Jackson Township (part 13 of 19)

At present the Sunbury shales have no economic value, but, owing to the cont(»nt of carbonaceous matter, in the future they may be utilized as a sourci* of oil and gas. They have no ceramic value.

The Cuyahoga formation includes the shales and sandstones from the Sunbury black shales below to the Logan shales and sandstones above. The contact of the Cuyahoga and Logan formations is not sharply defined in most of the area. In some localities the line of di- vision is marked by a slight disconfonnity that exists between the shales of the Cuyahoga and a heavy sandstone above, which has been named by Hyde the Byer member of the Logan. In other localities, where the Byer sandstone is poorly developed, the shales and sandstones of the Cuyahoga blend with those of the Logan with no apparent definite break; the interval from fossil horizons and texture changes is then the main reliance in separating the two formations. The thickness of the Cuyahoga formation varies usually between 300 and 340 feet. Primarily the formation is made up of shales, but in the lower half, especially, thin to massive layers of sandstone are found which may lie close together, or may be separated by intervals of many feet. They are correlative with the freestones worked at McDermott, Buena Vista, and Careys Run, in Scioto County.

Along the road on Straight Creek, just below the mouth of Meadow Run, in Section 8, Seal Township, one of the heavy brown stone layers is exposed. The layer varies from 2 to 4 feet in thickness, and the stone has an attractive brownish color.

In Section 2, Jackson Township, on land of Peter Bauer, several layers of the brown stone are exposed, one of which has a thickness ranging from 5 to 6 f^et, where measured. The layer is broken into large blocks, by joint planes, but is quite free from partings along the bedding planes. The stone is medium fine-grained and has good color. It is quite weather resistant, as the stratum stands out in bold relief along the hillside at an elevation of about 70 feet above the flood plain of the Scioto River. The thinner layers exposed below were not measured.

An exposure of the brown stone layers was also seen along the roadside near the Brown School, in Section 1, Jackson Township. A partial section taken at this point follows:

South of this, along the road in Straight Creek, near the central part of Section 10, one of the layers is exposed, and measured as given below:

The upper 8 inches of shelly stone, which has been loosened by weathering, is a part of the layer. Under heavy cover the entire bed is solid. The heavy layer seen on land of Peter Bauer is also exposed in a number of places near the base of the hills facing the Scioto River. It is persistent from his home north to the mouth of Cars Run. In the southwestern comer of Section 4, Jackson Township, on land of M. P.

Foster, the layer ranging in thickness from 3 to 4 feet is found about 60 feet above the Scioto flood plain. The average thickness of the blocks measured was 3 feet 6 inches, and the quality of the stone very good. North of this in an old quarry, from which a small amoimt of stone had been taken for some local use, the layer measured 3 feet 6 inches, and the interval from it to- the Sharon conglomerate, which caps the point, measured 260 feet. (Aneroid). Near the mouth of Cars Run the thickness exposed at one point was only 2 feet 6 inches. On Cars Run, near the Baptist Church, in Section 5, Jackson Township, brown sandstone layers are exposed at a number of points. The thickest layer seen measured from 1 foot 6 inches to 4 feet, averaging about 2 feet 6 inches to 3 feet. In the same section, near the mouth of Jackson Fork, a layer exposed measured from 1 foot 6 inches to 3 feet. Near where the road crosses Cars Run, in the northeastern part of Section 27, the following measurements were made:

Near the mouth of Hay Hollow, in Section 28, a layer exposed along the road measured 2 feet 9 inches in thickness. East of this, on land of John Richenbaugh, the section given below was measured along an old road:

One of the brown sandstone layers, measuring from 3 feet to 3 feet 6 inches, is exposed on the point north of the home of George Anderson, in Section 25, Jackson Township. The stratum, here about 30 feet above the flood plain of the Scioto, is correlative with the heavy layer exposed along the Scioto Valley south of Cars Run. North of this on land of Joseph Acord, layers measuring from 1 to 2 feet in thickness were seen.

Near the mouth of Hickson Run, in Section 17, Jackson Township, on land of Pearl E. Cash, the following measurements were made of the strata exposed along the bank of the stream near the river road.

This series of brown sandstones continues northward to Richmondale in Ross County. Some of the upper layers were also noticed along Little Salt Creek.

The weather resistant character of both the gray and brown sandstone layers at once stamp them as fit material for building purposes. Not all the layers though are sufficiently durable for exposed work, for some are shaly and break up on weathering. Both care and judgment should be exercised in selecting and grading the materials. The medium and massive bedded layers are usually the most durable, although this quality is not a function of thickness, for some layers measuring only a few inches are far more resistant than others measuring from 1 to 3 feet. In some layers the blocks show a faint concretionary structure, and on exposure break along concentric lines into spheroidal masses.

The coloring of both the gray and brown varieties is due mainly to the amount and to the state of the iron component present. This in the gray stone is present in the ferrous or reduced state mainly, while in the brown stone the iron has been oxidized to the ferric state. From surface indications the brown stones change gradually into the gray as the cover thickens. The layers in the brown stone series contain a larger amount of iron minerals than the layers in the gray stone series below, for the latter on weathering give only pale browns and yellows, which are not attractive. This is also shown by the association of the gray and brown stone layers found in some sections where the conditions for weathering were equally favorable to both. The difference between the composition of the material in the gray stone series and that in the brown stone series is shown by the following analyses made by Professor Wormley.'

With a few exceptions both the gray and brown varieties are finegrained, rather dense sandstones with clay and ferruginous minerals for the bonding material. The grains in the brown sandstone are usually somewhat coarser thap in the gray. The bedding planes in both are usually too faint to give pronotmced cleavage along these lines, the blocks breaking about as well in one direction as the other. On exposure, due to loss of water and oxidation changes, the rocks harden, but the fresh material is easily worked. The colors also in the weathered material are more permanent, so for exposed ornamental work this grade of stone should be used.

Both the brown and gray sandstones are well suited for building stone as they are strong and durable. There is a large amount of this material available in Pike County east of the Scioto River, as the outcrop of the strata extends from Scioto County northward to Ross. Along the outcrop and in restricted localities where the cover is shallow, the thicker layers should yield a large amount of high-grade material, suitable for plain and ornamental architectural work or heavy masonry. The deposits are not regularly quarried and marketed, at present, at any place east of the Scioto River.

The Logan formation is sub-divided by J. E. Hyde into three members, Byer, Allensville, and Vinton. They are made up of shales, sandstones, and fine-grained conglomerates. The Logan formation usually ranges in thickness from 100 to 150 feet. A section taken at the head of Buck Hollow, in Section 16, Jackson Township, shows the general character of the members:

Maxville Limestone

In Pike County the Maxville limestone is represented only by scattered fragments of cherty material, found along the contact zone of the Pennsylvania!! and Mississippian rocks, between which a pronounced disconformity exists. If the rocks of the Maxville limestone were laid down here, they were so completely removed by erosion before the deposition of the Pottsville material that only cherty fragments remain. The erosion agencies not only removed the Maxville, if deposited, but also in places cut deep into the Logan. A drop of from 50 to 75 feet in one-fourth mile in the elevation of the upper surface of the Logan is not uncommon, and here the Sharon conglomerate thickens proportionally. Evidently the formations were elevated above the water at the close of the Mississippian period, and were thus subjected to erosion for some considerable duration of time. Since the removal of the limestone is so complete, it hardly seems probable that the deposits had a thickness comparable with that found in eastern Scioto and southern Lawrence counties. The condition here rather suggests thin local deposits, or the cherty material found may have been brought in by currents from deposits to the south in Scioto County, or to the east in Vinton, where remnants of limestone strata yet remain.

rocks. There is a pronounced general difference in the nature and kinds of materials making up the Pottsville strata from those making up the Cuyahoga, Logan, and Maxville below. The Maxville limestone, when normally developed, is thick and quite pure, while the limestones found in the Pottsville are thin and generally siliceous. The sandstones in the Cuyahoga and Logan formations are compact, fine-grained, and, with few exceptions, argillaceous, while in the Pottsville the sandstones are open, friable, coarse-grained, and often highly micaceous. The shales of the former are siliceous, rather coarse-grained, and moderately plastic, while the shales of the latter are finer-grained, more plastic, and aluminous, and many contain notable amounts of carbonaceous matter. Coals and high-grade flint and plastic clays, common in the Pottsville, are not found in the formations below. The massive conglomerate at the base of the Pottsville is scarcely comparable with the thin fine-grained conglomerate of the Logan. In all respects there is a decided change in the character of the Pottsville rocks from those below. The Pottsville opens another chapter in the history of sedimentation.

The thickness of Pottsville rocks in Pike County is about 300 feet, of which about half is conglomerate, while the remainder is clays, shales, sandstones, coals, and iron ores. Only the lower part of the Pottsville is present, as the highest strata exposed are just below the horizon of the Quakertown or Wellston coal. The members present are Sharon conglomerate, Sharon coal, Sharon ore, and Sciotoville clay, which are taken up in ascending order.

Sharon Conglomerate

The Sharon conglomerate, the basal member of the Pottsville formation, normally is a massive conglomerate with coarse quartz pebbles, but in some localities these are wanting and there the member is a coarse-grained sandstone. In fact, the composition of the stratum grades from a sandstone to a loose conglomerate with but little fine material. These changes in the stratum may occur either in a short distance horizontally, or in a few feet vertically.

