an east and west range, being the same range and opening 
as the preceding. It is worked toa depth of 75 feet. The present party has mined 
here during tbe last year and a half, and produced 150,000 pounds. 

Langstatf & Gillan. Situated three-quarters of a mile northeast of the preceding, 
on the creek in Sec. 25. The lead ore is found here in a flat sheet in the first opening, 
near the water level and about 30 feet below the surface. Three men have been work- 
ing here twelve months, and have produced 60,000 pounds. 

The production of the Potosi district, including Rockville, British Hollow and Dutch 
Hollow, could not be definitely ascertained, as very little record has been kept of it. It 
is estimated at 80,000 pounds per annum. 

Mining in this district is generally abandoned in summer for farming, and resumed 
again in the winter, in the lack of other employment. In this way a large number of 
men are at work in the winter, each raising a small amount by prospecting, which forms 
in the aggregate the total product of the district. 


FAIRPLAY DISTRICT. 


The only mines in this vicinity which have recently produced anything are those of 
Black & Co., on the N. E. qr. of Sec. 24, T. 1, R. 2 W., and those of Williams & Co., 
near the center of Sec. 19, T. 1, R. 1 W. 

Black & Co. This property, which comprises in all about two hundred and 
forty acres, is owned by Messrs. Joseph and Thomas Sparks. It has been Inown to be 
rich ground for many years, and to contain, besides the ore, an inimense amount of water, 
which was the chief obstacle to be overcome. Previous to the operations of Mr. Black, 
it had been attempted by three separate parties, at as many different times, but always 
with more or less loss. 

Mr. Black commenced work on it in November, 1871, by means of pumping, and 


702 GEOLOGY AND TOPOGRAPHY OF THE LEAD R&GION. 


‘continued to add pumps, engines, and pumping machinery at intervals. At the time 
the mine was visited (June, 1874), there were in operation two steam pumps, and two 
large lift pumps, together with three boilers and two engines, one of them about thirty 
horse power. The company then contemplated adding a larger engine and machinery. 
Tt was estimated that about a thousand gallons of water per minute were being pumped 
from the mme, and when the lower opening is reached, which is thought to be about 
fifteen feet deeper, it will become necessary to pump about fifteen hundred gallons per 
minute. 

The mine is in the upper beds of the Galena limestone, which is here present in its 
full thickness, and indeed the first few feet of the shafts ave sunk through the lowest bed of 
the Cincinnati group, as may be seen from the yellow clay with the characteristic shells 
in any of the shallow, prospecting holes in the vicinity. The following section of the 
strata, penetrated in sinking the pump-shaft, will give a correct idea of the formations 
here represented: 

Cincinnati: Group. 


Ft. In 
Soil and clay bed... 2... ees cece eee e eee ee eee eee eee ee ee eens 20 
Pipe Clay... ss. cece eee cece eee entree een nee eee te eee eee e ees -- 10 
Bed of black clay.........-+-+++-+5 Hicks ceacadglsrunonapatd oiled dx sntiguanousbatense dda eee | 
Shaly layers... 6.0... cece cece eee eee eee erent et en ene nn eeees .. 10 
Galena Limestone. 
Galena limestone in thin layers.......... es cece eee eee eres teens 4 
Galena limestone cap in layers 4 feet thick, gradually increasing in 
thickness to the bottom. ...... 0. . cece cece eee eee cnet eee eenes 30 
Opening containing Ore... 11.0... eee eee eee ees weet a es 30 
Potal depth of Shaftiyivevave esses dees eetieteeeneanaaete ye 86 00 


The course of the vein is nearly east and west, and five shafts have been sunk upon 
it, the deepest of which has reached a point 105 feet below the surface. The opening 
now presents the appearance of a series of large rooms or caves, from 15 to 20 feet wide 
and about 15 feet high, for a distance of 600 feet. : 

The vein was crossed in several places by bars of hard rock, one of which was sixty- 
five feet in thickness. The bars always caused a decrease in the size of the opening, 
and sometimes nearly cut off the vein. In other places the opening contracted in width, 
in. which case the ore usually occurred in a solid sheet, sometimes as much as seven feet 
thick by seven and a half high. In the caves or larger parts of the opening the ore was 
found in large masses, weighing sometimes several thousand pounds. T'wo large mas- 
ses were found which weighed respectively fifty thousand and twenty-seven thousand 
pounds, With the ore large masses of rock were found mixed with loose dirt and a fine 
dark clay. The sides of the opening were much washed and worn by water, showing 
a very regular stratification with no appearance whatever of faults or dislocations. Each 
of the caves in the opening had a chimney going down, apparently to a second open- 
ing, which has never yet been proved or worked. The upper part of the opening was 

sometimes filled with a large key-rock, having a crevice on each side of it. Some- 
times, however, the key-rock was replaced by a flat-cap-rock containing crevices. 

The appearance of these caverns as we passed through them was a sight not soon to 
be forgotten. On the floor lay great masses of rock which had fallen from above, with 
clay continually moistened from the dripping walls and arching roof, and here and thero 
the feeble light revealed rich masses of glittering ore. , 


MINES — FAIRPLAY DISTRICT. 038 


The annexed section shows the relative position of the differ- 
ent portions of the vein: 

1. Crevice containing lead ore. 

2. Key-rock with crevices on each side. 

a 3. Opening containing lead ore with loose masses of rock and 
ay. 

4. Chimney going down to 

5. Secend opening. 

6. Galena limestone. 

te ‘The vein has not been worked over half the time since its 
= {= commencement, as frequent stoppages were necessary for the 
purpose of putting in new pumps and machinery. Work was 
discontinued here in February, 1876, but it is expected that act- 
ive operations will soon be resumed. 
= Mr. Black estimated that he had taken out about one million 
pounds of lead ore, at an expense of $40,000. 

Williams & Co. This mining property is situated about 
three-quarters of a mile northeast of Black's mine, and was op- 
== erated by the proprietors, Messrs. Thomas and Jeremiah Wil- 

n= : 7 

=, hams, and Mr. O'Connor. The water in this ground is not 

ee nearly so abundant as in the preceding. It is easily removed 
' with a common lift-pump, worked with a ten-horse power en- 

gine; the amount seldom exceeds 250 gallons per minute. Mining has been confined 

to the upper half of the Galena limestone. The lower clay beds of the Cincinnati group 

are also found here, but there is not so great a thickness of them as at Black’s mine. | 
The pump shaft commences at the top of the Galena limestone, and is sunk to a depth 

of one hundred and six feet, at which point the 
top of the second opening is found, after passing 
through the first opening, which is situated at a 
depth of forty-seven feet from the surface, and is 
probably identical with the first opening at 
Black’s mine, which it much resembles in its gen- 
eral appearance. The first’ opening here consists 
of a series of large caves or enlargements of the 
crevice, with chimneys going down to the second 
opening. 

The ore was found in masses mixed with clay and 
large pieces of stone which had apparently fallen 
from the roof or cap. The Lead ore from its great- 
er specific gravity usually occupies the lower part 
or floor of the opening. The course of the range 
is very nearly east and west, but bears a little 
north on its western end. The length of drifts in 
the top opening amounts to about nine hundred 
feet. Itis about worked out at the western end, 
but still continues good at the east. Several 
masses of lead ore were found in this opening 
weighing from fourteen to fifteen thousand pounds. 

A singular formation of ore was found in the top SEctI0N or CERES HN TEM Wits 
opening, as illustrated in the annexed diagram. 

1. Opening and crevice filled with loose masses of lead ore and rock, mixed with loose 
fine clay and sediment. 2. Thisisa bench about a foot in width on each side of the open- 


Fra. 16. 


T04 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


ing, and extending along the entire length of the cavo, a distance of 80 feet, on which 
shelf, and the sides immediately above and adjacent, the ore was deposited, fastened 
firmly to the wall, and exposing crystalline faces to the center of the opening. In other 
portions of the mine this bench was not observed, and the ore was usually attached in 
sheets to the side of the opening. 3. The lower opening. 4. The Galena limestone. 

The mine was discovered and opened in February, 1872, and since then has proba- 
bly been the most productive and remunerative mine in the district, on account of the 
comparatively small amount of water to contend with, and the large amount of lead 
ores obtained, which has been estimated at two anda half million pounds. Work was 
suspended on this mine in the fall of 1875, and has not since been resumed. 

Fairplay Level Co. A company, consisting of Messrs. Merry, Olinger, Rewell, 
Pier and Notte, having formed a stock company with a capital of $50,000, have been 
engaged during the last eight years in running a level on land owned by George 
Siddell & Co. The level is commenced on the E. half of the 8. W. qr. of Sec. 26, T. 1, 
R. 2 W.., about three-quarters of a mile below the village of Fairplay. It has been run 
eastward a distance of 2,200 feet, and thence south 70 feet; and has cost about $30,000. 
One ‘‘shift’’ of three men is the usual number employed, and it is not expected that 
the level will be completed for many years. Its greatest depth below the surface is 140 
feet, and 48 feet below the natural water level; one mile farther east it will drain about 
60 feet below the present water level. 

This level will unwater the whole of section 25, and will cut the following ranges in 
the third opening: The Crabtree, Thompson, Engine, Carns, Bruce, Lost range, 
Franklin, Seward, and Cave range. The openings in these ranges are vertical; they 
were formerly worked and abandoned with lead ore in them going below the water. 
When these ranges are unwatered they will undoubtedly be very productive. 

In the vicinity of Fairplay, about fifty men find employment in mining dwing the 
winter; in summer the mines areidle. The greater part of the lead ore raised in this 
district comes from the mines south of the village, and, exclusive of the two large mines 
previously described, has not exceeded 50,000 pounds per annum for the last six years. 


HAZEL GREEN DISTRICT. 


The Hazel Green district exhibits considerable activity at present in mining opera- 
tions; and the reports of smelters in this vicinity show that a large amount of ore is 
raised here. During the years 1872 and 1873, miners were attracted to other localities 
by the prospect of higher wages, which caused a temporary decrease in the production 
of lead ore; the mines, however, remained unimpaired. The miners have now returned, 
and the mines have regained their normal productive condition. 

The most remunerative and continuously productive portion of the district is the prop- 
erty of the Hazel Green Mining Company, otherwise known as Crawford, Mills & Co. 
It is situated on the N. W. qr. of Sec. 30, part of the 8. W. qr. of Sec. 30, part of the N. 
E. qr. of Sec. 30, part of the 8. E. qr. of Sec. 19, the 8. W. qr. of Sec. 19, the N. W. qr. 
of Sec. 19, the W. hf. of the 8. W. qr. of Sec. 18, all in T. 1, R. 1 E.; also the N. E. 
qr. of Sec. 24, and the E. hf. of the E. hf. of Sec. 25, T. 1, R. 1, W., comprising in all 
eleven hundred and six acres, on which over four hundred and fifty distinct mineral 
veins have been discovered and worked. 

During the early days of mining these grounds were wo-ked from the surface as deep 
as was then possible, which was only about thirty-five feet, when they had to be aban- 
doned. Pumping was tried on some of the larger bodies of ore, but as a general thing 
was found to be too expensive to be very remunerative, on account of the vast amount 
of water which the ground contained. In the year 1862, Crawford, Mills & Co, com- 
menced their level from a point on the Hard Scrabble Branch, and have been working 


MINES — HAZEL GREEN DISTRICT. 705 


it continuously ever since. Its total completed length is now about four thousand feet. 

It is a feature of this ground that it is traversed by several bars or belts of ground 
which are very hard and impervious to water. As soon as the level is driven through 
one of them, it unwaters the ground in all directions to the next bar. 

Sometime in the year 1871, one of those bars was reached which was'so hard that blast- 
ing with powder made but little impression on it. As an experiment, nitro-glycerine 
was tried and gave the greatest satisfaction, so much indeed that a factory has been es- 
tablished here, and it is gradually being introduced into the mines. It is at present 
used in Dubuque, Galena, New Diggings and several other places. It was at first re- 
gardcd with some dislike and distrust by the miners, but this prejudice is fast being 
overcome, and nitro-glycerine or some of its compounds will probably supplant gun- 
powder in the mines at no distant day. The factory at Hazel Green produced, during 
the first three years, about three thousand pounds of nitro-glycerine, and the demand is 
steadily increasing. 

On account of the position of the bars, it was found necessary to make three branches 
to the level, one of which is now completed and is gradually draining the western part’ 
of the ground. The northern branch when completed will undoubtedly unwater the 
rest of the ground. 

This level is an evidence of what can be done by scientific mining, when carried on 
persistently and systematically, with sufficient capital, applied with foresight and saga- ' 
city. It has cost the company twelve years of time and about $100,000. Its results are, 
that it has already repaid the outlay of capital by the ore raised from the ground un- 
watered by it, which would otherwise have been inaccessible. When completed, it will 
unwater the ground 135 feet below the natural water level on the ridge It furnishes 
employment to about 80 miners during the mining season, which without it, would 
hardly exceed half a dozen. 7 

Quite a large and clear stream of water is discharged from the mouth of the level, 
and is at present used to operate a furnace and three wash-places. 

The ore in the Hazel Green mines is usually found in sheets; this is its charac- 
teristic mode of occurrence. The ranges are approximately east and west, or north 
and south, the former being the most productive. Ore is also sometimes found in large _ 
bunches or pockets, containing sometimes several thousand pounds, and occasionally in 
‘Openings. The pockets are often lined with large and very regular cubes, affording 
handsome cabinet specimens. The total production since the discovery of these mines 
has been carefully computed from the smelter’s accounts at about 126,000,000 pounds. 
Their present product is about 800,000 pounds per annum. 

Mining in this vicinity is confined to the upper half of the Galena hmestone, which is 
here present in its entire thickness, the clay of the lower beds of the Cincinnati group 
being found near the village, on the road to Galena. A section of the strata from the 
top of the ridge to the level would present approximately the following features: 


Soil ands Aints eo osls ovale sans scakaiees Heke eabeeculalyudecnuie ated hws > 15 feet. 
Galenarliniestoney ousieneseecueiwits ioiveinsaie, erties ceduees 90 “ 
Shales or thin layers of limeston€........eccee ese e ete ee ne cee ee vee 10 
First clay opening .. 00... cece cece eee ence eect ene e ene ee en ences 10 “ 
Second lay Opening 2.2.05 waseves ensues sauaeaesanhon awn 20 
Flint opening to floor of LeVOliain copa reeaniasss case ascas aoce ean any 20 ‘ 
Total thicktess 0 cn0c ace vous ces adotapas cra gana o vined was 165 


The following are the parties who are now engaged in mining on the company’s land 
or have been during the course of the present survey: 
Wis. Sur. —45 


706 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Richard Eustice & Co. These parties were working in a new locality, and had, at 
the time they were visited, one of the handsomest displays of ore ever seen in the 
grounds. The bottom of the shaft had penetrated an opening filled with soft earth. 
The sides of the opening were lined with a body of ore which presented an unbroken 
mass of cubic crystals of various sizes, some of them being as much as six inches on a 
side, and of very perfect shape, affording very handsome cabinet specimens. There 
was not less than 10,000 pounds of lead/ore in sight, in a place about ten feet long. 
This body of ore is known to continue several feet deeper to the drift below. These 
diggings were worked until the'fall of 1875, and produced in all 120,000 pounds. 

Rowe & Rowe. This is 2 new range, and was discovered in March, 1874. It is an 
east and west sheet, in which the ore occurs in a crevice three or four inches wide, at a 
depth of about 60 feet below the surface, and about 35 feet above the flint opening. 
Work was suspended here in September, 1876. The total amount produced to that 
time was 50,000 pounds. 

Richard Eustice’ Diggings. Situated on the Phelps range, shafts are 90 feet deep, 
down to the clay openings. Length of drifts about 150 feet. The ore here occurs in vw 
sheet about an inch thick. The diggings were worked from June, 1872, to June, 1875, 
and produced about 40,000 pounds. Near these diggings, and about ten feet deeper, is 
an east and west sheet dipping to the north, carrying bunches of blende, which affords 
quite handsome crystals. 

_ Manwaring and Madison Range. This is an east and west range, and is some- 
times known as the Hinch range, from the name of a party who formerly worked it, and 
by whom it was abandoned in 1858. Since the level has been run, the water has fallen 
about 50 feet in this ground, and in December, 1873, work was resumed on it by Craw- 
ford, Mills & Co., since which time it has produced 40,000 pounds of lead ore. The 
shaft is down about fifty-five feet, or within six feet of the flint opening. Work was 
suspended on it in June, 1875. 

John Edwards’ Diggings. Situated a short distance further west on the same 
range. A flat sheet of blende is found here in the second opening, at a depth of 80 feet 
below the surtace. The order of deposition here is: 1st, pyrite; 2d, galenite; 3d, blende. 
During the winter of 1875-6, the product was blende, 10 tons; lead ore, 1,400 pounds. 

Bull Pump Range. This range was worked by Jackson & Co. during the years 
1873-4-5, producing 90,000 pounds. Work was suspended here in the fall of 1875. 

Bininger Range. This range has been worked at intervals since May, 1874. It is 
now worked by Stephens, Nankivel & Rowe; four men are employed, working vith a 
horse pump in the second opening. During the present year the product has been 
30,000 pounds. 

Big Pump Range. This range has been worked since October 1, 1876, by Rich- 
ard Eustice & Co. A small amount of ore has been produced from the first opening. 

McCoy Water-Wheel Range. Work was recommenced here about August 1st, 
1876, by Rowe & Son, in the first opening. 

Oates and Eustice. This party has been working during the last year and a half 
on a range 200 feet north of the west branch of the level. The lead ore is found in a 
flat sheet in the second opening. The opening is seven feet high and averages seven 
feet in width. The sheet is about one foot thick. The product to the present time has 
been 150,000 pounds. 

Clark’s Diggings. Two men have been working during the last year in the range 
next north of the McCoy Water-Wheel range. The ore is found as *‘ chunk mineral ” 
in the second opening, which is here six feet wide. The product has been 30,000 
pounds. 

Tregenza & Son. Work was commenced by this party in the fall of 1874, on the 
Drybone range, south of the Badger lot. ‘The works are in the second opening, which 


MINES — HAZEL GREEN DISTRICT. T07 


is here from 10 to 12 feet wide; and contains a flat sheet about five inches thick, of 
which the upper part consists of lead ore, and the lower of zinc ores. The product has 
been, zinc ores 20 tons; lead ore 20,000 pounds. Very handsome specimens of galenite 
coated with cerusite are obtained here. 

W.H. Eustice & Bro. This party commenced work in the fall of 1875 at Crawford's 
little pump shaft. They worked in the second opening during the winter of 1875-6, 
and suspended in the summer on account of water. The prospect is good and they ex- 
pect to resume work this winter (1876). Product 10,000 pounds. 

Edwards Estate. On this land there are several old ranges, now drained by the 
level of Crawford, Mills & Co., in which the following mining has been done: 

Peter Skinner, in the winters of 1874-5 and 1875-6, produced 100,000 pounds. 

Moffat & Co., in the same seasons, produced 80,000 pounds. 

Pierce & Trewather, in the same seasons, produced 70,000. Other parties in the 
same. time, in small amounts, 100,000. 

In addition to the parties already mentioned, there are, in the winter season, usually 
about sixty miners at work on the lands of the Hazel Green Mining Company. 


Diggings in the Village of Hazel Green not on the Lands of the Hazel Green 
Mining Company. 


McBreen & Co. Thisis an east and west sheet, connected with a quartering one avera- 
ging about an inch thick, situated on the land of Dr. McBreen, on the N. W. qr. of Sec. 
25,T. 1, R.1W. The range was worked in 1844, and the ore taken out to the water lev- 
el. The water having become much reduced by the Hazel Green Company’s level, work 
was recommenced in 1874, since which ‘time about 55,000 pounds of lead ore have been 
taken out. The diggings are in the upper beds of the Galena limestone, and not down 
to any opening. 

Torneal’s Diggings. A short distance southwest of the precedirg is arange con- 
sisting of twenty parallel crevices, about twenty-five feet apart, and bearing N. 15° E. 
Work was abandoned on them in 1850, and was recommenced by Mr. Torneal about 
eight years ago, since which time they have produced 42,000 pounds. Considerable 
time and labor have been expended in running a cross drift to prove the ground and as- 
certain the number and position of the crevices. The distance here to water is 80 feet, 
and the diggings are in the upper beds of the Galena limestone. 

Rowe and Vivian. This was formerly known as the Chizzem range, and is situated 
on Edward Williams’ land, in the southwest quarter of Sec. 25, T. 1, R. 1 W., in the 
southern part of the village of Hazel Green. It is a north and south range, and was 
worked and abandoned in 1854, Work on it was recommenced by the present parties 
in November, 1873. Since then it has produced 24,000 pounds. The full thickness of 
Galena limestone is here present, overlaid by a few feet of clay of the Cincinnati group. 
The deepest shaft is 106 feet, and the total length of drifts is about 190 feet. Work 
was suspended here in the spring of 1875. 

Williams & Bro. On Edward Williams’ land. This party commenced in the fall of 
1875, and are now mining in a range a short distance west of the diggings of Eustice 
& Co., in the village of Hazel Green. They are working on a vertical sheet, and have 
produced, to the present time, 20,000 pounds. 

Chandler’s Diggings. These diggings are situated on Mr. Wetherbee’s land, and 
on the Sulphur lot range. Work was conmmenced two years ago, ar-1 continued to the 
present time. The works are in the second opening, which is from six to eight feet 
wide, and contain a sheet of lead ore from one to two inches thick, and also large, ir- 
regular masses which afford handsome specimens. The mine has produced 500,000 


pounds, and is now very good. 


708 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Buncome Diggings. 


The Buncome Diggings form a sub-district belonging to Hazel Green. They are sit- 
nated on the Galena river near the mouth of Bull branch. They were formerly very 
productive diggings, and a few parties are still working in them. They are situated in 
the Brown rock, which is the lowest bed of the Galena limestone, and is here from twenty 
to thirty feet thick; and extends down to the creek bed at the State line, where the top 
of the Blue limestone may be seen. At the mouth of Bull branch the top of the Blue 
Limestone is found to be twenty feet above the bed of the stream. Mining is generally 
carried on here by drifting into the side of the hill. An example of this is seen on the 
land of Mr. Gabriel Mills on the N. W. ar. of Sec. 32, T. 1, R.1 E., where a flat sheet 
of ore was found on the top of the Brown rock, on which a number of short levels were 
run. Mr. Mills is now engaged in running a level on the top of the Blue limestone 
from the center of Sec. 32, westward, to prove the ground for blende, of which ore small 
quantities have been occasionally found. The Buncome ground is also remarkable as 
being the only locality in which native sulphur appears in sheet form. 

Carpenter & Bennett. These parties are mining on Mr. Mills’ land on the N. E. 
qr. of Sec. 32, T. 1, R. 1 E., on the east side of the Galena river. The workings are as 
usual in the Brown rock, and produce some lead ore and large amounts of carbonate of 
zinc and blende. Exactly how much could not be ascertained.. They“have worked 
continuously since 1872. 

Hicks, Fiddick & Co. Situated on the land of the Edwards estate, on the 8. W. 
qr. of Sec. 29, T. 1, R. 1 E. The diggings are abouta half a mile above the mouth of 
Bull branch, and are also carried on in the Brown rock. They are drained by a level a 
quarter of a mile long, discharging 100 gallons per minute, which was commenced in 
1868. The ore is found in flat and pitching sheets, and sometimes contains a little 
blende mixed with it. Twelve men are now employed here, and are producing a large 
amount of Smithsonite. Since the commencement of operations, about 400,000 pounds 
of lead ore have been produced. 

Gabriel Mills Diggings., This ground is on the N. W. ar. of Sec. 29, T. 1, R.1 E., 
on the ridge dividing Bull and Hard Scrabble branches, and contained the large lode 
mentioned in Prof. Whitney's report of 1862, on pages 285 and 286. The ore was dis- 
covered here in 1854, and has been worked uninterruptedly ever since, which is some- 
what remarkable, as a single range seldom continues uniformly productive through so 
many years. The property isowned by Mr. Mills, and is now being worked by William, 
Thomas and James Mills, and R. Pierce. The deepest shaft is 130 feet down to the 
brown rock, in which the ore is found in flat and pitching sheets. The ore from these 
diggings is always coated with pyrites, and some Smithsonite is found associated with it. 

The ground has produced about eight million pounds of lead ore, their present an- 
nual average production is about 50,000 pounds, with no sign of diminution. 

Simmons & Sons. N. E. qr. of N. W. qr., Sec. 32, T. 1, R.1 E. A very fine 
prospect has recently been discovered by this party on Mr. G. Mills’ land. They com- 
menced work about the Ist of September, 1876, with a horse pump. After sinking a 
shaft 14 feet deep, a flat sheet six inches thick was discovered in the upper pipe-clay 
opening. The sheet consists of lead ore, blende and pyrites, about half of the thickness 
being lead ore. 

There are also several isolated ranges lying between Hazel Green and Benton, and 
not properly belonging to either district. They are as follows: 

; Johns & Harvey. On the N. E. qr. of Sec. 6, T. 1, R.1E. The range was struck 
in 1858, and was worked for some time with an engine and pump, and then abandoned. 
Work was recommenced by Messrs. Johns & Harvey, in 1869, and they are now work- 
ing on the natural water-level, at a depth of one hunlved and ten feet below the sur- 


MINES — HAZEL GREEN DISTRICT. 709 


face, in the middle portion of the Galena limestone. The range bears slightly north of 
west, and makes ore in tumbling openings, mixed with clay and detached masses of 
stone. The opening is, in some places, twenty feet wide, but does not -correspond in 
geological position with any of the Hazel Green openings, as it is rather above them. 
Work was suspended here in the fall of 1874. Their production to that time was 
900,000 pounds of lead ore. 

Dawson’s Diggings are situated on the S. E. qr. of Sec. 32, T.2,R.1E. The 
general course of the range is east and west, but it is found to pitch in various direc- 
tions. They are worked about thirty feet below the surtace, in the upper measures of 
the Galena limestone. They were discovered in 1872. Since then they have been 
worked continuously, and have produced 80,000 pounds. 

Drybone Diggings. 8. W. qr. Sec. 28, T. 2, R. 1 E. Mining for drybone has now 
been carried on here by George Hoppenjohn for the last ten years. The diggings are 
known as the ‘‘ Bone Patch,”’ and are very shallow, not exceeding twelve or fifteen feet 
in depth. The Smithsonite occurs in bunches as float, and does not make in any regu- 
lar sheet or opening. The amount produced is about 50 tons per annum. 

Barney Kesson’s Diggings are situated about a quarter of a mile southwest of the 
preceding, on the same quarter section. Work is suspended on them during the sum- 
mer seasons. They are quite productive diggings and have yielded 50,000 pounds of 
lead ore per annum for several years. 

Anthony & Dixon’s Diggings. 8. E. qr. Sec. 21, T. 2,R.1E. These diggings 
are about a quarter of a mile south of the village of Jenkinsville, and are worked alto- 
gether for blende; although the ore contains a little drybone and lead ore. They are 
on the top of the Blue limestone, on which a level is now being run, and is completed a 
distance of 200 feet. 

The ore is very close-grained, shows no regular cleavage, and somewhat resembles 
an ore of iron. It is remarkable by being intersected with thin parallel plates or lam- 
ine of galenite lying very close together, presenting reflecting edges, and being a con- 
stituent part of the ore. 

The deposit was discovered in 1872, and has been worked continuously since. The 
production has been 180 tons of blende and 10,000 pounds of lead ore per annum. 

Kesting, Hines and others. A short distance southeast of the preceding, on the 
same quarter section, are three parties at work on some dry bone diggings. There are 
here several quartering ranges, having a southwest course. The Smithsonite lies from 
fifteen to sixty-five feet below the surface, and in the lower measures of the Galena 
limestone; it ‘‘makes’’ in flats, sheets and pitches without much regularity. The 
ground has been worked about ten years for drybone. The average annual production 
has been about 225 tons. 

Spensley, Winn & Co. Situated about a quarter of a mile southwest of Meeker 
Grove P.O. The above parties have been working here about five years. The ore is 
found in an irregular flat sheet in the upper pipe-clay opening. This ground has been 
worked at intervals during the last twenty years. The water is removed by a horse 
pump. The production of the last two years is as follows: 1875, blende, 300 tons, lead 
ore, 20,000 pounds; 1876 to Octuber 1st, blende, 400 tons, lead ore, 20,000 pounds. 

Greenwood & Miller. S. E. qr. Sec. 7, T.1,R.1 E. This is an east and west 
range, discovered by Cook, twenty five years since. The present parties became inter- 
ested in it in 1871. Five shafts from 70 to 90 feet deep have now been sunk, and two 
drifts of 300 feet each have been run. The ore is found here in a crevice opening, 
sometimes twelve feet high. The width of the opening is quite variable, as it is crossed 
by numerous north and south crevices, which usually cause it to expana in width. 
Bunches of ore are found at the crossings, but no regularsheets. The water is removed 
from the ground by a two horse pump of 12 inch bore, 6-feet stroke, which pumps about 


710 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


90 gallons per minute. It is estimated that the ground has produced a million pounds 
of ore, and its present annual product is about 300,000 pounds. 


NEW DIGGINGS DISTRICT. 


Considerable lead ore is now being raised in the vicinity of New Diggings, being 
mostly on the ridge immediately south of the village. The following section taken from 
the mines south of the village will give a correct idea of the relative position of the sev- 
eral beds and openings: : 


Ft. In. 
Goil and clay..... cece ces cece eee eee cree cree eree sence enteaes 14 
Galena limestone... seaxsag Peas oda eieders sey seer eee eas ne 60 
Bint bed ivaivowas dcccaracoars, tiers shai renee set Greece many es ara eR esgie es 1 2 
Shalecc.ie site shaw Rit Mh ee nae nad Neos, ates Saas hae Gate eae . 2 
First opening (sometimes called crevice opening)......+.+++++ ssees 5 
Tdmestone Capes cceia kes verve eth ascnes degeen desu a Red socizememnes 2 
Second opening (sometimes called flat opening)... ..--...+.+eese5+ 5 
Plinty T0GK: o..accessus ced kenedeceead ans Wha as demas Case Bde ae s 9 
Third opening (this is the principal flat opening)........-----+--- 4 
Galena limestone «4 ean se seine sstedeang avevads dia Benoa anaes AL os 
“Putty beds acess aaa eia ea neeg eee tees ea es pap ees Hee eee wes ic 3 
Galena limestone. « cisliess ccaw ergs oo edete dace sa ba ane ak Se 1 8 
Fourth Ope@mingys i: x-c0c. ance ceed 0-58 a tea es Sones sk aie a penuh elena Miaracacabedn Subsesee 6 
Galena: limestone ve<is cesg cee Gee eek 's Geis eles sie cine wading idaners wee 50 
Phin Opening ves s sues waeoe esd aiass Haan sae came tuchmudasee shies ceeds 3 
Brown rock to top of Blue limestone......... 0. ec ccc e eee eee eee eee 13 


3 
éB 
[| co | 


Champion Diggings. N. E. qr. Sec. 26, T. 1, R. 1 E., on the New Diggings ridge 
There are several ranges here having a general east and west course, one of which, 
known as Champion's old lode, has probably yielded more than any single range in the 
Lead region. This and the other ranges owned by Mr. Champion are drained by a 
level half a mile long. This was completed in the year 1865, at an expense of about 
seventy thousand dollars. It then drained the ground, and in four years, with the labor 
of eight men, 5,000,000 pounds of ore were taken out, which sold for about $500,000. 
This ore was contamed in an immense opening, in some places forty feet wide by twenty- 
five feet high. This principal opening is now worked out, but the range still continues 
productive, and has been worked uninterruptedly for the last ten years. Average pro- 
duct per year, 85,000 pounds. 

