DESCRIPTION OF THE TAZEWELL QUADRANGLE.

GEOGRAPHY. arch into two structural basins, one lying along Atlantic Ocean, except the southern part, where time probably occurred another period of degra­ the eastern and one along the western margin of the surplus waters of the region west of the Blue dation which was a partial cycle, since it resulted General relations- The Tazewell quadrangle the field. The one lying on the western side Ridge are carried to the Ohio River by the only in the reduction of areas of soft rock or those lias an area of 950.4 square miles, extending from has but a limited extent in the region outlined Kanawha and Tennessee rivers, and to the Gulf in especially favorable localities. Doubtless many latitude 37° on the south to 37° 30' on above, and is generally known as the coal basin by the Alabama River. other partial cycles of degradation have marked the north, and from longitude 81° 30' of western Kentucky. The eastern basin is more The positions of the streams in the Appalachian the geologic history of this region, but they have on the east to 82° on the west. It is named from extensive, comprising the great Appalachian coal Valley are mainly dependent upon the geologic been so short that they have produced no exten­

Tazewell, Virginia, the most important town field, which extends from the southern line of New structure. In a ogeneral wayJ theyJ flow Arrangement. sive or well-defined results. Each of the larger within its borders. The quadrangle is divided York to central Alabama, where it passes beneath in courses which, for long distances, ofstreams- periods of quiescence noted above was terminated between the States of Virginia and West Virginia, the later sediments that have been deposited are parallel to the mountains on either side, fol­ by crustal movements which elevated the form­ including portions of Tazewell, Smythe, Russell, along the Gulf coast. lowing the outcrops of the softer rocks. These erly low-lying plain into tablelands and plateaus. and Buchanan counties in the former and portions The rocks comprising the lower portion of the longitudinal streams empty into a number of Recent erosion has cut these elevated plains into of McDowell and Wyoming counties in the latter. series exposed in this division of the province are larger, transverse rivers which cross one or the a variety of forms, the topography of a particular The adjacent quadrangles are Oceana (on the prevailingly calcareous and outcrop in a broad other of the barriers limiting the valley. In the area depending upon its location with reference north), Raleigh, Pocahontas (on the east), Wythe- belt upon the crest and flanks of the Cincinnati northern part of the province these transverse to the main drainage lines of the province and ville, Abingdon (on the south), Bristol, Grundy arch. The rocks forming the upper portion of rivers are the Delaware, Susquehanna, Potomac, upon the rock character and geologic structure (on the west), and Warfield. the series are generally sandy and are found only James, and Roanoke, each of which flows east­ composing it. Thus the hard, level beds of rock In its geographic and geologic relations this in the two coal basins. ward to the sea. In the central part of the prov­ in the Cumberland Plateau were very effective in quadrangle forms a part of the Appa­ The topography of this division is varied, its ince the longitudinal streams form the New (or resisting the corrasion of the streams, and conse­ lachian province, which extends from character depending in a large measure upon Kanawha) River which flows westward in a deep, quently when this area was elevated it became a the Atlantic coastal plain on the east Appalachian the nature of the rocks forming the surface. narrow gorge through the Cumberland Plateau plateau with an extremely regular surface. In the * province. to the Mississippi lowlands on the west, Whether the coal-bearing rocks formerly extended into the Ohio River. From New River to north­ Appalachian Valley a similar plateau was doubtless and from central Alabama to southern New York. from basin to basin, completely capping the Cin­ ern Georgia the valley is drained by tributaries formed, but erosion has been so active along the /Subdivisions of the Appalachian province. cinnati arch, is at present an unsettled question, of the Tennessee River, which also crosses the soft rocks that great valleys are excavated, leav­ This province may be subdivided into three well- but it seems altogether probable that at no very Cumberland, Plateau in its course to the Ohio. ing the hard rocks in ridges, the summits of which marked physiographic divisions, throughout each remote period the surface sloped gently from the In Georgia and Alabama the streams flow directly generally represent the surface of the former of which certain forces have produced similar summit of the Cumberland Plateau and the hill­ to the Gulf of Mexico. plain. results in sedimentation, in geologic structure, tops of the West Virginia coal field to the high­ Topography of the Appalachian province. The movements which elevated these pene­ and in topography. These divisions extend the lands of the western basin, and that recent erosion The different divisions of the province vary much plains were very irregular, producing warped entire length of the province, from northeast to has cut from that plateau the low plains of central in their topography, as do also different surfaces which now stand at different altitudes i £ xi;J- ' rriv Conditions southwest. Tennessee and Kentucky. partsi oi the same division. Imsvana- erosion:governing rock in different portions of the province. The central division is the Appalachian Valley. Altitude of the Appalachian province. This tion is due to the fact that in parts andr|eo!ogic Topography of the Tazewell quadrangle. This It is the best defined and most uniform of the province as a whole is broadly arched, its surface of the province certain conditions of structure- territory lies mainly in the western division of rising from an altitude of about 500 feet along erosion have had the controlling influence in the province, but the southern extrem­ three. It varies in width from 40 to Central_ , .... di- 125 miles, and is sharply outlined on the eastern margin to the crest of the Appalachian shaping the results, whereas in other parts other ity includes a portion of the Appa­ the southeast by the Appalachian Valley* Mountains, and thence descending westward to conditions, have predominated, and the surface lachian Valley. The line separating Mountains and on the northwest by the Cumber­ about the same altitude on the Ohio and Missis­ features are modified accordingly. Thus, in the these main divisions passes through Horsepen land Plateau and the Allegheny Mountains. Its sippi rivers. Appalachian Valley rock character and geologic Cove, Richlands, and Doran. South of this line rocks are almost wholly sedimentary and in large The Appalachian Mountains rise gradually structure are the conditions which chiefly govern the forms of relief consist of long, straight ridges measure calcareous. The originally horizontal from less than 1000 feet in Alabama to more than erosion; in the Appalachian Mountains structure and narrow, intermediate valleys all trending N. strata have been thrust into great folds which in 6600 feet in western North Carolina. Altitudes. tM . of. plays only a secondary part, and in many locali­ 60° E. In the coal field north of the fault line many places have been compressed to such an From this culminating point they iJchAapnpa" ties the rocks are so nearly homogeneous that the topographic forms are extremely irregular, extent that the strata forming the folds have been descend to 3000 feet in southern Mountains- rock character has had but little effect on the the direction and continuity of the ridges having broken and crowded forward out of their normal Virginia, rise to 4000 feet in central Virginia, topography of the region; in the western division been determined apparently by the accidents of positions. That portion of the Appalachian Val­ and again descend to 2000 feet on the Maryland- the geologic structure is so simple that it has had erosion on nearly horizontal rocks. ley which lies within the States of Pennsylvania Pennsylvania line. only a small effect in the erosion of the region, Careful study of the topographic sheet reveals and Virginia may be subdivided into two areas The Appalachian Valley shows a gradual and consequently the surface features are largely the fact that there is a certain element of regular­ differing materially in topographic features. The increase in altitude from 500 feet or less in Ala­ due to the character of the underlying rock. ity in the topography of both the coal Re ular|t of eastern area consists of a broad valley which bama to 900 feet in the vicinityJ of Altitudes...... of. Throughout the entire province the surface field and the Appalachian Valley. This 5ilS£8o?;° in the former State is known as the Cumberland Chattanooga, 2000 feet at the Tennes- gcehAapnpa" forms are largely controlled by the altitude of element of concordance is the general peneplain- or Lebanon Valley and in the latter as the see-Virginia line, and 2500 or 2700 Valley< land,' which varies in relation to sea Cycles_ , of, elevation of the surface as marked by the tops of Shenandoah Valley. In the western area the feet at its highest point, on the divide between level as the surface is worn down by degra<»atlon- hills. In passing through the region, the traveler rocks lie in broad, open folds, and the outcrops the New and Tennessee rivers. From this point erosion or is uplifted by movements of the earth's is generally confined to the valleys, and conse­ of the hard beds on the sides of these folds give it descends to, 2200 feet in the valley of New crust. When the land is high the streams descend quently he sees but an endless succession of rise to long, generally straight ridges, which are River, 1500 to 1000 feet in the James River rapidly to the sea, corrading narrow gorges nearly irregular knobs and ridges with no apparent sys­ separated by narrow valleys formed on the out­ basin, and 1000 to 500 feet on the Potomac and to the base-level of erosion. By lateral corrasion tem or general altitude. Let him ascend an crops of the softer rocks. Farther south the Susquehanna rivers. These figures represent the these narrow gorges are gradually widened, and eminence, such as Bear Wallow, and he will rocks have been closely folded and very much average elevation of the valley surface, below the sides are reduced from precipitous cliffs to then perceive a plain below him, once doubtless broken, and consequently the surface of the entire which the stream channels are sunk from 50 to gentle slopes. The divides between adjacent continuous across the valley of Dry Fork, but Appalachian Valley has been worn down to an 250 feet, and above which the valley ridges rise streams are, little by little, worn away, and the now deeply trenched by every branch of that undulating lowland which, in Georgia and Ala­ from 500 to 2000 feet. surface becomes a peneplain gradually approach­ stream. When the contoured sheet is consulted, bama, is known as the Coosa Valley and farther The surface of the western division rises from ing base-level. With reference to the develop­ it is found that this regularity of summits is not north as the Valley of East Tennessee. an altitude of 400 or 500 feet along the Missis­ ment of the stream, such a period has been termed confined to any one area, but is characteristic of The eastern division of the province embraces sippi River to 2000 or 4000 feet along a cycle, and we may equally well apply that term most of the territory within the coal field. It is the Appalachian Mountains, a system which is the eastern front of the Cumberland to the degradation which occurs during the same also noticeable that this surface varies in altitude Plateau and the Allegheny Mountains. period. At the beginning degradation is active, from 1800 feet in the northwestern corner of the made up of many individual ranges Eastern di­ vision the bearing various local names, and which Appalachian This slope is not regular, but, in a general way, like the stream in its youth; it. grows more feeble quadrangle to 2000 feet near laeger; 2300 feet at extends from southern New York to Mountains. is made up of three terraces rising from the as the stream loses power; and finally it becomes Bradshaw and Welch; 2400 feet at McNiel Store, central Alabama. Some of its prominent parts river to the eastern margin of this geologic sluggish and inactive, suggesting the decrepitude Barrenshe Creek, and Kimball; 2500 feet on are South Mountain of