As a general rule, the conglomerate is highly cross-bedded; the horizontal planes vary from an inch or two, to several feet apart, while the inclined planes are usually closely spaced. The stratum seldom shows distinct breaks in deposition, except along the border of the field and in a few localities where the Sharon coal, which will be treated later, is present. The pebbles and sand grains are well rounded and polished, although at least 90 per cent of the material is crystallized quartz. In disappearing, it is characteristic for the stratum to end rather abruptly; it seldom thins out gradually as do the members above or below. Deateni Pike County. The largest pebbles n diameter.

- Brereiated bed composed of flint from the Maxvillr liir.calonr. quart* pebbles from the Sharon eonRlomerBle. and iron oxides for the bondinR component found on the contact of the Missisflippisn and Pennsylvaninn syslcms. This bed is quite conspicuous in ihc southeaRlern port of Pike County.

posits 50 or more feet thick in one hill may not be represented in the next. Both the upper and lower surfaces of the coaglomerate are also very irregular, the resultant of which gives great variation in the thickness from place to place. In Pike County the thickness of the Sharon conglomerate varies from a few feet to at least 150 feet, the latter noted in eastern Jackson Township. The conglomerate seems to fill the depressions in the surface of the Logaa, which may represent basins or old channel ways, but appear more like the former.

The origin of the Sharon conglomerate is a subject of interest. The material is largely crystallized quartz, and thus of igneous origin derived from the granitic rocks. Evidently the source was Archean rocks of the Laurentian Highlands or of the old Appalachians, but the northward trend of the conglomerate, the comparative size of the two fields, and the barriers along the granitic axis of the Appalachians, strongly favor their derivation from the great fields of crystalline rocks to the north. When the area of the conglomerate, the thickness of the stratum, often measuring from 100 to 150 feet, and the percentage of quartz present are considered, it means the breaking doWn of a large mass of crystalline rocks to furnish the material necessary to build up such a deposit. The igneous rocks in the average contain about 12 per cent of quartz.^ The crystals in only a small part of this* 12 per cent are as large as the sand grains and pebbles in the conglomerate. Further there was a large loss of coarse material through internal strains, which fractured the crystals into parts, and through the abrasion which was necessary to round the particles to the state of the conglomerate sand grains and pebbles. The volume of the Sharon conglomerate, under any consideration, must be multiplied by a very large factor to obtain the original mass of crystalline rocks from which its material was derived.

The lapse of time represented by the transition of quartz crystals from the igneous rocks to the rounded sand grains and pebbles of the Sharon conglomerate was also relatively great, for the elimination of associated minerals through chemical and physical agencies, could only be accomplished through long continued action. The character of the conglomerate suggests the work of two potent factors, the first of which is that of disintegration or rock decay, and the second that of differential sorting and deposition of the various liberated components, but both more or less active contemporaneously.

When a rock is exposed to atmospheric agencies it undergoes a partial decomposition and becomes gradually disintegrated. Some of its substance is dissolved by percolating waters, themselves of atmospheric origin, and is so carried away; the remaining material, partly hyd^ated and partly unchanged in composition, contains products which are easily separated from one another. The breaking do^Ti of a rock is effected partly by mechanical and partly by chemical means. Mechanical agencies, such as the grinding power of glaciers, the pounding of waves, erosion by streams, the dis- ruptive effects of frost or the action of wind-blown sand, tend to separate the particles of a rock and to furnish fresh surfaces to chemical attack. Unequal expansion, due to alternations of heat and cold, also assists in producing disintegration. Solution, hydration, disintegration, and mechanical sorting are the successive stages of rock decay. ^

The important magmatic minerals, such as feldspars, micas, pyroxenes, amphiboles, olivine, leucite, nephelite, pyrite, apatite, and titanium compounds, are attacked by the various chemical and physical agencies with ultimate disintegration of the original rock. Quartz, which is quite insoluble, and thus but little affected by the ordinary agencies, is left practically unchanged.

By solution, oxidation and hydration, then, a solid rock is converted into an aggregate of loose material, which may remain in places as soil or be removed. by the mechanical agencies of running water. As a rule the ch^nical processes are incomplete; some of the minerals are not entirely altered, and the loose products therefore exhibit many variations. In general terms, the streams separate the disintegrated materials into coarser and finer or lighter and heavier portions. The clay-like substances are generally light and finely divided, and therefore remain longest in suspension. The heavier sands and gravels are not carried so far, and thus a separation is effected. In these coarser portions are found quartz, together with undecomposed portions of various minerals; the lighter silts are less variable in composition.'

The composition of the Sharon conglomerate shows that the disintegration of the magmatic rocks, and the mechanical separation of the altered integrants /rom the more resistant quartz, were quite complete before final deposition. The original materials may have passed through many alternating cycles of chemical action and mechanical separation before the final deposition of the conglomerate. This is favored by the high percentage of quartz, requiring practically complete rock decay, and by the well rounded forms of the particles, requiring long continued or severe abrasion. If the materials in the conglomerate came direct from the parent rocks, we would expect during a time interval of short duration, a mixture of minerals and more angularity of the particles. The Sharon conglomerate thus appears to be the final product of various forces acting slowly but continuously.

What became of the associated materials is the question which next arises, since the quartz in the Sharon conglomerate constitutes only a small fraction of the 'total matter in the original crystalline rocks, from which it was derived. In the disintegration of magmatic rocks by solution, hj^dration, oxidation, and mechanical means, while the quartz is very resistant and but little affected, the associated minerals are altered to a variety of powdery or fragile minerals, or broken up into fine parts; for example, feldspars give kaolinite, micas alter to soft secondary products or break along the cleavage planes into thin plates, and ferro-magnesium minerals give a variety of products usually low- in the scale of hardness. When prolonged these forces thus tend to increase the dilBference between the average sizes of quartz particles and those of the alteration products of the other original integrants.

During transportation the coarse materials continually lag behind the finer products, so, applying this to the disintegration products of magmatic rocks, the quartz would be the lagging component. If the rocks decayed on the land, the fine alteration products would be carried farther by the rains, rivulets, and streams than the coarse unaltered quartz; if the breaking up occurred along the sea shore the finer materials would be carried far out into deep or quiet waters, while the coarse material would be left within the zone of wave action, or along the courses of strong currents. Due to the extreme hardness of quartz it is only slowly reduced by abrasion forces, but many associated minerals are easily ground to rock flour. The finer minerals would be the first to reach the sea, and the first to be carried away by moving oceanic waters. If the breaking up of the rocks occurred far inland, especially where the stream gradients were low, the finer materials would reach the sea far ahead of the coarse quartz. Sluggish streams would not transport the latter. If the beach line remained nearly stationary, and the shore not swept by strong currents, the distribution of the quartz would be local, but the finer materials widely scattered. The sedimentation of this fine material would form shales and shaly sandstones, such as make up the Mississippia o rocks.

The pebbles in the Sharon conglomerate are all highly abraded. In the main they are well rounded, indicating that the abrasion was produced through rolling action of currents, but some are flattened, indicating shore action. The cross-bedding of the stratum, highly pronounced, also indicates current action. Considering all points, the history of the Sharon conglomerate seems to indicate that the decay of the crystalline rocks reached an advanced state on low lying uplands; that the products were slowly transported to the sea, coarse materials lagging far behind the finer products; that the fine materials were distributed to the deep and quiet waters, forming shrle, while the coarse materials were left more localized along the margins; that a general elevation took place, converting much of the floor of the sea to land, and restricting the currents to narrow shallow passages; that the force of these currents was now sufficiently strong to transport the coarse quartz, and thus build up the conglomerate. It represents the final act of a series of agencies, which includes rock decay, transportation, selection of' material, crustal forces, and final deposition.

A few general sections showing the thickness and character of the Sharon conglomerate, and its relation to other members, will be given. The upper part of the Sharon conglomerate, with the Sharon coal, which has been mined for local use, and the Sciotoville clay above.

From the forks of the road on Gravel Hill, in the southeast comer of Section 19, to the ridge west, there is a rise in the upper surface of the conglomerate of about 50 feet in one-fifth mile. The roll or sudden change in the elevation ol the upper surface is similar to that noted at a number of places in Jackson and Scioto counties. Near the head of Andrew Hollow the CQnglomerate measured 60 feet in thickness; the lower part is made up of pebbles, loosely cemented, but the upper part is a coarse-grained sandstone, with only occasional pockets of pebbles.

West of this, on land of Willis Hartley, a conglomerate was also seen above the Sharon coal, which condition was noted in many localities in Pike and Jackson counties. The rocks here measured as follows:

Along the road west of the above, both the coal and the upper surface of the conglomerate rise 18 feet in about 100 feet. The Sharon conglomerate also thins going westward. In the same section, south of Allen Chapel, on land of Samuel Graw, the following rocks were exposed:

The rock above the coal is very similar to the true conglomerate below, in composition and texture, excepting that it contains fewer pebbles. The coal may be said to lie in the Sharon conglomerate. North of Allen Chapel, on land of Joseph Hartley, the Sharon coal is wanting, but the Sciotoville flint cby is foimd along the roadside lying above the conglomerate. A section taken here follows:

The Sharon conglomerate, varying from a coarse-grained sandstone to a very pebbly conglomerate, and from 10 to 70 or more feet in thickness, is quite persistent throughout Marion Township. In the eastern part of the township the upper surface of the conglomerate is found at an elevation of about 880 feet, while in the western part it is about 950 feet. In Union Township the conglomerate is found near the fiiunmits of the high hills and ridges east of Pecks Creek. The high knobs on the main ridges between Owl Creek and Dutch Run, and

Dutch Run and the Beaver Creek Valley, are capped with conglomerate, which varies in thickness from 10 to 60 feet. Where the deposits are thick the lower part is usually very pebbly, while the upper part is practically a coarse-grained sandstone. . The deposits are found above the 1,000 foot contour. The conglomerate was noticed on one hill only in Scioto TowTiship. Pine Knob, in Section 9, is capped with about 30 feet of pebbly conglomerate. The fragments indicate a continuous sheet of conglomerate in this area, which was cut away by erosion, leaving patches on the high places and ridges only.

