The History of Rock County, Wisconsin: Its Early Settlement, Growth, Development, Resources, Etc., Part 17

Author: Wesern historical company, Chicago, pub
Publication date: 1879
Publisher: Chicago : Western Historical Co.
Number of Pages: 899

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The Mississippi slope presents several conspicuous ridges and valleys, but their trend is toward the great river, and they are all due, essentially, to the erosion of the streams that channel the slope. One of these ridges constitutes the divide south of the Wisconsin river, already referred to. Another of these, conspicuous by reason of its narrowness and sharpness, lies between the Kickapoo and the Mississippi, and extends through Crawford, Vernon and Monroe counties. Still another is formed by the quartzite ranges of Sauk county and others of less prominence give a highly diversified character to the slope.

Scattered over the surface of the state are prominent hills, some swelling upward into rounded domes, some rising symmetrically into conical peaks, some ascending precipitously into castel- lated towers, and some reaching prominence without regard to beauty of form or convenience of description. A part of these hills were formed by the removal by erosion of the surrounding strata, and a part by the heaping up of drift material by the glacial forces. In the former case, they are composed of rock; in the latter, of clay, sand, gravel and bowlders. The two forms are often combined. The highest peak in the southwestern part of the state is the West Blue mound, which is 1,151 feet above Lake Michigan; in the eastern part, Lapham's peak, 824 feet, and in the central part, Rib hill, 1263 feet. The crest of Penokee range in the northern part of the state rises 1,000 feet, and upwards, above Lake Michigan.

The drainage systems correspond in general to these topograpical features, though several minor eccentricities are to be observed. The streams of the Lake Superior system plunge rapidly down their steep slopes, forming numerous falls, some of them possessing great beauty, prominent among which are those of the Montreal river. On the southern slope, the rivers, in the upper portion of their courses, likewise descend rapidly, though less so, producing a succession of rapids and cascades, and an occasional cataract. In the lower part of their courses, the

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HISTORY OF WISCONSIN.

descent becomes much more gentle and many of them are navigable to a greater or less extent. The rivers west of the Wisconsin pursue an essentially direct course to the Mississippi, attended of course with minor flexures. The Wisconsin river lies, for the greater part of its course, upon the north and south arch of the state, but on encountering the diagonal valley above mentioned it turns southwestward to the" Father of Waters." The streams east of the Wisconsin flow southerly and southeasterly until they likewise encounter this valley when they turn in the opposite direction and discharge northeasterly into Lake Michigan, through Green bay. Between the Green-bay-Rock-river valley and Lake Michigan, the drainage is again in the normal southeasterly direction. In the southern part of the state, the rivers flow in a gen- eral southerly direction, but, beyond the state, turn westward toward the Mississippi.

If the courses of the streams be studied in detail, many exceedingly interesting and instruc- tive features will be observed, due chiefly to peculiarities of geological structure, some of which will be apparent by inspecting the accompanying geological map. Our space, however, forbids our entering upon the subject here.

The position of the watershed between the great basins of the Mississippi and the St. Law- rence is somewhat peculiar. On the Illinois line, it lies only three and one half miles from Lake Michigan and about 160 feet above its surface. As traced northward from this point, it retires from the lake and ascends in elevation till it approaches the vicinity of Lake Winnebago, when it recurves upon itself and descends to the portage between the Fox and the Wisconsin rivers, whence it pursues a northerly course to the heights of Michigan, when it turns westward and passes in an undulating course across the northern part of the state. It will be observed that much the greater area of the state is drained by the Mississippi system.

The relationship which the drainage channels have been observed to sustain to the topo- graphical features is partly that of cause and partly that of effect. The general arching of the surface, giving rise to the main slopes, is due to deep-seated geological causes that produce an upward swelling of the center of the state. This determined the general drainage systems. On the other hand, the streams, acting upon strata of varying hardness, and presenting different atti- tudes, wore away the surface unequally and cut for themselves anomalous channels, leaving corresponding divides between, which gave origin to the minor irregularities that diversify the surface. In addition to this, the glacier-that great ice stream, the father of the drift-planed and plowed the surface and heaped up its debris upon it, modifying both the surface and drainage features Looked at from a causal standpoint, we see the results of internal forces elevating, and external agencies cutting down, or, in a word, the face of the state is the growth of geologic ages furrowed by the teardrops of the skies.