Pennsylvania, Blue Ridge division. The lowest terrace forms the valley of of old age. Sandy Ridge and on the lower course of Long of Maryland and Virginia, Great Smoky Mountains the Mississippi River and its larger tributaries, But the process of degradation is carried to Branch; and 2600 feet at Big Creek and Squire- of Tennessee and North Carolina, and Cohutta and it also appears in the central basin of Tennes­ completion only in case there is a constant rela­ jim. From this line it does not appear to rise Mountains of Georgia. Many of the rocks of this see. The second terrace forms the "Highland tion of land and sea, a condition which seldom much, but passes into the valley region at about division are more or less crystalline, being either Rim " of Tennessee and the upland plain of prevails for any great length of time. Usually the same altitude. It then gradually descends sediments which have been changed to slates and Kentucky ; its general altitude is about 1000 feet. the cycle of degradation is interrupted Interru ted to 2500 feet at Coombs Point and Snapp, and schists by varying degrees of metamorphism, or The third terrace is formed by the even top of by crustal movements which change cycles- probably 2400 feet near Honaker. igneous rocks, such as granite and diabase, which the Cumberland table-land, and farther north the relative altitude of land and sea. When ero­ This regular surface has the appearance of a have solidified from a molten condition. by hilltops which presumably mark the position sion is thus interrupted in any stage of its devel­ peneplain, above which stand the valley ridges, The western division of the Appalachian of a deeply dissected plateau that was formerly opment, some of the characteristic topographic portions of Sandy Ridge, and Bear Wallow, and province embraces the Cumberland Plateau, the continuous with the Cumberland table-land to forms remain among features of later development, in which the present streams have cut narrow Allegheny Mountains, and the low­ the south. The altitude of this highest terrace and they constitute a record of the conditions to valleys, in some cases 1000 feet in depth. The lands of Tennessee, Kentucky, and vis?onTnits" varies from 500 feet at the southern edge of the which they belonged. most noticeable feature of this surface is that it .~, ...... , . , T . extent and province to 1500 feet in northern Alabama, 2000 In the Appalachian province there are traces of extends over the hard sandstones of the coal field Ohio. Its northwestern boundary > t is structure.geologic indefinite, but may be regarded as coin­ feet in central Tennessee, and 2000 to 4000 feet peneplains at various altitudes which, if correctly as well as over the soft limestones and shales of ciding with the Mississippi River as far up as in Kentucky, "JVest Virginia, and Pennsylvania. interpreted, prove that at several the Appalachian Valley; rock character seems to Cairo, and thence extending northeastward across Drainage of the Appalachian province. The periods in the past the cycle of degra- inethe Apnpa- have entered but slightly into the determination the States of Illinois and Indiana. Its eastern western division of the province, with the excep­ dationJ A - was nearly1 complete.1 I rIne most, tachlansr of the extent of this peneplain. pronounced degradation probably occurred in the The ridges which stand above this old plain boundary is sharply defined in the north by the tion of small areas in Pennsylvania«/ and Direction_. .. of. Allegheny front, in the south by the Cumberland Alabama, is drained by streams flowing dralnase- Cretaceous period and resulted in the wearing show a slight correspondence in altitude which, escarpment. westward to the Ohio River. The Appalachian down of most of the surface of the province nearly taken in connection with the height of the ridges This, division is separated by the Cincinnati Mountain division is drained eastward into the to base-level. In late Eocene or early Neocene in the surrounding area, makes it seem probable that their crests mark the surface of a still older question of time when Clinch River will be somewhere in the western division of the Appa­ is the Honaker limestone, so-called from the town peneplain, which has been so long exposed to the captured at this point and transferred to the Big lachian province, and which separated this trough of Honaker, in Russell County. This limestone action of ^erosion that but few scattered . . Sandy system. from the great interior sea. Into this trough was nigh sum- varies in character from blue,' flaggyOOv to dark,/ remnants are left to mark its once even swept the waste of the continental area to the impure limestone and massive gray dolomite. It GEOLOGY. surface. Being older than the extended penepla!n- east which, hardened into sandstones and shales, ranges in thickness from 900 to 1000 feet. peneplain just described, it has been affected by STRATIGRAPHY. is now known as the rocks of lower Cambrian West of the Tazewell quadrangle this formation a greater number of crustal movements, and is The general sedimentwy record. All of the age. The land forming the barrier west of the is subdivided by a small band of calcareous shale consequently deformed to a greater extent than rocks appearing at the surface within the limits Appalachian Valley sank beneath the sea, and (Rogersville shale) into two distinct the newer plain. of the Tazewell quadrangle^ P are of sedi- Origin_. , of. the the coarse sediments of the preceding epoch gave limestones, the upper of which has The surface of the upper peneplain is possibly mentary origin, that is, they were roc*s> place to an enormous and widespread limestone been named the Marysville and the > t west. represented by the extreme summit of Hensley deposited by water. They consist of sandstone, deposit which marks the close of Cambrian and lower the Rutledge limestone. In Knob, north of Tug Kiver, and by Bear Wallow shale, and limestone, have an average total the beginning of Silurian time. This limestone passing eastward the Rogersville shale becomes at an elevation of 3100 feet, Stony Ridge at 3400 thickness of 17,000 feet, and present great presumably covers most, if not all, of the western more and more calcareous, until, on the western feet, and Paint Lick, Deskins, and House and variety in composition and appearance. The division of the province and extends eastward to edge of this quadrangle, the three blend into a Barn mountains at an elevation of 3500 feet. materials of which they are composed were orig­ the base of the Appalachian Mountains. From single limestone formation with about the same South of this line its position is uncertain ; the inally gravel, sand, and mud derived from the the proximity of this outcrop to the supposed thickness as the aggregate farther west. mountains vary in altitude from 3100 to 4500 waste of the older rocks and from the remains of shore-line of that period it seems probable that Nolichucky shale. Above the Honaker lime­ feet, but it is probable that neither of these plants and animals which lived while the strata the land area to the east was practically at base- stone occurs a bed of calcareous shale which extremes represent the altitude of the peneplain. were being laid down. level and that no coarse sediments were delivered varies in thickness from a knife edge The highest summits are generally due to the These rocks afford a record of almost uninter­ to the Appalachian sea from that quarter. In to 225 feet. It outcrops on the north- attitude of the hard sandstones which form the rupted sedimentation from early Cambrian to late early Silurian time this land area was elevated ern face of Kent Ridge in a narrow ridges, and they were probably hills at the time Carboniferous time. Not only do they furnish a and such great quantities of sand and mud were band which practically disappears at the eastern the older peneplain was produced. record of the conditions under which Conditions_ of swept into the sea that the formation of limestone edge of the quadrangle. It thins eastward like The peneplams which appear to be represented they were deposited, but they also dep°sitlon- was interrupted near shore, but farther out it the Rogersville shale, and finally merges into the by the regular hill-tops of the Tazewell quad­ record the conditions of the land from which they continued to form for some time. Finally, how­ limestones above and below, forming a great rangle are of wide extent, having been recognized were derived during the same period. In the ocean ever, the sea became too muddy for the formation mass which, in the Pocahontas quadrangle, has over most of the western division of this prov­ the waves alone are sufficient to sort very coarse of limestome, except in central Kentucky and been called the Shenandoah limestone. This ince. material; hence conglomerates are always indica­ Tennessee, and the entire Appalachian Valley shale is named from Nolichucky River in East Drainage of the Tazewell quadrangle. This tive of shore conditions; they also usually denote was covered with a thick deposit of shale. The Tennessee. territory is entirely within the watershed of the steep slopes and rapid erosion on the adjacent land continued to rise and the shore-line migrated Ohio River, but .its drainage is divided among land surface; but before solidification takes place northwestward, but the extent of this movement CAMBEO-SILUEIAN STEATA. three large tributaries of that stream. the level of the land may be so changed that the has not been definitely determined. In the Appa­ Knox dolomite. This is the greatest limestone That portion of the quadrangle which lies pebbles and bowlders are once more exposed to lachian Valley this shore-line is marked by a formation known in the province. It was early within the Appalachian Valley belongs mainly the action of the waves and are worked over deposit of clean beach sand, but the absence of named by Safford from Knox County, Tennessee, to the Tennessee system. Its largest again and redeposited, although at the same time rocks of this age over the southern point of the and as its outcrop has been traced continuously stream is Clinch River, which rises R?verelyst the surface of the land may be near base-level. Cincinnati arch seems to indicate that the sea from the type locality, the same name is appro­ about 6 miles east of Tazewell and Consequently, when such beds are used in inter­ margin did not migrate indefinitely westward, priate for this region. The formation is generally flows southwest in a somewhat irregular course, preting the physiographic history of the adjacent but was interrupted by a land area in central unfossiliferous,' so its exact ageo can not Age. and leaving this quadrangle near its southwest corner. land area, the evidence should be supplemented Kentucky and Tennessee. be determined, but the occurrence of 8?K2?xro1 South of Clinch Mountain the drainage belongs to by that drawn from other sources before it is During Devonian time the Tazewell quadrangle Silurian fossils in the upper portion dolomlte< Holston River, another branch of the Tennessee. regarded as conclusive. Sands may be trans­ was doubtless covered by the sea which extended shows that a part at least belongs to that period; as With one exception, the streams which drain ported by oceanic currents to great distances, but over most of the Appalachian province. In the to the remaining portion the evidence is negative, the coal field unite in the Big Sandy River, and their ultimate source must have been a land sur­ earlier stage of this period the land to the east of but seems to favor Cambrian; therefore, as the thus reach the Ohio by a direct north- B| Sand face having a considerable diversity of altitude the Paleozoic sea was probably near base-level, formation is a lithologic unit, it is provisionally western course. The principal one Rlver system- and streams of sufficient power to transport the but in the closing stage the land in the north­ classed as of Cambro-Silurian age. It is generally of these streams is Tug Fork, which crosses the sand to the sea. As the waste of the land is eastern part of the United States was greatly a gray, cherty magnesian limestone or dolomite, northern portion of this quadrangle and which carried into the sea it is assorted by the waves elevated and from this were swept immense quan­ with a thickness of about 2400 feet. East of receives the waters of Elkhorn Creek, Clear and currents, the fine mud being carried out into tities of sandy waste which even extended as far Tazewell the Knox dolomite unites with the Fork, Dry Fork, Panther Creek, and Knox Creek. comparatively still water before it gradually set­ south as Tazewell. Honaker