In the northeastern part of Beaver Township the Sharon conglomerate is massively developed, but south of this it thins or is wanting. In the central part of the township it is usually wanting, but where present it is represented by coarse-grained sandstones seldom more than 20 feet in thickness. In the western p*art of the township it is found on a few knobs only in the vicinity of the Rock Spring School, where it measured 45 feet in thickness. The upper surface of the conglomerate here has an elevation of about 1,020 feet. The conglomerate was found in Seal Township only on two hills, which are in Section 20. On one only loose blocks were seen, but on the summit of the other hill there is about 10 feet of the stratum in place. Here it is made up of loosely cemented pebbles, some of which are 2 inches in diameter. The elevation of the deposit is about 1,120 feet above the sea. In eastern Jackson Township the Sharon conglomerate is massively developed, the thickness often reaching from 100 to 150 feet. The elevation of the upper surface, marked by the outcrop of the Sharon coal, is approximately 950 feet. In the northern part the stratum extends westward to the Scioto Valley. Chimney Rocks are composed of conglomerate, the total thickness of which here is about 70 feet, and the elevation of the upper surface of which is about 1,100 feet. The main ridge between Hickson and Mutton rims is made up of massive conglomerate, wliile four high knobs have the sandstone above the horizon of the Sharon coal. Between Mutton Run and Hay Hollow the conglomerate is usually present on all the hills and ridges that extend above the 900 foot contour. The stratum on the high knob in the southwestern part of Section 24 measured 50 feet in thickness. The lower part is composed of coarse pebbles, loosely cemented, but the upper part is more sandy and contains only small pebbles. In Section 25, on L. T. Johnson's farm, the deposit, some 70 feet in thicloiess, shows 20 feet of very coarse material at the base, with 50 feet of sands containing smaller pebbles above. The same condition holds true also for the deposit noted on land of James Hartley, in Section 16. The high places on the main ridge between Hay Hollow and Jackson Run also contain heavy deposits of Sharon conglomerate, which measure from 40 to 90 feet in thjckness, and vary in composition from coarse sandstone to coarse conglomerate. The elevation of the highest part exposed is about 1,020 feet. No conglomerate was noted on the ridges between Jackson Run and Cars Run, although the elevations of soma of the high hills are above those to the north which contain conglomerate. The bed is wanting, because on a few knobs the sandstone above the horizon of the Sharon coal is present. The rocks making up the main ridges are Mississippian shales and sandstones. West of Cars Run no conglomerate was seen on the ridges, excepting on the high hill facing the Scioto in Section 4. This knob, capped with about 15 feet of conglomerate, has an elevation of only 920 feet, while many ridges and hills south, made up entirely of Mississippian rocks, rise from 1,000 to 1,M)0 feet above tide.

The Sharon conglomerate in Pike County has been used for many years for local purposes, but it has never been prepared for the market. The gravel from the conglomerate is the common road facing used in the eastern part of the county, for limestone and other hard rock are wanting. The conglomerate is widely distributed and the gravel easily obtained from the loosely cemented pebbly layers by plowing, picking, or shooting. The material, when composed largely of pebbles requires some time to thoroughly pack, but it then makes a good solid surface. If mixed with sand, or a small amount of clay, it packs more quickly and wearig better. From this material good roads may be made at a low cost. This gravel withstands the wear from heavy traffic better than the glacial gravel from the Scioto River, which is also used locally for road purposes. The gravel from the Sharon conglomerate is used, to a small extent, for concrete work, such as walks, culverts, foundations, and silos. It is quite free from clay, rock flour, or fragile material, but the pebbles and sand grains lack angularity, which gives an interlocking structure. On the whole the material makes a concrete with sufficient strength for all ordinary purposes.

The best economy would be obtained by sizing the material first, then proportioning each size to that amount required to give body and to fill the voids. For concrete work in general, this gravel cannot compete with the more accessible glacial gravel found klong the Scioto River, although the former is of much better quality. The coarse pebbles are suitable for decorative concrete work, as their rounded forms and light colors are attractive. For concrete work the sand from the Sharon conglomerate is also superior to that found along the Scioto River, as the latter contains a much larger amount of fine or silty material and fragile particles, due to the decay of mineral components.

This gravel, crushed and properly sized, would make an excellent sand-blast abrasive, for on account of the hardness of the quartz, and the sharp edges produced by breaking, its cutting power would grade high, and the material would not be easily worn out, but could be used a number of times. The crushing of the gravel would not be extremely difficult, as the pebbles are more or less fractured from expansion changes. Crushed gravel is also used in a small way for a number of minor purposes.

CoDunonly, a part of the Sharon conglomerate, and in some localities, the entire stratum, is made up of sands which contain at most only scattered pebbles or small pockets of gravel irregularly distributed. These sands, containing but little kaolinite, mica, or other aluminous minerals, are generally stained with iron oxides. In some deposits, locally, the latter component is also low, and there the crude sands are of glass sand quality, but they seldom reach the composition of the highest grades, although, if carefully selected and washed, very pure material may be obtained. The impure sands alone are usually somewhat lacking in bonding materials for general molding purposes, l)ut, if mixed with a small amoimt of argillaceous sand, they make good strong forms. The crude sands are well suited for pig beds or open casting work. In Pike Count}', the Sharon conglomerate has not been worked for general shipment, as the deposits are not favorably located with reference to the present railroads. The contemplated extension of the Chesapeake and Ohio Railway will make available some of the deposits in Union and Jackson townships. Evidently, due to the variety of materials that may be produced, these deposits will be of some considerable importance in the future and should be considered an asset, especially when favorably situated.

The Sharon and Anthony are the only coals represented in Pike County, and only the former has a thickness sufficient for mining. The area in Pike County forms the western margin of the Jackson field, and the stratum, with but few wants, may be traced, excepting where cut away by erosion agencies, directly to the town of Jackson, where it was first mined. Also from Beaver and Jackson townships the bed may be traced eastward to the Quakertown or Wellston coal field in Jackson County. Its northward extension into Ross County is represented by a few thin or bony deposits, found on the main ridge south of Peters Cave in Jefferson Township. The small field in Marion Township is also correlative with that in Madison Township, Scioto County. The Sharon coal, in Pike County, is of interest for its relation to the Sharon conglomerate, and for the local supply of fuel which it furnishes.

The Sharon coal may be defined in a general way as the first coal stratum above the Sharon conglomerate. Yet this does not always hold true, for, in some localities, a thick conglomerate is found above the coal, while in other localities the conglomerate is wanting below the coal; and, at a few places noted elsewhere, the Sciotoville clay with the Anthony coal above, lies on the conglomerate. The stratum is marked by irregularity of deposition. The upper surface of the Sharon conglomerate is very imeven, and the coal stratum lying close to this floor, is subject to many dips and rolls. It also varies greatly in thickness and composition. A 3 foot bed in a short distance may change to bone coal and carbonaceous shales, thin to a few inches, or be replaced completely. The bed is made up generally of one coal bench only, but this may have one or more bony partings. Normally, the Sharon coal lies from 30 to 40 feet below the Sciotoville clay, but this interval is subject to great variation. In Jackson County, at the abandoned Star Furnace mine, the clay in local areas forms the roof of the coal. The Sharon coal usually lies from 70 to 80 feet below the Quakertown coal, but the latter bed was not observed in Pike County. The structure of the stratum and its relations to other members will now be discussed.

Marion Township. - In Section 28, Marion Township, on land of Josephine McClain, west of the Stockdale-Beaver pike, the Sharon coal was formerly mined for local use. The section obtained is as follows:

The coal here is reported to vary from 1 foot 8 inches to 2 feet 4 inches in thickness. On the northern line of this section, near the home of Earl Brown, the blossom of the Sharon coal was seen in the road. To the west and north the Sharon conglomerate rises fast, the Sharon coal is wanting, and the Sciotoville clay, both flint and "pink eye/' was seen only a few feet above the conglomerate. The roll here in the conglomerate cuts out the coal. The Sharon coal was formerly mined for local use on land of John Swartz on Gravel Hill, Section 29. The coal is reported to have a thickness of from 2 feet to -2 feet 4 inches. A composite sectior taken there follows: formerly mined along the outcrop. The stratum is reported to vary from 1 foot 8 inches to 2 feet 4 inches. The quality of the coal is very good. Along the road in the northeastern part of the same section a heavy blossom of the Sharon coal was seen. The floor of the bed is massive, pebbly Sharon conglomerate and the roof a heavy sandstone. North of this in Section 17, on land of B. F. West, the bed, which has been worked in a small way, is reported to average about 2 feet in thickness. The roof is shale. In Section 16, along the road near the home of Fred Keppler, the blossom of the Sharon coal was seen above the massive conglomerate. In the well at this house, Mr. Keppler reports 2 feet 6 inches of stain. The coal in this region is probably rotten as the cover is shallow. In Section 14, near the home of John Lyons, thick exposures of Sharon conglomerate were seen. Mr. Lyons reports that there is a thick blossom of coal lying just above this, but it has not been prospected.