GEOLOGICAL HISTORY OF WISCONSIN.

In harmony with the historical character of this atlas, it may be most acceptable to weave our brief sketch of the geological structure of the state into the form of a narrative of its growth.

THE ARCHAAN AGE. LAURENTIAN PERIOD.

The physical history of Wisconsin can be traced back with certainty to a state of complete submergence beneath the waters of the ancient ocean, by which the material of our oldest and deepest strata were deposited. Let an extensive but shallow sea, covering the whole of the present territory of the state, be pictured to the mind, and let it be imagined to be depositing

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TOPOGRAPHY AND GEOLOGY.

mud and sand, as at the present day, and we have before us the first authentic stage of the history under consideration. Back of that, the history is lost in the mists of geologic antiquity. The thickness of the sediments that accumulated in that early period was immense, being measured by thousands of feet. These sediments occupied of course an essentially horizontal position, and were, doubtless, in a large degree hardened into beds of impure sandstone, shale, and other sedi- mentary rock. But in the progress of time an enormous pressure, attended by heat, was brought to bear upon them laterally, or edgewise, by which they were folded and crumpled, and forced up out of the water, giving rise to an island, the nucleus of Wisconsin. The force which pro- duced this upheaval is believed to have arisen from the cooling and consequent contraction of the globe. The foldings may be imaged as the wrinkles of a shrinking earth. But the contor- tion of the beds was a scarcely more wonderful result than the change in the character of the rock which seems to have taken place simultaneously with the folding, indeed, as the result of the heat and pressure attending it. The sediments, that seem to have previously taken the form of impure sandstone and shale for the most part, underwent a change, in which re-arrangement and crystalization of the ingredients played a conspicuous part. By this metamorphism, granite, gneiss, mica schist, syenite, hornblende rocks, chloritic schists and other crystalline rocks were formed. These constitute the Laurentian formation and belong to the most ancient period yet distinctly recognized in geology, although there were undoubtedly more ancient rocks. They are therefore very fittingly termed Archaan-ancient-rocks (formerly Azoic.) No remains of life have been found in this formation in Wisconsin, but from the nature of rocks elsewhere, believed to be of the same age, it is probable that the lowest forms of life existed at this time. It is not strange that the great changes through which the rocks have passed should have so nearly obliterated all traces of them. The original extent of this Laurentian island can not now be accurately ascer- tained, but it will be sufficiently near the truth for our present purposes to consider the formation as it is now exposed, and as it is represented on the accompanying geological map, as showing approximately the original extent. This will make it include a large area in the north-central portion of the state and a portion of the Upper Peninsula of Michigan. All the rest of the state was beneath the ocean, and the same may be said of the greater portion of the United States The height of this island was doubtless considerable, as it has since been very much cut down by denuding agencies. The strata, as now exposed, mostly stand in highly inclined attitudes and present their worn edges to view. The tops of the folds, of which they are the remnants, seem to have been cut away, and we have the nearly vertical sides remaining.

HURONIAN PERIOD.

As soon as the Laurentian island had been elevated, the waves of the almost shoreless ocean began to beat against it, the elements to disintegrate it, and the rains of the then tropical climate to wash it; and the sand, clay and other debris, thus formed, were deposited beneath the waters around its base, giving rise to a new sedimentary formation. There is no evidence that there was any vegetation on the island: the air and water were, doubtless, heavily charged with carbonic acid, an efficient agent of disintegration : the climate was warm and doubtless very moist -circumstances which combined to hasten the erosion of the island and increase the deposition in the surrounding sea. In addition to these agencies, we judge from the large amount of carbonaceous matter contained in some of the beds, that there must have been an abundance of marine vegetation, and, from the limestone beds that accumulated, it is probable that there was marine animal life also, since in later ages that was the chief source of limestone strata. The joint accumulations from these several sources gave rise to a series of shales, sandstones and limestones, whose combined thickness was several thousand feet.

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HISTORY OF WISCONSIN.