limestone, forming a mass of great thick­ Levisa Fork of Big Sandy has its source at the tles to the bottom, where, in the course of time, it The beginning of Carboniferous time is marked ness which was called by Rogers No. II, or the Gap of Sandy and receives Dismal and Slate is solidified into shale. As the surface of the land by marine conditions, but with many fluctuations Valley limestone, but which has since received creeks from the east. The small area north of is reduced toward base-level, the waste transported of level which resulted in a rapid alternation of the name Shenandoah limestone. Indian Ridge is drained by Indian Creek, a tribu­ by the streams becomes finer and finer until the strata of very diverse characters. The Pottsville The Knox dolomite appears at the surface in tary of Guyandot River. deposits in the sea, even near shore, consist series of the Carboniferous consists of sand­ four belts. North of Honaker a small outcrop The encroachment of the streams belonging to entirely of fine mud, which in time is hardened stones and shales which were deposited in a long, extends from the western edge of the quadrangle the Big Sandy system upon that of Clinch River into shale. Thus shale may represent rapid ero­ narrow trough of fresh or brackish water that to Stone Mountain. Near the crossing of Clinch is the most remarkable feature of the Big_. Sandy_ . sion on the surface of the land and deposition at extended northeast and southwest along the east­ River the formation is faulted off, but topography of this quadrangle. The gSf^on some distance from the shore, or it may represent ern margin of the coal field. This deepened as it is again seen toward Cedar Bluff in Distributionoflsthe Vn"x former has apparently robbed the latter Chnch Rlver' base-leveling and close proximity to the coast. time went on, and the sediments stretched farther a narrow Vline 01£ outcrop,J. andJ it'j. appears dolomite. of much of its northern drainage, and at present In a similar manner it seems possible that lime­ and farther northwest, until, toward the end of and disappears along this fault line until it passes is rapidly encroaching upon the main branch of stones may be deposited near shore during the ulti­ the period, the formations may have extended off the quadrangle to the east. The most promi­ Clinch River itself. At Grap Store, in Baptist mate stage of a period of base-leveling, although across the Cincinnati arch. The evidence regard­ nent line of outcrop of the Knox is on Kent Ridge, Valley, the head of Dry Fork is flowing at an under ordinary conditions of erosion they are ing the eastern margin of this trough is not con­ which crosses the quadrangle from northeast to altitude of 2000 feet, whereas, about a mile formed only at considerable depths and at suf­ clusive, but it seems probable that it did not reach southwest. The next two belts unite near the toward the southeast, Clinch River has an eleva­ ficient distances from the shore to be beyond the far beyond the present outcrop of the rocks center of the region, forming an irregular area of tion of 2300 feet. When it is considered that limit of the transportation of sand and mud. belonging to the Pottsville series. Finally the dolomite, whose outcrop in general corresponds to Clinch River carries a much greater Coal is formed from deposits of peat or from basin was elevated above water level, and the the position of two arches, one passing through volume of water than Dry Fork, and buried vegetation; consequently coal seams coal field was added to the eastern continental Tazewell, Liberty Hill, and Paint Lick, and the that the course of the former is directly indicate the presence of extended swamps of area of North America. other through Thompson Valley and Snapp. down the Appalachian Valley to the either fresh or brackish water, in which a luxuri­ Over much of this quadrangle the upper limit southwest, along greatly disturbed calcareous ant vegetation flourished from time to time, but CAMBEIAN STEATA. of the Knox is characterized by a thin bed of red, rocks, the encroachment will seem to be phenom­ which was frequently buried by great washes of Hussell formation. The lowest rocks known earthy limestone, in certain localities closely enal. Under the conditions which appear to sand and mud. in this field contain the Olenellus fauna and are approaching shale and in others carrying pebbles prevail at present, Clinch River certainly has a The sea in which the Paleozoic sediments were consequently of Lower Cambrian age. of chert in an earthy limestone matrix. decided advantage over Dry Fork and would tend laid down covered most of the Appalachian prov­ They consist of alternating shales, thin theCharacteraRusseii° of y . T formation. rather to rob it than to suffer at its hands, there­ ince and the Mississippi basin. The exact posi­ sandstones, and impure limestones. SILUELOT STEATA. fore we are forced to look for some other expla­ tion of its eastern shore-line is not known, but it Owing to the position of this formation along the Ghickamauga limestone. Above the Knox is nation than the geographical distribution of hard probably migrated westward at intervals through­ great fault lines, and to the complex folding a series of blue, flaggy limestones which are prob­ and soft rocks, or geologic structure. A compari­ out Paleozoic time, as the folding of the rocks which it has undergone, it is impossible to deter­ ably equivalent to the base of Rogers's No. Ill, son of the altitudes of the lower peneplain at lifted them above sea level. mine its full thickness, but there can not be less and are named from Chickamauga Creek, Georgia. many points shows that there is a low arch cross­ Since the character of the sediment is, to a cer­ than 600 feet of strata exposed in this quadrangle. Throughout the Tazewell quadrangle this lime­ ing the quadrangle in nearly an east-west direc­ tain extent, indicative of the attitude and configu­ The formation is named from Russell County, stone maintains a constant thickness of tion, which would account for the peculiar rela­ ration of the land, the history of the continental Virginia, in which it is present with its character­ from 900 to 1000 feet, but southeast- tionship between these streams. An arch in this area from which were derived the sediments now istic fauna. ward across the Appalachian Valley it peneplain means a comparatively recent uplift forming the rocks of the Tazewell quadrangle It is exposed in one line of outcrop which thins to only a few feet, and possibly dies out along its axis, and since this axis crosses Clinch should be found recorded in them. At present passes north of Baptist Valley and through Cedar altogether. This southeastward change in the River below the point mentioned, it would act as our knowledge will permit only the broadest gen­ Bluff, Sword Creek, and Honaker. character of the sediments indicates the existence a barrier in preventing the development of the eralizations. Along most of this line only the upper oftneRusseu of a shore-line in that direction during the closing 0 , . J . rjr , formation. stream above that point. The effect on Dry Fork The oldest known rocks of this quadrangle or more calcareous portion is exposed, stages of that period of limestone deposition. would be to stimulate its head branches, and con­ were deposited in a trough or broad strait which and consequently it has no marked effect on the From this shore came sand and mud which were sequently their cutting power would be increased, was bounded on the east byJ the con- Geologic_ , , topography; toward the western edge of the ter­ sorted and separately deposited according to the whereas the power of Clinch River would be tinental area then existing to the east- Apjafachfiane ritory, however, it becomes more sandy and forms laws of sedimentation, the coarse material near greatly diminished. This movement would ward of what is now the Smoky provlnce< rows of sharp, conical hills. shore and the fine farther out in the depths of explain the present attitude of the two streams, Mountains and the Blue Ridge, and on the west Honaker limestone. Overlying the Russell the ocean. and if the uplift still continues it will be only a by a land barrier which was probably located formation, along the northern face of Kent Ridge, Moccasin limestone. Between the, pure lime- stone of ttie northwest and the shales of the formation than to make possible misstatements the margin of a shallow sea which received coarse well quadrangle to the depth of several thousand southeast is an intermediate deposit of red, earthy regarding their areal distribution. material from a land area that lay to the south­ feet, forming the coal-bearing series of the region. limestone, which occurs typically on Moccasin In the Tazewell quadrangle the formation is east; and since these deposits do not appear Unclassified measures. At intervals along Creek, Scott County, Virginia. Along Clinch poorly exposed, except along the southern slope beyond the line of the Norfolk and Western Rail­ the margin of the coal field these formations were Mountain it attains a maximum thick­ of Clinch Mountain. Here it apparently pre­ road it is possible that the shore of the early upturned by the force which crumpled the strata ness of 400 feet and is mapped sepa- Jhas?tion serves the same characteristics as in the Poca­ Carboniferous sea was along that line, passing of the Appalachian Valley. In this mass indi­ rately: but in the vicinity of Stone Hm^toneon hontas quadrangle, and hence the same classifica­ near the towns of Radford, Wytheville, and vidual formations are not distinguishable, conse­ Mountain,ir I on the,1 margin oti. the,1 coali |J*thet Ieonthewest and tion is made. In the vicinity of Stone Mountain Marion. quently on the map it is represented as the field, it can not be separated from the there are a few isolated outcrops of this formation, In the New River region the Price sandstone unclassified rocks of the Pottsville series. adjoining formations. In the latter locality it is but the beds are so crushed and fractured that is overlain by a considerable body of bright-red Pocahontas formation. This is the lowest usually represented by beds of mottled, shaly they are almost unrecognizable. shale which also thins westward and does not division of the coal-bearing rocks, extending from limestone, so interbedded with the blue limestone appear on the Tazewell quadrangle. the top of the Bluestone formation to DEVONIAN STRATA. The famous below and the shale above that they are insepara­ Gre&nbrier limestone. The Greenbrier lime­ the roof of the Pocahontas coal. In Pocahontas coal seam. ble as a distinct formation. Romney shale. The basal portion of the great stone outcrops only on the border of the coal this interval of 360 feet there are sand­ Sevier sJiale. This shale increases greatly in mass of Devonian sediments is composed of black, field, where it overlies the Devonian shales with stones, shales, and a few coal seams, but those thickness from northwest to southeast across the carbonaceous shale, from 300 to 500 no apparent evidence of unconformity. The coals which occur below the Pocahontas seam are Appalachian Valley, but the lateral character feet in thickness, which is named from anddiltribu- limestone is generally dark blue and thin and of not much consequence. The forma­ extent of the outcrop in the Tazewell tiolffS?"" thei town ofn Komney,T» TTTWest i XT-Virginia. §!aTtion eofney the cherty at its base, graduating upward tion shows slightly in outcrop in the valley of quadrangle is so small that the change Seviersnale* i i i ,» ? -I -i i -i i ness °f Car- The change from this formation to the mto thin beds ot a light-O blue color,) and limestone. Elkhorn Creek and in most of the valleys east of in thickness is not noticeable. In House and green, sandy shale above takes place gradually finally becoming decidedly shaly at its Bear Wallow and Indian Creek. Barn, Paint Lick, Deskins and Clinch mountains, through interbedding, and is shown on the map by upper limit. It enters the Tazewell quadrangle Welch formation. Above the Pocahontas coal and in Morris Knob the thickness possibly varies the merging of patterns. The Romney shale shows from the east in two lines of outcrop which unite on for a distance of 700 feet there is no bed which from 1200 to 1400 feet. In Stone Mountain it is in but two places in the Tazewell quadrangle: Indian Creek and extend as a single trough as far can with certainty be identified throughout this very much thinner, but whether this is due to an one along Laurel Creek, on the southern side of as Doran. A second narrow syncline of this lime­ area, hence the whole is mapped as one formation