Work is now being carried on south of the old ranges, at the westerm end, in the 
Myers lot; a shaft has been sunk seventy-three feet to the first opening, which is here 
about 10 feet high, and from 20 to 30 feet wide. There are here three parallel crevices, 
one of which is about & feet wide. Seventeen men are now employed in the Champion 
Diggings. Mining is carried on continuously, and the annual product is about 200,000 
pounds. 

Craig Diggings are situated on the New Diggings ridge on the N. E. qr. of See. 
26 and N. W. qr. Sec. 25, T. 1, R.1E. There are here three principal east and west 
ranges, a few feet apart. The one which is now worked is known as the Simpson Pump 
range. These ranges were discovered in 1834. In the spring of 1874, a shaft was sunk 
on one of them, and they are now worked in the second opening. They produce only 
lead ore, found in a flat opening which is 100 feet wide, and has been worked to a length 


MINES— NEW DIGGINGS DISTRICT. 711 


of 150 feet. They ate worked only in the winter; and produce 40,000 pounds per 
annum. 

Craig, Sanders and Campbell. Work was commenced by this party in the fall 
of 1874, on the east end of the Simpson Pump range. The mining is carried on in 
the first opening. The product has been 258,000 pounds, the greater part of which was 
produced this year (1876). The extreme west cnd of this range has been worked by 
Craig, Stephens & White, during the past year, but has not yet produced anything. 

Craig Level Company. A company consisting of several persons residing in New 
Diggings and the adjacent towns, and representing an extensive capital, have been en- 
gaged for several years in running a level on the south side of the New Diggings ridge, 
for the purpose of unwatering the extensive east and west ranges on and near the sum- 
mit of the ridge. It is already so far advanced that it has lowered the water in the 
mine several feet, sufficient to admit of the production of enough lead ore to more than 
defray itsexpenses. Mining is now carried on on Pump range, the Mitchell range, and 
several others; the company are making several ‘‘cosscut drifts" for the purpose of 
prospecting their ground. The following are the principal mining operations now 
(Oct., 1876) in progress here. 

On the ground owned by Mr. Craig there are two men working the level; two men 
working south on a cross cut from the pump shaft range; and two men working a cross 
cut north from the same range. 

On the ground owned by Mr. March are four men working westward, and producing 
lead ore from the pump shaft range, and two men working a cross cut from the same 
range southward. 

On the ground owned by Mr. Bird there are four men prospecting on the eastern part 
of the Mitchell range, and four men working on an opening of that range, raising ore; 
also two parties of three men each prospecting on the east end of the pump shaft range. 

On the Dutch lot-are two men drifting from the Mitchell range southward; two men 
cross cutting from the same range northward; three men working westward on the 
range, and producing ore; two men working a sheet of ore on a north and south range. 

On the ground owned by Craig and Dunlap are three men working an old east and 
west range on the ridge; and three men prospecting and raising ore. 

The mining operations of the Craig Level company have been very productive of lead 
ore. The amounts produced previous to 1874 could not be ascertained. During the 
year 1873 it was 70,000 pounds, and from March, 1874, to October 1, 1876, the product 
was 2,075,470 pounds. 

Brown, Dodge & Co. This party, consisting of four men, have been working on 
the west end of the Mitchell range, on land owned by Col. 8. Scales. The product has 
been 10,400 pounds, ali raised within the last year. 

Harper, Hird & Co. Situated on the New Diggings ridge, a short distance west of 
the Craig diggings, on two east and west ranges, known respectively as the Wiley and 
Engine, on which the water has been reduced about four feet by the Craig level. They 
were quite large ranges, and were extonsively worked many years since. Work was re- 
sumed on them by the above parties in February, 1873. Since then, the product has 
been 303,000 pounds. The crevice of the Engine range is here about three feet wide, 
and the ore makes in the first opening; while on the Wiley range the crevice is ten 
feet wide, and the ore makes in the crevice and not in the opening. The ground is 
owned by Col. Sam. Scales, and four men are employed. 3 

The existence of lead and zinc ore in the upper pipe-clay opening (npper surface of 
the Blue limestone) is also known at New Diggings. A mining company, known as 
the Occidental, was in operation in 1873, by whom a level had been run on this open- 
ing, which resulted in the discovery of a flat sheet of blende ox lead ore. No work has 
‘been done here recently, but the prospect is considered good. 


712 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Catchall Diggings. N.W. qr. Sec. 30, T. 1, R. 2 E. These diggings have in 
former years produced large quantities of ore; exactly how much could not be ascer- 
tained. After lying idle for some years, work was resumed on them in 1870, by 8. and 
C. Vickers, J. and T, Peacock and John Henry. They were worked for a year witha 
horse-pump, and after that with a steam-pump, the former having been insufficient to 
remove the water. There are here two north and south ranges crossed by several east 
and west ranges, which produced blende and lead ore. The pump-shaft is located on 
one of these crossings, and is 48 feet deep. A series of levels was run from here to the 
New Diggings ridge by which it was ascertained that the top of the ridge was on a level 
with the bottom of the shatt; which shows that the openings existing at this place are 
above those at New Diggings, and probably near the middle of the Galena limestone. 
The Catchall diggings ceased being worked in January, 1878. The pump and engine 
still remain on the ground. The product during the three years of working is said to 
have been two million pounds. 

Howe & Alderson. S. E. qr. Sec. 15, T. 1, R. 1 E. This ground is situated a short 
distance north of the Democrat furnace, and belongs to the Leakiey estate. The 
range was discovered and worked about 1847, and work was resumed on it by the pres- 
ent parties about fourteen years since (1862). The general course of the range is east 
and west; the extent of the drifts is from 300 to 400 feet, in the course of which five 
flat openings and one crevice opening have been found. The flat openings are not far 
above the Blue limestone. There are eight shafts going down to the openings, from 30 
to 80 feet deep. The ore is generally small with wash-dirt, but little large or ‘‘ chunk- 
mineral” is found. The diggings are entirely free from water. During the past four- 
teen years they have produced about 1,000,000 pounds. Work was suspended here 
about January 1, 1876. 

John Rain & Co. S. E. qr. Sec. 31, T. 1, R. 1 E. The land is owned by Messrs. 
Hodge & Scales and the Field estate. The course of the range is N. 5° E. It is known 
as the Raspberry range, from the name of the man who discovered it in 1849, and some- 
times as the Dinsell range. The workings are all in the first of the New Diggings 
opening, although the second has also been reached. There are five shafts down to the 
opening, and about 500 feet of drift. The opening is quite variable in size, and is 
sometimes as much as thirty feet wide. The ore occurs as wash-dirt, although large 
pieces are occasionally found. The diggings have been worked for lead ore during the 
last seven years, since which time Messrs. Rain & Co. have taken out as follows: 1871, 
50,000 pounds; 1872, 100,000; 1873, 75,000; 1874, 75,000. The product for 1875-6 was 
not learned, but the mine is now productive. 


Diggings on the Leakley Estate. 


Robbins & Bros. Four men have been employed here during the last year, work- 
ing an east and west range with a horse pump. The amount raised is not known, but 
it is understood that the ground yields enough ore to pay good wages. 

Hall & Rain. §8. E. qr. Sec. 23,T. 1, R.1E. This isa new east and west range 
on the Leakley estate, discovered in 1873. The ore occurs in a crevice opening from 40 
to 45 feet below the surface. Four shafts have been sunk in it, and one drift run a dis- 
tance of 400 feet. About 119,000 pounds have been produced since they were discovered. 
Work was suspended this year (1876). 

E. Ashworth Diggings. 8. E. qr. Sec. 24, T. 1, R.1E. This is an east and west 
range on the Leakley estate, discovered in the fall of 1873. The workings at this place 
are confined by water to the first opening, which is here crossed by numerous quartering 
swithers from four to six feet apart. The crossings are the most productive parts of the 
opening, and the ore frequently comes up to the surface clay. At the time they wero 
visited, June, 1874, five shafts had been sunk about 35 feet decp; one of the drifts was 


MINES —SHULLSBURG DISTRICT. 713 


about 100 feet long, and there were several of 50 feet each. The product to that time 
was 4,000 pounds of lead ore, and fifteen tons of drybone. They have been working 
continuously since, producing small amounts. 

Phoenix Lead Mining and Smelting Co. Sec. 13,T.1,R.1E. <A great deal of 
mining has been carried on here since a very early day, and the ground has been very 
productive of ore. The principal vein, which is known as the Ellis sheet, was discov- 
ered by a miner of that name, about thirty-five years since. Its course is N. 20° E., 
and it has been worked for a distance of about half a mile. The workings so far have 
been confined to the Galena limestone, of which there is a thickness of 150 feet at the 
pump shaft, at the summut of the ridge. This shaft has been sunk toa depth of 115 
feet, leaving thirty-five feet of the formation unexplored, exclusive of the underlying 
Trenton limestones, which have here a thickness of about fifty feet. The sheet of ore 
is nearly perpendicular, and varies from two to eighteen inches in thickness as deep as 
the shafts were sunk. The same system of surface mining obtained here as at other 
places, by means of which the ore was extracted down to the natural water level but a 
short distance below the surface, leaving the main body of ore untouched. In this man- 
ner more than 2,500,000 pounds of lead ore were obtained. In the year 1865 a level 
was commenced with a view to drain the ground, and was prosecuted with slight inter- 
iuission until 1872. Its present length is 1,700 feet, and when completed it will drain the 
ground to a depth of 185 feet. Several other large east and west ranges traverse this 
ground, among which are the Bobineau, and the Dowd & McGinnis, on the W. hf. of 
the 8. E. qr. of Sec. 14, T. 1, R. 1 E., which have yielded heretofore not less than three 
million pounds. 


SHULLSBURG DISTRICT. 


Stopline Diggings. The property is situated on the N. W. qr. of Sec. 28, N. E. qr. 
of Sec. 29 and S. E. qr. of Sec. 20, all in T.1,R.3E. Although the mine is not in 
operation, it is in a condition to be worked on very short notice. 

The following information in regard to it was obtained from the owner, Mr. Edward 
Meloy, and personal inspection of the ground. Nearly if not quite the entire thickness 
of Galena limestone is present at this locality. The northern outcrop of the Cincinnati 
group is found about a mile to the southwest. The pump shaft has been sunk in a 
natural chimney to a depth of 112 feet below the surface, and has now reached what is 
known as the green bed or cap of the Shullsburg openings. The water was removed by 
an engine and lifting pump discharging 500 gallons per minute. All the water came 
up in the shaft through the chimney. While the pump was in operation, two springs 
situated respectively one-half mile east and northwest of the shaft ceased to flow. 
There are two principal ranges here, one bearing N. 30° E. from the pump shaft and 
worked for a distance of 800 feet northeast of the shaft, and the other bearing N. 10° E, 
about 140 feet west of the shaft worked about 500 feet, connected by a quartering range 
running north of east. 

These ranges were struck in 1863, and worked until 1869, and are thought to bea 
continuation of the Shullsburg elevator ranges. ‘l'wo shafts, sunk on the range, bear- 
ing N. 30° E., have turned out 1,000 pounds to the foot without any drifting and the 
whole tract within an area which would be embraced within three acres of ground has 
produced about 600,000 pounds. In every shaft from which ore has been raised, the in- 
dications of large bodies below are very strong, 

A very peculiar formation was found in sinking on the N. 30° E. range. Commenc- 
ing at a depth of 35 feet from the surface, a hard brecciated limestone sets in, filled 
with pyrites, and in some cases with galenite; this formation continues as deep as the 
shafts were sunk. This was not found on other ranges in this locality, and is a mode 
of occurrence peculiar to one range. * 


T14 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


The breccia consists of small, 
Fig. 17. angular pieces of Galena lime- 
stone, similar to the adjacent 
rock of the formation. It ap- 
pears to have been caused by 
the undermining and falling in 
of a portion of the formation, 
by a previous subterranean 
drainage. The rubbing and 
grinding of the sides of the fis- 
sure against each other in the 
course of the movement broke 
off pieces of various sizes, and 
the interstices and cavities were subsequently filled with pyrites. 

McNulty Mine. In June, 1873, work was recommenced on these old ranges, and 
considerable capital expended in erecting new machinery and buildings, the old ones 
having been previously burned. It is now owned and operated by Messrs. J. M. Ryan, 
of Galena, and M. A. Fox, of Shuilsburg. 

The mine is situated on the N. E. qr. of the N. E. qr. of Sec. 15, T. 1, R.2E., a 
short distance south of the village of Shullsburg. There is here a thickness of about 200 
feet of Galena limestone, or four-fifths of the entire formation. The ore is obtained in 
the usual opening common to all the mines of the Shullsburg district, between what are 
known as the green and clay beds, of which the green bed is regarded as the top and 
the clay bed as the bottom of the opening. In this mine the following stratigraphical 
information was obtained: Five feet below the clay bed, and 150 feet below the sur- 
face is an opening, and a bed of white rock two feet thick, then a layer of hard gray 
rock three feet. Below this was found a flat sheet of galenite, mixed with pyrites, and 
indications of an opening below. It is a peculiarity of the mining ground on this ridge, 
that all crevices south of the Shullsburg branch pitch or dip to the south, about six 
inches in ten feet, until the summit of the ridge is reached. Here, as in the south shaft 
of the McNulty, the crevices are vertical. In this shaft the crevice penetrates through 
the clay floor, and continues on going down, being the only crevice which has done so. 
Proceeding further south, over the crest of the ridge, the crevices all dip or pitch to the 
north. Taken together, this system of crevices seems to present a fan-like shape, ap- 
proaching one another as they descend. In the spring of 1876, a new east and west 
range was discovered in this mine, south of and parallel to the one already worked. 
It promises to be very productive of lead ore. The production of this mine from June 
1, 1875, to March 1, 1876, is as follows: 173, 200,000 pounds; 1874, 150,000 pounds; 
1875, 75,00 pounds; 1876, 210,000 pounds. 

Rickert, Stevens & Co. These diggings are situated on the N. W. qr. of the N. W. 
qr. of Sec. 14, about 500 feet east of the McNulty mine, and connected with it. Their 
geological position in respect to strata and openings are almost the same. The ore is 
found in the usual Shullsburg opening, but in a few instances it runs above it for a short 
distance, and then drops down again, presenting a saddle-shaped appearance. At the 
south shaft the rock is very much disturbed and broken, apparently in an area of about 
200 feet in diameter. It is in loose masses of all sizes and shapes, containing more or 
less ore scattered through it, and the fine earthy material known among the miners as 
sand. The strata pitch in every conceivalle direction and degree, from horizontal to 
vertical, crevices and veins cannot be followed through it with any degree of certainty; 
but at the borders of this disturbed area, as well as above and below it, the strata have 
their normal position, which is nearly horizontal. This is merely a local disturbance, 
and is probably due to the unequal hardness and solubility of the formation. Consider- 


VEIN-STONH Breccta, STOPLINE Diceines. 


MINES — SHULLSBURG DISTRICT. 15 


able of the limestone seems to have been removed by currents of water running through 
the opening, thus permitting large and small irregular masses to fall from above, and 
filling the interstices with the fine insoluble residuum of sand. 

Tn connection with this regularity was noticed a remarkable * ‘chimney ”’ about 36 
feet long by 20 feet broad, and extending upward further than has yet been followed. 

It was originally filled with loose masses of galenite rock and sand. In the ground 
on this ridge the strata dip on both sides toward the north and south line between Secs. 
14 and 15, on the west side about four feet in a quarter of a mile, and on the east side 
one foot in thirty rods. The ground is drained by a horse-pump into a level a short 
distance below the surface. The mine produces very handsome cabinet specimens of 
galenite and calcite, in the form of dog-tooth spar. 

The following section will serve to convey a general idea of the arrangement of the 
strata on this ridge: 


NOU and Clays: oi dais aiawinne men weetene cadcia ob 4 oedeedee 6 to 10 feet 
Galena Lmestone. ...... 00. ccc ccc c cece ee cee ee tessa eaeeeenee 100‘ 
Hit; DEQ: Sais scismiew ie aoainasedepad adn cioas aca denen Samauaegy 4to 8 * 
Green bed to clay bed, including the opening..............6005 14to1l8 “ 
Galena, limestone to top of Blue limestone...........0.eceeeaee 65 * 
Total average thickness..........-.6. cece eee ceereeeeee eee 195‘ 


This may be compared with the section taken at New Diggings, and given on page 
710 of this report. Reckoning upwards from the top of the Blue limestone to the top of 
the green bed, or cap of the Shullsburg opening, the distance is found to be about 80 
feet, and in the New Diggings section, from the top of the Blue limestone section to 
the top of the flmty rock, which is the cap of the third or main opening, the distance is 
82 feet. 

This establishes an identity of geological position of these two points. Measuring 
downward from the cap in the Shullsburg opening, its average distance is found to be 
sixteen feet to the bottom of the opening. In the New Diggings section the same dis- 
tance includes all that lies between the top of the third and bottom of the fourth open- 
ing, and finally each is underlaid by about the same thickness of unproductive rock. 
The correspondence between these openings is thus very distinctly marked. The un- 
productive beds in the New Diggings openings seem to disappear on going eastward, 
and finally the openings unite on reaching Shullsburg. 

In regard to the production of these diggings, it is estimated that the 8. hf. of Sec. 10, 
and the N. W. qr. of the N. W. qr. of Sec. 14, being an area of one mile long on a 


-course 8. 70° E., and three-quarters of a mile wide, including the McNulty and Rick- 


ert’s diggings, have produced since the commencement of mining operations not less 
than 100,000,000 pounds. 

The preceding information in regard to the mine of Rickert, Stephens & Co. was ob- 
tained at the time I examined them in June, 1873. Since then I have recently received 
the following information concerning them from Mr. John KE. Hoover, of Shullsburg, to 
whom I am also indebted for valuable information relative to the Irish Diggings and 
the McNulty mine: 

“The bearing of the crevice on which we (Rickert, Stephens & Co.) are now working 
is due east and west. The mineral is found about 12 feet below the green bed or cap, 
and is mixed with sulphur (pyrites). The rock is different from any before taken out of 
the-mines in this section. It is a dark blue, and mixed with sulphur and flint, and is 
very hard. In the opening there is copper rust or verdigris mixed with large balls of 
sulphur. Dog-tooth spar or tiff is also found in Jarge quantities, most of which is 


attached to the mineral. 


716 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


“The company commenced work in 1849, and on the present range in May, 1874. 
They are now operating a steam pump on what is supposed to be a continuation of the 
South digging range. The product trom June 1, 1873, to March 1, 1876, is as follows: 
1873, 377,120 pounds; 1874, 201,966 pounds; 1875, 318,690 pounds; 1876, 153,720 
pounds.” 

Silverthorn Mine. N. W. qr. Sec. 32, N. E. qr. Sec. 31, T. 2, R. 2H. The great- 
est thickness of Galena limestone found on the ridge was about one hundred feet. The 
ground is drained by a level run in the carbonaceous shale, on the top of the Blue 
limestone, which has here a very great thickness, being nowhere less than two feet, and 
in some places seven and a half feet thick. It seems in this mine to replace the pipe- 
clay opening. Itis very easy to work, and consequently this level has been compara- 
tively inexpensive. This shale, when dried, burns with a bright yellow flame and much 
smoke until the carbon is exhausted, but owing to the amount of calcareous matter it 
contains, it is not much reduced in bulk. These diggings produced in 1871, 200,000 
pounds, and in 1872, about 100,000 pounds. Their product in previous years could not 
be ascertained. Work was suspended on them in 1875. An analysis of lead ore from 
the Silverthorn mine gave the following results: Lead sulphide, 97.06; metallic lead, 
84.07; insoluble silicious residuum, 1.76. 

Dry Bone Diggings. Situated on the 8. W. qr. of the 8. E. qr. and the 8. E. qr. 
of the 8. W. qr. of Sec. 4, T. 1, R. 2 E. The ranges here run in nearly an east and 
west direction. The diggings are situated in the lower strata of the Galena limestone; 
the top of the Blue limestone is found a short distance down the stream. Although 
shallow, these diggings have been very productive of zinc ore, and are still successfully 
worked. ’ . 

Irish Diggings. Sec. 2,T.1,R.2 E. These diggings have not been worked for 
many years on account of water, but were formerly very productive and were abandoned 
with ore going down in the crevices. The greatest thickness of Galena limestone on 
this ground is about 150 feet. They could be readily unwatered by means of a level 
from some point on the Shullsburg branch. 

Meloy and Fox. In the early part of the year 1875, that part of the Irish Diggings 
known as the Findley Cave range was leased by Messrs. E. Meloy and M. A. Fox, of 
Shullsburg. It is situated on the N. E. qr. of Sec. 2, T. 1, R. 2 E., and comprises 99 
acres of land, lying about a mile northeast of the village. The range was worked du- 
ring the months of April, May and June, 1875, and in November of that year a steam 
engine and pump were erected, and it has been worked continuously to the present time 
(November, 1876). The pump shaft is now about 80 feet deep. Water is discharged 
into an adit connecting with the shaft at 20 feet below the surface, at the rate of 150 
gallons per minute. The course of the vein is N. 7° E., having a dip to the eastward 
of four feet in one hundred. The distance between the walls of the vein or crevice va- 
ries from two and a halt to seven fect, the space between them being filled with the 
vein matrix common to this neighborhood. The bottom of the pump shaft is six feet 
below the top of the flint beds (see section on page 715). The vein appears to continue 
downwards, the filling of the crevice being loose and allowing the water to pass readily 
through it. 

After sinking the pump shaft, the vein was drifted in, a distance of 60 feet to the 
northward; in the course of running this drift, 100,000 pounds of ore were extracted. 

The foregoing remarks show the condition of the mine in March, 1876. The produc- 
tion since then we have not learned. 

This range was workcd more than 30 years since, with a two-horse pump, as deep as 
water would permit, and large quantities of lead ore were obtained. These diggings 
could be unwatered to a much greater depth by means of a level from some point on the 
Shullsburg Branch. 


MINES — BENTON DISTICT. 717 


Bull Pump Range. Work is still carried on, on this range, which is situated on the 
Hempstead estate. It is operated by Messrs. Beebe, of Galena, and Wetherbee, of: 
Shullsburg. The amounts produced could not be ascertained. . 

Oakland Mining Co. The lands of this company are situated in the S. E. qr. of 
Sec. 6, the N. E. qr. of Sec. 5, the N. W. qr. of Sec. 4, and the 8. E. qr. of Sec. 4, all 
in T. 1, R. 2 E., comprising in all about 565 acres. 

This ground includes the old French range, which was discovered as early as 1839, and 
produced not less than 1.000,000 pounds. It is connected northward by some quartering 
crevices, and is known as the Earnest anct Townsend range. 

The thickness of Galena limestone here is about 170 feet. There are six shafts on the 
range, averaging about 50 feet each. The lead ore is abundant, but dips rapidly to the 
northwest beneath the water. The range has produced about 400,000 pounds. 

The ground is susceptible of drainage from the Shullsburg branch. It is not worked 
at present. 

The company also has a level nearly completed in the S. E. qr. of Sec. 4, which is 
run on the stratum of carbonaceous shale, or the top of the Blue limestone. At the 
working shaft there is a thickness of 90 feet of Galena limestone, of which the follow- 
ing section is given: 


Feet 
Clay and): SOs osueisls dus aguinnehs Vea Gia yea Genesee eck Res 18 
Yellow flinty limestone sasceccccae saver necseeebaee vag Gherwedeseoees 16 
Galena limestone containing calcite .... 00.600. e eee e eee e eee eee eee 20 
Blue sandy limestone cap....... sees ese e cece eee ence cee pete eee ee eee 6 
Red ochery clay with lead ore in flat sheets at top and bottom, also dif- 
fused through the mass forming wash-dirt.........+. sess e eee eeeee 12 
Tnexploted GAdEs + <a, «sec cnbsslsacneawanenan allasecy saseseehsereteens 18 
Total thickness...c.i vacudenscewiwad aeebeeo ner eases “Reve y er Oo oeee 90 


Considerable mining has been done in former years in the Blue sandy limestone mem- 
ber of the section, but the main opening appears to be in the red-ochery clay which un- 
derlies it, which, so far as explored, has been found to have a thickness of about twelve 
feet. and to contain a flat sheet of galenite nearly continuous, and of variable thickness, 
sometimes furnishing pieces of 500 pounds weight. 

The bearing of the sheet, so far as has been determined, is west of north and east of 
south, with a slight dip to the: southwest. Its area has not been determined, but so far 
as has been worked there are no indications of the opening, contracting or closing up. 


BENTON DISTRICT. 


In the immediate vicinity of the village of Benton, there are several parties perma- 
nently engaged in mining, besides others who mine only in the winter. The diggings 
are in the lower beds of the Galena limestone, yet not so low as the brown rock. 

The mode of occurrence of the openings in this vicinity is quite remarkable, and is as 
follows: There are numerous well defined north and south and east and west crevices, 
which are followed down with shafts until the random of the openings is reached. At 
this point, instead of the crevice leading into and being connected with the openings, as 
1s usually the case, the crevice usually closes up, and it is necessary to drift at right an- 
ules with the crevice for a distance of from ten to fifteen feet on each side, where the 
openings are usually found. The annexed diagram illustrates the relative position of 
the openings. A represents the vertical crevice on which the shatts are sunk. The dis: , 
tance from the surface to the top of the first opening is from five to fifty feet, according 
to the amount of denudation of the ground. BB represents the first opening, which is 


718 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


a flat flint opening four feet high. C C represents the second, which is also a flat flint 
opening, four feet high. D D represents the third, which is not a flint opening. lt 
is about four feet high, 
similarto Band C. The 
distance between the first 
and second openings is 
four feet of unproduc- 
tive cap rock; between 
the second and third, 
ten feet of similar rock. 
The openings are about 
fifteen feet wide, and 
sometimes as much as 
four hundred feet long. 

Having described the 
position and mode of oc- 
currence of the ore, the 
different diggings now 
in operation will be de- 
scribed. 

Bainbridge & Vip- 
ord. S. E. qr. Sec. 8, 
T. 1, R.1 E. This 1s 
an cast and west range 
somewhat near a mile long, which was worked about twenty-two years since and 
abandoned. Prior to 1854, it produced about one and a half million pounds. About 
seven years since some work was done on it, and one million pounds were produced. 
Work was recommenced on the eastern end by the present parties in February, 1874, 
and has continued to the present time (November, 1876). The annual product is about 
20,000 pounds. During the’ last year anda half they have been worked with a horse 
pump. 

Bainbridge, Mundy & Maighn. This is a quartering southwest and northeast 
range, about 100 yards north of the preceding. This range was never worked previous 
to March, 1874: It is now worked only in the winter seasons. It has produced in all 
about 50,090 pounds. The ore in these diggings and the preceding is found in openings 
detached from the main crevice. . 

Metcalf, Harker & Alexander. N. W. qr. Sec. 9, T. 1, R. 1H. This ground is 
situated on what is known as the Swindler mdge. It derived its name from the custom 
which formerly existed among the miners of cutting through and breaking into each 
other’s ground to steal the ore, which the complicated nature of the openings enabled 
them to do. This range was struck in 1871, and has been worked continuously ever 
since. The depth to the top of the first opening is fifty feet at this shaft, and on the 
ridge generally, although the opening is said to dip slightly to the west. Some water 
is encountered on the ridge, and the present parties have found it necessary to work a 
two-horse pump. The production to November 1, 1876 has been 600,000 pounds. 

Bainbridge Diggings. Situated on the EK. hf. of the N. E. qr. of Sec. 4, T. 1, R. 
1E. Work was commenced here by Mr. Thomas Bainbridge, of Benton, in the winter 
of 1874. In May, 1875, an irregular deposit of lead and zinc ore was discovered about 
fifty feet below the surface, having a course a little west of south. Three men are 
usually employed. Its production has been 25 tons of Smithsonite and 25,000 pounds 
of lead ore. 

Harvey’s Diggings. Situated on the same ground, and about 250 yards northwest 


SucorioN oF THE BENTON OPENING. 


MINES ~PLATTEVILLE DISTRICT. 719 


of the preceding. Work was begun here in the winter of 1875-6, and a large flat 
sheet of Smithsonite was discovered, which has been worked over 200 feet in diameter 
without reaching unproductive ground. It is found about 50 feet below the surface in 
the random or horizon of the flat flint openings. The ore is found in flat sheets inter- 
stratified with the formation. One hundred tons have been produced. 

McElroy Bros. Situated half a mile south of the village of Benton. This is a 
new discovery, made in the winter of 1875-6. An irregular flat sheet of Smithsonite 
was found at a depth of 50 feet below the surface, from which in two months, 15 
tons of ore were produced. Work was then discontinued during the summer. The 
above parties intend to work it again in the winter. 

M. J. Williams & Co. Situated on the 8. W. qr. of the 8S. W. qr. of Sec. 3, T. 1, 
R.1E. A large flat sheet of lead ore and blende, about one foot thick, was discovered 
in July, 1876, in the bed of Fever river, soon after a heavy flood which took place at 
that time. It lies on the upper surface of the Biue limestone, and on account of its sit- 
uation in the river, but little has been done with it. It is an excellent prospect, and 
will doubtless be remunerative, as soon as the water can be removed. 

McCaffery, Smith & Co. In the middle of October, 1876, these parties commenced 
work, sinking a shaft on the west line of the forty of M. J. Williams & Co. They found 
the same sheet of ore as there described. In the space of two weeks they had developed 
a fine prospect, and had produced about one ton of ore. 

Level Company. On the N. W, qv. of Sec. 29, T. 1, R. 1 E., a level is now being 
run by Messrs. Steves, Mason, Miller. Robbins, Broderick, Hoover, Thompson, Coltman 
and Farley, who own and have leased one hundred and thirty-iive acres m Secs. 20, 21, 
28 and 29. The level was commenced in the spring of 1870, and has now reached a 
length of one thousand feet. It is being driven on a flint opening near the top of the 
Brownrock, which is here about fourteen feet above the Blue limestone. 