At length the process of upheaval and metamorphism that closed the Laurentian period was repeated, and these sandstones became quartzites; the limestones were crystalized, the shales were changed to slates or schists, and intermediate grades of sediments became diorites, quartz- porphyries and other forms of crystalline rocks. The carbonaceous matter was changed in part to graphite. There were also associated with these deposits extensive beds of iron ore, which we now find chiefly in the form of magnetite, hematite and specular ore. These constitute the Huronian rocks. From the amount of iron ore they contain, they are also fittingly termed the iron-bearing series. As in the preceding case, the strata were contorted, flexed and folded, and the whole island was further elevated, carrying with it these circumjacent strata, by which its extent was much enlarged. The area of the island after receiving this increment was con- siderably greater than the surface represented as Laurentian and Huronian on the accompanying map, since it was subsequently covered to a considerable extent by later formations. Penokee range, in Ashland county, is the most conspicuous development of the Huronian rocks in the state. The upturned edge of the formation forms a bold rampart, extending across the country for sixty miles, making the nearest approach to a mountain range to be found within the state. A belt of magnetic schist may be traced nearly its entire length. In the northern part of Oconto county ,there is also an important development of this formation, being an extension of the Menomonee iron-bearing series. A third area is found in Barron county, which includes deposits of pipestone. In the south central part of the state there are a considerable number of small areas and isolated outliers of quartzite and quartz-porphyry, that, without much doubt, belong to this series. The most conspicuous of these are the Baraboo quartzite ranges, in Sauk and Columbia counties, and from thence a chain of detached outliers extends northeasterly through several counties. The most southerly exposure of the formation is near Lake Mills, in Jefferson county.

THE COPPER-BEARING SERIES.

Previous to the upheaval of the Huronian strata, there occurred in the Lake Superior region events of peculiar and striking interest. If we may not speak with absolute assurance, we may at least say with reasonable probability, that the crust of the earth was fissured in that region, and that there issued from beneath an immense mass of molten rock, that spread itself over an area of more than three hundred miles in length and one hundred miles in width. The action was not confined to a single overflow, but eruption followed eruption, sometimes apparently in quick succession, sometimes evidently at long intervals. Each outpouring, when solidified, formed a stratum of trap rock, and where these followed each other without any intervening deposit, a series of trappean beds were formed. In some cases, however, an interval occurred, during which the waves, acting upon the rock previously formed, produced a bed of sand, gravel and clay, which afterward solidified into sandstone, conglomerate and shale. The history of these beds is lithographed on their surface in beautiful ripple-marks and other evidences of wave- action. After the cessation of the igneous eruptions, there accumulated a vast thickness of sandstone, shale and conglomerate, so that the whole series is literally miles in thickness.

The eruptive portions have been spoken of as traps, for convenience; but they do not now possess the usual characteristics of igneous rocks, and appear to have undergone a chemical metamorphism by which the mineral ingredients have been changed, the leading ones now being an iron chlorite and a feldspar, with which are associated, as accessory minerals, quartz, epidote, prenite, calcite, laumontite, analcite, datolite, magnetite, native copper and silver, and, more rarely, other minerals. The rock, as a whole, is now known as a melaphyr. The upper portion of each bed is usually characterized by almond-sized cells filled with the minerals above men- tioned, giving to the rock an amygdaloidal nature. The native copper was not injected in a

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THolten state, as has very generally been supposed, but was deposited by chemical means after the beds were formed and after a portion of the chemical change of the minerals above mentioned Fa ad been accomplished. The same is true of the silver. The copper occurs in all the different forms of rock-the melaphyrs, amygdaloids, sandstones, shales and conglomerates, but most Lundantly in the amygdaloids and certain conglomerates.

This series extends across the northern portion of the state, occupying portions of Ashland, Bayfield, Douglas, Burnett and Polk counties. When the Huronian rocks were elevated, they "carried these up with them, and they partook of the folding in some measure. The copper- bearing range of Keweenaw Point, Michigan, extends southwestward through Ashland, Burnett and Polk counties, and throughout this whole extent the beds dip north-northwesterly toward Lake Superior, at a high angle; but in Douglas and Bayfield counties there is a parallel range in which the beds incline in the opposite direction, and undoubtedly form the opposite side of a trough formed by a downward flexure of the strata.