Union Township. - In Union Township, the Sharon coal was seen only on Gravel Hill, although there are other places with rock stratigraphically above the Sharon conglomerate. Coal for local use was mined for several years on the land of Jacob Fraser on Gravel Hill, in Section 19. The rocks measured there are as given below:

Here the coal is reported to have a thickness ranging from 1 foot 8 inches to 2 feet 4 inches. From Gravel Hill to the next ridge west the Sharon conglomerate rises about 50 feet, and the coal is probably wanting, for it was not found or reported. There are a few points west of Pecks Creek, also, with rocks above the Sharon conglomerate, but no coal was seen.

Beaver Township. - ^There is a small area of Sharon coal in eastern Beaver Township, although in part of this the bed is thin or bony. In Section 26, on land of Henry Bapst, the following rocks were exposed:

On the main ridge north of this the blossom of the Sharon coal was seen at several places, but no good sections were obtained. The coal is patchy and generally thin.

Jackson Township. - The most productive area in Pike County is in eastern Jackson Township, where the coal has a fair average thickness, and is father persistent. Coal for local use has been mined for

The Sharon coal was opened on land of J. W. Overly, in Section 2. Mr. Overly reports the thickness, where opened, to be from 2 feet 4 inches to 2 feet 6 inches, and the coal of good quality. The section taken along the road south of his home is as given below:

Coal has been mined for local use on land of Willis Hartley for many years. Here there is a pebbly sandstone above the coal, which is quite similar in character to the conglomerate below. On the outcrop there was only 8 feet of conglomerate exposed, but Mr. Hartley says in the hill this has a thickness of 20 feet. The shale or draw slate above the coal is also reported to be wanting under heavy cover. The section taken shows the following relations:

Along the road in the western part of the same section the coal rises about 15 feet in approximately 100 feet. The section measured is^as follows:

South of Allen Church, on land of Samuel Graw, the Sharon coal with the heavy conglomerate above is exposed at the old mines near his home. The section taken follows:

Sandstone, massive, interbedded, with scattered pebbles and thin gravel layers, resembling the conglomerate below the coal. May be called a conglomerate ,_ . 18

In the southern part of Section 3, on land of J. D. Walker, the Sharon coal is being mined for local use. The thickness is reported by Mr. Walker to var>* from 1 foot 5 inches to 2 feet 6 inches, but to average about 1 foot 8 inches. The quality of the coal is ver>' good The pebbly sandstone or conglomerate was seen above the coal here also. The following are the measurements of the rocks exiK)sed:

West of this, on the high knob in Section 4, the sandstone with pebbles found above the horizon of the Sharon coal is about 60 feet in thickness. It lies directly on the conglomerate, which is also very thick and very pebbly.

In Section 31, just north of Allen Chapel, the Sharon coal is wanting, but the Sciotoville clay Ues on the conglomerate, or the pebbly sandstone above the horizon of the Sharon coal. Xo distinct line of disconformity was noted between the two conglomerates. The section taken follows:

North of this, on the Isaac Wiekline farm, coal has been mined for a number of years, and the thickness is reported to varj' from 2 feet 4 inches to 2 feet 6 inches. The following section was obtained at the. mines:

On the northwest comer of Section 31^ on land of Jasper Bowman, the coal has been mined for local use. The bed here is reported to vary in thickness from 1 foot 6 inches to 2 feet 2 inches, and to average about 1 foot 8 inches. The heavy sandstone stratum is found above the coal, but in places shale, varying from a thin parting to 3 feet, separates the two. The following rocks were exposed for measurement:

In Section 30, on land of W. H. Sprague, the stratum is made up of bone shales with thin coal bands, while along the ridge northwest of this the coal is wanting. The section taken near Mr. Sprague's house is as given below:

In Section 22, near the home of Peter Lew, Jr., coal is mined for local use. The stratum is reported to have a thickness of from 1 foot 10 inches to 2 feet 8 inches. The bed shows irregularity of 'deposition, for there is a dip of 20 feet to the north in about 100 yards. The blossom of the coal was seen at a few places along the ridge north of this in Section 19, but, as the cover is shallow, it has not been worked. In the northwest corner of this section the rocks exposed were as follows:

On the high point near Chimney Rocks there are about 75 feet of strata above the horizon of the Sharon coal. The blossom of the coal was not seen. West of the main ridge in eastern Jacksou Township, which is the productive area, the coal seems to be very thin or completely wanting, although there are many hills above the horizon. On some of these the Sharon coal is replaced by the heavy sandstone above, which lies directly on the conglomerate. On some, both the Sharon conglomerate and coal are wanting, and the rocks near the horizon of the Sciotoville clay are in contact with the Logan sandstone or shales.

The estimated area of the small field in Marion and Union townships is only about 400 acres, of which, from surface indications, not more than 60 per cent is productive territory; while the area of the large field in Beaver and Jackson townships is approximately 2,000 acres of which, judging from the distribution of the mines, about the same per cent is productive. The total area in Pike County, in which the Sharon coal has sufficient thickness and cover for mining, is approximately 1,400 acres. Due to the uncertainty of the bed this estimate may be somewhat high. The coal for many years has contributed a i)8iTt of the local fuel supply. On Allen Ridge it is the main reliance. Although the coal has been drawn from a part of the productive area, the supply yet available is ample for local wants for many years. So far the mining has been done in a rather haphazard way, for the mines are worked usually only a few months during the fall and winter. The method usually followed is single entry with side rooms, little provision being made for ventilation or drainage. The coal cars are pushed by hand. The system used admits only of mining close to the outcrop, so the main bodies of the coa4 are yet untouched. The area and thickness of the bed, with the limited fuel demand, are not sufficient to warrant operation on a large scale. The bed varies in composition and structure in much the same way as in the Jackson field. In some localities it is made up of quite pure coal, in others of rough bony coal, and in others of black bony shales with thin coal bands. The coal averages rather high in ash, which is light colored and powdery, but low in sulphur. It has a good solid structure and a bright color. It bums readily and has good heating power. On the whole the bed is of importance for a local fuel supply. -

The sandstone which is found above the Sharon coal in a part of this region, and which in places is very pebbly, having all the characteristics of a true conglomerate, is of interest. The pebbles in this sandstone are similar in composition and shape, but average somewhat smaller in size than those in the true conglomerate below, both evidently derived from the same original source. It is questionable whether this pebbly sandstone should be considered a part of the Sharon conglomerate, although in some localities the two are quite alike in structure and general appearance. The Sharon conglomerate varies from a very coarse-grained pebbly conglomerate to a medium finep^rained sandstone, and this sandstone above the coal has the same usually to thin layers near the base of the deposit, or are distributed irregularly throughout the mass. This sandstone is pebbly only in local areas, while the Sharon conglomerate- generally contains more or less coarse material. Pebbles are common also to strata higher in the Coal Measures, notably, the Guinea Fowl ore, the sandstone below the Quakertown coal, and that above the Lower Kittanning coal. The time interval between the deposition of the Sharon conglomerate and this sandstone was of suflScient diu-ation to allow the deposition of the Sharon coal, and in some localities a few feet of shales and shaly sandstone. In the localities where the intervening coal and shales are wanting, as a general rule, there is a well-defined disconformity between the two deposits, but at some places no separation was evident. The deposition of the coal and shales involves elevation changes or restriction of current action. . In this sandstone, a part of the material, including the coarser pebbles, may have been derived also through erosion from land masses of conglomerate, the existence of which, during this period, is indicated by the pronounced disconformity noted in localities to the south, where the conglomerate ex:=^ tends into the upper measures to the horizon of the Sciotoville clay. The evidence points more to similarity of conditions during deposition - ^the same as existed during the formation of the coal beds - than to a direct relation between the two deposits. In the opinion of the writer, the pebbly sandstone deposits above the Sharon coal should not be considered a part of the Sharon conglomerate.

Only a few small pockets of ore, which were placed with some confidence on this horizon, were foimd in Pike County. In Section 23, Marion Township, on land of W. M. Lyons, ore was formerly mined for the Star Furnace Company, Jackson, Ohio. Mr. Lyons reports the stratum to vary in thickness from 4 inches to 1 foot 6 inches, and the ore to Tbe of good quality compared to other native ores. The ore was mined by stripping. Here the Sharon conglomerate is wanting and the stratum lies close to the Logan sandstone. No section was obtained, as the strata were more or less covered when the region was visited. The same ore was also mined for the same company south of this on lands of William Ehrman and G. W. Keller. Here the stratum is reported to have a thickness of from 10 inches to 1 foot 6 inches, and the quality to be the same as that on the Lyons property. This ore was also exposed along the road in the southern part of Section 3, Jackson Township. Here it lies close to the Sharon conglomerate which is massively developed. The value of the deposits is small.

the area the clay is replaced by massive sandstones, but even where the strata are mainly shales the member is seldom present. In Section 19, Union Township, on* land of Jacob Fraser, the Scioto ville clay was seen well above the Sharon coal. The relation of the Scioto ville clay to that of the Sharon coal and conglomerate below is about normal. The section taken on this land is as follows: p^ j^

In Section 28, Marion Township, on land of Earl Brown, pieces of good quality flint clay with a heavy *'pink eye" clay below were seen on the outcrop. Here the Sharon conglomerate shows a decided roll; the clay lies close to the crest of this and the Sharon .coal in the trough to the east. Along the road that leads from the ridge to McDowell Creek, in Section 27, the clay was seen also lying close to the conglomerate. The Sharon coal here is wanting. The rocks exposed are as given below: p^ ,^

North of Allen Chapel, in Section 31, Jackson Township, on land of Joseph Hartley, an exposure of very good flint clay was seen. It lies close to a conglomerate, the upper part of which appears to be the same as the pebbly sandstone or conglomerate found above the Sharon coal just south of Allen Chapel. The section recorded is as follows:

" The Sciotoville clay in Pike County has practically no economic value, for the deposits are small, widely scattered, and far from transportation facilities. The quality of the clay observed on land of Joseph Hartley is very good, but the territory apparently small. These deposits are of interest stratigraphically, for they form connecting links in. the chain of deposits extending northward from the Scioto County fields to those in Vinton County, and they also show the wide distribution of the Sciotoville clav.