The object of driving the level is to unwater the Drummond range, which runs east 
and west, and is supposed to be a continuation of the Craw range of Hazel Green, and 
the Nagle range of New Diggings. It is believed that when the level is completed it 
will wnwater the Drummond range toa depth of iorty feet below the present water 
level. 

The level now gives access to two openings in working it, and had, when visited, an 
inch sheet of lead ore in the working forehead. It may be remarked that these open- 
ings are lower than any of the Benton openings, and seem to be identical with those of 
the Buncome district. The product has been up to the present time 60,000 pounds. 


PLATTEVILLE DISTRICT. 


The diggings of the Platteville district comprise those situated in the immediate vi- 
cinity of the village, the Whig diggings and the Big Patch diggings. The mines near 
Platteville are all included in Secs. 9, 10, 14 and 15; and of these, the ones chiefly worked 
are situated on Secs. 9 and 10, a short.distance north of the village. The diggings here 
are very shallow; the deepest shatts are seldom more than thirty feet. The ore occurs 
in bunches, pockets and small openings in the clay crevices, and often comes up to the 
surface. Their geological position is about the middle of the Galena limestone. There 
are no large companies at work in this district, all the mining being done by parties of 
There are quite a large number of such parties, who form the ag- 


two or three persons. 
A tew of the more prominent are here given, and 


gregate production of the district. ° 
their annual production as nearly as could be ascertained. 


Stevens & PO Werd s sypulas caida ye eee iedeasadts a Ibs. 
ot) | F 
Lane & Law at 


Wales & Rowe...-.ceccece eee te cree settee ners eee e entrees 


720 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


C. Cornelius, Jr... . ccc cee cece een eee ene es * 8,000 Ibs. 
Thompson, Phillips & Colt.........--+- 200s erect eee eee eeees 12,000 ‘* 
Wom. Johnson... 0.2.0.0 0 ccc eee eee eens Lenten dete eee es 5,009‘ 
Burns & Conley... 00.00.00 ee eee cece eee eee eee teens 100,000 ‘ 
Sheppard 0.2.6... 6... cece eee ence eter een e eens 12,000‘ 
Leonard Coates. 0.0... cc ccc ce cee e ee n ee ene tenet enene 15,000 ‘* 
Carlyle, Hendershot & Co,..... 0.6.0 cee ee erence eee e eee e es 30,000 
Other sources in small lots......---.6- cee eee eet e eee ee 63,000 ‘* 
Motels: waeg a mwa donaes py Gow es Fem a Roh wiateemubavemtinghd ees acs 395,000 lbs. 


As most of the mining is done in the winter, none of the above mentioned firms were 
engaged in mining at the time the district was visited, and we are unable to give a de- 
tailed description of the several mines. 


Whig Diggings. 

This 1s a small group of east and west ranges in the 8. W. qr. of Sec. 7, T. 3, R..1 
W., on the ridge, on the west side of the Platte river, which properly belongs to the 
Platteville district. More orless mining is done here during all the year. The tollow- 
ing informatiou concerning them was obtained from parties now at work there. The 
diggings are all in the upper beds of the Galena limestone. The principal ranges are as 
follows: 

Gillis Range. This is the longest and largest range in the Whig diggings, being 
half a mile in length. The shafts are sunk on it from thirty to fifty feet deep, where a 
crevice opening from three to five feet high is found. There are from three to seven 
parallel crevices, which were discovered in 1839. Their total product since then has 
been about five million pounds. The present annual product is 15,000 pounds. 

Robbins Range. Situated a short distance north of the Gillis, It was struck in 
1840, and produced 500,000 pounds. Work was suspended on it, and resumed in 1866 
by Cronin & Stevens, who raised about 300,000 pounds. Less work is now done on it 
than on any of the others. : 

Duncan Range. Situated 150 yards south of the Gillis. It is a little more than a 
quarter of a mile in length. There are here two parallel crevices, and one opening 
which is from six to twenty feet high, and from five to forty feet below the surface, ac- 
cording to the contour of the ground. It is very hard ground to work, as everything 
has to be timbered. It still produces a little lead ore and a little Smithsonite, exactly 
how much could not be ascertained. The total product of the range is said to have 
been one and a half million pounds. 

The relative position of the openings here is as follows: 


Feet 
Hirst openings Aoag aise, 4s Saws Vee ariiulel se Peewieigs Mependen abe wiie anaes 6 
Uniproductivéroekirecawsias aca geretarslseanis ire Padisaatinees waned tear tans 9 
Second opening.......---...0.005 wi lesen Since avai daiy Sahwve Wobsehonaiisdodirineanichars steaming 8 
TAMeStONE CAPGins cherwiav anion wie talgumeunn demeaning eee Gaedued aeacke 9 


Third opening, height not known. 


Messersmith Range. This range is situated a short distance south of the Duncan, 
is about a quarter of a mile long, and has but one principal crevice. It is from five 
to thirty-five feet to the top of the opening; which is from five to ten feet high. The 
range is now worked out for lead ore, but still produces a small amount of Smithsonite. 

Missouri Range. Some work is done on this range at all times. It is situated a 
short distance south of the preceding, and is about a quarter of a mile long. It has one 
crevice, and an opening which is about seven feet high. It has produced 650,000 
pounds since it was discovered; and its annual yield is about 5,000 pounds. 


MINES — MIFFLIN DISTRICT. 21, 


Dutch Range. The range was discovered in 1840, and has been worked nearly 
every year since. It is a quarter of a mile long. The ore is found in bunches mixed 
with blue clay, in the first opening, which is from fifteen to thirty-fiye feet below the 
surface. No ore is found in the lower openings. It has produced in all 200,000 pounds, 
and its present annual average is 5,000 pounds. 

Wilkinson and Cronin Range is a quarter of a mile long, and was discovered in 
1868. The ore is found partly in the first, and partly in the second openings, which are 
here eight feet apart. It is from five to thirty feet from the surface.to the top of the 
first opening. There are here two ranges which have produced 300,000 pounds, and 
the range is now nearly worked out. 

Smith Range. This differs from any of the Whig ranges before mentioned, in hay- 
ing its cowse north and south, instead of east and west. The range is about an eighth 
of a mile long, and the distance from the surface to the top of the opening is from ten 
to sixty feet. The sheet was from one to four inches thick, and was worked in one 
place down to the Blue limestone. The principal bodies of ore were found in the Brown 
rock opening, which is much lower than the general run of openings at these diggings. 
The range is said to have produced 200,000 pounds, and is now worked out. 


Big Patch Diggings. 
The greater part of this group of diggings is situated in section 10, T. 2, R. 1 W. 


The general course of the range is N. 65° West. The ore is found here in crevice open- 
ings, and usually in the first opening. The following parties are now mining here: 


Dixon & Coats produced since February, 1876 .........-++.++0+ 400,000 ibs. 
Casper Linden produced since March, 1876.....-.-.++-+-+++05- 25,000 “* 
Tupper & Trowbridge produced during August, September, and 

October, 1876 ..... cc. cece cece cece eee tenet teen ee et ee eee 12,000 ‘ 
Peacock & Co., annual product -...----- 0s cece eee erence eens 18,000 “‘ 
Todd & Co., annual product..... 6.0... cece rece ee eet e eee e ences 10,000 ‘“ 
Haverness & Co., annual product ..... 66... cece een eee eee 15,000 “ 
Spink & Co., annual product ....-.. 6.0 e sees ee rete eee tenes 20,000 ‘ 


Hawkins, Thomas & Co. 8. W. ar. of Sec. 31, T.3,R.1/W. This is a discovery 
of the year 1872. The ore is blende, somewhat mixed with rock, and occurs in a flat 
sheet on the upper surface of the Blue limestone. The sheet has in some places a thick- 
ness of five feet; it lies in the bed of a small stream, and a level to drain it is partially 
completed. About 27 tons of ore have been produced. 


MIFFLIN DISTRICT. 


Mining operations heie are now chiefly confined to several parallel ranges, having a 
general northwesterly course, and situated about half a mile south of the village, in- 
cluding the Penitentiary, Dunbar and Owens ranges. The ore is found in flat sheets on 
the surface of the Blue limestone, in the pipe-clay opening. Some mining is also done 
on Sec. 10, T. 4, R. 1 E., in the vicinity of the Welsh settlement. ; 

Penitentiary Mine. 5S. W. ar. of N. E. qr. Sec. 34, T. 5, R. 1 EL This property is 
owned by Messrs. James, John and Calvert Spensley, Wm. Bainbridge, J. ad. Ross, 
Mrs. Mitchell and N. W. Dean. The mine was opened in 1842, and since then it has 
been very productive, and has been worked continuously to the present time. The mine 
is drained by a level containing a tramway on which the rock and ore are carried out of 
the mine. Sufficient water is removed to operate a large wash place. The distance 
from the entrance of the mine to the forehead is about 1,700 feet. The average width 
of the range is about 300 feet, and the thickness of the deposit from six inches to two 


Wis. Sur. —46 


729, GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


fect. Fifteen men are now employed here, the average being about twelve. Previous 
to 1864, the mine was worked chiefly for lead ore, producing in some years as much as 
170,000 pounds. It is estimated by Mr. Ross that it produced from 1862 to 1875, 
3,000,000 pounds of lead ore and 11,000 tons of blende. The production for 1875 was, 
blende, 375 tons; lead ore, 35,000 pounds. The production for 1876 was, blende, 600 tons; 
lead ore, 40,000 pounds. 

Jenkins, Miller & Co. These parties have been working during the last two and a 
half years on the Dunbar range, which is parallel to the Penitentiary, and a short dis- 
tance north of it. The land is owned by Messrs. Ross & Dean. This range has been 
worked during the last thirty years, and is drained by the Penitentiary level; the pres- 
ent workings are about 50 feet below the surface. The company produced during the 
year 1876, to October Ist, blende, 80 tons, lead ore, $8,000 pounds. Their annual average 
is blende, 80 tons, lead ore, 12,000 pounds. 

Rain, Young & Jenkins. These parties are now working on the Blades range, 
which is adjacent to the Dunbar, and sometimes connects with it. The present works 
are 50 fect below the surface. The ore is found in flat sheets, sometimes 70 feet in 
wlth, in the pipe clay opening, the height of the opening averaging five feet. The 
annual production is from 150 to 200 tons of blende, and from 10,000 to 15,000 pounds 
of lead ore. 

A short distance northeast of the Blackjack is the Owens range. It has not been 
worked during the last two years, but is considered good mining ground. 


CENTERVILLE DISTRICT. 


These diggings are like those in the village of Highland, in that they are alt situated 
quite close together, on Sec. 7, T. 6, R. 1 E., on the hill about a quarter of a mile east 
of the village. 

The land is all owned by Messrs. Top, Norndorf & Kroll. The miners are nearly all 
Germans, from whom the following information was extracted: 

The diggings were first worked in 1836, and have been worked continuously ever 
since, chiefly for lead ore, until within the last ten years, since which time they havo 
been worked for zinc ores. The workings are in the Brown-rock opening, and lie from 
five to fifty feet below the surface, depending on the amount of denudation. Very little 
trouble is experienced from water, and during the past two years the ground has been 
especially dry. The principal parties working here are as follows: 

Heller and Parish. These parties are working a southeast and northwest range, 
1,200 feet long and 600 feet wide. Their annual product is: Lead ore, 100,000 pounds; 
blende, 500 tons; Smithsonite, 400 tons. 

John Carter and Richard Samuels. On the same range as the preceding. They 
have worked here two years, and are producing 200 tons of Smithsonite and 5,000 
pounds of lead ore per annum. Other parties and their annual products are as follows: 

Schock and Flemmer. Blende, 200 tons per annum. 

Stepper and Mensing. Blende, 100 tons per annum. 

George Wieble. Blende, 200 tous; lead ore, 15,000 pounds. 


Blue River Paint Works. 


Situated on the 8. W. qr. of Sec. 7, T. 6, R.1E. At the time this establishment 
was visited, work had been suspended, and consequently did not appear in as flattering 
a light as its merits would probably justify. The building and machinery was still 
standing, in a condition to resume work without delay. 

According to the best information obtained, the paint was made from the ocher which 
is quite abundant in the Centreville diggings, and which furnishes quite a number of 
shades of yellow in its raw state, and an additional number on being bumed. The red 


MINES— HIGHLAND DISTRICT. 723 


paint, however, was derived from the upper bed of the St. Peters sandstone, which was 
crushed and washed; the red coloring matter being readily dissolved out by the water, 
from which it afterwards settled on being allowed to stand. The colors after being 
burned and ground were ready for the market. As many as fifteen different shades of 
red and yellow were manufactured. Several tons of paint were placed in market, and 
it was claimed to be a good and durable article. It is unfortunate that the manufacture 
could not have continued longer, and its qualities been more definitely ascertained and 
generally known. 


HIGHLAND DISTRICT. 


The diggings of the Highland district are all situated within a short distance of each 
other, and about a quarter of a mile north of the village. They are all in the Brown 
rock, the lower openings never have been proved. Most of the diggings are on what is 
known as the Drybone Hollow range. The names of parties mining, and the present 
condition of their diggings, are as follows: 

Samuel Hinderleiter & Sons. On the 8. W. qr. of Sec. 28, T. 7, R. 1 E., on the 
Drybone Hollow range. Thisis an east and west range from one-quarter to one-half 
mile long, and from two to three hundred feet wide. It was discovered in 1846, and 
worked entirely for lead ore. It is now divided into small lots of which Mr. Hinderlei- 
ter’s isone. The work is chiefly confined to going through the old diggings and taking 
out the Smithsonite left by former miners, no blende being found. The shafts are 
about twenty-five feet deep, which brings them to the top opening, three feet in height. 
The ore is found in a flat sheet, about a foot thick, with ocher and clay above‘ and be- 
low it. But little water is found here. The annual product of this lot is about thirty 
tons of Smithsonite. 

Mulligan & Francis. These parties have diggings in all respects similar to those 
already described, on a lot about 150 feet northwest of the preceding. 

Maguire, Kennedy & Co. S. E. qr. Sec. 28, T. 7, RB. 1 E, This is also on the Dry- 
bone Hollow range. The shafts here are from sixty to seventy-five feet deep, according 
to the surface of the ground. The workings are in the Brown-rock opening, which is 
here about eight feet high. The lead ore is found in a flat sheet in the bottom of the 
opening, underlaid by pipe clay. 

The blende was discovered in the spring of 1874, and is much mixed with rock. The 
ore has to be crushed, washed and separated. Water is removed from the diggings by 
means of a windmill and small pump, and is afterwards utilized to wash ore. The an- 
nual product is as follows: Lead ore, 200 pounds; blende, 100 tons: drybone 50 tons. 

Blackney, Donahue & Co. This ground is owned by Dr. Stanley of Highland, and 
is a part of the same range as the preceding, and situated but a short distance north- 
east of them. The range here makes two well-defined openings separated by a cap- 
rock. It is irregular in shape, and about sixty or seventy feet wide, with little water. 

The following is a section of their principal shaft. 


Feet, 
Galena limestone .. 0... cece eee cece teen ence eee eteeter es ereeennee 60 
First opening ..e.ecrecereeecree cece e escent eect erence nenetee nes 9 
Cap rock ..ce see ee ee ee eee te ee ee etree een eere tenses teeters e eens tes 2 
Second opening 1... sseeeeeeeeee tees e etree ee nent en ne et tee eee e es 4 


The ore is found in flat sheets, and is Smithsonite, blende, and lead, the former being 
rather impure. The present parties have been working here for the last seven years. 
The annual product has been as follows: Lead ore, 11,000 pounds; Smithsonite, 35 tons; 
blende, 35 tons. The ground here seems to be pretty much worked out, the product 


being chiefly derived from the old workings. 


{24 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Spensley & Co. This is also on the land of Dr. Stanley, and is a short distance east 
of the preceding. It is an east and west range, situated a little north of the Drybone 
Hollow range. The range is 130 feet wide, so far as has been worked, and may prove 
to be 200 feet in width each way from the center. The ore makes in pitches, and the 
sheet varies in size according to the number of feeders coming in from above. The lead 
ore occurs much mixed with rock, which necessitates crushing and jigging the entire 
product. 

The lot worked by these parties consists of about six acres, of which only about one- 
sixth has been explored. ‘The ore is blende and lead ore; some Smithsonite is said to 
be found in the north and northwest portions of the ground, while the blende is found 
in the southern part. The amount of water here is small, and is all removed by bail- 
ing, and hoisting in a barrel containing about 50 gallons. 

Three shafts have have been sunk, one of which is down to the Blue limestone, and 


is 100 feet deep 
The company have operated here for six years, with the following product: 


Blende. Lead ore. 
Year. tons. lbs. 
Tera aehddaittec abies Sar elma itulan sa tenet baile 70 60,000 
TTD: iincntioavowacnentetanamanegaer nena penlneen cians 150 120,000 
1873. .... Pec lenath sa hatha hist os Aa eia Ae cap hea hedge 350 150,000 
TST ccccsuasuslensisha suey aiden ntoaiea re ARE eke ad Ra Gae ke aaaNs 250 160,000 
TST Bnd saaeree Petes rds 8 aE AR Gunes Alaa heme Ar aToesietD Sa 300 257,000 ° 
AST Bcc excites Saaaitciarss Seba. sence nate nas enatine Aleve eis aeebes 325 300,000 


Siddel & Co. They are situated on the same range, worked in the same opening as 
Spensley & Co., and are located about 150 feet east of them. They are the most east- 
erly of all the diggings in this vicinity. One shaft has been sunk, and the ore has been 
found to make in the same manner as the preceding, except that this ground already 
furmshes' some Smithsonite from the north side. These parties have been working here 
for the last five years, during which time the average annual product has been as fol- 
lows: Lead ore, 70,000 lbs.; Smithsonite, 85 tons; blende, 70 tons. 

Flynn, Lynch & Co. On Dr. Stanley's ground, and about 300 feet southeast of 
Spensley & Co. Their ground is a lot 250 by 350 feet. One shaft has been sunk here 
80 teet to the top of the opening, which is here 6 feet high and 100 feet wide. The 
ground produces lead ore and blende, occurring in a flat sheet, mixed with the top layer 
of the Blue limestone and some pipe clay. The company has been working about five 
years, since which time, to October, 1874, they have produced 250,000 lbs. of lead ore 
and 700 tons of blende. 

Robinson's Diggings. Situated about 300 feet southeast of the preceding, on the 
ground of Mr. Barnard. These diggings are not being worked at present. They were 
commenced in the winter of 1871-2, and produced 4,500 Ibs. of lead ore and about 9 
tons of blende in the first two years. 

Williams & Edwards. Situated on the land of Mr. Lampe and about 500 feet 
west of the diggings of Blackney & Co., previously described. They are part of the 
Spensley and Lynch range. 

The works are in the Brown-rock, which here appears to divide into three subordinate 
openings. A section of their working shaft is as follows, all in the Galena limestone: 


Galena: Himestone saccade enna aus weae euace a. elewiilsleaed bance k Mise ei ao 
Hirst Openings ey iavesees: Leeegveevead oem ox ea hogs tatecaningsanenule’s 3 
Soft, unproductive SrouNd..c cas sece seed ccs a ve ead cee wenn newe nase 8 
Second! Openings chon secewacahun viivagee ew needed dee Nes eb atedy ermmanpinanihans 38 
Soft, unproductive. SrOUN( ss scpcccnncsiswaree eve een soa neeegeoageeras te 8 


Third opening to top of Blue limestone........cceeeeee cree e ce cece eee 8 


MINES — HIGHLAND DISTRICT. 725 


‘These diggings consist partly of old, and partly of new workings. Cross cut drifts 
are run through the old works in search of new ground, lead ore being usually found in 
the lowest opening. These parties have been working since 1870, and their product is 


as follows: 
Lead ore, Smithsonile, 


Year. lbs. tons. 
MOTO ween AS Nantes ia tee tee ante Ota DOLE ety aaa! 70 ,000 70 
TST Discpecitit aay. v ee aed aavae ised aan syhewladaaeeemaa means 70, 000 70 
DSN? 2s & fae hadersaiabatednya das asaie gia dewavocn aisle aula aaa ehaeahdlrcnae ene 80,000 80 
EST creeieart onacecsn a aeiathee Uta usher neaeek airgun tte 2 90,000 90 
US GA wel otiseisee Sear sfarb shane “la eda eaoe 4 WIC d Rea Mi is rete nascuet 90, 000 90 


The production of the years 1875 and 1876 was net ascertained. ; 

Harris & Stanley. Situated on the ground of Dr. Stanley, about 300 feet north of 
the windmill on Kennedy & Co.’s ground, previously described. These diggings are 
quite dry, being drained by the windmill pump. The range appears to be a branch of 
the Drybone Hollow range, about 500 feet long, running in a north and south direction. 
There are two principal openings exhibited in the following section of their working 
shaft: 


Feet 
Galena dimiéstone siacceiceie bes ced esa tend deanna es pilak ged oenurdaaee en 30 
Piet Open Sins acc tacscasineindou cain eas hn pres dad Genie dele sieeaaed seas ae4 ox 3 
Cap rock:(imestone) ossiwacacia sans caveeeen sees uaeaulace mess Seika ewe i 
Second opening............0 cece eee e eee e ee eee ee rt eee eee eee 6 


The ore occurs as usual in this district, in flat sheets. These paities have been work- 
ing here since Septeraber, 1871, since which time to October, 1874, the total product was 
as follows: lead ore, 40,000 pounds; blende, 35 tons; Smithsonite, 75 tons. 

Rowe & Co. Situated on the N. E. qr. of Sec. 28, T. 7, R.1 E, comprising 160 
acres. This is an east and west range, known as the Dunstan, discovered in 1846, and 
worked continuously since. It is about half a mile long, and 200 feet wide. The range 
is worked in the Brown-rock opening, chiefly for Smithsonite and lead ore. There are 
three working shafts from 50 to 75 feet deep. The opening is from 5 to 20 feet high. 
Their annual product is stated at, lead ore, 50,000 ibs., and Smithsonite, 50 tons. 

This was all that could be elicited relative to this ground, as the owners were quite 
reticent on the subject. 

The foregoing comprise all the diggings in the immediate vicinity of Highland, and, 
with the exception of the last (Rowe & Co.) they are all embraced in a tract of land 
not exceeding forty acres in extent. The same general geological charactenstics pu- 
vail in all, and they are nearly all connected together in the workings. The ore in most 
of them has to be crushed and jigged, and all except Kennedy and Maguire have to 
haul their wash dirt about a mile and a quarter to water. ; 

In these diggings, the openings below the top of the Blue limestone have never been 
worked or even prospected. If the several land-owners would take some concezted ac- 
tion, a level might be run up the Drybone Hollow, which wovld crain them to any depth 
required. Such a work, however, should he preceded by boring, to ascertain the pres- 
ence of flat sheets in the lower openings, the existence ot which is not improbable. 
| Mr. Solomon Spensley, who is well informed on the subject, says that the annual av- 
erage product of the mines is approximately as follows: Lead ore, 1,000,000 tbs.; dry- 
bone, 1,350 tons; blende, 1,200 tons. In addition to the preceding, there are some dig- 
gings situated south of the village of Highland. oe 

Davis & Co. Situated near the S. E. cor. of Sec. 5, T. 6, R, 1 E. This is a north- 
west and southeast range, discovered by a Mr. Styles in 1862. It has been proved to a 


726 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


distance of 450 feet, with an average width of 40 feet. The opening is in the Brown 
rock, and from four to six feet high. There are two shots, each about- 40 feet deep. 
The ore occurs in flat sheets, and is mostly Smithsonite and blende in about equal quan- 
tities, containing little lead ore. ~The ground was formerly worked chiefly for blende. 

The ground is estimated to have produced 2,400 tons of blende, and 1,100 tons of 
Smithsonite since 1862. Their present annual product is blende, 200 tons, and Smith- 
sonite, 150 tons. 

Manning & Delaney. Situated about 600 feet west of the preceding. It is an east 
and west range which was discovered twenty years since, and has been worked by sev- 
eral different parties, who have proved the ground in the Brown-rock opening for a dis- 
tance of 600 feet. The present parties have worked it for the past four years, princi- 
pally for Smithsonite, no blende being found until the spring of 1874. The deepest 
shaft is only 40 fect; sunk to the top of the Blue limestone, which is here estimated at 
25 feet. The St. Peters standstone is plainly seen in the valley a short distance below. 
The ground produced 600 tons of Smithsonite during the years 1873 and 1874. The 
diggings are quite dry. 

Hornsnoggle Ridge. Situated on the N. E. qr. of Sec. 5, T. 6,R. LE. This is an 
east and west range about half a mile inlength, which was discovered about twenty-five 
years since, and worked for lead ore in the Brown-rock opening; but is now pretty much 
worked out. ‘The only ore found on the ridge is drybone. The present annual produc- 
tion is about 1,500 tons. 

Beginning at the eastern end, and going west, the following parties are working: 

Joseph Call. Worked here since 1871, amount produced unknown. 

Borey & Newmeyer. Worked since 1872, produced 1,500 tons. 

Brinnen & Kelley. Worked on a lot here 20 years, product 1,000 tons. 


LINDEN DISTRICT. 


The principal diggings in this district are those of the Linden Mining Co., owned by 
Messrs. J. J. Ross and Wim. T. Henry, of Mineral Point. The property consists of the 
iE. hf. of E. hf. of Sec, 6, W. hf. of Sec. 5, N. E. qr. of 8. W. qr. of Sec. 7, N. E. qr. 
of S. E. qr. of Sec. 7, 8. hf. of 8. W. qr. of Sec. 8, 8. W. qr. of 8. E. qr. of Sec. 8, N. 
W. qr. of N. E. qr. of Sec. 17, S hf. of N. E. qr. of Scc. 17, all in T. 5, R. 2 E., and is 
situated a short distance west of the village of Linden. They were first opened in 1833, 
and worked by various parties up to 1853, altogether for lead ore, and in the middle 
beds of the Galena limestone. Prior to 1853, they are said to have produced 40,000,000 
ibs. of lead ore. 

Tn 1853 they were bought by a Pittsburg company, and operated with a water wheel, 
in the upper and lower pipe-clay openings, also for lead ore. The amount of lead ore 
produced by them was about 500,000 pounds perannum. The works finally became un- 
profitable, and were suspended by them in 1866. In this condition they remained until 
the spring of 1874, when they were bought by Messrs. Ross & Henry, by whom work 
was resumed in April. They are now operated for blende or blackjack, Smithsonite 
and such lead ore as incidentally occurs with it. On resuming work the principal ope- 
rations of the first six months were cleaning out the old shafts and drifts, erecting a new 
engine of thirty horse power, with a litt pump, together with the necessary buildings, and 
other machinery. The sheets worked here have a singular complication of “flats and 
pitches,”’ both in their connection with each other, and in respect to their general course, 
which can be best understood by reference to Plate XXX. The lines marked North, South, 
and Middle pitches, are inclined and flat sheets, consisting chiefly of blende, which are now 
heing worked. ‘The shaded portions represent the ground worked out, but leaving along 
the siles of the workings, and on the unworked portions of the several pitches, a sheet of 


PLATE, XXX 


Puwedg Y:Zoy-wiro0ag ayPUI PLO PpoytOMW punY8eayH FSF 
E 


Sumedg YOoYY-sseLH VY} UL UO poylow PUuNoaAy 


EPPS? LUG YS, 


M4 


= 


we Ping appv 


Tur Muawaukes Leroi. & Exon.Co. 


MINES —LINDEN DISTRICT. 727 


blende mixed with lead ore and associate minerals, of from one to three feetthick. At- 
tention is here called to the remarkable curvature of the sheets or pitches. Leginning 
at the well shaft, they take a northeasterly course, curving around to a northwesterly 
one at the engine shaft, and finally to a westerly one at the west pump shaft. But one 
parallel case is known in the entire Lead region. It is the Watkins range of the Dodge- 
ville district, situated in the same opening, and worked for the same ore. 

Although the blende usually occurs in a large sheet, yet it is frequently connected 
with two or three parallel smaller ones by veins or * pitches.’ The sheet often contains 
detached pieces of the wall or cap-rock, of vanous sizes, completely surrounded by ore. 
Large pockets occur in the bed, lined with very handsome crystals of calcite, one of 
which, recently removed from the mine, measures five feet by two. 

Another peculiarity noticed was the fin ing of several pieces weighing from one to 
five pounds, composed of wall-rock and ore, which were rounded and wom smooth, re- 
sembling small drift bowlders. They were found in the lower pipe-clay opening, and 
had probably been detached from the wall, at its junction with the ore. They must have 
undergone considerable erosion and transportation, or movement, by subterranean cur- 
rents of water. 

The workings in the vicinity of the engine shaft were first, examined. They extend 
in a westerly direction a distance of 1,300 feet, and have Leen worked to a width of 45 
feet, leaving a shcet of blende on the northern side from one to three feet thick. It has 
been proved by across cut to connect through to the north pitch, a distance of 180 feet. 
The same sheet has been worked in a southerly direction nearly to the well shaft, a dis- 
tance of 600 feet, leaving a large sheet of blende on its eastern side. These workings 
are in the glass-rock opening, and about twenty feet above the St. Peters sandstone. 

The following section of the engine shaft will explain their situation: 


Ft. In. 
Dump rock, clay and soil.........se0 cece eet e enter eee e neces 15 ois 
Galena; limestone cieccvee cade. Stugairtaaemegesneaawawncanue 72 6 
Ble liestowies ksiece yale vx see ssacwes od mehedvaraneneceheeeealos 6 6 
Pipe Cay uicwssusic aes ieeve asses she hoeatee aaleeemenaind: Ge VeeCle 1 
Glasstock? scaciesass. seeded Pak oanaG nee wamonmones yornnseees 5 
Glass-rock opening (Workings).......0.sesseee ceeee etree eee eens 4 
Buff limestone to bottom of shaft.......... 0.0 eee ese ence arene 8 
Buff limestone to St. Petors sandstone........seeee cece ere e ete ee -16 
otal donk ode ootner wae: Uke eee ase ae eed eed ee 1Zg8 0 


The workings at the well shaft were next examined. They are in the Brown-rock 
division of the Galena limestone, and about 26 feet above the lower workings. As will 
be seen on reference to the map, the ground is worked in an irregular shape about 300 
feet long, by 150 feet wide 

It is estimated that $200,000 worth of ore has been taken, in the course of all opera- 
tions, from this small, izregular piece of ground. It was full of large flat sheets and 
pitches, and was worked in some places to a height of 20 feet. It now produces 30 tons 
of zine ore per week, and considerable lead ore. This is exclusive of the ore raised by 
numerous miners working here on tribute. 

Fig. 19 illustrates the manner in which the flat and pitching sheets are connected in’ 
the ground. It is taken from a point on the south pitch, northeast of the well shaft. 