PALEOZOIC TIME-SILURIAN AGE.

POTSDAM SANDSTONE.

After the great Archaan upheaval, there followed a long period, concerning wnich very little is Ic rown-a " lost interval" in geological history. It is only certain that immense erosion of the Archaean strata took place, and that in time the sea advanced upon the island, eroding its stra ta and redepositing the wash and wear beneath its surface. The more resisting beds with- stood this advance, and formed reefs and rocky islands off the ancient shore, about whose bases the sands and sediments accumulated, as they did over the bottom of the surrounding ocean. The breakers, dashing against the rocky cliffs, threw down masses of rock, which imbedded them- selves in the sands, or were rolled and rounded on the beach, and at length were buried, in either case, to tell their own history, when they should be again disclosed by the ceaseless gnaw- ings of the very elements that had buried them. In addition to the accumulations of wash and wear that have previously been the main agents of rock-formations, abundant life now swarms in the Ocean, and the sands become the great cemetery of its dead. Though the contribution of each little being was small, the myriad millions that the waters brought forth, yielded by their remains, a large contribution to the accumulating sediments. Among plants, there were sea-weeds, and among animals, protozoans, radiates, niollusks and articulates, all the sub-kingdoms except the vertebrates. Among these, the most remarkable, both in nature and number, were the trilobites, who have left their casts in countless multitudes in certain localities. The result of the action of these several agencies was the formation of extensive beds of sandstone, with interstratified lay ers of limestone and shale. These surrounded the Archaan nucleus on all sides, and reposed on its flanks. On the Lake Superior margin, the sea acted mainly upon the copper and iron- bearing series, which are highly ferruginous, and the result was the red Lake Superior sandstone. On the opposite side of the island, the wave-action was mainly upon quartzites, porphyries and granites, and resulted in light-colored sandstones. The former is confined to the immediate vicinity of Lake Superior; the latter occupies a broad, irregular belt bordering the Archaan area on the south, and, being widest in the central part of the state, is often likened to a rude crescent. The form and position of the area will be best apprehended by referring to the accompanying map. It will be understood from the foregoing description, that the strata of this formation lie in a nearly horizontal position, and repose unconformably upon the worn surface of the crystalline rocks. The close of this period was not marked by any great upheaval; there

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HISTORY OF WISCONSIN.

was no crumpling or metamorphism of the strata, and they have remained to the present day very much as they were originally deposited, save a slight arching upward in the central portion of the state. The beds have been somewhat compacted by the pressure of superin- cumbent strata and solidified by the cementing action of calcareous and ferruginous waters, and by their own coherence, but the original character of the formation, as a great sand-bed, has not been obliterated. It still bears the ripple-marks, cross-lamination, worm-burrows, and similar markings that characterize a sandy beach. Its thickness is very irregular, owing to the uneven- ness of its Archaan bottom, and may be said to range from 1,000 feet downward. The strata slope gently away from the Archaan core of the state and underlie all the later formations, and may be reached at any point in southern Wisconsin by penetrating to a sufficient depth, which can be calculated with an approximate correctness. As it is a water-bearing formation, and the source of fine Artesian wells, this is a fact of much importance. The interbedded layers of lime- stone and shale, by supplying impervious strata, very much enhance its value as a source of fountains.

LOWER MAGNESIAN LIMESTONE.