Anthony Coal

The Anthony coal lies just above the Sciotoville clay, but in Pike '^ unty only a thin stain or blossom was noted, and that in but two tics.

Sandstone Near Horizon Of Sciotovillb Clay

The sandstones near the Sciotoville clay horizon in some localities are quite pure, approaching glass sand quality. They were noted especially in eastern Marion Township. On the high hill near the line of sections 27 and 28 the deposit measured 12 feet in thickness. The sandstone there is light colored, rather fine-grained, and quite free from clay, mica, or iron minerals. It is used locally for foundation and bridge stone. It appears to correlate with the sandstone observed near Glade in Jackson County.

Items Of General Interest

The large number of perennial springs in the regions where the Sharon conglomerate is well developed are of interest, as they afford an ample supply of very pure water for both man and beast. In this respect there is a marked contrast between these regions and those where the rocks are Mississippian shales and sandstones, for, in~ the latter, constantly flowing springs are few, and the waters of these generally poor. These springs usually issue from near the base of the conglomerate, which, as previously described, forms many bold cliffs and gorge-like valleys. In the heat of the summer, around those springs, especially when sheltered by the cliffs and trees, are foimd cool retreats for the live stock. Many of the springs have a strong flow of water, and issue well above the valley plains, so that irrigation in a small way may be carried on during the dry summer months, cheaply and profitably. Their value for truck gardening is worthy of consideration.

The high sandy ridges, especially in the regions ^here the Sharon conglomerate is prominent, are excellent fruit lands. The trees, when given proper attention, bear abundantly, and the fruit is highly colored and of excellent quality. Orchards on this ridge land may be cultivated and sprayed with ease. The conditions for marketing at present ' are somewhat unfavorable, but with the extension of good roads into the hilly regions these conditions will be improved. There is also some good fruit land in the old preglacial river valleys in eastern Pike County. The parts best suited are the high terraces and those on the main plains, which are well drained by small streams. The areas that are swampy, or have a hardpan close to the surface should be avoided.

A few small but very good orchards are found in the old Teays River Valley a few miles east of the Scioto River. The largest orchard in the region, however, is located in the valley of the Portsmouth River, about 1 mile east of Wakefield. The owner, W. W. Tibbals, kindly gave the following information concerning it: "The farm, which consists of 186 acres, is located on the top of a ridge, which has an elevation from 800 to 850 feet above tide. More than 100 acres are as level as the land in the Scioto bottoms. From this level tract the land slopes to valleys on the north, south, and west; hence it has natural conditions favorable for perfect air and water drainage. The orchard covers a territory of 80 or 90 acres, and consists of about 11,000 peach trees, the main varieties of which are Carmen, Belle, Elberta, Old Mixon, Stump of the World, Chairs Choice, Smock, and Salway.

"Modem methods have been employed in caring for the trees fnwn the beginning. The trees are headed low; hence more than 75 per cent of the fruit is gathered without ladders. The trees are sprayed from one to three times each year, which keeps them in good condition. The entire orchard has been cultivated from the time the trees were set. During May or June the ground is either plowed or disked. It is then harrowed frequently until late in July. Cow peas are then sown for a cover crop and for soil enrichment. The trees are very thrifty and the fruit produced is large and perfect. The fruit ripens just between the southern crop from Georgia and the northern crop from Michigan; hence it ripens at a time when fruit commands good prices. With the modem methods of orchard heating and smudging a crop failure seldom occurs. Considering the low price at which undeveloped land in Pike County is valued, I consider this an excellent territory for an investment of this kind."

Chapter Iv

This county is of special interest for its ceramic products. The manufacture of fire brick began in 1864, and the business has remained prosperous, as the ware enjoys a good reputation and a wide market. This region is also one of the recognized centers of the paving brick industry of the State. For years the charcoal iron furnaces were important, but these have been dismantled. The ores, coals, and limestones have but little economic value, but the vast wealth of clays and shales indicates a bright future for the established ceramic industry.

Scioto Coimty lies in the southern part of the State on the Ohio River, which thus forms its southern boundary. It is bounded on the east by Lawrence and Jackson counties, on the north by Pike, and on the west by Adams. The area of the county, according to the latest government estimate, is 640 square miles. That part of Scioto County east of the Scioto River only will be treated in this bulletin.

The surface of Scioto County has been extensively modified, both by the present streams and by preglacial streams. The region is rough and broken, except the flood plains of the Ohio, Scioto, and the preglacial Teays rivers. The flood plain of the Ohio along Scioto County is generally narrow, but that of the Scioto averages from one and onehalf to three miles. A preglacial stream (Teays) ran northward across the county through the California Valley from the present Ohio Valley near Wheelersburg into Pike County near the village of California. This old valley is from one to two miles wide and very level, excepting that part from Wheelers Mills, south, which has been dissected by the Little Scioto, and left notably terraced. The flood plain of the Little Scioto, north from where it enters the California Valley at Wheelers Mills, is usually very narrow, seldom exceeding one-fourth mile in width. The Pine Creek Valley in Scioto Coimty averages about one mile in width along the lower course, but narrows to one-half mile in Vernon Township. That part of the county that lies between the Scioto and the California valleys is exceptionally broken and rugged, as it has been dissected by many small streams, which have cut deeply into the Waverly sandstones and shales, thus forming hills with steep bluffs and narrow ridges. The area east of the California Valley, although traversed by numerous small streams, is more varied, as the soft coal formation strata have yielded more readily to erosive forces, which have thus widened the valleys and rounded the hills. An exception to this is in Madison Township, where the streams in cutting through the massive Sharon conglomerate have left the hills steep and the valleys gorge-like.

The Ohio River receives directly or indirectly the waters from the entire region. The Scioto River, which enters the county from the north, flows south, and empties into the Ohio at Portsmouth. It receives the drainage of only a small territory east of the stream, which comprises Valley Township and the western parts of Clay and Jefferson townships. The Little Scioto River, which is formed by. the junction of Brushy and Rocky forks, flows southward, and empties into the Ohio near Sciotoville. It is the most important stream in the eastern part of the county, and, as it lies in the basin of the old California Valley, it drains Harrison, Madison, and parts of Porter, Clay, Jefferson, Bloom, and Vernon town^^hips. - Pine Creek, which heads in Lawrence County, flows southward into Scioto Coiiinty, and empties into the Ohio above Wheelersburg. It drains parts of Green, Vernon, and Bloom townships.

A system of preglacial rivers, which flowed northward across the county, and greatly modified the topography, can be traced by their old valleys, that now are of special interest on account of their hist-ory, and on account of the fertile farming lands found in them. These old rivers left large areas of level or gently rolling lands, which otherwise would have been broken and hilly; thus the valuable uplands of Dogwood Ridge, with the level belt extending northward past Harrisonville and Stockdale, are but the flood plain of the old Teays River. The effects of the old rivers are shown also by the meanderings and directions of tbe courses of some of the present streams; for example, the waters from the head of Long Run, which rises about three miles from the Scioto, and three and one-half miles from the Ohio, travel over 30 miles before they finally reach the latter stream. The tortuous course and gorgelike valley of the Little Scioto, from Harrison Mills north to the county line, is due to the stream having been formed from several tributaries of the old Teays River. The history of the main stream has been givenby W. G. Tight, who made a careful study of the region. The two old rivers of importance recognized by him are the Teays and the Portsmouth. California Valley.' - North of Wheelersburg and near Stockdale, in Scioto

'Prof. Paper No. 13, United States Geological Survey. Drainage Modification in Southeastern Ohio and Adjacent Parts of West Virginia and Kentucky, by W. G. Tight, pages 57-58.

- Valley of the preglacial Teays Iliver near Wheelerebtirp, Scioto County. This valley is about 150 feet above that of the Ohio River, and more than 1 mile wide

B. - An old valley near Bloom Station in Scioto County cut at nearly right angles by Halea Creek. The main valley appears in the background.

County, and extending into Pike and Jackson counties, is the old California Valley, which has been described by the author and Mr. Frank Leverett, and correlated, with considerable confidence, with the Flatwoods and Teays valleys, on the basis of the grade of the old valley floor and the deposits found upon it, which consist of gravel beds of quartz pebbles overlain by silt deposits. The southern portion of this valley is very deeply cut by the Little Scioto River and its tributaries, but the northern portion, in the vicinity of California Flats, and the area extending thence northward to the Scioto at Waverly, are very perfectly preserved. Its featm-es may easily be observed from the train on the Ohio Southern Railroad at Beaver. Between the Ohio at Wheelersburg and the Scioto at Waverly this floor has at present at least five water partings across it, which is suggestive of the great length of time which has elapsed since its abando^unent and the establishment of the present drainage. The elevation of the valley floor where it is cut by the Scioto Valley is, as near as can be estimated, about 600 feet above tide. This would make a grade of about nine inches to the mile between St. Albans, W. Va., and this point, a distance of about 100 miles. As indicated in the articles referred to, the topographic features of the California Valley are quite identical with those of the Teays and Flatwoods valleys, and the history of the cycles through which this region has passed is almost exactly similar to that of the other valley.