Two sheets were observed. One, A, coming down through the drift, and pitching to 
the south, and the other coming in from the north cn a flat EK, making a pitch to D, 
a, second at flat C, and a second pitch at B, through the floor of the drift. : AtB it is only 
about three feet distant from the sheet A. It is known from the extension of the wor«s 


42a GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 
connected with the engine shaft that the two unite below and make a large sheet (as is 
usually the case), which continues down to the lower opening. 

At the west pump shaft 
a winze! was sunk by a 
former company to a 
depth of 40 feet in the == 
St. Peters sandstone, with 
the intention of penetrat- 
ing through the forma- = 
tion. Asmall amount of ~= 
plende is said to have 
been found, but no regu- 
lar sheet. Considerable 
ferruginous matter was ~ 
also found. 


reason ies the ground == = 
should not continue remunerative for a long time, as it is comparatively easy to work, 
and the amount of water relatively small. It seems quite likely that these ranges may 
connect on the north with Morrison’s diggings, p. 729, and on the south with the Faul dig- 
gings, p. 729; should the latter prove true the mines would all drain into the creek near 
Linden, and be worked at much less expense. 

It is estimated by the owners that during the first six months of their operation, the 
mine produced ten tons of zinc ores per day; and from that time to the present it has 
produced twenty tons of zinc per day, and more than 300,000 pounds of lead ore per 
annum. The value of all ores for the last two years is estimated at $500 per day. The 
mine now furnishes constant employment to one hundred and eighty miners and other 
employés. The owners have lately introduced the Ingersoll pneumatic drill with air 
compressor; and use Rend rock extensively, the explosions b:ing eltected by an electric 
battery. 

Poad, Barrett & Tredinnick Bros. 8. W. qr. of N. W. qr., Sec. 8, T. 5, R. 2 E. 
This is a very old mine, the property of Mr. John 
Heathcock, known as tle Robarts mine, on 
which work had been discontinued for several 
3/ years, until 1869, when it was again resumed. 
a The present party have been working about four 
12, es years, and have sunk ten shafts from 40 to 70 feet 
iearare fi : a : The water is removed by two horse pumps. 

west of the above parties, and on the saine 
3 range, are Kisselbury Bros., Hammerson and 
; 4, Sey 2 Trewatha. Also on the east end of the same 
; yrange are the Poad Bros., Tredinnick, Vial 

—==—~ 7 and Geach. 
The Robarts range has been traced for a dis- 
SECTION oF SuxETS INTHE Poap Minz. tance of a quarter of a mile, the ore being found 

1. Galena limestone, cap and floor of 1 flat sheets, 25 feet above the glass rock. The 
opening. 2. Sheet of Iron Pyrites 8 to manner in which the ore is deposited is very re- 
4 inches thick. 3. Sheet of Blende1in. markable, and is shown in the annexed sketch 
thick. 4, Sheet of Galenite1 to Ginches equi : ‘ ee 
sifele, ‘om which it appears that tie order of deposition 

was, Ist, pyrites; 2d, blende; 3, galenite. This 
is one of the few localities in the Lead region from which cerussite is ov ained, 


4 A winze is a subterranean shaft which docs not extend to the surface. 


Fie. 20. 


MINES— LINDEN DISTRICT. 729 

The three mines on the Robart's range are estimated to produce annually 200,000 
pounds of lead ore, and 100 tons of blende. 

Treglown & Sons and Capt. Wicks. §. W. qr. of N. W. qr. Sec. 8, on the west 
side of the Heathcock branch. Wearing & Goldsworthy, owners. This range was dis- 
covered about forty years ago, and has been worked continuously ever since. The present 
company have been working itduring the last two years in the glass-rock opening. 
The ore is found about fifteen feet below the surface; the width of the range is 45 
feet, drained by a level 40 rods long. In former years it was worked for Smithsonite at 
higher levels, and was quite productive. Its present annual production is, lead ore, 
5,000 pounds; blende, 100 tons. 

Adams & Son and Bowden. These purties are situated about a quarter of a mile 
southwest of Treglown & Wicks. They have been working during the last seven 
years on the Morrison range, producing annually about 50 tons of Smithsonite, and 
7,000 pounds of lead ore. Water was removed from these diggings by drilling a hole 
down to the glass-rock opening. 

David Morrison Diggings. W. hf. of 8S. W. qr. Sec. 8. The range is about 700 
yards long, 40 feet wide, and has a general north and south course. The range was 
discovered in 1846, and worked at various times for lead ore to 1874. Mr. Morrison 
then opened the main sheet of blende, since which time the production has been as fol- 
lows: in 1874, 90 tons; in 1875, 106 tons. During the present year the mine has not 
been worked, although it is still good. Therange is drained by a level 350 feet long. 
The ore is found in flat sheets from 7 to 10 inches thick, on the top of the glass rock. 

Richards & Faul Bros. These diggings are situated in the viilage of Linden, near 
the 8. E. corner of section 8, on land owred by Wm. George. The ore is found under 
the glass rock in a flat sheet from 10 to 14 inches thick, from 15 to 25 feet in width, and 
from 13 to 30 feet below the surface. The water is removed by a drain about 150 feet 
long. This mine was discovered in May, 1875. From that time to May, 1876, they 
produced 80,000 tbs. of lead ore, and 150 tons of blende. During July, August und 
September, 1876, they have produced 35,000 ibs. of lead ore, and 40 tons of blende. 

Thomas Tamblin. Zinc ores were discovered on the N. W. qr. of the N. W. qr of 
Sec. 10, T. 5, R. 2 E., on the 20th of December, 1875, on the land of Mrs. Thos. Shore. 
The general course of the range is nearly east and west, and is now worked at an average 
depth of 10 feet below the surface, and has been proved to a distance of 40 feet. The 
ore was found as a flat sheet of drybone, cropping out at the foot of a hill; on working 
into the hill the amount of Smitksonite was found to diminish, and the blende to in- 
crease; which seems to be an indication that the Smithsonite is.a secondary product, 
derived from the blende. It is estimated that two miners can produce here 100 tons of 
zinc ore per annum. , 

R. S. & W. J. Jacobs. S. E. qr. of 8. W. qr., and 8. W. qr of 8. E. qr. section 
7,T.5,R.2E. This mine was discovered in March, 1875. There are here four east 
and west sheets, from four to six feet wide and from four to six inches thick in the upper 
pipe-clay opening, separated from each other by six or eight feet of unproductive rock. 
They are worked about 20 feet below the surface. There is but a small amount of 
water, which is bailed out. Some very large isclated masses of lead ore have been 
found here. one of which, weighing 1,527 Ibs., was sent to the Centennial Exhibition. 
Small quantities of zinc ores are also found. The mine produced during the year 1875, 
of lead ore, 70,000 tbs., and in 1876, 40,000 ths. The mine has not been worked much 
during this summer, as the owners are engaged in farming. 


0 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


cS 


DODGEVILLE DISTRICT. 


The mines of this district comprise those in the immediate vicinity of the village; the 
zinc ore diggings situated about two miles east of the village, and those on Van Meter's 
survey, about four miles west of the town. . 

The most productive and profitable are those situated east of the village, worked for 
drybone, blence and lead ore. 

Evan Williams’ Mines. 8. W. qr. of 8. W. qr. Sec. 25, T. 6, R.3 E. These mines 
were discovered in 1844, and were worked at intervals until 1853. Since then Mr. Wil- 
liams has worked them continuously to date. The ore is found in flat sheets about 100 
feet wide in the lower beds of the Galena limestone; and the ground is drained by a 
level a quarter of a mile long. The annexed sketch, made from an underground sur- 
vey, shows some of the more recent works. 


Fie. 21. 


@ 


QR 


750 Fe. 


Puan oF Evan Wituiams’ Dieaines. 


Mr. Williams estimates that this range has averaged 50,000 pounds of lead ore per 
annum during the last twenty years. Previous to 1863, they were worked exclusively 
for lead ore. Since then they have averaged 100 tons per annum of blende; the pro- 
duction rising in some years to 200 tons. During the present year (1876) two men have 
been employed here, and have produced 30,000 pounds of lead ore and 125 tons of 
pblende. 

In November, 1875, Mr. Williams commenced working about 700 feet south of the 
preceding location. A flat sheet was found here at a depth of 90 feet, and has been 
proved horizontally a distance of 60 feet. This mine in the past year has produced, lead 
ore 15,000 pounds; blende, 50 tons. 

In July, 1876, Mr. Williams sunk a shaft 25 feet deep about quarter of a mile west of 
the center of Sec. 25, and discovered a flat sheet of blende about five inches thick, from 
which he has obtained about three tons of blende. 

Owens & Powell. On the 8. W. qr. of 8. E. qr. of Sec. 25 are some small drybone 
diggings on Mr. Willams’ land. Three men are employed here, producing five tons of 
ore per annum. ‘This is known as Rounds’ range. 

Jones, Farrager & Owens. 8. W. qr. of 8S. W. qr. of Sec. 25, near the west line 
of the section on Evan Williams’ land. This is an old range which has been worked 


PLATE, XXII 


SoU 
sauoy? YOu 


aNT 


“salar 
so) pup fiaqgoy fiaing fApuay 


fuse Mawannwe beri & Benn Ca 


MINES — DODGEVILLE DISTRICT. 731 


since its discovery in 1849. The range is drained by a level 300 yards long. The ore is 

found in flat sheets, from 45 to 80 feet below the surface. Five shafts are now open. 

pa diggings produce only lead ore. The arnual product is valued at from $3,000 to 
5,000. 

Mrddth Evans. N. E. qr. of N. W. qr. Sec. 25, on John Williams’ land. These 
diggings are on Morgan Jones’ old range, and have been worked during the last four 
years for Smithsonite. During the present year (1876) lead ore and blende have been 
discovered, and 65,000 pounds of lead ore have been produced and considerable blende. 

Hugh Jones. N.E. qr. of N. W. qr. Sec. 25. These diggings are on the eastern 
portion of the Watkins range. They were discovered in 1848. The present party com- 
menced work in 1864, The ore is found in an irregular flat sheet, from 100 to 200 feet 
wide, in the lower part of the Galena limestone. Its position will be best understood 
by reference to the diagram of the Watkins range. The annual product of this 
mine is, lead ore, 25,000 pounds, blende, 150 tons. 

Hendy, Davey, Sobey & Co. N. W. qr. of N. W. ar. Sec. 36, T. 6, R. 3 E. 
These diggings comprise the southern and western portions of the Watkins range. 
Their position is explained on the annexed map. 

Several persons have been engaged in mining here for a number of years. The ore 
is blende and lead ore, found in a flat sheet in the same opening and position as in the 
Hugh Jones diggings. The works extend eastward and will ultimately connect with 
them, the intervening space being about 100 feet. The mine has been and is now quite 
productive, the exact amount could not be ascertained. 

Samuel Clegg. N.E. qr. of S. E. qr. Sec. 26, T. 6, R.3E. The land is owned 
by Mr. A. P. Thompson, of Buffalo. The ore is found in a flat sheet in the glass-rock 
opening, and is obtained from three shafts, each 100 fect deep. Lead ore only is pro- 
duced; it was discovered in 1870, and produced in that year 20,000 pounds. Since that 
time to October 1, 1876 the total product has been 600,000 pounds. 

Wm. Carter & Owens. W. hf. of 8. E. qr. Sec. 26. Owner of land, A. P. Thomp- 
son of Buffalo. This is known as Edward Edwards’ range, and was discovered in 1853. 
The range has a general north and south course, but with some irregularities. It was 
worked north 500 feet, then west 600 feet, then north; the north and south portions 
being the most productive of lead ore. The mine is quite wet, but is drained by a level 
about 2,000 feet long. The number of shafts is nine, the greatest depth below the sur- 
face being 70 feet. The length of the drift is 1,250 feet. Mr. Carter has been working 
this mine for six years. During that time the product of the east and west portion has 
been 65,000 ‘pounds of lead ore annually, and in the north and south portions 150,000 
pounds per annum, with the same expense. 

Other parties working in this vicinity are Nicholas Bailey & Co. and John Bosan- 
co & Co. 

Joseph Pearce Diggings. This mine is situated in the village of Dodgeville, a 
short distance northwest of the court house. It is known as the Lowry range, and was 
discovered in 1836. It was not worked from 1850 to 1870, when Mr. Pearce commenced 
work on it, and has worked it continuously ever since. It is worked exclusively for lead 
ore, which is found in tumbling openings and in flat sheets from 50 to 70 feet wide. 
The range is drained by a level 800 feet long to a depth of 30 feet below the surface. 
The deepest shatt is 80 feet. 

There is considerable water in the mines, but much less than there was 25 years since. 
‘the water is removed by a horse pump worked during the daytime. The length of the 
range, so far as it has been worked, is 1,000 feet. During the last two years this mine 
has produced 200,000 pounds of lead ore; previous to this it only paid expenses. 

Lambly Range. N. E. qr. Sec. 28, T. 6, R. 3 E. This range has been worked con- 
tinuously for a great many years, and now gives employment to four men. It pro- 


732 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


duces lead ore to the amount of about 30,000 pounds per annum. Four years ago its 
annual product was 290,000 pounds, 
Porter’s Grove Diggings. 

These mines are situated in town 6, range 4 east. At present the following mines are 
in operation: 

Union Mine, Wm. Hendy & Co. Situated on the N. E. qr. of the N. E. qr. of Sec. 
28. The ore produced is lead, and in tumbling openings, at a depth of 70 feet and on 
the upper surface of the green rock. From two to five men are employed. The mine 
is drained bya level one-quarter of a mile long. 

Ridgeway Mine, Wm. Hendy & Co. Situated on the 8. E. qr. of the S. E. qr. of 
Sec. 21. This mine is owned and operated by the same parties as the preceding, and 
is on the same range, which is known as the north and south branch lot. From two to 
four men are employed. It is also drained by a level a quarter of a mile long. The 
mode of occurrence of the ore is also the same. The present owners commenced opera- 
ting them in 1872; since then the product of lead ore is as follows: 


Union Ridgeway 
: Mine. ine. 
DSTO sarge cacies acreoh are SARK DIGG LE RASS AS RD 300,000 ths. 44,000 Ibs. 
VST a cha averas os Suas bcdsbcoe Wrens yaceia SU aMen acess waite Sentara. 35,000 “ 44,000 ‘ 
VS 74 visscsts gesyie ee Mateos wie ek Wnts We WT) oer oe aS 16,000 ‘S 63,000 
Te pits Gosia elp as ete ace taste eA SE ENO 38,000 “ 44,000 “ 
1876 to Oct. Ist........00eecceeeeveseeeseeeess 29,000 “ 17,000 “ 


Frank, Farwell & Co. 8. E. qr. of N. E. qr. of Sec. 28. These parties commenced 
working on the Wakefield range in Oct., 1875. Previous to that time it had not been 
worked for twenty years. Most of the workings are at a depth of 35 feet below the sur- 
face, although some are as deep as 60 feet. The work is chiefly removing pillars of lead 
ore which have been left from former operations. The product from Oct., 1875, to Oct., 
1876, has been 14,000 tbs. 

Other parties mining in this vicinity are John and Thomas Paull, of Ridgeway, pro- 
ducing lead ore. 

Van Meter’s Survey. 

On the N. hf. ot the N. E. gr. of Sec. 18, T. 5, R. 3 E., are three very large ranges 
which have not to our knowledge been reported. Their general course is N. W. and S. 
E., and they are crossed by numerous north and south crevices. It is at these crossings 
that the largest bodies of ore are found. The ore is galenite, and is entirely free from 
any mixture of zinc ores. It is found in the green-rock opening. 

The northernmost of the three ranges, known as the Duke Smith, contained an open- 
ing in places 50 feet wide, somewhat intersected with bars. It was worked over a quar- 
ter of amile in length, and produced about half a million pounds of lead ore. It hag 
not been worked since 1853. 

A short distance south of this isa parallel range which produced over 200;000 ibs. in 
a distance of about 100 feet. The opening was about 30 feet wide. 

The third parallel range, 300 feet south of the Duke Smith range, has been worked 
since the winter of 1873-4, by Mr. John Hutchinson of Mineral Point. The lead ore 
occurs in large pockets containing crystalline pieces of from one to five hundred pounds 
weight. The opening is in the green rock and is from ten to twelve feet high. This 
range has been the least werked of all, but formerly produced about 100,000 pounds. 
It now yields ore of the value of $5 per day when worked. None of the ranges haye been 
worked to any great depth, and all were abandoned with ore going down in the cre- 
vices. The gradual diminution of water in the cointry has now made it possible to re- 
sume work. 


MINES — MINERAL POINT DISTRICT. 733 


Powell & Co. This party is working on what is known as the Nic Schillen range. 
Work was commenced in the spring of 1876, and continued for three months. The 
works are in the glass-rock opening and about 20 feet below the surface. The amount 
produced was 3,000 pounds. 

Richards & Burns. This party is situated south of the preceding, and on land of 
the Sterling estate. They have been working these during the present year in the 
green-rock opening, producing about 2,000 pounds per month. 

Powell Diggings. They are situated about a quarter of a mile north of Mr. 
Hutchinson's diggings. This is a new discovery and has been in operation about a year. 
The production has been 35,000 pounds. 


MINERAL POINT DISTRICT. 


These mines comprise those in the immediate vicinity of the city, and those of Lost 
Grove and Diamond Grove. Considerable mining is being carried on at these localities, 
which are among the oldest and most productive of the Lead region. They are all com- 
prised in towns 4 and 5, ranges 2 and 3 east. In addition to the lead ore, a great deal 
of zinc ore has been produced within the past ten years, and they now supply a large 
portion of the zinc ore of the Lead region. 

Terrill Range and Badger Range. These ranges are situated on lots 128, 129, 
130, 131, 132, 134 of Harrison's survey of the city of Mineral Point. They are old and 
well known ranges, which have been worked continuously for many years, and are now 
productive of Smithsonite and galenite. They furnish constant employment to about 
twenty-five men. : 

The mines are situated on a high ridge, from which the water drains naturally into 
the adjacent ravines, leaving the diggings constantly dry. The ore is found in flat 
sheets and “pitches” (inclined sheets). The ranges are from 150 to 200 feet wide, 
more than a quarter of a mile long, and contain ore at depths varying from 10 to 60 
feet below the surface. There are three principal openings in the lower beds of the Ga- 
lena limestone. The parties now working on the Terrill range are as follows: 

Matt Shields and John Linden. They have been working for three years, at an 
average depth of 40 feet, producing chiefly Smithsonite from the second opening. The 
sheet averages about ten inches in thickness. 

Pascoe & Collins. They have been working their present mine during the last 
eight years, producing Smithsonite, blende and galenite from the green rock and the 
green-rock opening. The Smithsonite is the most abundant, and the lead ore the least 
so. ‘Lhe workings are from 20 to 60 feet deep, and the ore is found in sheets from one 
to four inches thick. The blende is found at the greatest depth, and averages about 
four inches in thickness. 

Jacka & Waggoner. These parties have been working here eight years, at a depth 
of about 50 feet below the surface, but never having reached the lower opening. They 
estimate their annual production at 15,000 lbs. of galenite and 25 tons of Smithsonite. 
The range at this point is 200 feet wide. ; 

Hitchins & Terrill. They have been working at various times during the last ten 
years on the northwest end of the Terrill range, known as the brush lot, producing lead 


and zinc ore. This was formerly very rich ground, The work at present is confined to 


prospecting. 

Huxtable & Son. 
20 to 50 feet deep, producing large amounts of lead and zinc ore. 
be one of the best mines on the range. 


Parties working on the Badger range are as follows: 
Thos. Cox & Sons. These parties are working near the center of the range, and 


These parties are working near the center of the range, and from 
This is believed to 


134 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 

chave been mining here during the last ten years. The ore is found in three flat open- 
ings. The first is from ten to twenty feet below the surface, and contains chiefly Smith- 
sonite in sheets of three inches thickness. The second opening is ten feet deeper, con- 
taining the same ore, mixed with galenite, in sheets of three inches. The third open- 
ing is ten feet below the second, and contains chiefly blende in sheets averaging four 
inches. The description of these openings applies toall the other mines in the range. 

Other parties working on this range are Cox & Co., Jas. Hitchins & Holman, and 
Harris and partner. 

The mining ground on this ridge is owned in small lots by several parties, among 
whom are Messrs. Ross, Priestly, Tyck and Prideaux. [t was found impossible to ob- 
tain any information of the amounts of ore produced on this ridge, but it is safe to esti- 
mate ore to the amount of $600 per annum for each man, and this is probably much 
beneath the actual amount. . 

William Prideanx Mines. |S. E. qr. of N. W. qr., Sec. 30, T. 5, R. 3 E. This is a 
part of the Ashbank range, so called from the decomposed appearance of much of the 
surface lead ore. It was discovered more than thirty years since, and worked ex- 
tensively for lead ore. The course of the range is nearly northwest, and its average 
width about 25 feet. The principal product of the mine is Smithsonite, with some lead 
ore. The workings are chiefly in the green-rock opening, where the ores are found in 
flat and pitching sheets, from two to eighteen inches thick. The ground is dry and the 
workings rather shallow, seldom being more than fifty feet below the surface. In one 
place, where water was troublesome, it was removed by drilling a hole 54 feet deep, 
draining it off through a lower opening. During the present year (1876). about 51,000 
pounds of lead ore and some blende were obtained in the Brown-rock opening. Mr. 
Prideaux commenced work in April, 1873, and now employs six men. He estimates 
that from January 1, to October 1, 1876, the value of ores produced is $6,500, and 
-about the same amount from April, 1873, to January 1, 1876. ‘ 

A short distance southwest of the preceding, is a parallel range not worked at present, 
but regarded as a valuable mining ground. 

J. Jackson & Co. These diggings are also on the Ashbank range, and a short dis- 
tance eastof Wm. Prideaux. The ores produced are Smithsonite and galenite in nearly 
equal amounts, found in flat sheets in the green rock, and its opening from 15 to 40 feet 
below the surface. The range is about 40 rods long and 350 feet wide; ten shafts have 
been sunk upon it. Work was commenced here in 1868, since which time it has been 
continuous, the mines proving very productive. No exact amounts could be ascertained, 
but the owners estimate the value of ores produced since 1268 at $18,000; the present 
year being the most remunerative. 

Mitchell & Pollard. N. W. qr, of 8. W. qr. Sec. 30, T. 5, R.3E. This range is 
situated about 60 rods southwesterly from the Prideaux mines. These parties have been 
working about four years, producing Smithsonite and lead ore. The workings are shal- 
low and dry, similar to the Ashbank range, hut not so productive. 

Sinapee Diggings. These mines are situated on the N. E. qr. of 8. E. qr. of Sec. 
30. They were discovered in 1845, have been worked continuously since then, and now 
furnish employment to several parties, among whom are: i 

Samuel Prisk and Wm. Paynter. These parties commenced work in the fall of 
1875, and have produced during the last year about 50 tons of Smithsonite and some 
lead ore. The diggings are quite dry and average about 15 feet in depth. The ore is 
found in flat sheets the principal workings being in the glass-rock opening. Four men 
are employed here. This mine furnishes fine cabinet specimens of galenite. The range 
is about 500 feet long, from 100 to 150 fect wide, and has a general east and west 
course. The ore sheet is from two to four inches thick. 

Prisk & Coad. This is a parallel range situated about 300 feet south of the preced- 


MINES — MINERAL POINT DISTRICT. 735 


ing, and having about the same length, width and thickness. The above party com- 
menced work in the fall of 1875, and are now working in the upper pipe-clay opening. 
This mine is from 50 to 60 feet deep, and formerly produced over a million pounds. 
Two men are generally employed here, and produced during the last year alout 7,000 
pounds of lead ore. 

Samuel and Wm. Richards. These parties are working a short distance east of Prisk 
& Paynter. They have been engaged here about a year and a half, producing chiefly 
blende and lead ore. 

Bennett & Brady. Situated near the center of Sec. 29. A large amount of work 
has been done here, including a level to unwater the ground. They are quite product- 
ive of the ores of zinc and lead. 

Short & Co. Situated on the N. W. qr. of Sec. 29. Considerable mining has been 
done by these parties in this vicinity during the last few years. 

There are several very profitable mines in the northwestern part of Strong’s Addition 
to the city of Mineral Point, ail on land owned by Mr. J. J. Ross. They are as follows: 

Bohan & Co. Four men have been employed here during the last four years, pro- 
ducing Smithsonite and lead ore. The range is from 70 to 80 feet wide, has a general 
east and west course, and is worked to a depth of 70 feet below the surface. There are 
two openings, separated by about 20 feet of unproductive rock; the lower ore being 
the glass-rock opening. 

Connaughton & Casserly. These parties are working on an east and west range 
about 300 feet north of the preceding. They have been working here during the 
last two years, have sunk two principal shafts to a depth of 60 feet, to the glass-rock 
opening. This is an east and west range, about 60 feet wide, and has been drifted on 
to a distance of 100 feet. It produces chiefly blende, estimated by the owners at $800 
per year. 

John Wegler & Co. Situated about 300 feet northwest of the preceding. These 
parties are working in the same openings and producing chiefly zinc ores. Until very 
recently, two other parties were employed in this vicinity, this ridge having for many 
years been very good mining ground. 

Bennett & Co. This party is engaged in mining and prospecting about a quarter of 
a mile east of the preceding diggings. 

Near the corner of towns 4 and.5, ranges 2 and 3 east, are a number of ranges which 
have been worked for many years. Those situated on section one are the property of 
the Mineral Point Mining Company; those on the adjacent sections are the property of 
Mr. John J. Ross. * 

There are six principal crevices, running nearly parallel, on Secs. 36 and 1. Their 
general course is S. 70° E., and on entering Sec. 6, they run nearly east and west. The 
crevices Jead down to the opening between the Buff and Blue limestones, known as the 
glass-rock opening. The ore here is found in a flat sheet about a foot thick, and from 
70 to 140 feet wide, which has been worked for a distance of half a mile. 

The ores are galenite and blende, and occur associated with barite, and have to be 
separated before reduction. 

The mode of drainage in Mr. Ross’ mine is somewhat peculiar. Shafts were sunk at 
intervals to a depth of six feet below the opening, into the Buff limestone, where a bed 
is reached through which the water readily passes away. This mode of drainage was 
accidentally discovered in prospecting for the sheet. No ore of any consequence is found 
in the upper pipe-clay opening; occasional bunches have been found, probably not over 
20,000 ths. in all.’ These ranges have been worked at intervals for the last forty years 
by various parties. Active operations were commenced by Mr. Ross about ten years 
ago, since which time his ground has produced about 2,500,000 lbs of lead ore, and 
about 3,500 tons of zinc ores. During the whole time in which these mines have been 


736 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


worked, it is safe to say they have produced not less than eight million pounds of lead 
ore, and twice as much zinc ores. During the winter of 1874-5, eight men were em- 
ployed in Mr. Ross’ mines and produced ore to the value of $1,600. During the winter 
of 1875-6, four men were employed, producing ore to the value of $1,000. Work will 
probably be resumed this winter. 

On. the lands of the Mineral Point Mining Co. several parties are working on tribute. 
The amount this ground is producing could not be ascertained. 

Goldsworthy & Bro. These diggings are situated on lots 279-280 of Harrison's sur- 
vey, about a quarter of a mile east of the preceding and on the N. W. ar. of Sec. 6, T. 
4,R.3E. Thisis known as the Barber range, and has been worked in the winter 
season during the last six years. 

The ore is Smithsonite, much mixed with pyrites; it is found in the upper pipe-clay 
opening, in a flat sheet from 8 to 30 feet wide and from 18 to 24 inches thick, being 
most productive on crossing crevices. 

Four men are employed here producing about 20 tons per year. 

T. Lutey & Co. This party is working a short distance east of the preceding, on 
land owned by M. M. Cothren. They have been working on a continuation of the Bar- 
ber range for about two months (October, November, 1876) and have now a very good 
prospect. 

Most of the lead ore from the Barber range is obtained from the glass-rock opening, 
but it has never been worked for zinc ore. 

Suthers & Co. Situated on the southeast part of Harrison’s survey. Thisis a neay- 
ly east and west range, known as the ‘‘ Walla-walla,’’ and has been worked by the 
present party since 1865. The range is about 120 feet wide and has been worked inthe 
glass-rock opening to a length of about 1,000 feet, and at a depth of 73 feet below the 
surface. From three to six men are employed, working in the winter season. Tho 
mine produces lead ore and both kinds of zinc ore. The average annual product of 
lead ore is about 44,000 pounds. The products from January to April, 1876, of all kinds 
of ore were valued at $900. 

J. Arthur & Co. Situated on the S. W. qr. Sec. 6, T.4,R.3 E. This is an eastand 
west range, discovered about two years since, and worked continuously to the present. 
The ores are Smithsonite and lead ore, found in a flat sheet, from six inches to one foot 
thick, in the glass-rock opening, at a depth of 60 feet from the surface. The range is 
about 100 feet wide; its length is not yet known. It is situated on land owned by Mr. 
J.J. Ross. The ground is comparatively dry. 

Hoare Bros. Situated about 50 yards east of the preceding, and on thé same range, 
on land owned by Mr. J. Hoare. This party has been working here about two years, 
producing lead ore and Smithsonite from the glass-rock opening. The diggings are now 
very good. 

Nichols & Holmes. Situated on N. E. qr. Sec. 7, T. 4, R. 3 E., a short distance 
east of the old zinc works. There are some irregular flat sheets of zinc ore in the glass- 
rock opening, about 20 feet deep. They have been worked during the last two years 
and have produced considerable zinc ore. 

Harris & Lang. These diggings are situated about half a mile south of the pre- 
ceding. This is an east and west range situated in the glass-rock opening about 25 
fect deep. It has heen worked about a year, producing considerable zinc ore. 

In the vicinity of the Mineral Pot Town Hall, on the N. W. qr. of Sec. 5, T. 4, R.3 
E., are the following diggings: 

Prideaux & Henry. This is a north and south range, about 200 yards south of the 
Town Hall, which has been worked by the present party since 1866. The ores are lead 
und zinc, found in flat and pitching sheets from 8 to 10 inches thick, in the upper pipe- 


MINES — MINERAL POINT DISTRICT. 737 


clay opening, at a depth of from 1 to 60 feet below the surface. The range is from 60 
to 70 feet wide, and has been worked to a distance of 350 feet. 

Jeffrey & Bro. Situated about 100 yards south of the preceding, and probably on 
the same range. The range is here 100 feet wide, and produces lead ore, and both kinds 
of zinc ore, in about equal quantities, and considerable iron pyrites. The work has been 
chiefly done in the winter season during the last two years. 

Short & Foster. Situated about 200 yards west of Jeffrey & Bro., on an old north 
and south range, sixty feet in width. They have been working during the last two 
years in the winter season, producing lead and zinc ores from the pipe-clay opening. 
The digyings are about 40 feet deep. 