During the previous period, the accumulation of sandstone gave place for a time to the formation of limestone, and afterward the deposit of sandstone was resumed. At its close, with- out any very marked disturbance of existing conditions, the formation of limestone was resumed, and progressed with little interruption till a thickness ranging from 50 to 250 feet was attained. This variation is due mainly to irregularities of the upper surface of the formation, which is undulating, and in some localities, may appropriately be termed billowy, the surface rising and falling 100 feet, in some cases, within a short distance. This, and the preceding similar deposit, have been spoken of as limestones simply, but they are really dolomites, or magnesian limestones, since they contain a large proportion of carbonate of magnesia. This rock also contains a notable quantity of silica, which occurs disseminated through the mass of the rock; or, variously, as nodules or masses of chert; as crystals of quartz, filling or lining drusy cavities, forming beautiful miniature grottos; as the nucleus of oolitic concretions, or as sand. Some argillaceous matter also enters into its composition, and small quantities of the ores of iron, lead and copper, are sometimes found, but they give little promise of value. The evidences of life are very scanty. Some sea-weeds, a few mollusks, and an occasional indication of other forms of life embrace the known list, except at a few favored localities where a somewhat ampler fauna is found. But it is not, therefore, safe to assume the absence of life in the depositing seas, for it is certain that most limestone has orignated from the remains of animals and plants that secrete calcareous material, and it is most consistent to believe that such was the case in the present instance, and that the distinct traces of life were mostly obliterated. This formation occupies an irregular belt skirting the Potsdam area. It was, doubtless, originally a somewhat uniform band swinging around the nucleus of the state already formed, but it has since been eroded by streams to its present jagged outline.

ST. PETER'S SANDSTONE.

At the close of this limestone-making period, there appears to have been an interval of which we have no record, and the next chapter of the history introduces us to another era of sand accumulation. The work began by the leveling up of the inequalities of the surface of the Lower Magnesian limestone, and it ceased before that was entirely accomplished in all parts of the State, for a few prominences were left projecting through the sand deposits. The material laid down consisted of a silicious sand, of uniform, well-rounded-doubtless well-rolled-grains. This was evidently deposited horizontally upon the uneven limestone surface, and so rests in a sense

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unconformably upon it. Where the sandstone abuts against the sides of the limestone promi- nences, it is mingled with material derived by wave action from them, which tells the story of its formation. But aside from these and other exceptional impurities, the formation is a very pure sandstone, and is used for glass manufacture. At most points, the sandstone has never become firmly cemented and readily crumbles, so that it is used for mortar, the simple handling with pick and shovel being sufficient to reduce it to a sand. Owing to the unevenness of its bottom, it varies greatly in thickness, the greatest yet observed being 212 feet, but the average is less than 100 feet. Until recently, no organic remains had ever been found in it, and the traces now col- lected are very meager indeed, but they are sufficient to show the existence of marine life, and demonstrate that it is an oceanic deposit. The rarity of fossils is to be attributed to the porous nature of the rock, which is unfavorable to their preservation. This porosity, however, subserves a very useful purpose, as it renders this pre-eminently a water-bearing horizon, and supplies some of the finest Artesian fountains in the state, and is competent to furnish many more. It occupies but a narrow area at the surface, fringing that of the Lower Magnesian limestone on the south. See map.

TRENTON LIMESTONE.

A slight change in the oceanic conditions caused a return to limestone formation, accompa- nied with the deposit of considerable clayey material, which formed shale. The origin of the limestone is made evident by a close examination of it, which shows it to be full of fragments of shells, corals, and other organic remains, or the impressions they have left. Countless numbers of the lower forms of life flourished in the seas, and left their remains to be comminuted and consolidated into limestone. A part of the time, the accumulation of clayey matter predominated, and so layers of shale alternate with the limestone beds, and shaly leaves and partings occur in the limestone layers. Unlike the calcareous strata above and below, a portion of these are true limestone, containing but a very small proportion of magnesia. A sufficient amount of carbon- aceous matter is present in some layers to cause them to burn readily. This formation is quite highly metalliferous in certain portions of the lead region, containing zinc especially, and con- siderable lead, with less quantities of other metals. The formation abounds in fossils, many of them well preserved, and, from their great antiquity, they possess uncommon interest. All the animal sub-kingdoms, except vertebrates, are represented. The surface area of this rock borders the St. Peter's sandstone, but, to avoid too great complexity on the map, it is not distinguished from the next formation to which it is closely allied. Its thickness reaches 120 feet.

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The History of Rock County, Wisconsin: Its Early Settlement, Growth, Development, Resources, Etc., Part 17

Author: Wesern historical company, Chicago, pub Publication date: 1879 Publisher: Chicago : Western Historical Co. Number of Pages: 899

Author: Wesern historical company, Chicago, pub
Publication date: 1879
Publisher: Chicago : Western Historical Co.
Number of Pages: 899