The deposits on these old valley floors differ markedly from those on the floors of the present through-flowing streams, that is, the Ohio and Scioto rivers. In the preglacial valleys the deposits are characterized by the presence of thick beds of clays with interbedded sands and by the absence of notable amounts of gravel, the pebbles of which are composed of limestone or igneous minerals, while along the Ohio and Scioto rivers the deposits are marked by the thick beds of sands and gravels, and by the composition of the materials, some considerable part of which is from limestone and granitic rock. In general the deposits are of two distinct types, and they represent two periods in the history of the streams. Thin beds consisting, in the main, of sandstone bowlders and pebbles, flint from the Maxville, Pottsville, and Allegheny limestones, and quartz pebbles from the Sharon conglomerate, which outcrops in the adjacent hills, are usually found lying on or close to the bed-rock, while above this are present heavy beds of light gray or bluish clays, where unweathered, with interbedded sands, which in places are highly comminuted. These deposits represent the deposition work of the streams during their period of normal activity. Along the margins of the old valleys, and on the water divides of the streams now dissecting them, heavy beds of clays, highly stratified, and distinguished by their plastic, soapy character, and by their freedom from sand, compose the upper layers of the valley deposits. These clays were laid do^Ti in quiet waters during the slack-water or flood stage, which resulted from the damming of the lower courses of the streams by the advancing ice sheet.

Portsmouth Valley.* - Excepting the Teays River, the most important of these old streams thus mapped and described by Tight is the Portsmouth, which, flowing northward from the city of the same

Between Soiotoville and Portsmouth the valley is again constricted, and there is another col, which wiU be called the Portsmouth col. The valley is not so narrow at the Portsmouth col as at many other points where it has cut through old divides, but the bordering hills are very high, rising from 350 to 400 feet above the river, and presenting very steep faces and often vertical cliffs to the river front, so that, while the valley is not so narrow, the location of a col at this point seems certain.

At Portsmouth the river valley bends southwestward and increases considerably in width. To an observer in the Scioto Valley the valley of the Ohio below Portsmouth seems the natural and direct continuation of the Scioto, and to the observer in the valley of the Ohio below Portsmouth, looking up the river, the Scioto Valley seems the natural and direct continuation of the Ohio Valley, as the Scioto River Valley broadens as one passes up the Scioto^ while the valley of the Ohio narrows rapidly upstream above Portsmouth.

These features at this point are very suggestive with reference to the direction of the old drainage lines, and indicate that the old valley was continuous between the Scioto and the portion of the Ohio below Portsmouth.

It is interesting to note that all the smaller tributaries of the Ohio further downstream in this section enter the valley in a direction opposite to the course of the river. At Quincy, at the mouth of Kinnicoiiick Creek, the topographic features indicate that the continuation of the valley of the Kinniconick was normally up the present Ohio Valley, or northeastward; and below the mouth of the Kinniconick the Ohio Valley begins to narrow rapidly until it reaches another marked constriction, in the vicinity of Manchester, where it is evident, from the steep sides of the valley walls and the elevation of the table-land on each side, that the river has here crossed another col, which win be known as the Manchester col.

East of Lucasville, and also in the northern part of Valley Township, northeast of Clifford, fragments of what evidently represent parts of the old Portsmouth River Valley are distinctly noticeable, as these high plains contrast strangely with the rugged topography of the country eastward, where the hills rise about 400 feet above them, or with the flood plains of the Scioto about 150 feet below these high plains. The elevation above tide of the surface of these plains, where least disturbed by the dissecting streams, is about 680 feet, while that of the rock floor, as nearly as could be determined, is about 640 feet. These figures agree with those of the California Valley, and thus tend to establish its relationship to the preglacial drainage. A comparison of the deposits on the rock floor of these upland plains to those on the flood plains of the Scioto shows also that the materials forming them were not derived from a common source.

The deposits on the flood plains of the Scioto are made up of alternating beds of gravel, sand, and silts, the first often very thick and the particles well sorted. On examination the pebbles, in the main, are found to be granite or limestone. This material is of glacial origin, as the gravel trains are easily traced to the drift sheet farther north. The deposits in the upland valleys east of Lucasville and northeast of Clifford are different in character. The headwaters of the Portsmouth River, as defined by Tight, reached the Upper Silurian limestones in Adams Coimty, Ohio, and Lewis County, Ky. The main basin was carved from Devonian and Carboniferous rocks, which consist principally of shales and fine-grained sandstones. Irregular deposits of Maxville limestone, Sharon conglomerate, Sciotoville clay, and thin coals are found on the high ridges along the eastern rim of the basin. Fluvial deposits derived from such rock would be clays and fine-grained sands principally. The rock floor of these old stream beds is formed of Cuyahoga shales and sandstones, and the deposits at present, as nearly as could be determined, are from 20 to 50 feet in thickness. The deposits, where examined, show the following jgeneral structure and composition: on the bedrock there is a layer only a few feet in thickness, which is made up of clay, sand, and gravel, with some bowlders, ore nodules, and cherty masses; the next layer, which constitutes the main body of the beds, consists of irregular interbedded sheets of variable thickness of clays and of fine-grained sands, with some pebbles and cherty material scattered promiscuously throughout the mass, while the upper layer is usually clay. The bowlders examined were sandstone, and their texture is ^bout what would be expected from locally derived sandstones or freestones. No limestone bowlders were noticed, but they may be present, for, owing to a lack of exposures, the chances of observing the lower layer of these deposits are few. The ore nodules are evidently from local sources, as ferruginous concretions are abundant in the Cuyahoga and Logan shales. On the horizon of the contact of the Pennsylvanian and Mississippian rocks there is found a thin, rather persistent stratum, which is made up of brecciated cherty material from the Maxville limestone, quartz pebbles from the Sharon conglomerate, and iron ore, the latter acting as the bonding material. This stratum, occurring well towards the summits of the ridges east of the Scioto, is the source of the cherty material now found incorporated with the clay, s^nd, and gravel on these old valley floors.

The gravel deposits are made up principally of two kinds of pebbles; one derived from the local sandstones, and another less abundant/ originally derived from igneous rock. The percentage, shape, and size of the quartz pebbles in the latter suggest strongly that this material was derived mainly from the Sharon conglomerate, which is present in local areas in the eastern part of the basin, and not from the drift sheet to the north.

The disintegration of shales and argillaceous sandstones produces sediments consisting of clays and fin^-grained sands. Since this class of rock makes up the thick strata of the basin walls, fluvial deposits in the valleys, under normal conditions, would be, in the main, sediments of this type. The evidence thus tends to show that the sedi-? ments were derived from local material and laid down by the old pre- Rlacial stream. From the above it is thus seen that there is a marked difference between the deposits in these upland valleys and those along the Scioto. The latter bear distinctly the stamp of glacial influence, while the former do not.

From a consideration of basin areas the Portsmouth River was only about one-fifth the size of the present Scioto, which has obliterated most of the preglacial valley from Portsmouth to Waverly. The course of the old stream, judging from the few distinct remnants of the old valley, was somewhat tortuous, but well intrenched in the broken land. The valley of the Scioto River averages between IJ and 2 miles in width, while that of the Portsmouth, as nearly as can be determined, was about 1 mile.

These old preglacial rivers, which flowed northward through the territory for a very long period, cut broad valleys, and reduced the contour of the adjacent hills to more gentle slopes, thus developing large tracts of level or moderately level lands which are quite fertile, and well suited for agricultural purposes. The area of this land in the California Valley alone amounts to more than 30 square miles, and that in its tributaries amounts to at least 20 square miles. The area of this land in the original Portsmouth Valley cannot be determined, for a large part of the Scioto Valley is the work of the present stream, but the area was evidently less than that in the California Valley, as the volume of water, owing to the more restricted basin, was much smaller. The fragments of the old valley seen east of Lucasville and northeast of Clifford have an area of about 10 square miles.

These old valleys are not only of value for their fine farming lands, but they afford natural outlets for roads and railroads. Most of the pikes of the county follow them closely.

All the surface rocks in this region are of sedimentary origin, having been deposited by the agency of water. They consist of sandstones, conglomerates, shales, limestones, coals, iron ores, and clays. The thickness of the Mississippian sandstones and shales, which varies from place to place, is usually about 800 feet, while that of the Peimsylvanian strata, measured from the bottom of the Sharon conglomerate, if present, to the Middle Kittanning coal, which just caps some of the highest knobs, is approximately 490 feet; hence the total thickness of Carboniferous rocks is between 1,200 and 1,300 feet. All the stratified rocks found in this region belong to the Mississippian and Pennsylvanian, except the gravels and silts deposited by the old preglacial rivers and those laid down by the present streams, which belong to the Quaternary. All the strata have a fairly uniform dip south of east. Figured from the Sciotoville clay deposits as a base, the dip east is 43 feet to the mile, that south 13.5 feet, and that south of east 44.5 feet.

first described, as they have no direct relation to the rocks of the Missis* sippian and Pennsylvanian systems, which are then taken up in ascending order, beginning with the oldest.