Mankey & Son. Situated about 150 yards 8. E. of Jeffrey & Bro. They have been 
working during the last. twelve years on a north and south range. The product is lead 
ore found in vertical crevices, and in flat sheets in the green-rock opening at a depth of 
40 feet from the surface. 

All the diggings on this hill are dry; and most of them are remunerative, but the 
amounts of ore produced could not be ascertained. 

The mining land is owned by Messrs. Henry, Coad, Prideaux and Woodman. 

About a quarter of a mile north of this ridge is the Mineral Point Hill, lying di- 
rectly east of the city. The following parties are mining there: 

Vivian & Sleep. This party is working a nearly east and west range, the most 
southerly of several parallel ranges which cross the hill. The range is about 50 feet 
wide, and produces zinc ores, chiefly Smithsonite, from the upper pipe-clay opening, 
which is here about 25 feet below the surface. They have been working here during 
the last thirteen years, operating during the entire year. 

Brown & Cluthers. They have been mining about a year on a parallel range 150 
feet north of the one last mentioned. The range is about 50 feet wide, and produces 
zinc ores, chiefly blende. The ore is found in flat and pitching sheets in the pipe-clay 
opening. 

James Dunn & Son. This party has been working about three years on a range 
150 feet north of the preceding. Both kinds of zinc ores are produced from the upper 
pipe-clay opening, which lies here about 40 feet deep. 

Trewilla & Strong. This party has worked about eight years in this vicinity, and 
one and a half years on their present range, producing zinc ores. 

Goldsworthy & Hocks. Situated about one-fourth of amile east of Vivian & Sleep. 
They have been mining about a year, producing blende. 

The mining land in this hill is owned by Messrs. Hutchinson, Henry, Curry, Gundry 
and Washburn. The ranges all bear a little north of west and south of east, and have 
never been worked below the upper pipe-clay opening. 

‘The earliest mining in this vicinity was done on the Mineral Point Hill. The ranges 
were formerly very productive, and have been worked continuously for many years to 
the present time. There are a few other parties mining within a few miles of Mineral 
Point. They are as follows: 

Rogers & Mankey. Situated on the N. E. qr. of Sec. 8, T. 4, R. 3 E., on land 
owned by Mr. Suthers, near Rock branch. This is a new discovery made in October, 
1876, bemg a flat sheet of Smithsonite in the Brown-rock opening. ; - 

J effrey & May. Situated a short distance north of the preceding. This is also a 
new discovery made about the same time as the preceding, being a flat sheet of zinc 
ores in the glass-rock opening. The prospect is very good. ; 

Badcroft Diggings. Sec. 15, T. 4, R.3 E. Work was begun here in 1872, and has 
been continued at intervals since. Three men have been employed, chiefly in prospect- 
ing, and a small amount of lead ore has been produced. The ore is found in flat and 
pitching sheets in the pipe-clay opening, about 20 feet below the surface. 


Wis. Sur. —47 , 


738 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Shepard & Co. Situated on the N. E. qr. of the N. E. qr. of Sec. 22, T. 4, R. 2 E. 
Work was commenced here in August, 1876, on the old Maloney range. This rango 
has a general east and west course, and yields lead ore and blende from the pipe-clay 
opening, which is here about 25 feet deep. The ore occurs in a flat sheet from 4 to 5 
inches thick, the blende forming the top and bottom of the sheet, and the lead ore the 
central part. The product has been, to December, 1876, lead ore, 1,500 pounds; 
blende, 3 tons. The ground is dry, and the prospect is considered good. 

Clebenstein Diggings. They are situated on the same ridge and a short distance 
east of the preceding. They are now operated by August Cain, who has been mining 
about a year. They were operated from 1865 to 1875, by Mr. Clebenstein, and pro- 
duced large amounts of lead and zinc ores. The ore was found in flat sheets, in the 
pipe-clay and glass-rock openings. 

H. Josephs Diggings. Situated on the W. hf. of the 8. W. qr. of Sec. 5, T. 4, R. 3 
E. Mining was commenced here in 1871, and continued until the fall of 1874, when it 
was discontinued on account of water. The ore found here was exclusively blende, 
which occurred in a flat sheet, in the green-rock opening. The width of the sheet was 
about-80 feet, its greatest thickness three fect, and it was worked for a distance of 800 
feet. The greatest depth below the surface is 70 feet. During the years 1873-4 this 
ground produced about 1,000 tons of blende. 


Diamond Grove Diggings. 


These diggings are situated on Secs. 25 and 26, T.5,R.2E. They produce chiefly 
zinc ores, found in flat sheets in the pipe-clay and glass-rock openings. The following 
parties are now mining here: 

Cain & Read. Situated on the N. W. qr. of Sec. 25. This party has been working - 
on the Rodersdorf range during the winters of 1873-4 and 1874-5. The ore, which is 
Smithsonite, is found in the glass-rock opening, in a range from 16 to 20 feet wide, and 
200 feet Jong. The production during the first season was 1714 tons, in the second sea- 
son, 20 tons. 

Robert Conley & Sons. Situated on the 8. W. qr. of Sec. 25. Mining has been 
carried on here by the above party during the last ten years on an east and west range. 
Both kinds of zinc ore and lead ore are found here in the pipe-clay and glass-rock open- 
ings, but chiefly in the latter. The range is from forty to sixty feet wide, and has been 
worked a distance of 150 yards. During the last year and a half the product of lead 
ore has been 60,000 pounds, and sixty tons of zinc ore during the last two years. 

Biddick Diggings. A valuable deposit of lead ore has lately been diseovered on 
the 8. W. qr. of Sec. 24, T. 5, R. 2 E., on which four men are now employed running a 
level. Four flat sheets, from one to four inches thick, are found here situated above 
one another, in the upper pipe-clay opening. It has not yet been sufficiently worked to 
determine its actual extent. 

Martin Bros. & Cramer. Situated on the 8. W. qr. of Sec. 25. This and the pre- 
ceding are on land owned by Mr. James Spensley. They have been mining here on an 
east and west range, which was discovered two years since. The ore is Smithsonite; 
and is found in the glass-rock opening, which is here from ten to thirty feet deep. 

Spensley & Brown. Situated on the N. E. qr. of Sec. 26, T.5,R.2E. Six men 
have been employed here since July 1876 driving an adit in the glass-rock opening. The 
adit is 200 feet long, and drains an east and west range. The product has been, lead 
ore, 36,000 pounds, blende, six tons. 

Opir & Lancaster. Situated on the N. W. qr. of Sec. 26. This party is working 
the same range, 450 yards west of the preceding. It is here known as the Lancaster 
range, and has been worked by the present party about a year. From three to five men 
are employed, and the product has been 150 tons of blende. It is worked by an adit. 


MINES —CALAMINE DISTRICT. _ 739 


McDermott & Co. Mining has been carried on here by Mr. McDermott for about 
26 years, on the McShane & Gray range. The ore is found im flat and pitching sheet, in 
crevices and crevice openings in the Galena limestone above the flat openings. The dig- 
gings now produce lead and zine ore. The average annual product is about 30,000 lbs. 
Four men are employed here. 

Schlosser & Co. This party has been working four or five years on the east end of 
the same range as the preceding. The ground is dry, and the lead ore is found about 
40 feet below the swface. The annual product is about 10,000 ibs: 

Wm. and Thos. Thrasher. This party has worked in this vicinity about fifteen years, 
on a parallel range situated about a quarter of a mile southeast of Schlosser & Co. The 
product is chiefly lead ore. 


Lost Grove Diggings. 


These diggings are situated on land owned by Mr. J. J. Ross, on Sec. 38, T. 5, 
R. 2 E. Mining is confined here to the winter season. The ground is dry, and the ore 
is found in flat sheet in the glass-rock opening. The following parties are mining here: 

Rigger & Arthur. This party has been working two years on an east and west 
range, producing lead ore and Smithsonite. The range varies from 25 to 50 feet in 
width, and lies from 30 to 40 feet below the surface. The product is valued at $1,200 
per annum. 

Clayton & Co. Situated about a quarter of a mile northwest of the preceding, have 
been working during the last twelve years on the Jim Brown range. This is an east 
and west range, from 50 to 60 feet wide, and lying about 70 feet below the surface, pro- 
ducing exclusively lead ore. The product has been about 20,000 pounds per annum. 

Garden & Son. Situated about one-fourth of a mile south of the preceding. They 
have been working about two years and have produced about $400 worth of ore. 

Robert Brown & Co. Situated about half a mile east of Clayton & Co., and on 
the same range. The diggings here are from 25 to 50 feet deep. They have been 
working about three years and have produced about 30,000 pounds per annum. 

Furfer & Co. They have been working on a range near Brown & Co., during the 
last eight years, producing lead and zinc ore. 


CALAMINE DISTRICT. 


There are several tracts of land situated on Secs. 18 and 19, T. 3, R. 3 E., which were 
formerly quite productive; but little work is now done on them. They are situated on 
the west side of the Pecatonica river, on the ridge which separates the Wood and Bon- 
ner branches. The ridge slopes abruptly on all sides but one toward the various 
streams which nearly inclose it. 

On the summit of the ridge there is a thickness of about one hundred feet of Galena 
limestone, underlaid by fifty feet of the Blue and Buff limestones, below which is the 
sandstone. All these formations may be distinctly seen in passing from the summit of 
the ridge to the valley of the Pecatonica. 

During the winter of 1876-7 some mining was done here by Mr. Charles Mappes, of 
Belmont, on an east and west range lying from 30 to 40 feet below the surface. Four 
men were employed, working on a flat sheet of blende and galenite. The amount pro- 
duced could not be ascertained. Some Smithsonite is also produced in this vicinity. 


Yellowstone Diggings. 

Pierce & Son. Some work has been done here during the winter seasons of the last 
three years, in a range a quarter of a mile north of the Newkirk range, situated on the 
S. W. gr. of Sec. 14, T. 4, R. 4 E. The lead ore is found in a vertical sheet in a crevice 
opening about fourteen feet below the surface. In the winter of 1874-5 the product 


740 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


was 18,000 pounds, and in the following winter about 1,800 pounds. No mining is 
done here in the summer. 


WIOTA DISTRICT. 


This is a small group of east and west ranges, crossed by north and south crevices, 
situated in the N. W. ar. of Sec. 19, T. 2, R.5 E. But very little mining is done here; 
the annual production of the whole district does not exceed 40,000 pounds. The ore is 
lead, occurring in the middle portion of the Galena limestone, and there does not seem 
to be any regular opening. There are several parties here, among whom the principal 
ones are as follows: 

Purcell & Harden. They are at work in the old Hamilton diggings, removing the 
pillars from the old workings which were abandoned many years since. They are un- 
able to go any deeper, or make any new discoveries, on account of water, which is here 
quite plentiful. The ground is owned by the Ridgeway Mining Co., of Madison. 
Messrs. Purcell & Harden have worked here two years, and during that time have pro- 
duced 20,000 pounds of lead ore. 

Smith & Anderson. Situated a short distance north of the preceding, and form the 
northern part of the Hamilton diggings. This does not appear to form any regular 
range. The ore occurs in east and west shects, in very hard rock, and seldom in open- 
ings. the diggings have now been worked since January, 1873, and have produced 
80,000 pounds. 


MONROE DISTRICT. 


These are the most easterly diggings in the lead region, and are chiefly interesting for 
that reason. They are situated about three miles and a half north of the city of Mon- 
roe. At present only two parties are at work. 

T. H. White & White. Situated on the N. E. qr. of Sec. 14, T. 2, R. 7 E. 
The ore is found here ina flat sheet, accompanied by pipe clay, about twenty-three 
feet below the surface. The general course of the sheet is northwest and southeast 
and produces only lead ore. The ground is quite free from water. The present parties 
have been working here six years, during which period they have produced 90,000 
pounds of lead ore. 

Frame & Co. Situated on the 8. E. qr. of Sec. 10, T. 2, R. 7 E., on the land of 
Mr. Henry Wilber. This is an east and west range, about half a mile northeast of the 
preceding. It was discovered in 1844, and has been proved for a distance of 700 feet. 
The lead ore is found in both vertical crevices and flat openings. There appear to be 
three principal vertical crevices, connected in places by horizontal sheets. 

They were worked by Mr. John Monahan, from 1870, to February, 1872, chiefly in 
the winter season, during which time he produced 50,000 pounds. Mr. Frame took the 
ground in 1874, and produced 4,000 pounds in the first six months. The production 
since then could not be ascertained. The ground is quite dry, and the workings are 
about fifty feet below the surface. 

It is not probable that any extensive deposits exist in this vicinity. The ground ap- 
pears rather to be such as, by careful working, will afford moderate wages to a few 
persons. 


COPPER IN THE LEAD REGION. TAL 


COPPER IN THE LEAD REGION. 


At present no mining for copper is done in the lead region, nor has there been for 
several years, except at Mineral Point in the years 1873 to 1876. Indications of its pres- 
ence are found in many places through the mines, as an associate mineral in the lead 
veins. The most systematic attempt at copper mining was made at Mineral Point. 

Mr. James Toay, who is well acquainted with thé past history of the enterprise has 
landly furnished the following statement: 

“Sometime in the year 1837 or 1838, copper was first discovered on the S. E. qr. of 
Sec. 32, T. 5, R. 3 E., one mile northeast of the Mineral Point court house. The crev- 
ice had a course 8. 85° E., and had been traced for over one-third of a mile. This lo- 
cality has not been worked since 1842. A great amount of copper was obtained. 

“Tt is reported that over one and a half million pounds of copper were taken out, 
which would include all kinds of ore: ‘Smalls,’ which would not yield more than ten 
to fifteen per cent of copper; and the stone or ‘ Prill’ ore, yielding twenty-five to thirty 
per cent. 

‘*Some of the ore was smelted at the old furnace owned by William Kendall & Co., 
and some at the new Baltimore furnace, owned by Ansley & Co. About 50,000 pounds 
was sent to England or Wales for reduction, which indicates that parties here did not 
at that time understand the proper method of smelting copper.! 

“Sometime in 1844, S. P. Preston came here, and went into partnership with Kendall 
& Co., and after that they had no trouble in smelting copper successfully. 

“The amount of copper sold from Kendall & Co.’s furnace from 1841 to 1846 was 
217,702 tbs. This was about ninety-five per cent. pure copper, and sold for fourteen 
cents per pound. 

‘‘Two other furnaces have been worked; one by Charles Bracken, to what extent I 
have no knowledge, but know he smelted considerable copper ore from his own land. . 
The other was owned by Curtiss Beach. Here a great amount of copper ore was smelt- 
ed, taken from the Beach diggings. The greatest amount of ore that Kendall & Co. 
smelted was taken from the Kendall diggings. 

“It is probable that with the increased advantages in the present price of copper; in 
obtaining coke instead of charcoal for smelting, and in shipping facilities, that copper 
mining may now be made a profitable business at this place if properly managed.” 

During the years 1873, 1874 and 1875, about 200 tons of copper ore were produced by 
Mr. Toay from the mines near Mineral Pot. An attempt was also made to smelt it 
in 1874. No very large amount was smelted, as the common blast furnace was not ex- 
actly adapted to its reduction. The ore is a sulphuret of copper. The exact amount 
produced could not be learned. 

The ranges referred to in the foregoing statement of Mr. Toay are situated as follows: 

Ansley Range. Course §. 85° E., running from the center of Sec. 32, T.5,R.3E., 
one-third of a mile long. 

Kendal Range. N. E. qr. of Sec. 5, and N. W. ar. of Sec. 4, T. 4, RB. 3 E., run- 
ning from near the quarter post of Secs. 5 and 382, nearly to the center of Sec. 4.; length, 
about two thousand feet. | 

Beach Range. E. hf. of Sec. 4, T. 4, R.3E. Crossing the center line of Sec. 4 one- 
quarter of a mile east of the center of the section, and running 600 feet from that point 
on a course N. 85° W., and 600 feet on a course S. 85° E. 


1 Two specimens of copper ore from the Mineral Point district, 8. E. qr. of Sec. 32, T. 5, R.3E., 
were analyzed with these results: No.1 gave metallic copper, 38.78 per cent. No.2 gave copper, 


4.48 per cent. 


742 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Wasley Range. S. W. qr. of the S. E. qr. of Sec. 32, T. 5, R.3 E. Course 8. 85° 
E.; length, about 1,000 feet. 

Ballard Range. S. E. qr of the S. E. qr. of Sec. 32, T. 5, R. 3 E, Course N. 30° 
E.; length, about 800 feet. 

Besides these there are several small north and south ranges on the N. E. qr. of the 
N. W. qr. of Sec. 5, T. 4, R. 3 E. 

Traces of copper ore are also found at many points north of Mineral Point, in the 
diggings between that city and Dodgeville. 

A specimen of ore containing a considerable carbonate.of copper was presented by 
Hon. H. H. Gray, of Dodgeville. It was found about fifteen feet from the surface, on 
the 8. W. qr. of Sec. 22, T. 2, R. 3 E. 

Specimens of sulphuret of copper were obtained from some old diggings on the 8. 
W. qr. of Sec. 8, T. 1, R.5 E. The course of this range is about 8. 20° E. Copper 
was mined here as early as 1838, and two or three loads of ore were brought to Mine- 
ral Point for reduction. A specimen from this locality afforded 10.86 per cent. of metal- 
lic copper. 


STATISTICS OF ZINC ORE. 


The statistics of the production of zinc ores are believed to be complete, and to em- 
brace the annual production from the year 1860 (at which time the zine ores began to 
be utilized) to October, 1876. The ore is all consumed at La Salle, Ill., by four com- 
panies. By far the greatest quantity of the ore is shipped from Mineral Point; the other 
points are Platteville, Council Hill, and Galena. 

The blende is shipped in its crude state, as it comes from the mines; but the carbo- 
nate of zinc (drybone) is previously roasted or calcined, by which process it loses its 
carbonic acid, which constitutes about one-third of its weight, and is decreased in bulk 
in the same ratio. The small amount of water, which is usually present as a mechani- 
cal mixture with the ore, is also driven off. 

The ore is calcined in a small and inexpensive furnace, resembling a lime-kiln im its 
structure and object, capable of containing about sixty tons of raw ore. Such a furnace 
will roast about twenty-five tons of ore in twenty-four hours, and requires the labor of 
six men at eight hours apiece (three shifts). From eighty to one hundred pounds of 
bituminous coal are required for each ton of ore. 

The cost of carrying the ore through this operation is from fifty to sixty cents per ton. 
The cost of a fwnace and requisite tools is about $300. 

The following are the amounts of zine ores produced in the lead region from 1860 to 
October 1, 1876. The table has been prepared from the hooks of the four manufacturing 
companies, to whom I am greatly indebted for their ready codperatioa and assistance; 


Smithaonite, Blende, 

Year. lbs. lbs. 

1BG0 228: axeGabereseton in hee eee B90000° nas ev ezan 
TSG a2e3 is, Soke oeoyadak sn se) noi. ae eee 266,000 eee 
1862} avsxuerhastsichaac seas itiuearinenat Gulden. ese, 
1863 Spy sc vaeae fare ‘haven opthDac. ae doaetac es 1,120,000 we 
BEE hss once Gaede ine ied ae ee eee 3,178;388 kk eaveeye. 
OGD ste tiie Nien ae nat ncc eae dues 4,198,200 9 ...ce.eee 
18G6 sae cover cose scons esuincd mean 4 aeons TSB S88 ee ope 
TBGT siete usa os nadesereck ieee 5,181,445 841,310 
186862 6 wuesogseenaeveop devavua aaeenes 4,302,383 3,078,435 


TT SE eR oR a GE OAS SE Oe reen 4,547,971 6,252,420 


PLATE, XXXII 


OUTLINE MAP 


of thee 
LEAD REGION 
showing the several VUining Districts 


WUACES . 


aid the F 


PILLISL 9 bd HED 


za “AL fg I svhung 1 T ia 
+ At 3 . ) ‘\ 
mavshenat Ou, POW 
@ Fe P20 Bojpdarag \ 
P224ISUG Dingspprry, : \ 
4 = iN 
Cp 
99 24BS2(T| 20.4.4 ell re WS 
Shur Org yFpvq Ag 7) | aAny 
¥ aLL GAY Py pheysuy 18090, / : 
T fr 2, 
3 @ “Or 
cbasmeeny S29 eee 2. \\ 
‘eS ALT 27724 27RD, i Ty 
— Bushing Bry ree 


b—— - 


“IS2G FL, Fj 


sburbbig a} 


PA0LZ 


FILLISIC| 


Cr 


OL0) 83,107 | 


hits Ph, 


P PuOMDAA p dA0tE 2) 


, 
PIrysg usages 7) 


SIPRULNT 


So) 
ADPUAD, P07 | 


VMOTI 372) 


720-87, 


T 
7 


eee : 


(T pragybipy 


if 


sHurbbrq 40abig 


fen 
220 tL 7 @ 


PILI Hnog2ag 


‘ 
& seas I UNMTE 
: | 
9 | 
c 


5 
PIVLISIT — 7) 


a 
fon) 
ty 


‘OO LN 


Vout 


Tie Muawarner Lerao. & Evan Co. é 


STATISTICS OF THE PRODUCTION OF LEAD ORE. 743 


Smithsonite, Blende, 

Year. lbs. lbs. 
TS 10:6 ehutales oe eae sit Guns amore 4,429,585 7,414,022 
DG Tee ace secant to seadaeee nt as oe Ream 2 der ind 16,618,160 9,303,625 
TOTO in eee tana tee a iae Soc of Cutan teeta 27,694,574 16,256,970 
1S7Bac: Risener orirce aes es 20,538,946 15,089,514 
[Sida scisecgae viene cnn s0 pe eG ae4 64a kaos 15,123,050 19,500,465 
1S To Seereseeeceretet tec netsh a wets walcaen 11,878,210 20,538,190 
1876, to October Ist... 6... cece cece eee eee 12,168,540 17,181,490 

Total. Giscieu hoes Sunguisice saeesawaguanee 188,953,730 115,456,441 


The following statistics of the shipment of ores and metals over the Mineral Point 
railroad were furnished through the kindness of Mr. C. Spensley, of Mineral Point: 


Year, Lead, lbs. Zinc Ores, lbs. Spelter, lbs. Lead, White, lbs. 
TBS Tisnincaearscassinaesa ISO 490) <“aicakivasie  esactea-~- ssweeaes 
1858.00. cece ee SABI5I GrockEeg- GepescsS,  iateiace 
TBS 9 occ wees ees Q091920-  eeeseeeeeee! eeu’ ce aise 
L860 ncekcwaw mess 3,548,335 940000 twterame = sarees 
VSG Lrnssrescsisnie-asteroe 2,360,663 BOOKO0O wissas®. ciievideas 
1862. ....eeeceee SSITIEL Le rscorsens,  omuioenen  -aasiaaes 
1863. osanccsadies 2,180,570 840;000° kkhideee. 8 aed 
1864) wcccteneaeeees 1,763,769 2,380,000 sane eee cae eee 
T8635. siciaten said s 2,708,478 3,148,650 9 eeeadsey ede we maee 
L866 iia sdieisn Soares 1,837,720 5,380,000 108,400 sae anes 
IS6Tinss cctiecose 2,854,000 2,660,000 701,210 67,510 
1868) sad camiwese 6 2,854,397 4,484,000 630,580 983,010 
T96O caters: GP Gates 1,948,000 8,780,000 seveaeee 1,317,370 
1870: vaveceausiie 4,352,400 12,740,000 seas 1,360,000 
BT c eeeeacs cere 3,027,520 QITAO000 = aixcesa eel cheaters 
1872, vencieensers 3,577,777 30,900,000 wee cere tee ee eee 
IB TBs awnceteretiaacs’s 1,972,230 OTA14,000 — swilexatne «sew 
VST4isisercceieg- 4 os 3,077,020 23:022;000° eahiendee  —cdaeeeries 
1870. cokasewsewes 2,632,940 81,538,000 bse ewarn —— Sateieacene 
1876, to October 1, 2,402,000 23,538,000  aaseees wee eee 


These estimates will include the greater part of the pig lead, and the zinc ores pro- 
duced in the northern, central, and eastern parts of the Lead region; and all the spelter 
and zine white produced at the old Mineral Point Zinc Works, which have lately been 
torn down and sold. 

The statement of zinc ores shipped by the railroad is much too small to represent the 
true production of this part of the Lead region, as no allowance is made for overloading 
the cars, and for calcination, which would make the amount fully one-fourth greater. 


STATISTICS OF THE PRODUCTION OF LEAD ORE 
in the Lead Region, from January 1, 1862, to October 1, 1876. 


During the progress of this survey, much-time and care have been devoted to this 
portion of the work, in writing to and personally soliciting information from all persons 
possessed of it, and especially from the smelters. We have sought to prepare a state- 
ment of the amount of lead ore produced annually in each district, and a conbimed esti- 


mate of the total amount for the Lead region. 


744 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


Had it been possible, it would have been preferable to prepare the statement of each 
district from the mines therein contained; but it is seldom that a written account has 
been kept by the owners, of the lead ore produced from any range, mine, or diggings, 
extending back a sufficient number of years to furnish the information required. 

Statements of the production of individual mines and ranges have been frequently 
furnished, and when they were belicved to be reliable, they have been incorporated in 
the preceding part of the report. Such statements, however, are usually based on the 
memory of the persons who give them, and are therefore somewhat liable to error. 

The lead ore produced in each district is seldom exported from it as such, but is 
usually reduced by the furnaces of that district, and then exported as pig lead. There- 
fore it was believed that the most accurate statistics could be obtained from the books 
of the smelters; accordingly circular letters have been sent to each of them, to which 
in most instances they immediately responded, giving a full and complete statement 
taken directly from their books, and leaving nothing further to be desired. Some were 
unable to do so, as their old accounts were lost or nuslaid, and some, perhaps, were un- 
willing to have a detailed statement of their business published. All who did not 
respond to the circular were personally visited, and a statement giving the general 
average obtained. Although some of the individual statements herewith submitted 
may be lable to slight error, yet itis confidently believed that the estimates are, as a 
whole, rather too small than too large; and that they are as reliable as it is now possible 
to make them. We are thus enabled to give the products of the separate parts of the 
district, and a total of the whole. 

In presenting these statistics, besides the product of the furnace, some remarks will 
be added as to the localities of the mines which form its supply, and the number and 
kind of furnaces, 


BEETOWN DISTRICT. 


Commencing in the western portion of the Lead region and proceeding eastward, the 
first is the Beetown furnace, in which is smelted all the ore of the Beetown diggings, 
together with that of Muscalonge, Nip and Tuck and Hackett's diggings. 

The furnace is owned and operated by Hon. Christopher Hutchinson, by whom it was 
built in 1868. Previous to that time, all of the ore of the above mentioned district was 
smelted at Potosi. It is a reverberatory furnace, known as a Drummond, with a capa- 
city of 9,009 pounds of ore in twenty-four hours. 

It consumes one and three-fourths cords of oak wood, and is operated by two men. 
The number of pounds of lead ore smelted, from June 19, 1868, to October 1, 1876, is 
as follows: 


Year. Pounds of Ore. Year. Pounds of Ore. 
W868 i estate sae Gws 800,000 LB Bieavevsdcanneeauawes 850,000 
1860 soy daceca ume geees 1,100,000 1S Acc c aaa nates 1,000,000 
I8T0s.0%5 seaside sanaas 1,700,000 VS Nite ssereaeiecians aoeary avis 800,000 
OB Wil eiavees tease te wre erties 1,300,000 VB TGs sswwits amore renee 700,000 
TOUQ esc 2 eae sehen 2 ace 900,000 -_ 

MD otalli cts. dhs paces nata Aare ar Dama a ere ae eas 9,150,000 


PLATTEVILLE DISTRICT. 


Proceeding eastward, the next is the Platteville district, which has two furnaces, both 
near the village. Here is smelted all the ore raised in the Platteville and Whig dig- 
gings; and also that from Big Patch in the town of Smelser: 


STATISTICS OF THE PRODUCTION OF LEAD ORE. 45 


Year. Furnace No.1. Furnace No. 2 Total. 
1SG2 naiccnteas sees see ae 800,000 350,000 1,150,000 
1863 sods Ane ecko 600,000 350,000 950,000 
VS G4 sce Sais ca wtacstecaxceioten 600,000 350,000 950,000 
PSGO seh s cetevtdnanae ede 500,000 350,000 850,000 
TS OG a disteiialy erveeeeerge 3 500,000 350,000 850,000 
LSGT sis v6 82a 40d Sea Rove oneares 500,000 350,000 850,000 
LB GS sts 0.5 sue Guten toreahiasttctalie 450,000 850,000 800,000 
ASO Dias Sake creak ebnn pretemns 450,000 350,000 800,000 
TOTO isioet slaavate 4 oaretioaenicteres 450,000 350,000 800,000 
IST papesscencted.o das ovation 600,000 850,000 950,000 
IBiDii gd todaha wile ten maieales 600,000 350,000 950,000 
LSB AAG ale sucenedy aa wees 400,000 200,000 600,000 
TEei7e SOON a ety tte er eee 500,000 kee eee 500,000 
TST Diiecseleis. 08 9.2 ehe te eaunaroen 504,000 ik eee eee 504,000 
TB 16 S08 Gy iav'owSasdienladtaeets 1,044,000 eee 1,044,000 
Total vasawwuids Gasceewss 8,498,000 4,050,000 12,548,000 


The above table gives in round numbers the product of the Platteville district since 
1861; it is, however, only an approximation made by the smelters themselves, and be- 
lieved to be tolerably correct. Furnace No. 1, owned by Meésrs. Straw & Spensley, is a 
blast furnace having two hearths, and is situated about half a mile south of the village. 

Fumace No. 2, owned by Mr. Coates, is situated near the railroad depot. It is a blast 
furnace of two hearths, and has not been worked since some time in 1873. Nothing 
more than a verbal statement of its annual average could be obtained. 


POTOSI DISTRICT. 


There have been, at various times since 1861, four furnaces operating in the vicinity, 

of which only two are now worked. They are as follows, in kind and condition: 
Vance's Furnace ceased work in - - 1868 
Gibson & Co. ceased work in - - - 1871 

A. W. Emery’s furnace, situated near Rockville, is a reverbatory, with a capacity of 
6,000 pounds to every 24 hours. Thomas Hymer & Co.’s furnace, situated near British 
Hollow, is a blast furnace of one hearth. 

Previous to 1868, all the ore from the Bectown district was smelted at these furnaces, 
in addition to that which they now smelt, which comprises the mines of Potosi, British 
and Dutch Hollows, and Rockville. 