actual decrease in thickness toward the northwest Clinch Mountain, and the other on the northern stone shows north of the other outcrop, but it is and named from the county seat of McDowell or to a thinning produced by intense folding and side of Stone Mountain. small and contains only the basal portion of the County, West Virginia. In the description of faulting is uncertain. The formation changes Kimberling shale. The green, sandy shale and formation. The full thickness of the limestone Pocahontas quadrangle this is subdivided at the gradually from calcareous shale at the base to sandstone which lies above the Romney is present is present only along a portion of this line, hence horizon of the Quinnimont coal into two forma­ sandy shale at the top, and is named from Sevier in its full thickness only south of Clinch Moun­ it is difficult to determine the extreme variation tions; but it is doubtful if this coal can be recog­ County, Tennessee. The Sevier shale, Moccasin tain, where it measures about 3000 feet. In the in thickness. It probably ranges from 900 to nized in the Tazewell quadrangle, consequently limestone, and Chicamauga limestone were col­ syncline north of Baptist Valley it shows in two 1000 feet. the line of division has been dropped. The lectively referred by Rogers to No. Ill in his lines of outcrop, but on neither side is the full Bluefield shale. Between the top of the lime­ Welch formation includes many beds of sand­ Virginia series of rocks. measure present. This formation varies in char­ stone and the base of a heavy bed of sandstone stone which form conspicuous cliffs along Tug Bays sandstone. This formation attains a acter from a fine, green shale at the base to a which is mainly instrumental in preserving Stony River above Welch, but in other localities they thickness of from 300 to 400 feet and is named thin-bedded sandstone near the top, with some­ Ridge at its present altitude, is a body of shale are not prominent. The formation includes many from the Bays Mountains in northern times thin beds of coarse conglomerate. ranging in thickness from 1150 to 1250 feet. It important coal seams in various parts of the area, Tennessee. It consists of red, sandy The Kimberling and Romney shales, as a whole, is very calcareous at its base and is with difficulty but the absence of recognizable beds in the for­ shale at the base, which passes by represent No. VIII in Rogers's classification, but distinguishable from the limestone which under­ mation renders the correlation of such seams a insensible gradations into red sandstone at the top their exact equivalents in the New York series lies it. The calcareous shale passes upward into difficult matter. Its outcrop is limited mainly to of the formation. It outcrops near the summits have not yet been determined. clay shale, which in turn gives place to sandy the eastern part of the area. of all of the valley ridges, but it is usually con­ The great increase in thickness of the Devonian shale with thin beds of sandstone. This formation Raleigh sandstone.- In the eastern half of this cealed by the debris that falls from the formation shales, in passing from south to north, is one of shows only in the trough east of Baptist Valley quadrangle the most prominent formation is the above. the most striking features in the stratigraphy of post-office. Raleigh sandstone. It is coarse, some­ Clinch sandstone. All of the more prominent the Appalachian province. Thus the entire shale Hinton formation. This is a heterogeneous times conglomeratic, heavy bedded, and valley ridges owe their existence to this plate of series is probably wanting southeast of formation composed of almost every kind of sedi­ about 100 feet in thickness. On Tug heavy sandstone, which has preserved a line passing through Rome, Georgia, mentary rock and about 1200 feet in thickness. River it makes an imposing series of cliffs from their summits at or near the general and Gadsden, Alabama; at this line the It is a portion of a great mass of similar rocks the tunnel below Davy to Welch; on Spice Creek level of the Cretaceous peneplain, while , , . , . , -i t nian shales which extends from the top of the , it extends from Roderfield to Indian Gap; on shale comes in as a thin wedge° which alongvalley. the t Lower por- the areas immediately adjacent have been worn increases northward to 25 feet in thick Bluefield shale to the base of the coal- $£$£* Clear Fork, throughout its entire length; and on down to form the present valleys. It is a mas­ ness at Chattanooga, 800 feet at the southwestern bearing formations, and is usually serles' Dry Fork, from near the mouth of Crane Creek sive, coarse, white sandstone varying in thickness end of Clinch Mountain, 1800 feet on the Virginia- referred to as the "Red shales," because of its to the mouth of Jacob Fork. In the western half from 200 to 250 feet, and is named from Clinch Tennessee State line, 2000 feet at Little Moccasin prevailing constituent. The Hinton formation of the quadrangle it loses its massive character Mountain, the most prominent of the valley Gap, 3000 feet on the eastern edge of the Taze­ consists of the lower portion of this aggregate, and becomes only shaly sandstone but still retains ridges in southern Virginia and northern Ten­ well quadrangle, and 4000 or 5000 feet on New extending upward from the base of the sandstone about its original thickness. This sandstone is nessee. The Bays and Clinch sandstones were River. previously described to a heavy plate of conglom­ named from Raleigh County, West Virginia, called by Rogers the Red and White Medina, erate or sandstone which is classed as a separate where it is the most striking feature of the great or No. IV. The Clinch forms the summits of CARBONIFEROUS STRATA. formation. gorge of New River. House and Barn, Deskins, Paint Lick, and Clinch In the Tazewell quadrangle the strata belong­ Princeton conglomerate. On the Pocahontas Dismal formation. Above the Raleigh sand­ mountains, Morris Knob, and the peak south of ing to this period are of much more importance quadrangle this a is coarsely conglomeratic and stone is a mass of coal-bearing rocks about 490 Tazewell. than the strata of any other geologic period very prominent formation. Toward the west it feet in thickness which resembles very closely the Rockwood formation. Above the Clinch sand­ because they contain coal, which is the most becomes finer, showing on the Tazewell quadran­ Welch formation. The chief difference is that stone occurs a heterogeneous mass of shales and valuable mineral product that has so far been gle only as a coarse sandstone. It is about 40 the coal seams are neither so numerous nor so ferruginous sandstones from 300 to 400 feet in found in the territory. feet in thickness and outcrops in two lines which valuable. In the western portion of the quad­ thickness. This is one of the principal iron- The original classification of Rogers, together unite near the eastern edge of the area ; beyond rangle a heavy lentil of conglomerate appears in bearing formations of the province, but with the present subdivisions, are presented in this point it is not known as a separate formation. the middle of this formation, serving to distin­ in the Tazewell quadrangle there are descending order in the following table: Bluestone formation. This constitutes the guish it still further from the Welch. The for­ no known ore bodies that are thick upper portion of the " Red shales." It is about mation as well as the lentil of conglomerate is No. XIII.Lower Coal group. . . .. enough to work. The most conspicuous member 800 feet in thickness and consists of Upper por- named from Dismal Creek, which drains a large area in the western part of the field. is a coarse, white sandstone which occurs at the Dotson sandstone. shales, sandstones, and impure lime- extreme top and serves to separate this formation Bearwallow conglomerate. stones. It shows in the Stony Ridge senes> i Dismal conglomerate-lentil. This lentil of con­ Dismal formation. from the one immediately overlying it. This No. XII. .Great Conglomerate. -( (Dismal conglomerate-lentil.) syncline south of Horsepen Cove, and in some of glomerate is well developed in the basin of Dismal 1 Raleigh sandstone. formation represents a part of Rogers's No. V, and Welch formation. the valleys of the coal field. Creek and south of Sandy Ridge. It is here a takes its name from Rockwood, Roane County, Pocahontas formation. Unclassified measures. On the map there is a coarse conglomerate, varying in thickness from Tennessee, where it has furnished ore for com­ fBluestone formation. line of outcrop of the red shales just south of the 100 to 120 feet. Toward the east and north it J Princeton conglomerate. mercial use for twenty-five years. - 1 Hinton formation. fault which forms the southern border of the coal loses its character and can be traced only a short No. XI. -j [Bhiefield shale. ( Grreenbrier limestone Gfreenbrier limestone. field. These are highly contorted, and since they : distance. SILURO-DEVONTAN STRATA. are faulted on both sides it is almost impossible \ Bearwallow conglomerate. Above the Dismal No. X. . . .Montgomery grits. . . . .Price sandstone. G-iles formation. In the Pocahontas quad­ to classify them. They belong to the two preced-j formation is a sandstone or conglomerate about rangle the beds above the Rockwood formation Price sandstone. This formation overlies and ing shale formations, probably including portions 60 feet in thickness, which is named from the consist of shalyJ limestone,' massive ,_Transition is closely associated in character with the upper, of both; but their equivalence is so uncertain high ridge west of Dry Fork. Over most of the limestone, chert, and coarse, yellow sSSrEKSd0 sandy portion of the Devonian shales. Between that they can not be ascribed to either, and con­ area it is a coarse conglomerate which attains its sandstone. The geographical distribu- Devonian- greatest development along Tug River from Tazewell and New River the formation Coal-bearing_ , . , sequently they are mapped as unclassified rocks tion of these beds is uncertain ; they are generally is of considerable thickness and con- formation- of the Red shale series. Nigger Branch to Short Pole Branch, but in some so covered on their outcrop that their presence sists of sandstones, shales, and some coal seams, localities the pebbles are absent and it is only a over the entire quadrangle is a matter of some but it diminishes rapidly in thickness westward COAL-BEARING STRATA. coarse sandstone. doubt. It was deemed inadvisable to show them and changes in character so that it is an incon­ The upper limit of the Red shales marks an Dotson sandstone. Above the Bearwallow individually in the Pocahontas folio, consequently spicuous formation on the Tazewell quadrangle. abrupt transition from rocks that are prevailingly conglomerate occurs about 60 feet of shale sur­ they were grouped under one formation and It probably does not exceed 200 feet in thickness calcareous to those in which calcareous matter is mounted by 120 feet of coarse but thin-bedded named from Giles County, Virginia. in its outcrop south of Clinch Mountain, but almost wholly wanting, Conditions appear to sandstone. This sandstone forms the Roughs on The upper portion was called by Rogers No. toward the northwest, where its horizon is have changed from open sea to fresh or brackish Tug River below the mouth of Bull Creek, and VII, or Oriskany sandstone, and the lower, or exposed, there is no trace of the formation. There water lagoons where, from time to time, immense it is therefore named from the town of coal swamps flourished, which were subsequently Dotson, which is located at that place. fflpSttseviitiep limestone portion was called No. VI, or Lower is no visible unconformity at this point, and it is scries* Helderberg. The former is undoubtedly of uncertain whether the formation is merged with buried by quantities of sand and mud that were. Although fossil plants have not yet Devonian age, and the latter is probably Silurian ; the strata above or is altogether wanting. This swept into the basin from the surrounding land been found near the top of this sandstone, they but it seems better to group them together as one formation appears to have been deposited along areas. Such sediments accumulated in the Taze- have been collected from both above and below Tazewell 3. it. According to the determination of Mr. the northwest, producing southeastern dips on and by a broken line where their existence is i )art of the region from which it has been eroded David White the fossils found below belong to both limbs of the fold. In the southern portion lypothetical. In the sections faults are repre­ ts former position had to be calculated from the the Pottsville series, and those found above of the Appalachian Valley, where this type of sented by lines whose inclination shows the prob­ ocks which appear at the surface. If the rela­ to the Lower Coal Measures; therefore it seems structure prevails, scarcely a bed can be found able dip of the fault plane, the arrows indicating tion of a coal seam to the top of this sandstone is altogether probable that the top of this formation which dips toward the northwest. Out of the ;he direction in which the strata have moved on cnown at any point, its horizon can be determined agrees with the top of the series at Pottsville, overturned folds the faults were developed, and its opposite sides. at any other point by measuring up or down from Pennsylvania, notwithstanding the fact that in with few exceptions the fault planes dip toward These sections delineate the structure better she contour the required distance. the Tazewell quadrangle the series is much the southeast and are parallel to the bedding ;han any verbal description, but a few words of From these contours, which are shown on the thicker than in the type locality. planes. Along these planes of fracture the rocks xplanation will be added. From the southern conomic sheet, it is apparent that the structure is Sequoyah formation. This consists of sand­ moved to varying distances, sometimes as great dge of the quadrangle to a line passing through very irregular, and that most of the irregularities stones and shales overlying the Dotson sandstone as 6 or 8 miles. Baptist Valley, Cedar Bluff, and Honaker the show no connection with the folds of the Appa- and extending upward in the series to the top of There is a progressive increase in degree of 'olds are all of the open type, and no faulting is achian Valley. Near the southern margin of the a heavy sandstone 450 feet above the base of the deformation from northeast to southwest, result­ :ound. The mountains are almost all synclinal field, however, there is a well developed anticline formation. In this interval there are some coal ing in different types of structure in different in structure and the valleys are eroded on the hat is parallel to the valley structures. This seams, but they have not been thoroughly pros­ localities. In southern New York the strata are anticlines. 'old begins near Pocahontas and reaches its pected and their number and value are not well but slightly disturbed by a few inconspicuous North of this belt of open folding is a com­ greatest development on the eastern edge of the known. folds, except in a narrow belt along the south­ pound fault, which, at intervals, is represented by Tazewell quadrangle. From this point it grad­ Tellowa formation. All of the rocks of the eastern margin of this division, where the rocks a single break; but it is more often TheB tlst ually descends westward and disappears north of Tazewell area that overlie the Sequoyah forma­ are sharply folded and faulted to a considerable divided into two faults separated by a Valley*ault- Honaker. tion are included in the Tellowa, which is similar extent. In Pennsylvania many new folds are narrow belt of Knox dolomite. This remnant The value of such contours depends almost in composition to the underlying formation, except developed farther west, and all are of increased probably represents a syncline which, in the great wholly upon the accuracy with which they are that it carries some larger coal seams. It has only magnitude, but the folds are open, and, as a rule, rushing, has been almost obliterated. located. In the present case it was impossible to a limited outcrop in this area and consequently the dips are gentle, except along the southeastern The structure immediately north of this fault use the spirit level for this work, hence they were is of no great economic value. margin, where the same structure prevails that is an be fully understood only by a study of the determined by the aneroid barometer, and are Rocks higher in the Carboniferous series were found in New York. This type of structure region to the eastward. On the farther edge of only approximately correct. The aneroid work undoubtedly deposited over this region, but ero­ holds throughout Virginia, except that in the the Pocahontas quadrangle, the strata north of the is based on railroad surveys along Tug and Clinch sion has been so extensive that they are now gone, southern portion many of the folds are broken by Baptist Valley fault are unbroken and nearly rivers and a connecting line along Dry Fork. horizontal. The strata on the southern side of and no indications remain of the amount of the great overthrust faults. In Tennessee open folds MINERAL RESOURCES. material removed. are the exception and faults are the rule. The this belt are slightly upturned, and, in the process Appalachian Valley is here composed of a suc­ of folding, the hard beds have apparently broken, That portion of the Tazewell quadrangle which STRUCTURE; cession of blocks, tilted toward the southeast and allowing the softer strata to now in and replace lies within the Appalachian Valley is but scantily Definition of terms. As the materials forming separated from one another by fault planes which the broken members. This small fault cuts out supplied with minerals of value. the rocks of the Appalachian Valley were depos­ dip to the southeast at the same angle that the the lower portion of the Greenbrier limestone Barite. So far as known, barite is the most ited upon the sea bottom, they must originally strata dip. In Alabama the faults are fewer in and all of the other formations to and including abundant mineral. It occurs in the upper por­ have extended in nearly horizontal layers. At number, but their horizontal displacement is the top of the Devonian shales. Westward, tion of the Knox dolomite, and in its geographi­ present, however, the beds are usually not hori­ much greater, and the folds are somewhat more the folding is more pronounced; a decided anti­ cal distribution is limited mainly to the southern zontal, but are inclined at various angles, their open. cline is developed in Abbs Valley and a syncline slope of Kent Ridge. The most productive edges appearing at the surface. The angle at In the Appalachian Mountains the same struc­ in the valley of Mud Fork. Still farther west­ locality so far discovered is on the banks of which they are inclined from a horizontal plane ture is found which marks the Great Valley, such ward the anticline develops into a fault, which Clinch River 3 miles below Gardner. It is here is called the dip. In the process of deformation as the eastward dips, the close folds, the thrust passes through Shrader and Richlands. A few dug from the residual limestone clay and hauled the strata have been thrown into a series of arches faults, etc.; but the force of compression has of the formations are wanting in the upturned to Gardner, where it is washed and ground ready and troughs. In describing these folds the term resulted mainly in the development of cleavage edge of the syncline which lies north of the for the market. At present the work at this syncline is applied to the downward- structure in the rocks. broken anticline; they are supposed to have mine is suspended. bending: trough and the term anticline synciines?' The structures above described are manifestly been broken in the process of folding and to Iron ore. But little iron ore is known in the ° ° and faults. to the upward-bending arch. A syn­ the result of horizontal compression which acted have been replaced byr the lower rocks. Tazewell quadrangle. The Rockwood, which is clinal axis is a line running lengthwise in the in a northwest-southeast direction, at structure is In passing westward across the Tazewell quad­ the great iron-bearing formation of the Appa­ synclinal trough, at every point occupying its right angles to the trend of the folds XSfiSt rangle the syncline lifts, and at Doran nothing lachians, carries in this area nothing but ferrugi­ lowest part,-toward which the rocks dip on either and cleavage planes. The compression pression- but Devonian shale shows in outcrop across the nous sandstones, which are too siliceous to be side. An anticlinal axis is a line which occupies probably began in early Paleozoic time and con­ trough. West of Clinch River and at the extreme considered as ore. On Short Mountain, however, at every point the highest portion of the anti­ tinued at intervals up to its culmination after the point of the fold a portion of the southern limb, the Rockwood shales contain some red hematite, clinal arch, and away from which the rocks dip close of the Carboniferous. which shows at no other point except south of which appears to be of excellent quality and on either side. The axis may be horizontal or In addition to the horizontal force of compres­ Graham, has been preserved and thrust toward which may extend in places into this territory, inclined. Its departure from the horizontal is sion, the province has been subjected to forces the northwest into the center of the basin. The but at present no such deposits are known. preservation of the overturned limb of the syn­ called the pitch, and is usually but a few degrees. which have repeatedly elevated and depressed its COAL. In addition to the folding, and as a result of the surface. In post-Paleozoic time there have been cline after the northwestern limb is obliterated is continued action of the same forces which pro­ at least three and probably more periods of anomalous in Appalachian structure. By far the most important mineral resource is duced it, the strata along certain lines have been decided oscillation of the land, due to the action The Appalachian coal field is in the form of a bituminous coal. Seams of coal are found in all fractured, allowing one portion to be thrust for­ of vertical forces. In every case the movement great trough in which the strata dip gently from of the measures above the Bluestone formation, ward upon the other. Such a break is called a has resulted in the warping of the surface, and the sides toward the center. Since the except those which are composed entirely of Tazewell quadrangle includes a portion sandstone, and since these formations are found fault. If the arch is eroded and the syncline is the greatest uplift has generally coincided with « -, . field. buried beneath the overthrust mass, the strata at the Great Valley. of the southeastern margin 01 this only in the northern portion of the quadrangle the surface may all dip in one direction. They Structure of the Tazewell quadrangle. Since trough, the rocks comprising its coal field are the coal seams show in outcrop only in the region then appear to be deposited in a continuous series. the Tazewell quadrangle includes parts of two of generally supposed to have a regular, northwest­ north of the fault line which passes through Folds and faults are often of great magnitude, the great subdivisions of the Appalachian prov erly dip. Close examination, however, shows that Shrader, Richlands, and Doran. Of course there their dimensions being measured by miles, but ince, the area may be divided into two districts such is not the case; that the dips, though gener­ are many of these seams which are too thin or they also occur on a very small scale. which differ radically in their geologic structure. ally toward the northwest, are exceedingly irreg­ too much broken up by partings to be of value, Structure of the Appalachian province. Each In the district which lies south of a line through ular; and that the inequalities bear but little but there are a number which are of sufficient subdivision of the province is characterized by a Richlands and Shrader the strata are bent into relation to the general structure of the province. thickness and of the requisite quality for profit­ distinctive type of structure. In the Typesof great anticlines and synclines. Along the north This great irregularity, which may have resulted able mining. plateau region and westward the rocks structure- em margin of this district the thrust has been so partly from inequalities of the ocean floor upon Coal in the Pocahontas formation. The lowest are generally horizontal and retain their original severe that the folds have broken, producing which the beds were deposited, but which is more seam known in the Tazewell quadrangle occurs composition. In the valley the rocks have been great thrust faults which have complicated to a probably due to the compression that folded the on Vail Creek near its mouth. The seam is not steeply tilted, bent into folds, broken by faults, great extent the otherwise simple folding. North rocks of the Appalachian Valley, has made it very entirely exposed, but it shows a thickness of 2 and to some extent altered into slates. In the of the line above mentioned the rocks are nearly difiicult to trace coal seams from place to place, feet 8 inches. It is about 150 feet above the top mountain district faults and folds are important horizontal and show but little effect of the force and has caused innumerable errors in their corre­ of the red shales. Sixty feet below the Pocahon­ features of the structure, but the form of the which folded and crushed the strata of the Appa lation. tas seam (No. Ill) there is a coal seam which rocks has been changed to a greater extent by lachian Valley. Structure contours. The determination of the ranges from 2 feet 6 inches to 3 feet 8 inches in cleavage and by the growth of new minerals. Structure sections. The sections on the struc­ exact "lay" of the coal seams is of so much thickness. This seam shows along Tug River In the valley region the folds and faults are ture sheet represent the strata as they would importance to both prospector and from the eastern end of the quadrangle to Tug operator that an effort has been made theeRaiefgh River post-office, where it passes below water parallel to the old shore line along the Blue appear in the sides of a deep trench L _. sandstone. Ridge, extending in a northeast and southwest cut across the,i country.i rniI heir position A.