Lower Kittanning, Newcastle, or No. 5 coal. Lower Kittanning clay and shale. Ferriferous, Limestone, or Baird ore. Vanport, Ferriferous, Hanging Rock, or Gray

Recent River Deposits

Deposits of alluvium and gravel, which were laid down principally during inundation periods, and which vary greatly in thickness, are found on the flood plains of the present streams. Along the Ohio and the Scioto rivers these deposits consist generally of thick beds of gravel, overlaid by beds of sand and clay. The gravel is largely of glacial origin, as it contains much limestone and granitic materials, which have been transported from the glaciated regions by the glacial and present streams. It is hard to define the work done by the glacial and by the present streams, as the latter receive a large quantity of material from the same source as the former received their loads.

The gravel beds along the Ohio, and especially along the Scioto, furnish much material for concrete, ballast, and road work. For concrete work the gravel is usually graded by screening into sizes, which may then be proportioned to the quantity of each desired. The bulk of the gravel thus used at Portsmouth is taken from the Scioto beds. The Norfolk & Western Railway used large quantities of this gravel for ballast, and formerly the county roads in the Ohio and Scioto valleys were faced with it. At present limestone has largely replaced gravel for road work. Most of the sand used in this vicinity in concrete, cement, and lime mortars was formerly taken from the Ohio and Scioto beds, but at present it is taken mainly from the latter source, as the sand beds along the Scioto are more available, and the sands contain fewer coal particles, which are objectionable for cement facings and for

We obtain our material from the Scioto River, some being taken directly from the bed of the stream, and some from a bar thrown up by the current. Our apparatus is an overhead cableway with clam-shell bucket operated by a three-drum friction engine. The material is dumped from the bucket into a hopper which feeds it to the revolving screens where it is sized and washed at the same time and thence conveyed by gravity to the storage bins. We have three grades of material: the mixed sand and gravel just as it comes from the river; the washed, screened sand; and the washed, screened gravel. We have been in operation for only a year ami a half and estimate our sales for the year 1913 at about fifteen thousand yards. Our material has given good satisfaction for plastering, brick-laying, concrete, and aU that class of construction work.

The deposits laid down on the flood plains of Pine Creek and the Little Scioto are largely the work of the present streams, while those found on the terraces and' uplands are due mainly to the preglacial^ streams. The present streams do not head in the glaciated region, and they were not at any time directly connected with it; hence the gravel foimd along these streams contains but little granitic material, except some quartz pebbles foimd along ^the Little Scioto which are derived from the Sharon conglomerate. The gravel is composed mainly of soft sandstone, derived from the Carboniferous rocks, but, owing to lack of better material,^it is used locally for concrete work and for road facing. The sands along these streams contain silty material, which restricts their efficiency for cement mortars, as the extremely fine silica or alumina from this material becomes a component of the cement which is thus thrown out of the proper silica-alumina-lime ratio. They are used only to supply the local needs.

The clays of recent origin found along Pine Creek, and 'along the Ohio, Scioto, and Little Scioto rivers, are valuable for ceramic purposes, but as yet they have been used to only a small extent. They are well fitted for the manufacture of drain tile, both common and face red brick, fire proofing, and roofing tile. Several small yards at Portsmouth formerly worked these clays for common brick, but they now use Cuyahoga shale.

The company was organized in 1877 and incorporated in 1S96. The days used are of alluvial origin and are obtained from the upper flood plain of the Ohio River. The deposit, about 12 feet in thickness, consists of light or imweathered oby, and of yellow or weathered clay. Both clays have much the same working properties. Th^ have excellent plasticity and are quite free from deleterious materials, such as bowlders, iron concretions, or sand. The mining of the material is a simple matter, as aU that is required is to remove the soil, then loosen the clay by explosives, or by the pick. The ware is manufactured as follows: The clays are first put through a crusher to break up the lumps, then they are formed into a plastic mud in a pug mill. The properly tern- - pere<i mud then goes to the tile machine which shapes it into the size of ware desired. No difficulty is encountered here, as the clay produces an excellent body which is quite free from laminations, or body checks, and sufficiently strong to withstand factory handling. The ware is dried both in steam driers and on open floors, the method followed depending somewhat on the weather conditions and on the size of the tile. When thoroughly dry the ware is set in the kiln which is of the rectangular down-draft type and is 14 by 34 feet in size. Coal is used for fuel. The total shrinkage of the ware is moderately low; hence a rather uniform ware is produced. The vitrification range is sufficiently long to give good economy in the quantity of standard waxe produced. The clay goes to a good body which, when properly burned, has a deep cherry red color. AM sizes of standard and special tile are made for the trade, wliile red brick are produced when ordered. The shipping facilities are the Norfolk & Western Railway, and the Ohio River.

These deposits are the work of the preglacial streams, and of those formed by the shifting of the former during the Glacial Period. These old river deposits are well represented by the undisturbed gravel and alluvium in the California Valley on Dogwood Ridge, north of the village of Wheelersburg, and on the flat lands from Wheelers Mills to Stockdale, in Pike County. The deposits are made up of sand and clay with but little gravel and are often 40 or more feet thick. Clays make up the bulk of the beds.

The later deposits formed along the streams during glacial time are well defined by the terraces on the lower course of the Little Scioto River. Near the mouth of the river these deposits are principally fine-grained sands, but* farther up the stream they are clays, with but little sand; hence it appears that the former were laid down in slowly moving currents, while the latter were deposited in still or slack waters, or under lake-like conditions that existed in this valley during Pleistocene time. In the Scioto Valley only remnants of these old deposits are found. The preglacial deposits are made up mainly of sands and clays, while those of glacial age are gravels and sands. The clays are by far the most important of these Pleistocene deposits, although they are used but little at the present time.* These beds contain large amounts of clays, well fitted for the manufacture of the common grades of ware, such as drain tile, both common and face red brick, roofing tile, and fire proofing.

The strata that make up the hills just east of the Scioto River belong to the Mississippian system. As the rocks dip eastward these beds go under cover a few miles east of the Little Scioto. They disappear on the Ohio near Haverhill; on Pine Creek, near Powellsville; on Plum Fork near the Harrison-Bloom Township line; on Frederick Creek near the Baltimore & Ohio Southwestern Railroad; on Laurel Lick Run near Pinkerman; on Bear Run, in Section 4, Bloom Township; on Holland Fork, in Section 24, Hamilton Township, Jackson County; on Meadow Run or Little Scioto near Mabee; on Bucklick Creek, in Section 16, Hamilton Township, and north of this nepr the Scioto- Jackson County line. The formations that make up this series of rocks are Bedford, Berea, Snnbury, Cuyahoga, Logan, and Maxville. From surface measurements and from drill records the total thickness of the six formations is between 600 and 800 feet. Just east of the Scioto River the estimated thickness varies from 700 to 800 feet, while in the eastern part of the county the measurements obtained from drill records place the thickness between 600 and 700 feet. The rocks of the Maxville formation are limestone, while those of the other formations are, in the main, siliceous shales and argillaceous sandstones. The Bedford, Berea, and Sunbury formations in southern Ohio have not been subdivided, but the Cuyahoga and Logan formations have been separated by Hyde into several members, which will be named later. ^

In Scioto County, east of the Scioto River, the Bedford formation appears along the flood plain of this stream in ,the northern part of Valley Township. Owing to deep cover it is seldom exposed for observatioli, and is not available for economic uses. This formation consists of shales with thin and medium bedded sandstones which are widely spaced.

In that part of Scioto County discussed in this bulletin the Berea formation is above the waters of the Scioto River in Valley Township. The formation is made up of sandstones, which vary in thickness from 1 inch or less to as much as 5 or 6 feet, and of shales which are also quite variable in thickness and usually very siliceous in character. As a general thing the bulk of the deposit consists of sandstones, although this is not always the case. Along the outcrop these sandstones are light gray or slightly yellow in color, but under heavy cover they are light blue, owing to the presence of ferrous oxide pigments. In the main, these sandstones are composed of finely divided quartz, with clay and iron compounds for the cementing material.

The Berea sandstones are well exposed in the cut of the Norfolk & Western Railway near the pumping station at the village of Clifford. Most of the layers at this place are from 2 inches to 3 feet in thickness. The usual measurement, however, is from 6 inches to 2 feet. The layers are highly ripple marked, and are broken into blocks by joint planes. A few of the layers show concretionary structure and a marked variation

^J. E. Hyde, Stratigraphy of the Waverly Formation of Central and Southern Ohio, The Journal of Geology, Vol. XXIII, Nos. 7 and 8, October-November and November-December, 1915.

in thickness. Most of these rocks are quite weather resistant, but a few of them have a tendency to shell when exposed to severe conditions. In this area the Berea sandstones have been used only for minor purposes, such as walks, foundations, culverts, and retaining walls.

The Sunbury formation, which is composed of dark shales, is the next division of rocks in ascending order in the geological column. East of the Scioto River the beds are found above drainage from the vicinity of the village of Lucasville to the Scioto-Pike County Une. Records of drill tests made in southern Ohio tend to show that the Sunbury shales and also the Berea sandstones are quite persistent. The usual thickness of the Sunbury formation is from 20 to 30 feet, although these measurements do not represent the extremes. These shales are characterized by their large content of carbonaceous matter. In this respect they bear a close resemblance to the shales of the Ohio formation of the Devonian system. Further, they are conspicuous on account of their dark, or coffee brown, color, and on account of their finely stratified structure. They are hard fissile shales, not easily attacked by weathering agencies, and they often contain many small concretions of pyrite. The Sunbury shales are not economically important at present, yet they may be utilized in the future as a source of valuable compounds produced by destructive distillation.