A detailed statement of the ore smelted at the several furnaces could not be obtained, 
but from the verbal statements of the several smelters, the following estimate has been 
prepared which is believed to be nearly correct: 


Povnds of Lead Pounds of Lead 
Year. Ore Smetted. Year. Ore Smelted. 
VEG Qelerarciarsiele one a seies cans 6,050,000 VS 1O.« ssi cuvececacesateiteanstooe seve 1,900,000 
1863 adie csc res eee 5,120,000 VST aisiai scp seaiscseanieisrelecs 2,230,000 
USGA dase adoapcets Re Ss 5 4,500,000 18722 semiancaconaiae ctstinetas 1,400,000 
TRGB seis ieee overt saan 5,200,000 NSD saci stet res Seo 1,500,000 
(B66 ieccnearirnaieeens 4,400,000 LST 4s veces oeeviscen ais orns 750,000 
WO6 Te siicidaaaeda sess < 3,500,000 BIO Meesireeas vlerwaseus 700,000 
TSU Reels rons aise _ 2,600,000 1876 to Oct. Ist........ 650,000 
1869: ssiecarivnvestea setae 2,200,000 ase 


Total from January 1, 1862 to October 1, 1876............. 42,700,000 


746 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


HAZEL GREEN DISTRICT. 


This district embraces all of the mines in the vicinity of the village of Hazen Green, 
and, indeed, all the ore produced between the Sinsinawa river and the Coon branch of 
the Galena river. 

The furnace is a new blast-furnace of one hearth, and a capacity of 100 pigs (of 70 
pounds each), in twenty-four hours. It is owned and operated by Messrs. Crawford, 
Mulls & Co., who furnished the following statement from their -books. It is situated on 
the Hard Scrabble branch, about a mile southeast of the village of Hazel Green. 


Pounds of Lead Pounds of Lead 

Year. Ore smelted. Year. Ore smelted. 
LSE? 3 oaicuniveus none n 2,027,047 DONO senateisrewe sinew Peo sie asses 1,223,250 
1868 sonceeteesangeans 1,262,640 LSE stacsiats apaeelosdem. eee 1,230,917 
1864 -.c4 sani ntaaeuenies 837,597 TBTD sais. ews eoasee ales 1,278,524 
IBG5itdsdasedsendee sis 758,821 1878 5 es3b dai vaconedasdes 1,046,626 
TSG6 snd ond totic 797,421 TOUR iiSiiconedan Gaaietee 830,174 
186 Tiviii srsteeunte ss 1,334,640 1875) eteocimenrk mates 735,395 
LBBB is silecgre-O tiegesce ht tie dees 1,541,670 1876, to October Ist.. ... 723,193 
1869 eacay tse oaes 1,315,970 —— 

Total from January 1, 1862 to October 1, 1876 ..........ecceoe 16,938,885 


NEW DIGGINGS DISTRICT. 


This district embraces the diggings in the vicinity of the village; all east of the Coon 
branch of Galena, river as far as T. 1, R. 2 E., and the mines in the vicinity of Benton. 
The furnace is a blast of two hearths, and is known as the Democrat furnace. It is 
situated about two miles north of New Diggings. It was worked from 1864 to 1869 by 
Mr. Geo. Wilde, of Dubuque, and since then has been worked by T. G. Stevens & Co. 


Pounds of Lead Pounds of toad 

Year. Ore smelted. Year. Ore smelted. 
1 BG Bi i diictenitsameriicrmaicao aie 1,050,000 1S Osi cts wad caeea ln arate 2,200,000 
DEG Bis sts ce scicnatea sabe euavsronaaata 1,200,000 UOT s eos asaied ede, wisiaieaea 1,700,000 
186A. Mitre edecetactonions 1,125,000 TST Daa tic ors eaves daa ve 1,650,000 
TSG is.s daneaarceanedtervererne 1,200,000 TSiBiever scutes veeasies 1,128,000 
IS66ssuiwnnneet bitewes 1,100,000 Tides haces eee eee bas 1,200,000 
196 Taavecne soci ceseens 1,150,000 TST elos ce even dnenion 1,200,000 
VS6B esse sascgucranaceyaperer siete 1,200,000 1876, to October Ist... 1,300,000 
TO ecerasasaeeeniey .- 1,100,000 ———— 

Total from January 1, 1862, to October 1, 1876............000. 19,503,000 


In addition to this, there was smelted at the Jefferson furnace, by T. G. Stephens & 
Co., as follows: 


Pounds of Ore Pounds of Ore 
Year. smelted. Year. smelted. 
1862s veces peneeseetaes 1,098,988 18E6s sits somnenneries 1,078,415 
TRS seen cly te ered 1,326,193 ARG Ti es acs eacce serra 1,050,597 
LEGA eccis aussie: aeesineais 1,112,095 TB GS ree tihies loa ysicheys 1,429,158 
LESGB onctecicshinstiae uta ates 1,078,609 O69 2: ca weustiaesice aus 1,515,323 
Mal eS elewa he Ducati aigd|s Va Pee Goren agai oA hls 9,684,333 


The furnace used was a Drummond, witha capacity of 7,000 lbs. per twenty-four hours, 


STATISTICS OF THE PRODUCTION OF LEAD ORE. T47 


SHULLSBURG DISTRICT. 


The mines embraced in this district are situated in T.1, R. 2 E., and some in the 
south part of T. 2, R. 2 E., being not a very large but quite productive district. 

There are two furnaces in operation in the district. No. 1 is now operated by My. B. 
Spensley, of Shullsburg, and was formerly owned and operated by Messrs. Quinch & 
Estey, of that place. It is a blast furnace of two hearths, situated a short distance 
west of the village, on the Shullsburg branch. No. 2 is also a blast furnace of two 
hearths, capable of smelting 12,000 pounds of ore in twenty-four hours, with six men. 
lt is also situated near the Shullsburg branch, about four miles below Shullsburg. Prior 
to June Ist, 1873, it was operated by Messrs. Joseph Hutchinson & Sons. At that time 
it was leased to Mr. Wesley Spensley, for a term of three years, and is now operated by 
Messrs. Spensley & Hutchinson. A full account has been furnished of their production. 


Pounds of Lead Pounds of Lead 


Year. Ore smelted at Ore smelted at Total, 
Furnace No, 1. Furnace No. 2. 
L862 esacedieee ox Fare Ane vncenasar en 1,000,000 800,000 1,800,000 
DBO B iocaie sin cacelgis saree a ease ela 1,000,000 700,000 1,700,000 
WSCA ass eta leok oes vie ese ais 1,000,000 400,000 1,400,000 
USGostatnteccecwaetasaae 1,000,000 1,000,000 2,000,000 
1866. c.taetes evs ens 1,000,000 1,000,000 2,000,000 
ISO Te adieu casted Vea aes 1,000,000 1,200,000 2,200,000 
WS68isscia ened rrey es - 1,000,000 700,000 1,700,000 
1869...... eran. 1,000,000 200,000 1,200,000 
US TO xacatiinccnetsc keemees 1,463,986 400,000 1,863,986 
VST Eitadectiven chen ae sha 1,250,362 400,000 1,650,362 
TO ewcensuw: seat essees 1,146,448 300,000 1,446,448 
1873 ccccesktesawt ies See 1,084,221 250,000 1,334,221 
ABTA > saiataclanpueistepnode chee 1,000,000 700,000 1,700,000 
TST cad ade sa ciaeteee aoe 900,000 900,000 1,800,000 
1876, to Oct. Ist.........- 625,000 1,000,000 1,625,000 
peoeeenent ee eee a 
Total a:cs 2226 seer sen 15,470,017 9,950,000 25,420,017 


MINERAL POINT DISTRICT. 


The ore smelted at the Mineral Point furnaces is derived from all the mines and dig- 
gings in the vicinity of the city. Ore is also brought here in many cases from long dis- 
tances. The ore of the following districts is also smelted here, viz: Mifflin, Linden, Lost 
Grove, Diamond Grove, Duke’s Prairie, and Wiota. 

There are two furnaces now in operation. No.1 owned by Mr. James Spensley is 
situated one mile west of the city, on the Spensley branch of the Pecatonica. Itisa 
reverheratory, with a capacity of 6,500 Ibs. per day. There is also a blast furnace here 
of two hearths, but it is seldom used, except for smelting slag and large ore. 

Fumace No. 2, is situated about a mile above No. 1, on the same stream, and is ope- 
rated by Mr. John Spensley. There is here a es furnace of three hearths, and a re- 

he latter is the only one now used. 
< one has been given by Mr. James Spensley of furnace No. 1, and is in- 
serted below, with the exception of the years 1862 and 1863, which pre Dee estimated 
from an average of the others. The amount of ore smelted at furnace No. 2, from 1863 
to 1872 inclusive, is estimated by Mr. John Spensley at 7,273,764 lbs. As the annual 


748 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


product in this district has been comparatively uniform, the average annual product 


may be estimated at one-tenth of it. 
The production of the Mineral Point District will then stand as follows: 


Year. Furnace No.1. Furnace No. 2. Total. 

P86? casa ae as va 8aRa wes 1 Re 1,264,562 727,376 1,991,938 
VB GB ngs gia aia) seein Gea. ayaters eases 1,264,562 727,376 1,991,938 
1864 tak posseaalieee 956,622 727,376 1,683,998 
T86O ncess es cciews es tle 1,161,682 727,376 1,889,058 
TSGB cgsicvcvecenevoes sees 1,426,682 727,376 2,154,058 
VSG Taawitawantie in hernakes 1,316,232 727,376 2,043,608 
TSG8 sess Geta: nen ne 1,525,334 727,376 2,252,710 
1869 xeeceoes senabiaacs 1,805,334 727,376 2,532,710 
IB10 cia cer eierews- eee he 1,464,930 727,376 2,192,306 
TST aes ake da menaawer 1,263,296 727,876 1,990,672 
O72 pevacanaoncs towns. 934,000 727,376 1,661,376 
ASTD wares seaiste ite ieland atic are 791,512 727,376 1,518,888 
VOTE nian ola a tawie rae cmants 900,000 950,000 1,850,000 
[Qa cedvaseaait ues cee 900,000 1,100,000 2,000,000 
1876, to Oct. Ist..... ..-- 755,350 700,000 1,455,350 


TOtal. «5 sed 2506's mere se edh din 17,730,098 11,478,512 29,208,610 


DODGEVILLE DISTRICT. 


This district comprises all the mines in the vicinity of the village of Dodgeville, Van 
Meter’s survey, and all ore raised north and east of Dodgeville. 

There are two reverberatory furnaces here. No. 1 is owned and operated by Messrs. 
Hendy & Mundy, and has a capacity of 6,000 pounds per day. This furnace com- 
menced work in 1869. No. 2 is owned by Messrs. Bennett & Georges, and has a capac- 
ity of 7,500 pounds per day. Both are situated a short distance north of the village. 
Full statements have been received from furnace No. 1, and from furnace No. 2, with 
the exception of the last three years, which have been estimated. 


Year. Furnace No.1. Furnace No. 2. Total. 

TBGDs see isiractecdicieteatiaasintee — xaos war 1,369,989 1,369,989 
1BC8 ic iicatiaacnnauaaGiad~ aden Bavcs 1,055,441 1,055,441 
1864 cin ce ndalandwadiuns. eluates 905,511 905,511 
1865: moseeenetainakestawse  warcasegs 866,407 866,407 
DOGG each tein tact aetes ieee an 1,154,298 1,154,298 
DBO Teiatissarrabivewsnn meant tex ea caes 1,191,939 1,191,939 
[268i ccraucwr wR veeeeeees aoe RES 1,046,081 1,046,081 
1B60 ecu cecal wares Mike 184,000 978,718 1,162,718 
ISTO Aauded omdomeunl ume 435,000 939,617 1,374,617 
TST was eietslaudtens eos atensetalelele ¥ 737,000 1,195,259 1,932,259 
1GTOisaesnsinceeveeessaads 934,000 902,320 1,836,320 
US Bins sicher ccrtictearaisnseereop eva tenet 626,000 815,999 1,441,999 
TIBIA. ce.chnhcasnpoe ides auestrmrkanentie 695,000 900,000 1,595,000 
ToT csevciys Aadeuusmbmerebae 340,000 900,000 1,240,000 
1876, to October Ist........ 400,000 700,000 1,100,000 


Total...cscecsssvecccsenes 4,351,000 14,921,579 19,272,579 


STATISTICS OF THE PRODUCTION OF LEAD ORE. 749 


HIGHLAND DISTRICT. 


This district comprises the mines in the vicinity of Highland, Centerville, and the 
Crow Branch diggings. The furnace is a reverberatory. The amount of ore smelted in 
the district is not very large; exactly how much could not be ascertained. It is about 
500,000 pounds per annum, or seven and a half millions since 1862. 


From the foregoing statistics, the following general results may be deduced. There 
are now seven reverberatory or Drummond furnaces in operation, with an average daily 
capacity of 7,000 pounds of ore each; and five blast furnaces of. two hearths, and two of 
one hearth each, the average capacity per hearth being 100 pigs, or 10,000 pounds of ore 
per 24 hours. In addition to these there are nine blast furnaces of two hearths each, 
not at present worked, but nearly all in good repair. Some of them have been sup- 
planted by the reverberatory furnace, which is preferred for fine ore, and some by new 
furnaces built in adjoining localities. 

Combining now the several amounts of lead ore already given as the product of the 
different districts for the several years since January 1, 1862, we find the total produc- 
tion of the Wisconsin Lead region to have been as follows: 


Total Product, Total Product, 
Year. lbs. Year. lbs. 
1869 siniicaseakica se 17,087,912 1870s sean ease 18,754,159 
1968 saat eeer ere ee 15,105,577 Tkedsested agit 13,484,210 
1864.26 ae newtdovceess 13,014,201 VOC D iis cica cmd a 11,622,668 
TOG5 chegecna lacey 14,337,895 1875 scares shee c's 9,919,734 
1866 swanerenata cannes s 14,029,192 NBA cncoatis esate 9,625,174 
WRG Uscsicdenis acete epee oe se 13,820,784 UBT D sia dase wna a ieio-8 9,179,395 
R68. sioner ee ae wees 13,869,619 1876, to Oct. Ist .... 8,747,543 
SCO cia cesses 13,426,721 —— 
Total from January 1, 1862, to October 1, 1876...........+- 190,974,784 


Besides the smelters already mentioned, there are numerous others operating outside 
of the Wisconsin Lead region, in Illinois and Iowa. The following information was ob- 
tained relative to their production: 

The parties smelting in Dubuque are: 


J. & W. G. Walters, annual amount.....-+eceeereeereeereee 900,000 ibs. 

Coates and Brunskill, annual amount......+seeeee eee ecco 900,000 tbs. 

Fern and Simpson, annual amount ...... 06+. ee eeeeereeceees 650,000 ibs. 
Parties smelting in Galena are: 

Thomas B. Hughlett, annual average since 1862 .......--.++- 1,800,000 tbs. 

Spensley's Furnace, present annual average.......-- See or 1,000,000 ibs. 
Richard Bowden, or Galena Furnace, smelted as follows: 

Year 1874. .0cceccecccctecrceseseccnenareareeteaceecesenes 930,000 ibs. 

Year 1875. ccccceeccccn ec cr ete n cere cn ece esse nanenetees 850,000 ibs. 

Year 1876, to October Ist... +... seseeeeee serene ceeeeeenees 630,000 ibs. 
Hon. Henry Green, of Elizabeth, Illinois, smelted as follows: 

Year. Pounds. Year. Pounds. 

11 6 Rees 575,113 WS2bdoxcewcawieiarce sees 615,406 

ee eon 821,720 1876, to October Ist.... 442,602 


Mr. Green remarks that seven years ago the mineral field which supplies his furnace 
produced three times as much ore as at present. 


* 


750 


GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


The amounts smelted by Richards & Co., at their fwnace in Warren, Illinois, are ap- 


proximately as follows: 


Year. Pounds. Year. 
VORB sissies eitserieraies iaigare’s 450,000 TB 7S wisisisveisceiare paras iegeave-w 
IST 4 iicinesnense nance 1876, to October Ist.... 


300,000 


Pounds. 
250,000 
200,000 


Tnasmuch as no detailed statements could be obtained from any of these parties, or 
anything more than the foregoing approximations, it is impossible to give a correct and 


reliable account of the several amounts they have smelted since 1862. 


By comparing 


their present product with that of other parties in former years, it is estimated that 
they have smelted, since January 1, 1862, about one hundred million pounds. , 

As it is a matter of interest to compare the present production of the mines with tha 
past, I have taken the liberty to reproduce the following statistics of the Upper Missis- 


sippi Lead mines, the product being given in tons of metallic lead.! 


Price per cwt. 

Year. Tons. in St. Lovie. Year. Tons. 
TE QR iis so eee ees 150 TBS D isso iwissasenies 11,976 
TOA is etiw'oiécaa's 78 TSAO ces eeeris 11,987 
1825: b cesseccs 297 1841 ......... 14,150 
L826 vse one's 428 dinase 

TB QT wialetsiacsas 2,313 $4.50 1842 sie eveees 13,992 
S28 ii sis eatin 4,958 3.30 1843 wessvesse 17,477 
1B 29 isc. seis orend 5,957 2.00 1844 ......... 19,521 
1880: ss:02a8e0s 5,081 2.13 Co ee 24,328 
1981 sqosesnces 5,369 3.00 BAG tes tater 93,513 
1832 mirais cereus 5,401 4.25 TSA Ts. die xa aac 24,145 
1833 55 ssienaiorsians 6,068 4.13 1848 2.0... a 21,312 
1884s ie asszees 7,699 4.25 TAGs aceon x6 19,654 
Saeko ota bl 8,469 5.00 T850s.000s pee. 17,768 
1836 ...... 11,390 5.13 LSSL ved e deans 14,816 
LES Tis eee sie 9,708 TBD Dc we dys eiis 12,770 
1888. ccacess 10,811 1858) -es0wavees 13,307 


Tam also indebted to Messrs. N. Corwith & Co., of Galena, for the 


densed statement of the production of the Upper Mississippi Lead mines: 


Years. Pigs. 
iS 5 ro) Lots eae eae ee eC ae Bere eee 664,118 
TBST to ICA co vcacuaanercuctactadaaes abcscwes. 1,591,950 
TOUT ate arsG ale lwkea's annnedcaenaes< waawese 6,170,357 
18510 IBBY ps eissiessecco wae cdatad cvlichecwndates 4,609,553 
TSGL TODS lisse isios o3s Sack a-<veea anes s eekan ees 2,419,985 
USB ees siaitetd as se ete 2: 408034-00aa ear 200,000 
IQIDes caine vedegeeascudesd gua eenadldeed 200,000 
BVA saree iam avnneecGeelaihe Aah ae 150,000 
W187 bi wcschae niin openenor con vaicr ace 150,000 
POO IS 1G.ohsileawaewaceexnub-de Sous ced eas 125,000 


1See Whitney’s Metallic Wealth of the United States, 1854, p. 421. 
? The weight of a pig of lead is about 72 pounds. 


Price per cwt, 
in St. Louis. 


$4.38 

4.38 

3.50 
At Galena. 


following con- 


Tons. 
23,244 
59,718 

215,979 
161,334 


CONCLUDING REMARKS. 


1 
st 
_ 


CONCLUDING REMARKS. 


In the preparation of this report, I have been actuated by many considerations which 
have to a great extent determined its character and contents, Inthe first place, the 
space which can justly be devoted to the Lead region in a report on the entire state is 
necessarily small, and involves a judicious selection of the material collected and pre- 
pared. 

In the course of my examinations in the Lead region, I have found in all places, and 
among all persons connected with the mining interests, a general expression of a desire 
for information in regard to the condition of the mining industry in those portions of 
the Lead region more or less remote from the ones in which they reside. To furnish 
such information is undoubtedly a legitimate object of a work of this kind, and to it, 
therefore, I have devoted about two-thirds of this report, reserving the remainder for 
the geological and topographical examinations contemplated by the law. 

Among other subjects which I have been obliged to omit is the much-argued ques- 
tion of mining in the Lower Magnesian limestone. No discussion of this question can do 
it justice which does not take into consideration the origin of the crevices, and the man- 
ner of deposition of the ores and assuciate minerals contained in the mines now operated, 
since these questions are the only premises from which we can derive any reliable con- 
clusions. 

The discussion of this question would have occupied more space in the report than I 
felt justified in devoting to theoretical questions, at the expense of what appeared to me 
to be important practical facts. 

The subject of drainage in our mines is one of great importance; at present it is ef- 
fected by pumping, and by levels or adits. Pumping is at best but a temporary expe 
dient, and when steam is employed it is a costly one; it effects the drainage of only a 
comparatively small area, and when the pump ceases to work, water immediately returns 
Expensive pumping operations are only warranted where large bodies of ore are known 
to exist, within a small area of ground. 

On the other hand, the drainage effected by a level is permanent and extensive, al- 
though the original outlay of capitalis large. Our mines have now been worked so long 
that it is known in each mining locality how many ranges have been worked to the nat- 
ural water level, and the comparative value of the veins of ore left in them when aban- 
doned. With this foreknowledge it is not difficult to arrange a level that will not only 
drain the previously known ranges, but will also make it possible to work any others 
which may afterwards be discovered in its vicinity; a system which is further favored by 
the well known parallelism of the ranges. 

The stratum in which levels can be most rapidly excavated, and with the least ex- 
pense, is the upper or thin-bedded portion of the Blue limestone (Trenton). There are 
no interstratified beds of clay above it, and usually nothing to prevent the drainage of 
all the Galena limestone; but as the strata sometimes contain slight flexures, it is not 
always possible to drive a level in the same formation. Levels driven in this, the upper 
pipe-clay opening have the additional advantage of proving one of the most produc- 
tive openings known in the Lead region. 

Judging from the number of levels which have been excavated, and the success which 
has usually attended them when completed, the system of mining by levels seems to 
offer the safest field for the employment of capital. seo 

The recent inventions and improvement in pneumatic, or compressed air drills, and 
in mining explosives, such as dynamite and rendrock, are daily rendering the excava- 


tion of levels a much less laborious task. 


752 GEOLOGY AND TOPOGRAPHY OF THE LEAD REGION. 


There is another method by which drainage of mines has sometimes heen effected, 
and which might in many other places be employed to advantage. It is Ly simply drill- 
ing a hole from the bottom of the mine to some of the underlying clay beds of the 
Trenton. In this way a passage is often effected for the escape of the water, of which 
it will often avail itself until the opening becomes closed with mud from the mine, when 
a new hole has to be drilled. 

In many portions of the Lead region, but more especially in the southern and centra 
parts, there is a desire which has often been earnestly expressed to me, that a survey 
should be made of the ore-bearing ranges both old and new. Such a survey, to be of 
any practical benefit, should be made with a transit and level, and with the utmost 
accuracy. It should be made underground when possible, and when not, it should be 
made on the surface, locating the ranges from the shafts. The survey of each district 
should be referred to certain fixed points, whose location and elevation should be accu- 
rately ascertained. The location of these points with reference to each other could at 
any time be ascortained by triangulation if thought necessary. The whole should then 
be mapped on a suitable scale and published with the field notes. 

The advantages derived from such a survey are chiefly the following: (1) In ranges 
which are now worked, it would be easy to reproduce on the surface the areas worked 
out below, and from the known course of the range the miner could, with considerable 
certainty, locate his shafts so as toreach the unworked portions, thus effecting a large 
saving of time, labor and money wasted in prospecting. (2) The surface of the Lead 
region is rapidly becoming an agricultural country. In many places the old shafts are 
being filled, the dump piles are being removed, and all surface vestiges of once val- 
uable ranges are becoming obliterated. Many of these ranges were worked many 
years since for lead ore alone, to the natural water level, and abandoned with valuable . 
bodies of ore still remaining in them; and in view of the increasing production of zinc 
ore, which is now between three and four times that of lead ore, it is not unlikely that 
it may become profitable to work them again. From a survey such as is outlined 
above, the location of old shafts and ranges could at any time he restored. (3) It would 
conduce to the systematic working of the mines in the future, by forming a basis to 
which private surveys could be referred, and would indicate the points where levels 
could be most successfully placed for the drainage of the mines. 

These are but a few of the advantages which will occur to persons actually engaged 
in mining. Probably there is enough money wasted in prospecting every year, which 
would he saved by such a survey, to carry it on to a successful termination. 


INDEX. 


A. 


Acknowledgments, 89, 93, 412, 651. 
Adams County, 529, 566. 
Age of Milwaukee Cement Rock, 397. 
Agriculture, 41. 
Ahnapee, elevations, 107. 
spring, 148 
river, 204. 
drift, 228. 
Albion, elevations, 435. 
Trenton limestone, 558. 
Albite, 28. 
Amphibole, 28, 
Analysis Es pane 6938. 
carbonaceous shale, 673, 680. 
cement rock, 396. 
glass rock, 681. 
greensand, 536. 
iron ore, 331, 498. 
kaolin, 468, 469, 471, 476. 
limestone, 152, 282, 284, 292, 298, 309, 
388, 345, 381, 390, 393, 399, 543, 560, 
561 


61. 
marl, Os 
pig iron, 332. 
sous, 196. 
St. Peters sandstone, 680. 
waters, 31, 146, 152, 161, 660. 
Andrews, Dr. E., 96. 
Angelica, elevations, 107. 
Lower Magnesian limestone, 283. 
Trenton limestone, 303. 
Anglesite, 29, 693. 
Annual Report of 1873, 5. 
1874, 45. 
1875, 67. 
Ansley Range, 741. 
Antisdel, 89. 
Apatite, 29. 
Appleton brick, 237. 
flux used at, 341. 
Galena ice a at, 312. 
springs at, 148. oer 
Avelieatt formations, general description, 
248, 461. 
areas, isolated, 248, 501. 
table of isolated areas, 503. 


Wis. Sur. — 48 


Arlington, elevations in, 442. 
general description, 585. 
Lower Magnesian limestone, 547. 
St. Peters sandstone, 556, 
Arrangement of report of Cent. Wis., 411. 
Arsenical Nickel, 28: 
Arsenides, 28. 
Artesian Wells, 149. 
in Auroraville, 150-159, 
Byron, 150, 155. 
Calumet, 150, 158, 
Fond du Lae, 150-154. 
Green Bay, 150. 
Janesville, 151, 166. 
Madison, 50, 533. 
Manitowoc, 150, 162. 
Milwaukee, 151, 164, 336. 
Oakfield, 150, 155. 
Oshkosh, 150, 151, 155, 158. 
Palmyra, 151, 161. 
Poysippi, 150-159. 
Racine, 151, 163. 
Rushford, 150, 159. 
Sheboygan, 151, 164. 
Taycheedah, 150, 154. 
‘Watertown, 150, 160. 
Whitewater, 150, 162. 
eee Union Junction, 151, 162, 


possibilities of obtaining, at other 
points, 167. 
Ashford, elevations, 107. 

Niagara limestone in, 350, 356. 
Ashippun, Cincinnati shales in, 317. 
Niagara limestone in, 340, 343. 

Aephal vom, 29, 
Auburn, elevations in, 107. 
Aurora, Artesian wells in, 150, 159. 
cranberries in, 186. 
Avon, elevations in, 107, 169. 
Aztalan, elevations, 107. 
Trenton limestone in, 801. 


B. 


Bacon, os 98, i 
Baileys Harbor, 
No aeen limestone at, 352, 358. 


T54 


Ballard Range, 742. 
Bar, 691. 
Baraboo, 595. 
ranges, 427, 504, 523. 
elevations, 446. 
river, 420. 
Barite, 29, 693. 
Bark river, 136. 
ee cote! Observations, 106, 429, 


Barry, Rev. A.C, 152. 
Bartholomew Ss Bluff, 264, 265. 
Barton, elevations, 107. 

Bass Lake, 1389. 

Beach Formation, A, 219. 

B, 224. 

C, 225. 

D, 225. 

Beach line, 131, 226, 228. 

elevations of, 228. 

Bear Lake, 140. 
Beaver Dam, elevations, 107. 

peat in, 244 

springs in, 143. 

Trenton limestone i in, 301. 
Beetown District, 695, 744. 
Belgium, elevations, 107. 
Bellevue, elevations, 107. 
Beloit, elevations, 107. 

dnft, 213, 215, 226. 

Trenton limestone in, 292, 297, 298, 


Berlin, Springs, near, 142, 149. 

red clay at, 223. 

oka i ‘319, 520. 

orphyry a 

Posdan sandstone, 267, 
Big Bend, Oconto river, 267. 
Big Bull Falls, 486, 494, 

Big Foot Prairie, 136. 

Black Creek, 281. 

Black lead, 27. 

Black river, 421. 

Black River Falls, 493, 546, 565. 

station, 499. 
Blaney, J. V. Z., 35, 146, . 

Blende, Black J ack, 28. 
Bloomfield, elevations, 107. 
Blue Beds, pa 291, 296. 
Lower, 291, 2 
Blue limestone, OL, 560, 680. 
Blue Mounds, 661. 
Bode, Gustavus, analyses by, 30, 35, 72, 
86, ’g8, 146, 164, 282, 309, asi, 390, 393° 
Borings i in peat, 242-245, 
Bornite, 692. 
Bowlders, 208, 218, 618. 
of clay, 210. 
of gravel, 219. 
Bowlder Clay, 217, 220. 
Bow’s Hill, 266. 
Bradford, elevations, 107. 

(salena limestone in, 308. 
Brandecke, Dr. L., analysis by, 161. 
Brick, manufacture of, 235, 630, 665. 

fire, 470) 

Brighton, elevations, 107. 


GEOLOGICAL SURVEY OF WISCONSIN. 


Brillion, elevations, 107. 
marble, 347. 
Bristol, 601. 
elevations, 107, 108, 441. 
Lower Magnesian limestone i in, 547. 
Brooks, Maj. T. B., 45, 60, 64, 72. 
survey ot 1874, 60. 
Brookfield, elevations, 108. 
Brooklyn, springs in, 149. 
Lower Magnesian limestone, 277. 
Brown, Rev. W. F., 93. 
Brown’ county, Cincinnati shales i in, 318, 
Brown Deer, 397, 399. 
Brown Rock, 291, 695. 
Brown’s Lake, 140. 
Buckert’s Fountain, 161. 
Buell, I. M., 
Buff limestone, 291, 560, 680. 
Buff beds, Ups, 291, 293, 
Lower, 291. 
Buildin Mee 249, 284, 290, 304, 308, 
ae 342, 347, 382, 388, 545, 5B, 562, 669, 


Bull Fails, 483. 
Burnett, elevations in, 108. 
Burlington, dritt, 203, 206, 208, 211, 212. 
elevations, 108. 
Niagara limestone near, 372. 
Burke, 601. 
elevations in, 439. 
Byron, 135 
Niagara limestone in, 344. 
Springs in, 148. 
Artesian wells in, 150, 154, 155. 
Byron Beds, 835, 345-348, 384, 


C. 
Calcite, 29, 693. 
Calamine, 29, 693. 
district, 739. 
Calamus, elevations, 108. 
peat, 244. 


‘Trenton limestone in, 277. 
Caledonia, elevations, 108, 443. 
cranberries, 186. 
Lower Magnesian limestone in, 277. 
Potsdam sandstone in, 589 
quartzite, 504, 512. 
Calumet, elevations, 108. 
Artesian wells i in, 150, 158. 
Cambria, 544. 
Camp bake, 136. 