* Undergroundrelations of to bring out the structure more iully level, and also on Adkins Branch with a bed-sec­ ^ . IT the strata. direction for very great distances. Some of these with reference to the map is on the line than it is possible to show it on the structure tion as shown in fig. 1. faults have been traced 300 miles, and some folds at the upper edge of the blank space. The ver sections. Since the different beds of coal, shale, At present the most important seam is No. Ill, even farther. Many folds maintain a uniform tical and horizontal scales are the same, so that and sandstone appear to be parallel, the determi or Pocahontas, so named by the original dis­ size for great distances, bringing to the surface a the actual form and slope of the land and the nation of the "lay" of any one bed will be coverers from its position in the series single formation in a narrow line of outcrop on actual dips of the strata are shown. These sec approximately correct for any other, except that of coal seams at the point of discovery, hontas°£oai the axis of the anticline, and another formation tions represent the structure as it is inferred from the absolute elevation will be different. The and also from the place of its first in a similar narrow outcrop in the bottom of the the position of the strata observed at the surface Raleigh sandstone is selected as the most promi development. This seam has been traced over syncline. The folds are also approximately equal On the scale of the map the minute details oJ nent stratum, and on its upper surface points oJ much of the territory along the eastern side of to one another in height, so that many structure can not be represented, and therefore equal elevation are connected by lines, and since the quadrangle by the Flat Top Coal Land Asso­ parallel folds bring to the surface the foidspof thl the sections are somewhat generalized from the these contour lines are horizontal they indicate ciation. Unfortunately, all of these prospect 1 Valley. same formations. The rocks dip at all dips observed in a belt a few miles in width along the irregularities of the surface on which they are holes had fallen shut at the time of the present angles, and frequently the sides of the folds are the lines followed. drawn. Over most of the quadrangle the Raleigh work, and but few measurements of the seam compressed until they are parallel. Where the Faults are represented on the map by a heavy sandstone shows at the surface, and consequently were obtained. folds have been overturned, it is always toward solid line where their presence is well determined its elevation is easily determined; but in that There are two mines in operation on this seam. Both are located on Elkhorn Creek, near Vivian, grounds these seams, covering an interval of 290 in No. 11 of the table of analyses. This seam, bony streaks, which give the heavy percentage at which point, the seam varies in thickness from feet, have been grouped and named from the type with a thickness of 9 feet and the bed-section of ash in analysis No. 16. This seam also shows :5 feet 8 inches to 6 feet 3 inches. It "passes locality, Horsepen group. Most of the large shown in fig. 20, has been opened at Smith Store, along Levisa Fork in the vicinity of Shack Mills, below water level at Kimball, but reappears at seams in the quadrangle fall within the limits of 4 miles east of Horsepen, where it has been mis­ but no measurements nor samples of the entire railroad grade in the bend of the creek above this group. taken for the Pocahontas seam. seam could be obtained. the mouth of Upper Belcher Creek. At Helena The lowest seam of the Horsepen group is On Indian Creek this seam makes a fair show­ South of Sandy Ridge this seam shows in a it has been reached by the drill at 198 feet below about 150 feet above the base of the formation ing and has been opened in a number of places. number of places. It is opened on Coal Creek, railroad grade, where it has a thickness of 5 feet or the Pocahontas seam. It is exposed On the eastern fork it shows directly above the a mile above the railroad, but the mine has been 4 inches and a bed-section as shown in fig. 2. back of the schoolhouse at Horsepen, Horeep7ner opening on the Middle Horsepen seam. It varies abandoned, as the seam was found to be too thin On Tug Kiver this seam has been opened at a where it shows a total thickness of 4 in thickness from 4 to 6 feet (fig. 21), and in this to mine profitably. Its bed-section at this point number of points, but at the time of examination feet 9 inches, but it is much broken by shale part­ locality has a heavy sandstone roof. A sample is shown in fig. 31, and its analysis in No. 17 of the slipping in of the earth from above had ings, as shown in fig. 10. A sample taken from from this opening gave analysis No. 12. the table. A sample from an opening one-half closed all but one. The Flat Top Coal Land this opening, exclusive of the shale partings, This seam appears to extend over a considerable mile farther up the creek gave analysis No. 18. Association give the following measurements of yielded analysis No. 4, but the coal was consider­ portion of the Tazewell quadrangle, but it grows On Big Town Hill Creek, near its mouth, this the seam at various points. They are evidently ably weathered and the analysis is hardly a fair thinner toward the north. At Peeryville it is seam has been opened and its bed-section at this total thicknesses of the seam, including all part­ representation of the quality of the coal. This only about 2 feet in thickness, and at Welch, point is shown in fig. 32. It has also been opened ings. At the mouth of Harmon Branch the seam has been opened above Rlchlands, on Big where it has been opened to supply the town, it in two places near the sharp bend in Middle thickness of the seam is 8 feet; one mile below, Creek, where perhaps it is better developed than is but 20-J- inches in thickness. This mine has Creek, and its bed-section at the opening beneath 8 feet 7 inches; at Tug Kiver post-office, 9 feet; at any other point within the quadrangle, but been abandoned and another seam higher in the the road is given in fig. 33. On Laurel Creek it and at each of four openings on Sand Lick Creek, even here it proved to be extremely variable and series supplies the local market. A sample from varies in thickness from 4 to 5 feet, and it has 8 feet. The opening at Tug River post-office is rather expensive to mine. Its bed-section at an the lower seam gave analysis No. 13. been mined in a small way to supply the local still accessible, showing a total thickness of 8 old opening below the mine is shown in fig. 11. About 100 feet above the Upper Horsepen trade for a number of years. This seam is prob­ feet 9 inches with a bed-section as shown in fig. 3. About a mile above the mine the lower parting seam, or 250 feet below the top of the Raleigh ably present in all the stream valleys west of On Long Branch, near the point at which the of clay has disappeared, leaving a much more sandstone, is another coal which seems to be Doran, but its exact position and thickness are seam passes -beneath water level, the Flat Top attractive seam, as is shown in fig. 12. A sample limited to the central portion of the quadrangle. unknown. Company reports this sean\as 10 feet 11 inches from the lower bench at this point yielded analysis On Indian Creek, 2 miles south of Bear Wallow, Toward the southern margin of the field, the in thickness. On Big Creek it is opened in the No. 5. West of Big Creek the downward pitch of this seam shows 2 feet of clear coal. On the trail Dismal conglomerate is somewhat broken and vicinity of Squirejim, where it shows a thickness the anticline carries this seam below water level. which crosses from Big Creek to Barrenshe Creek complex. It is as coarsely conglomeratic as at of 4 feet 6 inches (fig. 4). On Jacob Fork the This seam is not known to attain a workable it shows also, but its full thickness could not be any other point in the field, but it seems to split, Pocahontas seam shows at water level about one thickness north of the territory just described. determined. At Peeryville it is exposed directly and a coal seam appears in its lower portion. On and one-quarter miles above the mouth of Big One of the best seams in the region is 120 feet above the town, but at the point opened the seam the ridge between Big Town Hill and Mud Lick Creek. The full thickness is not shown at this above tjie Lower Horsepen seam, or 270 feet is very irregular, and it is impossible to form an creeks this seam has been opened, showing a point, but the water has washed out a block of above the Pocahontas coal. It is well shown in estimate of its value. thickness of 3 feet 5 inches and a bed-section as coal which measures 5 feet by 6 feet by 18 inches, the region about Peeryville and War Creek, and There are probably two coals above the last- given in fig. 34. On the ridge between Indian hence the seam must be of considerable thickness. the seam will hereafter be referred to as the War mentioned seam, but their occurrence is uncertain and Middle creeks it shows a thickness of 4 Southward from this point the seam rises rapidly, Creek coal. This seam is not known with cer­ and little can be said respecting their thickness feet (fig. 35). In each case it has a coarse sand­ reaching an altitude of 180 feet above water level tainty south -of War Creek. It may possibly be or extent. stone roof and consequently is somewhat variable at the mouth of Cucumber Creek, where it shows present on Indian Creek, but if so it has lost Coals in the Dismal formation. Closely over­ in thickness. a thickness of 6 feet 3 inches and the bed-section much of its thickness and is broken up by a thick lying the Raleigh sandstone is a coal horizon which At present only one coal seam of importance shown in fig. 5. shale parting. On War Creek and Dry Fork it has appears to be present over most of the Tazewell is known in the Dismal formation above the con­ On Dry Fork, about 1£ miles below the mouth been opened in seven or eight places. Through­ quadrangle. It is probable that it is not one glomerate. This has been opened at Bradshaw of Keevvee Creek, the Pocahontas seam rises out the area prospected it holds a constant thick­ continuous seam, but a general coal horizon in (fig. 36), but since the conglomerate is wanting above water level. The total thickness at this ness of from 4 feet 4 inches to 5 feet. Two which the seams vary slightly in their stratigraphic at this point, their exact relation is difficult to opening is 3 feet 8 inches, but it is so much cut measurements of the seam on War Creek gave position. determine; the conglomerate appears, however, up by partings, as shown in fig. 6, that it is of the sections shown in figs. 13 and 14. Fig. 13 is At Welch this seam rests directly upon the to be represented by a sandstone which occurs 10 not much value. A sample from the upper por­ from an opening on the left side of the creek sandstone. It has been opened here for local or 15 feet beneath the seam. tion of the seam gave analysis No. 1 in the table about one-half mile above its mouth, and a slightly use, but it is a poor seam. Its bed-section is Coals in the Dotson sandstone. Although this of analyses. Its heavy percentage of ash is weathered sample from this opening gave analysis shown in fig. 22 and its