This formation has been subdivided by Hyde into three members, which are Henley, Buena Vista, and Portsmouth. Rocks belonging to this formation are found along the east bank of the Scioto River from the Ohio River northward to the Scioto-Pike County line. They extend well towards the headwaters of the eastern tributaries of the Scioto River, and appear along the courses of some of the western tributaries of the Little Scioto River. Along the Ohio River the formation passes below drainage near the mouth of the Little Scioto, just east of the village of Sciotoville.

The Henley member, which forms the lower part of the Cuyahoga formation, consists of siliceous shales, which as yet have not been used, but are well suited for ceramic purposes. The Buena Vista member lies above the Henley and is made up of sandstones and shales, which east of the Scioto River in this county have but little value. The Portsmouth member, which forms the upper part of the Cuyahoga, consists of shales that constitute one of the most valuable assets of Scioto County.

In a general way the Portsmouth member is represented along the courses of the streams in the area lying between the preglacial California Valley and the Scioto River. These deposits are very im- portant along the Ohio River from Portsmouth to Sciotoville, where they form the basis of an important paving brick industry. The following section, taken at the mines of the Peebles Paving Brick Company, shows the general r -racter of the deposit:

The Portsmouth shales in this locality are fossiliferous, and afford good collecting. The fossils are usually found in ferruginous concre-. tions.

Economic Value

The Portsmouth shales form the basis of the extensive paving brick industry in the vicinity of Portsmouth and Sciotoville. The quantity of suitable material in these beds is practically unlimited, as the shales have been attacked only at a few places along the outcrop. At present the mining is confined to blasting the shales from the sides of the hills, or to working the beds by short entries. Owing to the availability and thickness of the shales the cost of mining the material is low.

The working qualities of these shales are excellent. On exposure they weather down to mud with good plasticity. This property is also easily developed in the manufacture of the shale into brick by grinding it in dry pans, screening to remove the coarse material, and working with water in a pug mill. This process produces a good bonding of the mass. For paving brick, the column, as it is forced through the die of the brick machine by the auger, must not crack or laminate, as these are vital defects. In general, excess plasticity develops lamination, while insuflScient plasticity produces crack. This shale gives a column not subject to either of these defects to any considerable extent. The brick show good structure throughout.

The brick are then pressed, loaded on cars, and taken to the drying tunnels. With many shales the direct loss of ware in the tunnels, due to cracks and checks, seriously impairs their value for ceramic purposes. Drying strains which develop during the burning of the ware as cracks, checks, warping, or dishing, are also often produced in the drying tunnels. Ware from this shale dries safely in almost any type of drier. From the drier the ware goes to the kilns, where it is set and burned. For paving brick certain general qualities are demanded by the trade. Brick, to withstand heavy hauling when laid in the streets, must be free from laminations, checks, and cracks. If these are present the brick are soon reduced to small pieces.

Shales with high drying and fire shrinkage are liable to warp and twist during burning.. With this shaJe the total shrinkage is low; hence but little ware is lost through this defect. The shrinkage generally reported is one-half inch drying and one-half inch fire, or the total shrinkage is approximately one inch per foot. Vitrification develops the hardness, toughness, and low absorption required in this class of ware in which the finished product must be a dense, stony mass. The components to be considered here are of two kinds: those that tend to fuse to a glassy mass, and those that tend to remain rigid or resist solution. If the former predominate, the mass fuses to a brittle glass, with but little toughness or abrasive power. If the components producing rigidity are in excess, then the mass has an open, porous structure, unfitted to withstand the strains required. When the components are properly adjusted, a dense, stony, tough mass is produced, which resembles what is obtained from the natural Portsmouth shale. The vitrification range is another important item. This is the interval from incipient fusion to deformation. If this range is short the brick on the head of the kiln will be fused before those on the bottom of the kiln have started to vitrify, so ware will be lost either by overbuming on the head or by imderbuming on the bottom,. The most active common components are magnesia and lime, which are both low in this shale. The bimiers at the present plants have no difliculty in obtaining good results from top to bottom of the kilns.

The colors usually demanded for first-class brick by the trade are from dark red to nearly black. The iron oxide in the shale is sufiiciently high to give a dark red in a hard burn, under oxidizing conditions of firing, and a nearly black under reducing conditions during the latter part of the bum. The white or yellow scum on brick gives them an unsightly appearance, although it is not detrimental to this class of ware. The scum is produced either during drying in the tunnels or during the first stages of water-smoking in the kiln, but generally in the former. If the water in the green brick, which holds soluble salts in solution, is allowed to collect in beads or drops on the surface of the ware, and is then evaporated, the salts are deposited and remain as scum. Care in the drying and in the water-smoking of the ware will usually overcome this defect. The quantity of soluble salts in the Portsmouth shale is small, but scum is produced at times in the ordinary practice of manufacture. Formerly, glazed paving brick were demanded by the trade, but this grade at present is seldom required. The siliceous nature of the clay, and the high temperature of maturity, reported to be from 2,000 to 2,200° F., are both favorable for ease of salt glazing.

All points considered, the Portsmouth shale stands as one of the best in this state, or even in the United States, for the manufacture of high-grade paving brick. The deposit extends from the western boundary of the county to the Little Scioto River. The shipping facilities of the region are also good. The low freight rates on the Ohio River open the markets along this stream, and along the Mississippi. The two railroads, the Norfolk & Western and the Baltimore and Ohio Southwestern, afford means of shipping directly into the eastern, northern, and western markets.

This region is also favorably situated for fuel, as the Baltimore & Ohio Southwestern Railroad connects directly with the Wellston and Hocking coal fields, while the Norfolk & Western Railway enters the great southern West Virginia and southwestern Virginia fields. Gas from the West Virginia fields is also piped to this region, and is used by two firms as the main fuel supply. The firms manufacturing paving brick from the Portsmouth shale are as follows:

The Portsmouth Paving Brick Co , Portsmouth, Ohio. The Peebles Paving Brick Co , Portsmouth, Ohio. The Carlyle Paving Brick Co., Sciotoville, Ohio. The Scioto Fire Brick Co., Sciotoville, Ohio.

The plant, located in the northern part of Portsmouth, conomenced making brick in 1892. The material used is weathered and unweathered shale (Portsmouth) front the beds in the hill just north of Portsmouth. These are mined along the outcrop from surface workings, by quarrying. The power at the factory is furnished by two 80-H. P. boilers with one 150-H. P. engine. The brick manufacturing equipment proper is one Phillips & McLaren dry pan, one Freese pug mill, one American Clay Machinery Company brick machine, and one Bonnot repress. Waste heat is used in drying. The eight down-draft kilns have a total capacity of 840,000 brick. Coal is used exclusively in burning the ware. The capacity of the plant is 25,000 standard paving block per day. Tests on our ware rate it with the best made in the United States. The ware is marketed principally in Virginia, West Virginia, Ohio, Indiana, Kentucky, and Michigan.

The plant of The Peebles Paving Brick Company is located about one mile east of the city of Portsmouth in Scioto County, and is bounded on the north by the rails of the Norfolk & Western Railway, and on the south by the Ohio River. The company was organized on Feb. 5th, 1902, for the purpose of manufacturing vitrified paving brick exclusively. The holdings of the company consist of two separate and distinct plants, each having a daily capacity of approximately 50,000 brick.

The shale from which the brick are made is dug from the face of the hills about one quarter of a mile distant from the plant by a Marion Model-60 steam shovel, and is hauled in dump cars by locomotives to the plant. The power plant consists of four horizontal tubular boilers, each rated at 125 H. P., which supply power for one Harris Corliss engine which at present is developing about 250 H. P., and one Excelsior slide-valve engine which is furnishing approximately 240 H. P. Each engine has its own plant to run, which consists of two 9-foot Bonnot dry pans, one 12-foot Bonnot pug mill, one "C" Special Bonnot brick machine, one E. M. Freese Model-T-60 reciprocating cutter, and on our No. 2 plant two Bonnot Canton-Special repressers. The product from this plant is repressed block and from the No. 1 plant it is the Dunn wirecut lug block, which of course does not require pressing.

The brick are dried by the waste heat system which is supplied from cooling kilns by exhaust fans. The No. 2 plant has ten rectangular down-draft kilns each having a capacity of about 110,000, while the brick from the No. 1 plant are burned in the Haigh process continuous kiln which has 69 chambers each holding approximately 12,000 brick. Recent reports of testa which we have received from various cities using our block show them to average about 16 per cent imder the Specifications for Testing Paving Brick as prescribed by the National Paving Brick Manufacturers' Association.

Our shipping facilities consist of Baltimore & Ohio Southwestern, and Norfolk & Western railroads, and the Ohio River. We ship annually several million brick by water to down-river points.

The Carlyle Paving Brick Company was organized May 2, 1905, and is an Ohio corporation. Our capital stock ' is $80,000, although we have invested double this amount since the plant was organized. Our plant is located one mile west of Sciotoville, Ohio, on the lines of the Norfolk & Western, and Baltimore & Ohio Southwestern railroads, Portsmouth electric line, and Ohio River. We have facilities for loading by rail and by river. The Ohio River has been of great assistance in disposing of our output. We have been able to ship by water to all southern points located on the Ohio and on the Mississippi rivers, and have thus disposed of from thirty to forty per cent of our output. '