Cam mn aes 569. 

Canfield H., 412, 515. 

Canal from Lake Michigan to Mississippi 

river, 420. 

Carlton, elevations, 108. 
Niagara Ameen, 378, 379. 

Carr, E. S., 

Cascade Falls, 318, 333. 

Casco, elevations, 108, 213. 
Niagara limestone in, 354. 

Castle Rock, 6 

Cedar Creek, a 

Cedar Lake, 140, 


INDEX. 


Cedarburg, elevations, 108. 
spring, 108, 149. 
building stone, 383. 
Niagara limestone at, 362, 878, 379. 
Celestite, 29. 
Cement Rock, 295-405. 
Center, elevations, 108. 
Trenton limestone in, 303. 
Centerville, elevations, 109. 
Dritt in, 228. 
Centerville District, 722. 
Centralia, 475, 530. 
Central Wisconsin, report on, 407-639. 
District, 410. 
Area ot, 409. 
Surface features, 413, 424. 
River systems, 413. 
Watersheds of, 424. 
Former drainage of, 426. 
oe of topography to geology, 


Geological formations of, 448. 
Drift and drittless areas, 448. 
Vegetation and soils, 449. 
Topographical subdivisions, 453. 
General geological structure of, 457. 
Archean rocks of, 461-524. 
Lower Suurian rocks of, 525-607. 
Potsdam sandstone of, 525-547. 
er Magnesian limestone of, 547- 
555. 
St. Peters sandstone of, 555-558. 
Trenton limestone of, 558-562. 
Galena limestone of, 562. 
Local details, Silurian formations, 
563, 607. 
Quaternary deposits, 608-632. 
Microscopic lithology, 637-639. 
Cerussite, 29, 694. 
Chalcopyrite, 28, 693. 
aE a : ve 
Chalybeate Springs, 148. 
Charaherlin, J. HL, v., 52, 93, 106. 
Chamberlin, T. C., 6, 44, 46, 64, 65, 66, 
71, 85, 427, 502, 504, 506, 521, 542, 543, 
553, 557, 559, 673. 
Party of, 1873, 8. 
Party of, 1874, 51. 
Champlain, 219, 224. 
Chandler, Dr. C. F., 146, 165. 
Charlestown, elevations, 109. 
Chert, 268. 
Chilton, 108 2 
Chimneys, ae 
Christiann, elevations, 170, 436. 
Trenton limestone in, 558. __ : 
Cincinnati Group, in Eastern Wisconsin, 
814-326. . 
in Lead region, 689. 
Fossils in, 315, 320. 
Clark County, general, 563, 
Special references, 461, 529, 541. 
Clay Banks, elevations, 109. 
Clear Lass 140. 
fton. 2 
Sepa made at, 238. a 
Cincinnati formation at, 518. 


aT 
Or 
Or 


Clifton, Niagara, limestone at, 339. 
Clinton, elevations, 109. 
Jron ore deposit, 327-335. 
Clyman, elevations, 109. 
Coal, 316, 317. 
Cobb, J. M., 171. 
Cold Spring, elevations, 109. 
Columbia County, general, 579. 
epeqal references, 529, 532, 534, 547, 


Columbus, elevations, 442. 
Lower Magnesian limestone in, 547. 
St. Peters sandstone in, 556. 
Como Lake, 139. 
Comstock, Gen. C. B., 61, 104. 
Conant’s Rapids, 478, 564. 
Concord, elevations, 109. 
Cranbernes in, 186. 
Conglomerate, 254. 
Conover, A. D., v, 9, 651. 
Cooperstown, elevations, 109. 
Niagara limestone, 350, 354, 383. 
Copper, 27, 210, 619. 
Carbonate, 28. 
in Lead Region, 741. 
Copperas, 29. 
Coral Beds, Upper, 335, 351, 357, 384. 
Lower, 335, 348, 351, 384. 
Coral Reefs, 369-371. 
Cottage Grove, 600. 
Elevations, 437. 
St.Peters sandstone in, 556. 
Courtland, elevations, 444. 
Lower Magnesian hmestone in, 547. 
St. Peters sandstone in, 556. 
Trenton limestone in, 558. 
Cranberries, 182, 186, 187. 
Crawford, J. W.T., 9. 
Crevice, 689. 
Cross Plains. elevations, 436. 
St. Peters sandstone in, 556. 
Trenton limestone in, 559. 
Cuprite, 28. 
Current, along shore of Lake Michigan, 
130, 182. 
Cyanite, 29 


BIN 


Dale, elevations, 109. 

Dalles of the Wisconsin, 570. 

Dana, Prof. J. D., 79, 370. 

Dane, elevations, 170, 440. 
Lower Magnesian in, 547. 

County, general, 597. : 
Special references, 529, 534, 558. 
Daniells, Prof. W. W., analyses by, 6, 60, 

64, 72, 284, 285, 339, 345, 381, 680. 
Daniels, Edward, 68, 69, 95, 647. 
Darien, 206. 

elevations, 109. 
Darlington, 681. 
Darwin, Chas., 370. 
Davies, Prof. J. K., 26, 6 
Davis, W.N., 158. 
Day, Dr. F. H., 369, 871. 


756 GEOLOGICAL SURVEY OF WISCONSIN. 


Dayton, Mendota bods, 266. 
Deerfield, elevations, 438. 

St. Peters sandstone in, 556. 

Trenton limestone in, 558. 
Dekorra, elevations, 438. 
Delavan, clevations, 109. 

Springs, 147, 149. 

Lake, 136, 139. 
Delafield, Sane 105, 213. 

Springs, 31, 

Cragtieteen 186. 

Drift, 211. 

Niagara limestone in, 339, 343. 
Delona, elevations, 447. 
Dendritic Markings, 550. 
De Pere, elevations, 109. 

Galena limestone, 312. 

Cincinnata shales, 318. 

Tron ore, near, 333. 
Devil’s Lake, 507-511. 
Devonian, 395-405. 
Diagonal valley, 99. 
Diggings — 

oi ans & Bowilen, 120, 

Adkinson, 698. 

Alderson, J, 700. 

Anthony & Dixon, 709. 

Arthur & Co., 698, 736. 

Ashworth, E., 712. 

Baderott, 737. 

Brainbridge, 718. 


Brainbridge, Mundy & Maighn, 718. 


Brainbridge & Vipond, 718. 
Bennett & Brady, 735. 
Bennett & Co., 735. 

Benton District, 717. 
Biddick, 738. 

Big Patch, 721. 

Big Pump, 706. 

Bininger Range, 706. 

Black & Co., 701. 

Blackney, Donahue & Co., 723. 
Bohan & Co., 735. 

British Hollow, 700. 

Brown Bros. & Parish, 696. 
Brown & Co., 739. 

Brown & Cluthers, 737. 
Brown, Dodge & Co., 710. 
Bull Pump Range, 706, 717. 
Buncome, 708. 

Cain & Read, 738. 
Calamine, 739. 

Carpenter & Bennett, 708. 
Carter & Owens, 731. 
Carter & Samuels, 722. 
Catchall, 712. 

Centerville, 722. 

Champion, 710. 

Chandler's, 707. 

Clark’s, 706. 

Clayton & Co., 739. 
Clebenstein, 738. 

Clegg, Samuel, 731. 

Conly & Sons, 738. 
Connaughton & Casserly, 735. 
Cox & Sons, 733. 

Craig, 710. 


Diggings — continued. 
Craig Level Co., 710. 
Craig, Sanders & Campbell, 710. 
Crossly, J. & Co., 696. 
Crossly & Bass, 696. 
Curmow & Pillow Range, 700. 
Davis & Co., 725. 
Dawson's, 709. 
Diamond Grove, 738. 
Dilger, 700. 
Dodgeville District, 730. 
Drybone, 709, 716. 
Drybone Hollow Range, 723. 
Duncan Range, 720 
Dunn & Son, 737. 
Dunstan Range, 725. 


_~ Dutch Hollow, 701. 


Dutch Hollow Level Co., 701. 

Dutch Lot, 711. 

Dutch Range, 721. 

Edwards Estate, 707. 

Edwards, John, 706. 

Emery & Davis, 700. 

Eustice, Richard & Co., 706. 

Eustice, W. H. & Bro., 707 

Aad a ley 
airplay Level Co., 704. 

Farwell & Co., 782. 

Flynn, Lynch & Co., 724. 

Frame & Co., 740. 

Furfee & Co., 739. 

Garden & Son, 739. 

Gillian, Henry, 700. 

Gillis Range, 720. 

Goldsworthy & Bro., 736. 

Goldsworthy & Hocks, 737. 

Graham Mining Co., 697. 

Grant, 699. 

Greenwood & Miller, 709. 

Griswold, 700. 

Hackett’s, 767. 

Hall & Rain, 712. 

Hamilton, 740. 

Harper, Hird & Co., 711. 

Harris & Long, 736. 

Harris & Stanley, 725. 

Harvey, 718. 

Hawlans, Thos., & Co., 721. 

Hazel Green Mining Co., 707. 

Hayward Range, 700. 

Hendy, Davey, Sobey & Co., 731. 

Heller & Parish, 722. 

Hicks, Fiddick & Co., 708. 

Highland District, 723. 

Hinderliter & Sons, 723. 

Hitchins & Terrill, 733. 

Hoare Bros., 736. 

Hornsnoggle Ridge, 726. 

Howe & Alderson, 712. 

Hutcheroft & Thomas, 698. 

Hutchinson, Dewey & Co., 698. 

Huxtable & Son, 633. 

Trish, 716. 

Jacobs, R. 8. & W. J., 729. 

Jacka & Waggoner, 733. 

Jackson & Co., 734. 

Jeffrey & Bro., 737. 


INDEX, 57 


Diggings — continued. 


Jeftrey & May, 737. 

Jenkins, Miller & Co., 722. 
Johns & Harvey, 708. 

Jones, Hugh, 731. 

Jones, Farrager & Owens, 780. 
Joseph, H., 788. 

Kessans, Barney, 709. 
Kesting, Hines & Co., 709. 
Lambly Range, 731. 
Langstaff & Gillan, 701. 
Leakeley Estate, 712 

Level Company, 719. 

Linden District, 726. 

Linden Mine, 726, 

Loomis & Co., 698. 

Lost Grove, 739. 

Lutey & Co., 736. 

Maguire, Kennedy & Co., 723. 
Mankey & Son, 737. 
Manning & Delaney, 726. 
Manwamng & Madison Range, 706. 
Martin & Cramer, 738. 
McBreen & Co., 707. 
McCaffery, Smith & Co., 719. 
McCoy Water-wheel Range, 706. 
McDermott & Co., 739. 
McElroy Bros., 719. 

MeNulty, 714. 

Meloy & Fox, 716. 

Meredith, 699. 

Messersmith Range, 720. 
Metcalf, Harker & Alexander, 718. 
Mifflin, 721. 

Mills, Gabriel, 708. 

Mineral Point District, 733. 
Mincral Point Mining Co., 735. 
Missouri Range, 720. 

Mitchell & Pollard, 734. 
Moffat & Co., 707. 

Monroe, 740. 

Morrison, D., 729. 

Mulligan & Francis, 723. 
Muscalunge, 697. 

Nichols & Holmes, 736. 

Nip & Tuck, 697. 

Oakland Mining Co., 717. 
Oates & Eustice, 706. 

Opir & Lancaster, 738. 

Owens & Powell, 730. 

Pascoe & Collins, 733. 

Peak & Blair, 701. 

Pearce, Jos., 731. , 

Pearce & Son, 739. 
Penitentiary, 721. 

Phillips & Walker, 699. 
Phenix Mining & Smelting Co., 713. 
Pierce & Trewather, 707. 
Pigeon, 697. 

Platteville District, 719. 
Porter's Grove, 732. 

Powell & Co., 738. ‘ 
Poad, Barrett & Tredinnick, 728. 
Prideaux & Henry, 736 
Pridcaux, Wm., . 

Prisk & Coad, 734. 

Prisk & Paynter, 734. 


Diggings — continued. 
urcell & Hardin, 740. 
Rain, J., & Co., 712. 
ere Young & Jenkins, 722. 
aspbe ange, 712. 
Richards, 735. . ‘i 
Richards & Burns, 733. 
Richards & Faul, 729. 
Rickert, Stephens & Co., 714. 
Ridgeway Mine, 732. 
Ridgeway Mining Co., 740. 
Rigger & Arthur, 739. 
Ritter & Bock, 698. 
Robarts Range, 729. 
Robbins & Bros., 712. 
Robinsons, 724. 
» Robbins Range, 720. 
Rockville, 699. 
Rogers & Mankey, 737. 
Ross, J. J., 735. 
Rowe & Co., 725. 
Rowe & Rowe, 706. 
Rowe & Vivian, 707. 
Rup & Son, 701. 
Schlosser & Co., 739. 
Shepard & Co., 788. 
Shields & Linden, 783. 
Short & Co., 735. 
Short & Foster, 737. 
Showalter & Payton, 698. 
Shullsburg District, 713. 
Siddell & Co., 724. 
Silverthorn, 716. 
Simmons & Sons, 708. 
Sinapee, 734. 
Skinner, Peter, 707. 
Smith & Anderson, 740. 
Smith Range, 721. 
Spensley & Brown, 738. 
Spensley & Co., 724. 
Spensley, Winn & Co., 709. 
Stone & Bryhon, 700. 
Stopline, 713. 
Suthers & Co., 786. 
Swindlers Ridge, 718. 
Tamblin, Thos., 729. 
Ternll & Badger Ranges, 733. 
Thomas & Co., 698. 
Treglowns & Wicks, 729. 
Thrasher Bros., 739. 
Trewilla & Strong, 787. 
Torneal, 707. 
Union Mine, 732. 
Van Meters Survey, 732. 
Vivian & Sleep, 737. 
Warfield Range, 700. 
Watkin Range, 731. 
Whig, 720. 
White & White, 740. 
Wilcox, 696. 
Wilkinson & Cronin Range, 721. 
Williams & Bro., 707. 
Williams & Oo., 703. 
Williams & Edwards, 724. 
Williams, Evan, 730. 
Williams, M. J. & Co., 719. 
Wiota, 740. 


758 


ggings — continued, 
eae & Co., 735. 
Yellowstone, 739. 
Zig, 701. 
Districts, Eastern Wisconsin, 94. 
Central Wisconsin, 409. 
Lead region, 645, 689. 
Dodge county, 143, 170, 271. 
drift in, 203, 215. 
St Peters sandstone, 286, 287. 
iron ore, 328. 
Dodgeville district, 730, 7 
Dolomite (see ee 8, 339, 693. 
Domes of rock, 202. 
Door county, 225, 368. 
Dorward’s Glen, 511. 
Dover, elevations, 109. 
Drainage, Eastern Wis., 128. 
Central Wis., 413. 
Lead region, "652. 
Changes in, 174, 657. 
Drift, Eastern Wis., 199-239. 
Central Wis., 608-632. 
Lead region, 665. 
Driftless region, 608, 632, 665. 
Drift soils, 189. 
Duck Creek, building stone, 308. 
Galena limestone, 312. 
Dunes, 233. 
Dunkirk, elevations, 434. 
Lower Magnesian limestone in, 548. 
Trenton limestone in, 558. 
Dunn, elevations, 436. 
Lower Magnesian limestone in, 548. 


E. 


Eagle, elevations, 109. 
cranberries, 186. 
drift, 209-211-212. 
Cincinnati shale, 316. 
Niagara limestone, 340, 342. 
East Troy, elevations, 109. 
Castleman’s quarry, 203, 359. 
Eastern Wisconsin district, 91. 
Acknowledgments, 93. 
Extent of district, 94. 
Previous publications relating to the 
region, 99. 
Topography, 97. 
Elevations, 106. 
Hydrology, drainage, 128. 
Origin ed geological relations of 
lakes, 137. 
Water supply, 141. 
Artesian wells, 149. 
Water power, 171. 
Changes in drainage, 174. 
Native vegetation, 176. 
Soils, 188. 
Quaternary formations, drift, 199. 
Glacial drift, Kettle Range, 205. 
Bowlder Clay or Tull, 217. 
Modified drift, Champlain, Beach For- 
mation A., 219. 
The Lower Red Clay, 221. 
Beach Formation B., 224. 


GEOLOGICAL SURVEY OF WISCONSIN. 


Eastern Wisconsin ie tick _ continued. 
Upper Red Clay, 225, 
Beach Formations C. and D., and Mod- 

ified Red Clay, 225. 
Terraces, 22. 
Lake encroachnient, 230. 
Dunes, 233 
Erosion and deposit in progr 
Industrial value of drift, 
Brick, 235, 
Shell marl, 239. 
Peat, 240. 
Table of formations, 247. 
Archean formations, 248-256. 
Lower Silurian. Potsdam sandstone, 
257-267. 

Lower Magnesian limestone, 268-285. 
St. Peters sandstone, 285-290, 
Trenton limestone, 290-305 
Galena limestone, 305-314. 
a shales and limestone, 314, 
VEE Silurian. Clinton iron ore, 327, 


Niagara limestone, 335-389. 
Lower Helderberg, 390-394. 
Hamilton cement rock, 395-405. 
Eaton, elevations, 109. 
Eaton, Prof. J. H., 49, 412, 504, 594. 
Eau Claire river, "486. 
Economic considerations, drift, 234-630. 
Archzean formations, 465. 
Potsdam, 545 
Lower Magnesian ae a 284, 554. 
St. Peters sandstone, 290. 
Trenton limestone, 304, 652, 683. 
Galena limestone, 307, 683 
Cincinnati shales, 316. 
Clinton iron ore, 327. 
Mayville beds, 340. 
Lower coral beds, 349. 
Mean Racfne and Guelph beds, 


Lower Helderberg, 394. 
Hamilton cement rock, 400405, 
Eden, elevations, 109. 
Niagara limestone in, 344-346. 
Edgerton, 338. 
Edgerton, B. H., survey, 14. 
Egg Harbor, 204, 228. 
elevations, 109, 229. 
Elevations, Eastern Wisconsin, 106. 
Central Wisconsin, 428. 
Lead region, 650. 
Oconto county, 14. 
of lakes, 28, 24. 
of summits, 24. 
of beach ridges 228, 229. 
ot junction St. Peters and Trenton, 169 
R. R., 16-23. 
Madison to Eloy, 429, 
Elroy to Mermillon, 480. 
Waterloo to Madison, 430. 
Edgerton to place Earth, 450. 
el Douglas to Randolph, 431, 
Tomah to Wausau, 431. 
Amherst to Merrillon, 482. 


8, 233. 


INDEX, 


Elevations — continued. 
Portage to Stevens Point, 433. 
Been Det to N. line of township, 


Elba, elevations, 109, 170. 
Lower Magnesian limestone in, 472. 
Trenton limestone, 301. 
Elizabeth Lake, 139. 
Elkhart Lake, 140. 
Elkhorn, 212. 
Ellington, springs, 149. 
Lower Magnesian limestone, 280. 
Emmet, elevations, 110. 
Empire, elevations, 110. 
springs, 148-149. 
jagara limestone in, 344, 346. 
Encroachment, Lake, 230. 
End, Hon. George, 164. 
Epidote, 28 
Erin, elevations, 110, 213. 
Erosion in progress, 233. 
Eureka, 276. 2 
Excelsior, elevations, 447. 
quartzite, 504. 


F. 


Fairfield, elevations, 447. 
Fairchild, Gov. L., 71. 
Fairplay district, 701. 
Farmington, elevations, 110. 
Fault, 280, 289, 332. 
Featherstonhaugh, G. W., 67, 95. 
Feldspar, 28. 
Fertilizer, peat as, 245. 
shell marl, 239. 5 
Fiord features, 202, 204, 205. 
Fire brick, 470. 
Fish creek, 204, 228, 229. 
Fish remains, 396. 
Fisher, Prof. Davenport, 49. 
Fitchburgh, elevations, 435. 
St. Peters sandstone in, 556. 
Trenton limestone in, 558. 
Flintville, Galena limestone at, 313. 
Fluvial pairs, 136. 

Flux, 332, 338, 341, 365, 383, 562. 
Fond du Lac county, 143, 170, 206. 
Artesian wells at, 150, 151. 

Galena limestone at, 310. 
Niagara limestone near, 346. 
Building stone near, 343. 
Forests, 177, 175, 449, 660. 
removal of, 175. 
Forrest, elevations, 110. 
Forrestville, elevations, 110. 
Niagara limestone in, 352, 354, 
Formations of Eastern Wisconsin, 247. 
Central Wisconsin, 460. 
Lead region, 668 
Fort Winnebago, 585. 


ion, 444. 
F oscil of drift material, 209, 210, 213. 


dam, 245, 261, 262, 670. 
2 Sore Mogens 271, 276, 283, 554, 


675. 


759 


Fossils — continued. 
of St. Peters, 288, 558. 
of Trenton, 292, 294, 296, 299, 320, 561. 
of Galena, 307, 314, 320, 685. 
ot Cincinnati, 315, 316, 320. 
of Mayville beds, 339, 340. 
of Byron beds, 346. 
ot Lower coral beds, 349. 
of Upper coral beds, 351, 353. 
of Waukesha beds, 858, 359. 
of Racme beds, 372, 377. 
of Guelph beds, 379, 380. 
of Niagara group, 384. 
of Lower Helderberg, 392, 393. 
ot Hamilton, 396, 399, 400. 
Foye, Prof. J. C., 172. > 
Fox Lake, elevations, 110, 170. 
Trenton limestone in, 301. 
Galena limestone in, 310. 
Fox River, 100, 420, 422, 423. 
elevations of, 424. 
Illinois, 129. 
Fountain, 568. 
Fountain prairie, elevations, 443. 
Lower Magnesian in, 547 
Fountains. See Artesian. 
Franklin, elevations, 110, 111, 445. 
Freedom, elevations, 446. 
Quartzite in, 504, 518. 
Fredonia, elevations, 111. 
Milwaukee river in, 131. 
Lower Helderberg in, 392-394. 
Fort Atkinson, Trenton, 301. 
Galena limestone in, 309. 
lime, 308. 
Fuel, peat as, 245. 
Fulton, elevations, 111, 169. 
Trenton limestone in, 300. 
Furnaces, iron, 332. 
lead, 749 


G. 


Galena limestone in Eastern Wis., 305. 
in Central Wis., 562, 562. 
in the Lead Region, 683. 

Galenite, 28, 554, 672. 

Garnet, 28. 

Garrison, C. B., land of, 476. 

Gault, J. C., 162. 

Geikie, Prof., 208. 

Geodetic survey, 25, 62. 
Geology of Eastern Wisconsin, 91. 
of Central Wisconsin, 407. 

of Lead Region, 643. 
Geological relations of lakes of East- 

ern Wisconsin, 137. 

Genesee, elevations, 111. 

Niagara limestone in, 359, 383. 

lime, 383. 
Geneva Lake, 136-139. 
Germantown, elevations, 111. 

Niagara limestone in, 363, 364. 
Gibson, elevations, 112. 

Niagara limestone in, 352, 354. 
Gibralter Bluff, 587, 


760 


Gillette, slenaihons, 112. 
Gillet, E. J., 
Gillmore, on a. A., a 401, 405. 
Glacial drift, 205, 630, 
features, "98, 130, 13 “t37, 139, 199. 
lakes, 139 
movements, 199. 
striee, 200, 201, 205, 625. 
Glass rock, 991, 695. 
Glass sand, 290, 558, 546. 
Glauconite, 29, '959, 961, 536. 
Gneiss (see ‘Archean rocks), 463, 501. 
Gold, 27, 466. 
Gouge, 691. 
- Government surveys, 24. 
Grafton, elevations, 112. 
Niagara limestone in, 862, 372, 377, 
7 
Grand Chute, springs, 148. 
Granite (see Archean formations), 248, 
463, 501, 521. 
intrusive, 463, 
Marion, 552. 
Mukwa, 248. 
Grand Rapids, 188, 284, 471, 477, 530, 
546, 564, 
Granville, elevations, 112. 
Niagara limestone in, 365, 377, 379. 
Lower Helderberg limestone, 391. 
Hamilton cement rock, 339. 
Grant river, 656. 
Graphite, 27. 
Gray. Hon. H. H., 742. 
Green Bay, 187, 318, 334, 
elevations, 113. 
Artesian wells, 150. 
peninsula, 201, 202, 204, 342, 346, 363. 
valley, 99, 129, 199, 200-202, 923. 
valley, cause of, 101. 
river system, 129, 182. 
Green Lake, 138, 139, 266, 529. 
county, 578. 
county, drift in, 217. 
Potsdam sandstone in, 264. 
Lower Magnesian limestone in, 272. 
St. Peters sandstone in, 289, 
Trenton limestone in, 301. 
Green Rock, 291, 695. 
Greenbush, elevations, 113, 
drift in, 211. 
Greenfield, elevations, 113, 44 
Niagara limestone in, 460, 369, 872. 
lime, 882 
quartzite, 504. 
general description, 594, 
Guelph limestone, 335, 377-383, 384. 
Gypsum, 29, 315, 319. 


H. 


Hackett’'s district, 659. 

Hagerman, J. J., 470. 

Hall, Prof. J., 69, 95, 351, 411, 504, 527, 
528, 545, 559, 649, 687, 

Hamilton cement rock, 395, 405. 

Hamilton, or Lower Helderberg ?, 79. 


GEOLOGICAL SURVEY OF WISCONSIN. 


Hampden, Lower Magnesian limestone in, 
547 


St. Peters sandstone in, 556. 
Trenton limestone in, 558. 
Harmony, elevations, 114. 
Hartford, elevations, 114, 213. 
springs in, 149 
Cincinnati shales in, 317. 
iron ore in, 332 
Niagara limestone in, 340, 3438. 
Haven, Geo., 55, 65. 
Hebron, elevations, 114. 
cranberries, 186. 
Helderberg, Lower, 79, 390. 
Hematite, 28, 329, 693. 
Henry, W. T., 680. 
Herman, elevations, 114, 
springs my 148, 149 
drift in, 2 
Cincinnati shales in, 318. 
Highland eerie aa 749. 
Hiner, Hon. W. H., 153. 
History of previous ie veys, 67. 
Hitt, H. D., 155. 
Hogsbacks, 207. 
Holden’s Lake, 139. 
Holland, elevations, 114. 
Honey Greek (Walworth county), 129. 
(Sauk county), 591. 
elevations, 446. 
a uartzite, 518, 504. 
otsdam. ’sandstone, 582, 534. 
Lower Magnesian limestone, 552. 
Hood, G. R., 328. 
Horicon mar sh, peat, 343. 
Niagara limestone near, 344, 
a (see Archean rocks in text) 


Hortonia springs, 142, 148, 149. 
Lower Magnesian limestone, 277. 
Hoy, Dr. P. B., a 163, 934, 821. 
Hoyt, Dr. J. W., 
Hovey, W. A., Bae 
Hubbard spriny s, 149. 
iron ore, 328. 
Hubbs, Rev. G. S., 253. 
Humphreys, Gen. A. A., 61. 
Hunt, Dr. H., 136. 
Hunt, Dr. T. 8., 585. 
Hunter, Geo., fountain of, 151. 
Huronian, 251, 465. 
Hutchinson, K. M., cn 
Hutchinson, Hon. G., 
Hydranlic lime, 284, oe, 305, 341, 400 


Hydr aia compounds, 29, 
Hydrology, 128. 
Hydrozincite, 28. 


rT, 


Industrial value, see Economie consid- 
erations. 
Introduction to report of Central Wis., 


ee Wis., 93. 
Lead region, 645, 


INDEX. 


Intrusive granite, 463. 
Iron, 27. 
Carbonate, 29. 
Ore, 28, 327, 334, 498, 546. 
Sand, 292, 259, 
Sulphate, 29. 
Ironton, Potsdam sandstone, 532. 
Irving. R. D., 6, 44, 46, 64, 66, 71, 206, 
260, 261, 332. 
Party of 1873, 7. 
Party of 1874, 46. 
On Central Wis., 497. 
Isolated ridges, 428. 
Arcnwean areas, 501. 
Ives, Frank, survey of, 63. 


J. 


Jackson, 114, 115. 
County, 461, 529, 541, 563. 

Jacksonport, elevations, 115. 
Niagara limestone near, 354. 

Janesville, elevations, 115. 
Artesian well at, 151, 166. 
Trenton limestone at, 300. 

Jefferson, elevations, 115. 
County, 140, 143, 170, 215, 271. 
Galena limestone in, 309. 

Jenney, F. B., 7. 

Johnson, J. H., 156. 

Johnson, Prof. 8. W., 197, 245. 

Johnstown, 115. 

Jordan, 181. 

Junction City, 481, 482. 

Juneau county, 529, 533, 566. 


Ki 


Kaolin, 466, 467, 468, 469, 470, 471, 476. 
Kaukauna, building stone, 308 
Galena limestone at, 312. 
Kendal Range, 741. 
Kenosha County, 130, 139, 163, 211. 
Kettle Range, 105, 200, 201, 205, 615, 680. 
material of, 208-210, 618. 
structure, 210. ' 
relative abruptness of sides, 211, 
general relationship, 212 
summit altitudes, 213. 
origin, 210-214, 630. 
Kettles, 206, 214. 
Kewaunee, elevations, 115. 


brick, 237. 
Nisbet limestone in, 352, 354, 368, 


372. : 

County, 211, 225. 
Kewaskum, elevations, 115. 

Niagara limestone in, 350, 356. 
Kennicott, Robert, 96. 
King, F. H., 8, 53, 55, 66, 93, 318. 
Kingston, Potsdam sandstone, 264. 
Knapp, Capt., 89. 
Kni nt EA G 
Knobs, 676. : 
Knowledge, Importance of Geological, 13. 


Knowlton, 482, 483, 530. 
sehikonong, elevations, 115. 
e, 188. 


iak 

renton limest i 

Kossuth, aaa one in, 300. 
L. 


La Grange, 316. 
Springs in, 148, 


» oll, 
Labradorite, 28. 
Lake, Town of, 115. 
Bear, 140. 
Bass, 139. 
Brown, 140. 
Buffalo, 423. 
Cedar, 140. 
Camp, 139. 
Clear, 140. 
Como, 139. 
Delavan, 13), 
Devils, 507. 
Elkhart, 140. 
Elizabeth, 139. 
Geneva, 129, 141. 
Green, 139, 141. 
Holdens, 139. . 
Horicon, 137. 
Koshkonong, 138, 141. 
Long, 140. 
Mary. 139. 
Michigan, 104, 137, 140. 
Muskego, 134. 
Oconomowoc cluster, 140. 
Pewaukee, 140. 
Pleasant, 189. 
Pigeon, 140. 
Poygan, 137. 
Puckawa, 138, 140. 
Round, 140. 
Rush, 138. 
Silver, 139, 140. 