analysis, exclusive of the is classed as a sandstone formation, it is such only doubtless due to the many thin partings which No. 6. Fig. 14 represents the seam as shown in shale partings, is given in No. 14 of the table of in its upper part; the lower portion, about 60 occur throughout this portion of the seam. Near an opening on the right bank of the creek near analyses. feet in thickness, consists mainly of shales and the mouth of Vail Creek its thickness increases its mouth, and a slightly weathered sample from At Indian Gap it shows a thickness of nearly contains at least one coal seam. This was seen to 4 feet 7 inches, but it still contains a shale this place yielded analysis No. 7. This seam 4 feet, but the opening was in such a condition at the head of Adley Branch, below Peeryville, parting near the center of the seam (fig. 7). . passes beneath water level at Peeryville, where it that a detailed measurement could not be made. where it is 2 feet 5 inches in thickness. A sam­ On Beach Creek, nearly opposite Sayersville, a has been quarried from the bed of the river for On Spice Creek numerous openings have been ple from this opening gave analysis No. 19. A large seam has been opened, which is probably many years. made on this seam, but in all cases the abundance seam at about this horizon is reported on the the Pocahontas coal. It is 6 feet 3 inches in The Middle Horsepen coal occurs 239 feet of partings has been a source of great disappoint­ lower portion of Dismal Creek as 7 feet in thick­ thickness without a parting (fig. 8). The coal at above Lower Horsepen seam and 110 feet above ment to those interested in its development. An ness, but it was not seen. this opening is hard and splinty, differing very the War Creek seam. At Horsepen opening at the mouth of Little Day Camp Branch, Coals in the SequoyaJi formation. There are much in appearance from that at any other open­ the seam shows 4 feet of clear coal Horsepen e 180 feet above Spice Creek, shows a total thick­ several seams in this formation, but none are T i seam. ing on this seam. The upper half of this seam is (fig. 15), and a fair sample from this ness of 4 feet 5 inches with a bed-section as shown known to be of great commercial value. A seam badly weathered at this opening, unfitting it for opening yielded analysis No. 8. This seam is in fig. 23. On Shabby Room Branch, a mile from about 175 feet above the Dotson sandstone was chemical analysis, but probably it was originally probably present on Indian Creek, but its exact Spice Creek, this seam has been opened, but it is seen at a number of places. On State Line Ridge, of about the same quality as the lower half, a equivalent is still a matter of some doubt. A still broken by partings as shown in fig. 24. On near the head of Mill Branch, it has the sample of which yielded analysis No. 2. Still mine has been opened near the upturned measures Spice Laurel Branch, 1£ miles above its mouth, section shown in fig. 37. On the same ridge it farther up Beach Creek, on a branch which enters on the right hand side of the creek, and is being this seam has been thoroughly prospected, but shows at the point where the road from Bradshaw from the north, a coal has been opened which is worked to supply the local demand. The bed- the partings are even worse than in the surround­ passes down into the valley of Slate Creek. At supposed to be the Pocahontas, though it may section of the seam at this mine is shown in fig. ing region. Its bed-section at this point is shown this point it has the bed-section shown in fig. 38. belong to a higher horizon. It has a total thick­ 16, and the analysis of a sample which includes in fig. 25. It also shows in the road on the summit between ness of 4 feet 9 inches, but it is broken by a the two lower benches of the coal at the mine is This coal horizon reaches its greatest develop­ Bull Creek and Guess Fork of Knox Creek. A thick shale parting which is shown in the section, given in No. 9. This seam presumably shows 2J ment on Dismal Creek, but since the shale partings coal which is supposed to be the same as the ones fig. 9. A sample from the upper bench yielded miles above Harman, on the eastern fork of the are also thicker and more numerous, TheDislnaI just mentioned can be seen in natural outcrop on analysis No. 3. creek, about 130 feet above water level at the forks the seam is in reality but slightly Creekseam- the hill back of laeger, 600 feet above railroad West of this point the Pocahontas seam is of the creek. It is here badly broken up by shale improved. The seam is spoken of in this region grade, but it has not been prospected and but below water level, unless, perhaps, it is exposed partings as shown by the diagram in fig. 17. as ranging from 10 to 14 feet in thickness, and little is known regarding its thickness or quality. in the upturned rocks along the edge of the basin. On Big Creek above Richlands this seam has much is expected from its development. The About 250 feet above the Dotson sandstone is Even if this seam should be found in the upturned been opened .directly over the opening on the character of the seam shows that such hopes can a coal which was seen at only one place in this strata it is doubtful if it would pay to work, for Lower Horsepen seam, but it proved to be too not be realized, and great disappointment is in quadrangle. It shows on Adkin Branch, opposite the rocks are badly crushed, rendering mining thin to work profitably, and the mine was store for those who are anticipating large for­ the mouth of Horse Creek, about 530 feet above dangerous and expensive. Since the top of the abandoned after an entry had been driven 1200 tunes from its commercial development. On the the railroad, with the section represented in fig. Pocahontas formation is drawn at the top of feet. The bed-section at the end of this entry is extreme head of Dismal Creek, within a mile of 39. the coal seam of the same name, the line of divi­ shown in fig. 18, and a sample from the same the triangulation station on Bear Wallow, this Coals in the Tellowa formation. By far the sion on the general geologic map represents the place gave analysis No. 10. This seam is doubtless seam is exposed in the bed of the creek with a most important coal seam in these upper measures outcrop of the Pocahontas coal. In the region exposed in some of the stream valleys west of Big thickness of 4 feet 6 inches and a bed-section as is one which barely enters this quadrangle, but covered by the surveys of the Flat Top Company, Creek, but it passes below water level before it shown in fig. 26. A sample taken at this point, which is prominent lower down Tug River. It the positions of these openings were determined reaches Coal Creek. including everything except 6 inches of the upper occurs about 600 feet above the Dotson sand­ by transit and level; in the territory west of that The Middle Horsepen seam is not known in portion of the seam, which was badly weathered, stone with a section as shown in fig. 40. A covered by these surveys the elevations were all the northern portion of the Tazewell quadrangle; when analyzed gave the result shown in No. 15 sample from a mine on Long Pole Creek furnished determined by the aneroid barometer, based on a it may may be present, but if so, it is probably of the table. analysis No. 20. railroad survey along Dry Fork. too thin to attract attention. About 5 miles above McNiel Store this seam SOILS. Goals in the Welch formation. This formation In the type locality at Horsepen there is a heavy shows its greatest development (figs. 27 and 28). carries a greater number of workable seam 60 feet above the last described On Lick Branch, about 3 miles above McNiel In that portion of the Tazewell quadrangle coal, which is called the Upper Horse- Horsepenr Store, it shows a decided thinning of the shale which lies within the Appalachian Valley the coals than any other in the Tazewell Pengrorupof scum. area. At Horsepen-r-r several11 large seams seams. pen seam; it has a thickness of 8 feet partings, and is represented by the bed-section in soils are almost as clearly differentiated as the occur which range in position from 250 to 440 and a bed-section represented in< fig. 19. The fig. 29. Fig. 30 represents the seam as it shows rocks from which they are derived, and a map of feet above the Pocahontas seam. On paleobotanic analysis of a sample from this opening is shown at McNiel Store, but the bottom bench is full of the areal geology will suffice to show the general Tazewell 5. distribution of the different kinds of soil. The residue, consisting mainly of sandy and clayey general three kinds of shale arenaceous, alumin­ Portions of the Knox dolomite yield a very soils are the result of the decay and disintegration material, remains to form the soil. ous, and calcareous it follows that the resulting good soil, but its outcrop is so generally covered of the rocks immediately beneath; hence there is a Something of their genesis being known, soils soils will range from sandy clay to a rich limestone by the chert which weathers out of the limestone close agreement between the character of the soil may be classified according to the underlying clay, with all the intervening grades. The Kim- that its value is greatly impaired. and the original rock from which it is derived. rocks, and the geologic map may be made to do berling shale gives the poorest soil of the region, Baptist Valley and the region about Honaker It is not intended by this statement to convey duty as a map of soils. True, there are some small but little of its outcrop being cultivated. Many are noted for the good quality of their soil, which the idea that the soil has all the chemical constit­ exceptions to this rule. In a country whose of the coal-bearing shales form but little better is the product of the Honaker limestone. uents of its parent rock, for by the very process slopes are as steep as those of the Tazewell quad­ soils. The great shale formations of the Lower From an agricultural standpoint, the coal field of soil-making a large proportion of the more rangle, there must be considerable o.verplacement Carboniferous produce much better soils, for is the poorest region within the limits of the Taze­ soluble material is removed, leaving the bulk of of soil by washing down of material derived many of their beds are strongly calcareous. The well area. On the hills the soils are all derived the soil composed of the less soluble residue. from the overlying formations. Since the crests Sevier shales are quite rich in calcareous matter from the underlying shales and sandstones, and are Sedimentary rocks, such as are found in this of the ridges are always formed by beds of sand­ and form good soils; but generally they are quite consequently thin and poor. Even the meager region, suffer decay by the removal of the cement stone, the overplaced soil is universally sandy inaccessible, since they universally outcrop on flood-plains which occasionally border the streams which binds the particles together. If the and detrimental to the soil of the valley below. the steep northerly slopes of the Clinch sandstone are but little better than the soil of the upland, cement be siliceous, as in quartzites and some Sandy soils. Such formations as the Bays, ridges. for they are composed almost entirely of sand sandstones, the rock .resists solution efficiently Clinch, Rockwood, Price, and Princeton sand­ Soils derived from limestones. As a rule, these derived from the disintegration of the sandstones and is but slowly altered; but if the cement be stones, together with much of the coal-bearing are the best soils of the region. Ranking highest and sandy shales which compose the great bulk calcareous it is soon removed and the rock is rocks, give a poor soil, varying as slightly as the as a producer of rich soils is the Chickamauga of the rocks of the coal field. broken down. Thus calcareous sandstones are rocks vary from which it is derived. Pure sand­ limestone, which has made Tazewell County soon reduced by this process to a mass of sand, stone, like the Clinch and some beds in the Car­ famous as a blue-grass region. MARIUS R. CAMPBELL, and calcareous shale to clay. In limestones the boniferous series, produces nothing but white or Second in importance as a soil producer is the Geologist. calcareous matter is dissolved and the solution is yellow sand, whereas other sandstones associated Greenbrier limestone, but in this territory its out­ carried off by running water, either on the sur­ with shales give a very sandy clay soil. crop is so restricted that it becomes of minor June, 1898. face or through underground passages; while the Soils derived from sliales. Since there are in importance.

1 able of analyses of coals from the Tazewell area.

VOLATILE FIXED ^ VOLATILE FIXED No. MOISTURE. MATTER. CARBON., ASH. SULPHUR. PHOSPHORUS. TOTAL. APPEARANCE OF COKE. QUALITY OF COKE. No. MOISTURE. MATTER. CARBON. ASH. SULPHUR. PHOSPHORUS. TOTAL. APPEARANCE OF COKE. QUALITY OF COKE.

1 0.29 16.00 70.99 12.72 0.62 Trace. 100.62 Sooty. Partly dense, coherent. 11 2.24 24.65 63.77 9.34 0.65 Trace. 100.55 Semi -brilliant. Dense, mostly coherent.

2 0.62 22.36 70.35 6.67 0.91 do. 100.91 do. Dense, coherent. 12 0.52 22.88 65.24 11.36 0.73 do. 100.73 Sooty. Mostly dense, coherent.

3 0.42 27.19 59.88 12.51 1.30 do. 101.30 Brilliant. Coherent. 13 2.46 18.45 62.93 16.16 0.54 do. 100.54 do. Non -coherent.

4 0.39 25.29 64.24 10.08 1.17 do. 101.17 do. do. 14 0.21 19.32 70.42 10.05 0.72 do. 100.72 Brilliant. Coherent.

5 0.66 25.91 64.23 9.20 1.19 do. 101.19 do. do. 15 0.50 22.09 71.78 5.63 0.62 do. 100.62 do. do.

6 8.42 82.86 48.83 9.89 0.51 do. 100.51 Sooty. Non-coherent. 16 1.88 18.80 54.54 24.83 0.54 do. 100.54 Sooty. Partly coherent.

' 7 5.89 22.55 60.72 10.84 0.55 do. 100.55 do. , Coherent. 17 0.66 30.08 55.90 13.36 0.74 do. 100.74 Brilliant. do.

8 0.15 25.61 68.54 5.70 0.94 do. 100.93 Brilliant. do. 18 0.77 33.31 59.22 6.70 0.65 do. 100.65 do. Coherent.

9 0.58 29.68 61.75 7.99 0.79 do. 100.79 do. do. 19 0.14 24.20 71.63 4.03 0.85 do. 100.85 do. do. Part brilliant, 10 0.38 28.80 65.40 5.42 0.57 do. 100 57 do. do. 20 0.57 30.79 66.52 2.12 0.68 do. 100.68 part earthy. Dense, coherent.

SECTIONS OF COAL SEAMS EXPOSED IN THE TAZEWELL AREA. . SCALE: 10 FEET = 1 INCH.

FIGURE 1. FIGURE 2. FIGURE 3.: FIGURE 4. FIGURE 5. FIGURE 6. FIGURE 7. FIGURE 8. Clay and Shale Sandstone.... £!' ; Shale bone.-l' !"' Shale, Bone...... 3" Coal.....2'4" Coal...... 3'8' ; Shale...... 7 Coal.....6'2"

Bone...... ! Clay.

FIGURE 9. FIGURE 10. FIGURE 11. FIGURE 12. FIGURE 13. FIGURE 14. FIGURE 15. FIGURE 16. Shale Coal...... 4" Shale.....24" ggg^g Coal...... 4" Clay and Clay bone.....8' Coal.....I'O" Coal....4'0" Coal .....11" Bone...... 6" Shale...... 6' Coal.....!'6"

FIGURE 17. FIGURE 18. FIGURE 19. FIGURE 20. FIGURE 21. FIGURE 22. FIGURE 23. FIGURE 24.

Shale...... 2" ESSSSS Coal!.'! '.'.. .2" Coal..... 2'2" Bone ... Coal.... 1'2" Coal.....!'4" Bone . Shale... Coal...... 5" Garb. shale- Shale .. .1' 1" Shale...... 6 Coal....!'24" Coal..... I'O" Coal...4'to G' Shale... Coal.....!'3" Shale.. Coal.....2'5" Coal....!'14" Bone.....^" Bone ...... 3 Bone ...... 3" Coal.... I'O" Coal.....2'7' Coal.....3' S*

FIGURE 25. FIGURE 26. FIGURE 27. FIGURE 28. FIGURE 29. FIGURE 30. FIGURE 31. FIGURE 32.

Bone...... 3" Coal...... 10" Coal.....!'6" Clay...... 9" Coal...... 8" Shale...... !" Bone...... £" Bone .. ...A" Coal.....2'3" Coal...... 3" Carb. shale Coal.....I'O" Bone. Dirty coal .2" Shale...... J" Shale...... 6" Coal.....2'4" Coal....2'94" Clay.....!'2" Clay...... 5" Shale.... I'l Coal..... I'O"

FIGURE 33. FIGURE 34. FIGURE 35. FIGURE 36. FIGURE 37. FIGURE 38. FIGURE 39. FIGURE 40 Carbona- pg^^^ES Coal...... ceous shale | Coal.....V 4" ____ Coal....I'll' Shale...... !' Coal.....4'0" Bone....3^0' Shale...... !' Coal and Coal.....3'5" Sandy clay 0" Coal.....2'0" Shale...... 1" &5SH| Coal"".'. '. 2* bone...7J' ^^^^ Coal. , 3' 6" Coal.....2'9" Bone...... 8" Coal...... 8*"