Wind, 140. 

Origin of, 137. 

Geological relations of, 137. 

Encroachment, 230. 

Michigan Valley, 104, 187. 
elevation of, 104. 
system, 129, 132. 

Lake Mills, elevations, 116, 170. 

Springs, 148 

Cranberries, 186. 

Peat, 244. 

Lamartine, 154. 

La Prairie, 116. 

Lapham, Dr. I. A., 5, 44, 45, 71, 95, 108, 
130, 145, 156, 161, 2381, 257, 400, 470, 
498, 619, 655. 

Report of, 1873, 5. 
Report of, 1874, 45. 


162 


Lapham, Chas., 106. 
Ss 3, 470 


Lapham’s Peak, 213. 

Lathrop, Rev. 8. E., 98. 

Latitude and Longitude, 61. 

Laumonite, 29. 

Laurentian, 465. 

Law of Survey, 5. 

La Valle, Potsdam sandstone, 532. 

Lead, Carbonate, 29. 

Ore, statistics, 743. 
Region, 689. 

Lead Region, report on, 643. 
Introductory and historical, 645. 
Elevations, 650. 

Topography, 652. 
Drainage, 652. 
Springs and wells, 658. 
Prairie and forest, 660. 
Mounds, 661. 
Soil and subsoil, 663. 
Peat, 664. 
Brick clay, 665. 
Glacial drift, 665. 
Geological formations, 668. 
Potsdam sandstone, 668. 
Lower Magnesiau limestone, 671. 
St. Peters sandstone, 675. 
Trenton (Blue and Buff ) limestone, 680. 
Galena limestone, 683. 
Cincinnati group, 685. 
The Lead Region, 689. 
Mining terms defined, 689. 
Mineralogy, 691. 
Present condition of mines, 695. 
Beetown district, 695, 744. 
Potosi district, 699, 745. 
Fairplay district, 701. 
Hazel Green district, 704. 
New Diggings district, 710, 746. 
Shullsburg district, 713, 747. 
Benton district, 717. 
Platteville district, 719, 744. 
Mifflin district, 721. 
Centerville district, 722. 
Highland district, 723, 749. 
Linden district, 726. 
Dodgeville, 730, 748. 
Mineral Point district, 733, 747. 
Calamine district, 739. 
Wiota district, 740. 
Monroe district, 740. 
Copper in Lead Region, 741. 
Statistics of zinc ore, 742. 

of lead ore, 744. 
Concluding remarks, 751. 

Leadhillite, 29. 

Lebanon, 317. 

Ledge, The, 318. 

Leeds, Lower Magnesian limestone in, 547. 

Lemonweir river, 418. 

Lesser, 281. 

Lewiston, 444. 

Life. See Fossils. 

Lima, 116. 

aa 305, 308, 341, 347, 880, 382, 


GEOLOGICAL SURVEY OF WISCONSIN. 


Limestone, Mendota, 260, 535, 542. 
Lower Magnesian, 268, 547, 671. 
Trenton, 290, 558, 680. 

Galena, 305, 562, 683. 
Niagara, 335, 686. 
Lower Helderberg, 390. 
Hamilton, 395. 

Limonite, 28. 

Lincoln, 116. 

Lindina, 568. 

Linden District, mining, 726. 

Linear topography, 612, 626. 

Linn, 116, 213. 

Lisbon, 259, 367. 

Lithographic stone, 348. 

Lithography, microscopical, 637. 

Lithological characters, given under 

each formation. 

Little Green Lake, 273. 

Little river, 134. 

Little Sturgeon Bay, Cincinnati shales, 

314, 319. 
Tron ore near, 334. 
Niagara limestone, 344. 

Little Suamico, 116. 

Lode, 690. 

Logan, Sir W. E., 81. 

Lodi, 586. 
elevations, 442. 

Potsdam sandstone in, 544. 
Lower Magnesian limestone, 547, 

Lomira, 135. 

Long Lake, 140. 

Lower Helderberg limestone, 390. 

Lower Magnesian limestone. 
Eastern Wisconsin, 268. 

Central Wisconsin, 547. 
Lead Region, 671. 

Lowell, elevations, 116, 170. 
Trenton limestone in, 301. 

Lowville, elevations, 443. 

Lower Magnesian limestone in, 547. 

Lucas Point, 260. 

Lynden, 117, 223. 

Lyndon, 570. 

Lyons, 117. 


M. 


Macadamizing, 394. 
Mackford, Lower Magnesian in, 272. 
Trenton limestone in, 301. 
Madison, 532, 533, 543, 604.. 
Elevations, 437. 
Sandstone, 260, 585, 542. 
Magnesian_ limestone. (See Limestone.) 
Lower, in Central Wisconsin, 547. 
Eastern Wisconsin, 268 
Lead Region, 671. 
Magnetic iron sand, 239. 
Magnetite, 21, 222, 239, 493, 520. 
Magnolia, elevations, 117, 169. 
St. Peters sandstone in, 289. 
Trenton limestone in, 289. 
Malachite, 29, 694. 
Manganese, 28, 693. 


INDEX. 


Manitowoe, elevations, 117. 
Artesian oul 150, 162. 
Brick, 237 
County, 206, 210, eu i a 225, 283. 

Manitowoc Rapids, 1 

Maple Grove, 117. 

Maple Valley, 117. 

Mapleworks, 565. 

Marathon City, 490. 

Maps, list, report of 1873, 44, 64. 

1874, 64, 


Marble, 347. 
Bisreolion, she ag 444, 
uartz-po: old. 
Marcasite, oR 692. 
Marinette, cranberries, 186. 
Galena limestone in, 313. 
Markesan, 217. 


Marion, granite, 522. 
Marl, 239. 
Marsh, E. S., 34. 


Marshes, 181, 240, 450. 
Marsh Ve etation, 181. 
Marshfield, 117, 993. 
Marquette ‘County, 578, 529, 541. 
uartz-porphyry, 251, 520. 
Mary Lake, 139. 
Mayville Beds, 335, 336, 345, 384. 
Mines, 328, 329, 334. 
Mauston, 539. 
McChesney, J. H., 95. 
Medina, elevations, 170, 439. 
St. Peters sandstone i in, 556. 
Trenton limestone in, 558. 
Melanterite, 29. 
Memee, 118, 213, 223. 
Menaccanite, 28. 
Menasha, 137. 
Hyeions 118. 
Brick, 2: 
Trenton limestone i in, 302. 
Galena limestone in, 811. 
Mendota limestone, 260, 535, 542. 
Menomonee, elevations, 118. 
River, 132, 132. 
Lower Magnesian i in, 284. 
Menomonee Falls, elevations, 118. 
Niagara fossils, 372. 
Mequon, 118. 
Merrimac, 590. 
Elevations, 446. 
Quartzite, 504. 
Merrillon, 531. 
Merriman, G. L., 8, 93. 
Merton, 118. 
Meteorology, 131. 
Metomen, 128. 
Hee 118, 170. 


ei also desoriptions of Archean for- 
mation: 

Microscopic  Litholog ry, 637 

Michicott, 118. : 


Middleton, 603. 
g Elevations, 437. 
artzite 
aia mining eisinic, 721. 


763 


Milford, 118, 170. 
Milton, 118. 
oe elevations, 118, 119. 
River, 130. 
Artesian wells, 151-164. 
Drift, 220, 222, 228. 
Lake encroachment, 232. 
Brick, 237. 
Niagara limestone, 365-372. 
Lower Helderberg, 390. 
Cement rock, 895-405. 
nee catalogue of 127. 
Lead Region, 691. 
See of, 691. 
in St. Peters, 679, 
in Trenton, 683. 
Waters, 30-31, 88, 146. 
Springs, 146. 
Winetal Point, 738, 747, 
Miner, Cyrus, 166. 
Mitchell, 119, 213. 
Montello Granite, 521-523. 
Monroe District, 740. 
Montrose, elevations, 434. 
St. Peters sandstone, 556. 
Trenton limestone, 558. 
Montpelier, 119. 
Moraines, 199, 205-217, 630. 
Ground, aie. 
Moraine Lakes, 189. 
Morrison, 119. 
Mosel, 119. 
Mosinee, 483, 484. 
Mounds, Lead Region, 661. 
Moundville, Quartz-porphyry, 520, 523, 
Mount Pleasant, 119. 
Movements, of drift agencies, 199, 229. 
Mt. Maria, 266. 
Mt. Tom, 277. 
Mud Cracks, 276, 519, 345. 
Mud Creek, Guemies; 390. 
vane se 
Mundig, 2 
Munro, J., 7 
Murrish, J., Gl, 647. 
Musealunge, district, 695, 
Muskego, elevations, 119. 
Granite, 248. 
Lower Magnesian limestone, 277, 279. 
Lake, 140. 
Musquito Hill, 280. 
Mountain, 564. 


N. 


‘| Narrows, of Baraboo river, lower, 513. 


of Baraloo river, upper, 515 
of Narrow Creek, 577 
Necedah, quartzite, 523. 
Neillsville, 531, 550, 565. 
Neenah, brick, 938, 
Trenton. Jimestone near, 302. 
Galena limestone near, 311. 
Newark, 119, 120. 
New Berlin, 120. 
Newbury, 131. 


764 


Newbury, Prof. J. S., 81, 396. 

New Cassel, 350. 

New Denmark, 120. 

New Diggings district, 710, 746. 

New Holstein, 120. 

New London, 142, 280. 

New Lisbon, 568. 

Newton, 120. beast 
Nixgara Limestone in eastern Wis., 33: 
in Lead Region, 686 
Niccolite, 28. 
Nip-and-Tuck district, 695. 
Norway, 120. 


O. 


Oak Creek, 120, 121. 
Oak Grove, 121. 
Oakfield. Artesian Wells, 150. 

Niagara limestone in, 344, 346, 347. 
Oakland, elevations, 121, 170. 

Cranberries, 186. 

Trenton jimestone in, 301. 
Observatory Hill, Quartz-porphyry, 519. 
Oconomowoc, elevations, 121. 

River, 136, 

Lakes, 140. 

Cranberries, 186. 
O'Connor, C., 151. 

Oconto County, Brook’s surve 

River, 132, 133. 

Lower Magnesian limestone in, 271. 

Oconto Falls, 281, 285. 
Oolitic Structure, 269, 550. 
Openings, definition, 327, 690. 
Oregon, elevations, 434. 

St. Peters sandstone in, 556. 

Trenton limestone, 558. 
Ores, 679, 683. 
Organization, 6. 
Orthoclase, 2%. 

See also descriptions of Archzean rock. 

Organic Remains, see Fossils. 
Origin, of Lakes, 138. 
of Kettle Range, 213. 
of Kettles, 214. 
Osceola, 121. 
Oshkosh, Artesian Wells, 150, 151, 156. 
Building Stone, 308. 
Galena limestone, 310. 
Ottawa, 145, 316. 

Springs, 149. 

Cranberries, 186. 

Dritt, 211. 

Niagara limestone in, 342. 

Otter Lake, 139. 
Otsego, 584. 

elevations, 443. 

Lower Magnesian limestone, 547. 
Outagamie County — 

Potsdam sandstone in, 264. 

Lower Magnesian limestone in, 271. 
Owen, Dr. D. D., 68, 95, 268, 410, 527-528, 

535, 502, 647 
Oxygen Compounds, 28. 
Ozaukee, see Port Washington. 


a 


ry, 60. 


GEOLOGICAL SURVEY OF WISCONSIN. 


P. 
Packwaukee, 546, 579. 


_| Paint Works, Blue river, 722. 


Palmyra, 316. 
elevations, 121, 213. 
Artesian well, 151,161. | 
drift, 209, 211. 
springs, 31, 145, 147. 
Paleontology (see Fossils). 
Paris, 121. 
Part I, Annual reports, 1. 
Part II, Eastern Wisconsin, 91. 
Part ILL, Central Wisconsin, 407. 
Part 1V, Lead region, 643. 
Passage beds, see Transition. 
Peat, 29, 240, 664. 
Peninsula, see Green Bay. 
Pentenwell Rock, 572. 
Pensaukee, elevations, 121, 122. 
Galena limestone, near, 313. 
Percival, J. G., 68, 95, 250, £10, 504, 523, 
528, 542, 647. 
Peshtigo, river, 132, 134. 
Cranberries, 186. 
Potsdam sandstone on, 267. 
Lower Magnesian limestone on, 283. 
Trenton limestone on, 303. 
Petroleum, 29. 
Pewaukee, elevations, 122. 
lake, 140. 
strie, glacial, 200. 
Cincinnati shale, 317. 
beds (Waukesha), at, 346. 
Niagara limestone in, 358. 
lime, 381. 
Pecatonica river, 655. 
Phiogopite, 28. 
Pierce, elevations, 122. 
Niagara limestone in, 354, 
Pigeon Lake, 140. 
Pike River, 130. 
Pilot Knob, 576. 
Pine Bluff, 250, 520. 
ume ange 677. 
ipeclay, opening, 695. 
Pipeclay, 691. ©” 
Pitts Mill, 491. 
Platteville, mining district, 719, 744. 
Platte River, 656. 
Platte Mounds, 661, 686. 
Pleasant Lake, 139. 
Pleasant Prairie, 122. 
Pleasant Springs, 600. 
elevations, 436. 
Lower Magnesian limestone in, 548, 
Trenton limestone in, 558. 
Plover, 481. 
Plumbago, 27. 
Plymouth, ee ah 
elevations (Sheboygan county), 122, 
drift, 211 ye vm) 


Pockets, 690. 

Polk, 122. 

Pompey’s Pillar, 677. 

Porphyry, 249, 250, 251, 519-521, 
Portage County, 461, 529, 541, 568, 


INDEX. 


Port Edward, 468. 
Port Washington, brick, 237. 
springs, 149. 
drift, 223, 228. 
asl. | 


lime, 7 
Ports de Morts, 353. 
Porter, 122, 163. 
Portland, elevations, 122. 

dritt, 202, 214. 

uartzite, 252, 256. 

Trenton limestone in, 301. 
Post-Glacial features, 98. 
“ Pots and Kettles,” 206. 
Potholes, 206. 

Potosi district, 699, 745. 
Potash Kettle Range, 205. 
Pottery, 239. 
Potsdam sandstone, i Eastern Wiscon- 

sin, 257-267; in Central Wisconsin, 
525; in Lead region, 668. 
Powers. L. N., 469. : 
Poy gan, Lake, 137. 
ower Magnesian in, 277. 

lime, 285. 
Prairies, 177, 184, 449, 660. 
Prairie du Sac, 591. 

elevations, 445. 
Preble, 122, 123. 
Pre-glacial features, 97. 
Prehnite, 29. 
Previous publications, 95, 527, 647. 
Primrose, elevations, 434 

Trenton limestone in, 599. 
Puckawa Lake, 188. 
Pyrite, 23, 692. 


Q. 


Quartz, 28. 
See also descriptions of Archzan rocks. 
Quartzite, Portland and Waterloo, 252, 
256. 
Baraboo, 504, 519. 
Necedah, 523. 
Rib Hill, 485. 
Quartz-Porphyry, 249, 251, 519, 521. 
Quaternary formations, Eastern Wis- 
consin, 199. . 
Central Wisconsin, 608. 
Lead Region, 665. 


R. 


Robbins, cea land, 477. 
e CO} , 140. 
eas eee tals, 151, 163. 
drift, 226. 
erosion, 2h 932, 234. 
brick, 237. 
Fmpostane, 335, 360, 377, 384. 
lime, ee 
Rainfall, 34, ; . 
Randall, elevations, 123, 213. 
Kettle Range, 211. 
Randall, Dr., 531. 


765 


Randolf, 583. 
elevations, 445. 

Lower magnesian limestone in, 547. 

St. Peters sandstone in, 556. 

Trenton limestone in, 558. 
Range, 689, 

Rantoul, 123. 

Raplin, 365. 

Rattlesnake Rock, 575. 

Raymond, 123. 

Reconnoissance, 1875, 72. 

Red Clay, lower, 220, 221. 
upper, 225, 
modified, 225. 
sou, 193, 196. 

Reedsburg, elevations, 446. 
quartzite, 517. 

Potsdam sandstone, 532, 541. 
Reefs, ancient coral, 369. 
Relations of streams on opposite sides of 

Kettle Range, 135. 

Report of 1873, 5. 
of 1874, 45. 
ot 1875, 67. 
on Eastern Wisconsin, 91. 
on Central Wisconsin, 407. 
on Lead Region, 643. 

Rhine, elevations, 123, 223. 
drift, 211. 

Rib Hill, 485, 489. 

Richfield, 123. 

Richmond, cranberries, 186. 
drift, 206, 211. 

Richland, 355. 

Rio, Potsdam sandstone in, 544. 

Ripon, elevations, 123, 170. 

Lower Magnesian, 274. 

Trenton limestone in, 301. 
Ripple marks, 276, 319, 345. 
Roches moutonees, 614. 
Roche-a-Cris, 540, 572. 
Rochester, 123. 

town of, 140, 143, 169. 

Rock, elevations in town of, 123, 169. 
St. Peters sandstone in, 287, 288. 
Galena limestone in, 308. 
Trenton limestone in, 297. 

Rock Lake, 140), 215. 

Rock River Valley, 102, 129, 199, 202, 

492, 217. 

system, 129. 

east branch, 135. 

water-power, 171. 

Rockland, 121. 

Rockville, 356. 

Rocky Run, 492. 

Rominger, Dr. C., 84, 96, 234, 313. 

Rosendale, 123. 

Round Lake, 140. 

Roxbury, elevations, 440. 

Lower Magnesian in, 547, 
Rubicon River, 186, 333. 
Rudolph, 564. 

Ruger, E., 171. 

Bush Lake, 138, 275. . 

Rushford, Artesian wells, 150, 159. 

Russel, 123. 


766 


Rutland, elevations, 170, 484. 
Trenton limestone in, 558, 


S. 


Salem, 123. 
Sandstone, calcareous, 337, 

Potsdam, 257, 525, 668. 

St. Peters, 285, 555, 675. 
Sapronite, 29. 
Sauk County, 579, 529, 532, 553, 534. 
Sauk City, Lower Magnesian, 548. 
Saukville, elevations, 123. 

Niagara limestone in, 368, 378, 379. 
Scapolite, 28. 
Schleswig, 123. 
Scott, 585. 

elevations, 124, 444. 

Lower Magnesian in, 547. 
Scoular, James, 332. 
Seoville, 8, 155. 
Seed-Ore, 329. 
Selenite, 319. 
Seneca, quartz-porphyry, 520. 
Sevastopol, 124. 
Seven Mile Creek, 310. 
Shaw, S., 8, 93. 
Shawano, Lake, 130. 

county, red clay, 223. 

la Magnesian limestone in, 271, 


280. 
Sheet, definition, 670. 
Sheboygan, elevations, 124. 
coynty, 140, 206, 209. 
Artesian well, 151, 164. 
drift, 228. 
lime, 382. 
brick, 237. 
Niagara hmestone, 378, 379. 
Sheboygan Falls, elevations, 124. 
Niagara limestone, 378. 
Sherman, 124. 
Shields, elevations, 124, 170. 
Trenton limestone, 301. 
Shopiere, 299. 
Shot-ore, 229. 
Shullsburg District, 718, 747. 
Shumard, Dr. B. F., 596. 
Siderite, 29. 
Silicified Fossils, 351. 
ila Lower, Eastern Wisconsin, 
Central Wisconsin, 525. 
Lead region, 668. 
Upper Suurian, 327. 
Silver Lake, 139, 140. 
Silver, 27. 
Single’s Mill, 489. 
Sinks, 206, 214, 661. 
Sinsinawa, 661. 
Smithsonite, 29, 694. 
Soils, Central Wisconsin, 449, 451, 599. 
Eastern Wisconsin, 188, 316. 
Origin, 188. 
Descriptions, 190. 
Prairie loam, 191, 196, 198., 


GEOLOGICAL SURVEY OF WISCONSIN. 


Soils, Eastern Wisconsin — continued. 
Lighter marly clay, 192, 198. 
Heavier marly clay, 192, 198. 
Red marly clay, 193, 196. 
Limestone loam, 194, 198. 
Silicious sandy, 195, 198. 
Calcareous sandy, 195. 198. 
Humus, 195, 196, 198. 
Alluvial, 196, 

Magnesian character of, 197. 
Lead region, 663. 

Somers, 124. 

Spar, 29. 

Specular ore, 330. 

Sphalerite, 28, 692. 

Springs, 30, 88, 658. 

Barnes, 147. 

Beloit Iodo-Magnesian, 146, 147. 
Bethesda, 32, 146, 147. 
Big Spring, 145. 
Cedarburg, 148. 
Druecker's, 144. 
Dousman’s, 32, 145. 
East Troy, 32. 
Eureka, 32. 

Fountain, 146, 147. 
Gihon, 146, 147. 
Hackett’s, 32. 

Horeb, 146, 147. 
Hygeia, 146, 147. 
Lowe’s, 32, 147. 
Mineral Rock, 32, 147. 
Mitchell's 142. 
Nemahbin, 32, 147. 
Oakton, 32, 147. 
Richmonds, 32, 147. 
Siloam, 32, 147. 
Schwickhart, 32. 
Sheridan, 147. 

Stowe’s 145, 

Telulah, 148. 

White Rock, 146, 147. 
Chalybeate, 148. 
Salons, 148. 
Travertine, 148. 

Trout, 149. 

Spring Prairie, 124. 

Spring Valley, 124, 125, 169. 

Springdale, 559. 

Springfield, 603. 

Elevations, 438. 
Lower Magnesian limestone in, 547. 

Springvale, elevations, 444. 

Lower Magnesian limestone in, 547. 

Star, Hon. W., 284. 

Sterling, W. C., 328, 332. 

Steele, "Pres. G. M., 172. 

Stiles, 283. 

Stockbridge, elevations, 125. 

Cincinnati shales, 318. 
Iron ore, 333. 
Analysis of limestone, 338. 
St. Fee Sandstone, eastern Wisconsin, 


Central Wisconsin, 555, 
Lead region, 675. 
Strize, 200, 201, 205, 625. 


INDEX. 


Strong, Moses, 6, 44, 46, 55, 64, 65, 66 
71, 543, 560, 597, 609, 610, 643... 
Party of, 1873, 9. 
Party of, 1874, 55. 
Sturgeon Bay, 204. 
Elevations, 125. 
Springs, 149. 
Cranberries, 186. 
Niagara limestone, 346, 348, 352, 354, 
368, 372. 
Terraces, 228. 
Starin, F. J., 106. 
Statistics, of zinc ore, 742. 
of lead ore, 743. 
Stevens, W.C., 93. 
Stevens Point, 480, 580, 546, 564. 
Strikes, 464. 
Stratigraphical Arrangement, See un- 
der the several formations. 
Sugar Creek, elevations, 125. 
Stream, 129, 136. 
Cranberries, 186. 
Peat, 243. 
Sulphides, 28. 
Sulphur, 27, 692. 
Summits, etc., 24. 
Elevations, 125. 
Cranberries, 186. 
Peat, 245. 
Sumpter, 590. 
levations, 446. 
Quartzite, 504, 518. 
Sumner, 125, 170. 
Sun Prairie, 601. 
Elevations, 439. 
St. Peters Sandstone, 556. 
Swallow, G. C., 51. 
Sweet, E. T., 7, 49, 72, 235, 332, 412, 470, 
673, 680, 681, 689. 
Swezey, G. D., 52, 93, 106. 
Swither, definition, 690. 


We 
Tale, 29. ' 
Taycheedah, elevations, 125, 223. 
Springs, 149 


Artesian wells, 150, 154. 
Cincinnati shale, 318. 
Niagara limestone, 339, 340. 
Taylor, Gov. W. R., 71. 
Tetrahedrite, 20. 
Terraces, 228. 
Theresa, springs, 149, 
Drift, 215 


Rocke river Ria 

Thiela, H. F., F 

Thickness, Potsdam, 257, 460, 528. 
Lower Magnesian limestone, 271, 460, 

514, 551. 

St. Peters sandstone, 460, 555. 
Trenton limestone, 291, 460, 681. 
Galena Se 685. 
“ncinnati shale, 315. 
Ton iron ore, 330, 333, 334. 
Mayville beds, 338. 
Byron beds, 346. 


767 


Thickness — continued. 
Lower coral beds, 351. 
Upper coral beds, 353. 
Timber, 175, 450, 660. 
Tiff, 29. 
Tiles, 229. 
Till, 199-217. 
Toay, James, 741. 
Topographical characters. 
Potsdam, 533 
Lower Magnesian limestone, 548 
St. Peters sandstone, 556. 
Trenton limestone, 559. 
Topographical maps, 647. 
= SRRvER 16 
‘opography. 
Eastern Wisconsin, of, 97-127. 
Central Wisconsin, of, 413-447, 453. 
Lead region, of, 643-652. 
Tourmaline, 29. 
Trains of bowlders, 202, 252, 253. 
Transition beds, 298, 297, 287, 348, 542. 
Travertine, 144, 148, 318. 
Trenton, elevations, 125. 
Trenton limestone in, 301. 
Trenton limestone. 
Eastern Wisconsin, 290, 305. 
Central Wisconsin, 558. 
Lead region, 680. 
Troy, elevations, 125, 445. 
akes, 13: 


, 139. 
Troughs, glacial, 130, 181. 139, 201. 
Trout springs, 149 
Turtle, elevations, 125. 
Creek, 136 
Lake, 139. 
Trenton limestone, 299. 
Galena limestone, 308. 
Twin river, east, 132. 
Two Rivers, elevations, 125. 
river, 182. 


U. 


Unconformability, 391, 462. 
Union, elevations, 125, 126, 169. 
Trenton limestone, 301. 

Utica, elevations, 125. 


Wie 


Value, see economic considerations. 


Vanuxem, 80. | . . 
Vegetation, native, of Central Wisconsin, 
7 


of Central Wisconsin, 449. 
of Lead region, 660. 
Vein, defined, 690. 
Vernon, elevations, 126. 
Verona, elevations, 485. 
Trenton limestone in, 558. 
of Lead region, 660. 
Vienna, elevation, 448. 
Lower Magnesian limestone, 547. 
St. Peters sandstone, 556. 


708 


W. 
Wad, 28. 
Walworth county, 126, 131, 186, 189, 206, 
211, 342. 


town of, 212, 2138, 
springs in, 149. 
Warren, Gen. G. Ky 26, 421, 585. 
Waring, Geo. W., 160. 
W: ashbur n, Gov, ¢. C., 6, 71. 
Washington county, 126, 136, 140, 206. 
Wash Dirt, 691. 
Wasley Range, 742, 
Water, 28. 
Water power, 141, 170. 
of Rock river, 171. 
ot Fox river, 172. 
of Milwaukee river, 174. 
of Sheboygan river, 174. 
of Manitowoc river, 174. : 
of Wolf, Oconto and Peshtigo rivers, 
173, 176. 
Water supply, 141. 
Water lime. See Hydraulic lime. 
Waterford, 126. 
Waterloo, elevations, 126, 170. 
brick at, 238. 
quartzite, 252-256, 
ower magnesian limestone at, 271. 
St. Peters sandstone in, 290. 
Trenton limestone in, 301. 
Watertown, elevations, 126. 
Artesian wells, 150, 151, 160. 
brick, 2 
lime, 308. 
Galena limestone near, 309. 
Watershed, 128. 
Waubakee, limestone near, 392. 
Waukesha, county, 140, 206, 211, 316, 342. 
elevations in town of, 126. 
springs, 144. 
limestone, 335, 357-360, 384. 
lime, 382. 
fossils at, 372. 
Waupun, elevations, 126. 
luilding stone, 308. 
Galena ang tone at, 310. 
Wausau, 486, 48 
Wanshara ne 529, 533, 541, 578. 
Wautoma, 546. 
Wauwatosa, elevations, 126, 127. 
Niagara limestone at, 365, 368, 372. 
Wayne, elevations, 127. 
Rock river in, 185. 
Wernerite, 28. 
Wells, Artesian, 149. 
in Lead Region, 658. 
West Bend, 131. 
Elevations i in, 127. 
Westfield, elevations, 446. 
Quartzite, 504, 517. 
Potsdam sandstone, 532. 
Westford, elevations, 127, 170. 
Trenton limestone in, 504. 
West Point, 586. 
Elevations, 446. 
Lower Magnesian limestone in, 547, 
St. Peters sandstone in, 556. 


¢ 
GEOLOGICAL SURVEY OF WISCONSIN. 


Westport, 602. 
qievations, 439. 
Lower Magnesian Hineearene, 547, 555. 
Wheatland, elevations, 127 
Whitfield, Prof, R. P., oy 262 268, 358, 
587, 554, 561, 585, 5 
Whitefish Bay, 399. 
White river, 128, 129, 136, 203. 
Whitewater, 206. 
Elevations, 127, 218. 
Springs near, 148, 149. 
Artesian wells, 150, 162. 
Drift at, 209, 211. 
Brick tiles and pottery, 239, 
Peat in, 242. 
Lime, 308. 
Galena limestone in, 309. 
Whitney, Prof. J. D., 57, 68, 69, 528, 559, 
560, 609, 622, 647, 667. 
Whitney's Rapids, 466. 
Whitney’s Bluff, 319, 344, 
Whitemore, D. j., 86, 400. 
Whittlesey, Col. Co 59, 95, 206, 211, 631. 
Wight, Dr. O. V 
Wil pore 3H. B40. 
Wilson, J., Jr., aps of, 13. 
Wilson, J. H., 103, 171. 
Wild’s well, 153 
Wilke Lake, 140. 
Winchell, Prof. A., 504, 596. 
Winchell, Prof, N. H., 96, 204, 288. 
Wind Lake, 000, 
Windsor, elevations, 440. 
Lower Magnesian limestone. 
Winfield, 447, 593, 597. 
Winkler, C., 35. 
Winnebago ‘county. 
Potsdam aden in, 264, 
Lower Magnesian limestone, 271, 277. 
Winneconne, 275. 
Wiota mining district, 740. 
Wonewoe, 568. 
Wood, Paul B., 106. 
Wood, J. W., 595. 
Wood county, 563, 461, 529, 541. 
Woodland, 532. 
Woodville, 127. 
Woodward, S. S., 160. 
Wooster, T.C., 8 52, 98, 100. 
Worrall, Col. Jos., 103, 172. 
Worthen, A 
Wright, Chas. E ., 72, 78, 76, 520, 637. 
Wright, N, D., 8, 93. 
Wrightstown, bt 
Wyocena, 443. 


x, 


Yellow River Valley, 490. 
York, elevations, 441. 


Lower Magnesian limestone, 547. 
Yorkville, 127. 


Zinc, carbonate, 29, 683. 
bloom, 29. 
ore, statistics, 742.